PRE- AND POST-KATANGAN GRANITOIDS OF THE GREATER LUFILIAN ARC ? GEOLOGY, GEOCHEMISTRY, GEOCHRONOLOGY AND METALLOGENIC SIGNIFICANCE Volume 1, Text By Alberto Lobo-Guerrero Sanz Supervisor: Professor Laurence J. Robb A thesis submitted to the Faculty of Science University of the Witwatersrand, Johannesburg For the Degree of Doctor of Philosophy Johannesburg, March 12, 2005 PRE- AND POST-KATANGAN GRANITOIDS OF THE GREATER LUFILIAN ARC ? GEOLOGY, GEOCHEMISTRY, GEOCHRONOLOGY AND METALLOGENIC SIGNIFICANCE By Alberto Lobo-Guerrero Sanz Supervisor: Professor Laurence J. Robb A thesis submitted to the Faculty of Science University of the Witwatersrand, Johannesburg For the Degree of Doctor of Philosophy Johannesburg, March 12, 2005 A single watch is enough to tell time. If you have acces s to more than one watch, you can?t decide whic h time is right. "... You must learn to live with the rules of the geology game, however frustrating: (1) collect bi ts of data, however incomplete, that bear on a problem, (2) eval uate them, and (3) come to a conclusion, however imperfect. T hen (4) be read y to accept and analyze pertinent new da ta, and (5) repeat." John E. Warme, Professor in Applied Stratigraphy Colorado School of Mines, Gol den Colorado, 1992 Prospectus. Aknowledgements I thank my father for his unconditional suppor t, for guiding me into the world of geology and mineral deposits, and fo r encouraging me to continue advancing my education. I thank Andrea, my wi fe, for accepting to delay our wedding one year (the first year of this Ph .D. research). I also thank her support, understanding and patience during the long days and nights, Christmasses and holida ys that were sp ent developing ideas and editi ng multiple drafts. v ABSTRACT This document reports observations , findings and conclusions of the re search pro ject entitled ?Pre- and Post-Katangan Granitoids of the Gr eater Lufilian Arc - Geology, Ge ochemistry, Geochronol ogy and Metallog e n i c Signific a n c e ? . The pro je c t, structur ed and sup er vised by Pro f essor Laure nce Robb, was designed to study granitoids that comprise the Greater Lufil ian Arc. Its main aims were to define the vario us grani toids, and study their role in Katanga n orog enesis and mineral izati on. Main fieldwork was concentrated in northwestern Zambia and northern Namibia. The Greater Lufilian Arc is a curvilinear belt of Ne oprot e r o z o i c Kat ang a n sedime n t s that was deform e d during the Pan African oroge ny in Zambia and the De mocr at i c Repu blic of C ong o, and the westwa r d extension of similar rock sequences into Botswana, Angola and Namibia. The mobile belt of the Greater Lufilian Arc also comprises a dominantly Pale o prote rozoic basement of defor med granitoids, and a diverse suite of Pan-African gra nitoi ds that intrude t he Katanga n sequences. A total of 1500 samples were collected in the fiel d; 351 plutonic rocks were anal ysed. 157 chemical analysis wer e compiled from vario us well-docume nted sources, to reach a total of 508 samples anal ysed in the databa se. 38 new zircon U-Pb SHRIMP II and laser ablation ICP-MS ages were pro duced. The majo rity of intrusive rocks from the Greater Lufilian Arc that were an alysed (60%) had midalkaline characte. 33% were suba lkaline and 7% were alkal ine. Mafic rocks are cl osely associat e d to felsic rocks in most domains of the Arc. Two thirds of the gabb roid s were mid alkaline, 1/6 alkaline and 1/6 subalkaline. The average rock type di stribution for the entire Lufilian Ar c closely resem bles that of the Hook Granit e Batholith in Zambia. A frequent field obser va tion is the persistent clustering of small bodi e s of red-alt ered gra nitoids, gabb roids, massive magn etite-hematit e and quartz pods that are link ed to ages aro und 550 and 750 Ma. The four-roc k association is related to iron oxide- c oppe r-gol d (IOCG) miner aliz ation, and seems to be a character i s t i c of c ontinental extension anoro genic envir onment s. Another recurrent featur e observed in most outcrops of the study area is the presence of two or more contrasting types of pl utonic rocks, includin g mafic, ultramaf i c and alkaline plugs and dikes. The multipli c i t y of rock types in a small are a seems to be a charact e r i s t i c of cont inental exten s ion ano rog e nic envir onment s. Quartz pods, hydrothe rmally-empl a ced iron oxid e bodies and roun d-pe b ble hyd rothe rmal breccias are features that occu r often in and around IOCG system s throughout the Greater Lufilian Arc. The main granitoid perio ds of empla c ement pres ent in the study area of the Arc are li sted on Tabl e 1. Several mor e restricted events occurred at 1700, 1600, 880 and 460 Ma. Table 1 Main Granitoid Terranes in the Greater Lufilian Arc Age (Ma) Rock types Location Environment of Emplacement Notes 5 5 0 ?50 Granite, alkali granite, quartz monzon ite, syenite, gabbr oids Otjiwarongo, central Namibia, Kaokoland, Damaran intrusives (Namibia), Hook Granite, NW Zambia (Zambia) Continental epeirogenic uplift The period may be brok en into 3 discrete events. 750 ?50 Granite, alkali granite, syenite and gabbroids with fels ic and mafic volc anics Copperbelt, Kalengwa- Kasempa, NW Zambia (Zambia); Khorixas Inlier and Summas Mountai ns (Namibi a ) Rift-re la t e d and continental epeirogenic uplilft. Intrude Roan and Nguba Litholog i es ; overlain by Kundel un g u and equiva l e n t sedime n t s . 1 1 0 0 ?50 Granitoids and fels ic to mafic volc an ic s South of the Copperbelt, West of Lusaka (Zambia); around Omitiomire, Kaokoland and the Witvlei area (Namibia ) Continental rift- r e l a t e d environments Surrou n ds Kapvaa l Craton from Namaqu a la nd to Irumide Belt in Zambia 1 9 0 0 ?100 Foliated alkali granie, quartz mon z on i t e and granite Copperbelt basement, Mkushi- S e r e n je , NW Zambia, Domes region (Zambia); Kaokoland, central Namibia, Kamanjab Batholith, Grootfontein Inlier (Namibia) Not well defined; probabl y formed in an anoro ge n ic continental extension environment Period can be brok en into 4 discrete events vi The Zambian Lufilian Arc and Damara re gion of Namibia behav e d as indepe n d e n t enti t i e s from 2200 to 2000 Ma. They also beh aved significantly differen t from 1400 to 850 Ma. Geological history of the two main portion s of the Gre ater Luf ilia n Arc is consist e n t from circa 800 Ma to the presen t, and especially during the last 600 million years. Most areas studied in the Arc show pol ycyclic geological histories. Repeated anor oge nic intrusive eve nts are a common denomin ator. Prolonge d crustal histor ies have resulted in superimposition of events. Granitoid rock suites with closely matching chemistr y and macroscopic features have been found to form two or three times in the same regi on, with up to a thousand million years of age difference. These features preclude lithologi cal or detailed geochemical correlation of plutonic rocks. At least ten clusters of ring comple xe s were identi f ied in the Arc. Cl ustering of multiple anoro genic ring complex intr usions can form batholith i c size bodie s . Cl usters are made by amalgam atio n of multiple ring complex e s of varyin g chemic a l compos i t i o n and si ze. Most of their rocks are midalka l i n e . Volcani c and plutonic rocks of roughly the same composit i o n occu r together. Total duration of ring complex cluster cycles avera ges 110 Ma, and their pla n view geom etry is roughl y that of an isosceles triangle. Information currently available on geoph ysics, geochron olog y, rock distribution and geochemistry from the Hook Granite Batholith (Zambia) fit quite we ll with an intracontinental, anoro genic, ring comple x cluster origin. The Nchanga Granite (Zambia) has all the characteristics of an anor oge nic granite ring complex, and might have contributed to the origin of copper in its environs. Several sour ces of evide nce indicate that the Kamanja b Batho lith (Namibia) is an ano rog en i c cluste r of ring complexes. Volcanic and pluton i c rocks of simila r compos i t i o n make the batho l i t h . Geolo g i c a l hist ory for the Khorixa s Inlier and the Kamanjab Batholith are significantly different. Complete Wilson cycles were not ide ntified in the st udy areas of the Great er Lufilian Arc. The domi nant magmatic process, as evidenced by the vol ume of extrude d rock, is anorog enic continental epeir oge nic uplift, closely-f o l l o w e d in time by a rift-rel a t e d granit o i d emplac e m e n t . C oalesci n g and overprin t i n g aulacoge ns seem to be the main geol ogical event in the Arc. Incipient migmatitization and alter a tion of Paleopr oterozoic rocks modi fied their chemistry to a point wher e their enviro nment of em placement cannot be i dentified by traditional geochemical means. The anomal ous thorium content in some gra nitoids of the Greater Lufilian Arc induced and maintai ned long-lived, large convective cells of hydrotherm al fluid flow. E-W-trendin g regional fracture systems, that run para llel to the elo ngation of the Arc, play an imp o rtant role in the emplacement of magm atism and IOCG mineralization. Thos e structures are gene rally par allel to the main Lufilian Arc trend, and could have been no rmal syn-rift faults reac tivated multiple times during geolo gical history. At least eight discrete periods of mineralization were ide ntified in t he Gre ater Lufilian Arc. There is a wide-spr ead series of midalkaline in trusions emplaced aroun d 750 Ma that prod uces a variety of mineral deposits. Another eve nt took plac e around 540?4 0 Ma. Five less well defined events oc curred at ~1970, ~1930, ~18 66, 1097- 10 59 and ~460 Ma. The domin ant dep osit type is iro n oxide -coppe r -gol d mineralization, but other types of mi ne ral deposits are present in the Arc. At least two di stinct events of disseminated coppe r mi neralization associated to midalka lin e gra nitoid intrusives were ide ntified in the Kamanjab Batholith; the firs t took place arou nd 1975 Ma and the second aro und 1928 Ma. The main IOCG events that have be en identified in the Great er Lufilian Arc took place during eight time perio d s . The rocks of many IOCG de posi t s and prospe c t s in t he Arc are pri s tine. There is no significant deformaton invol ved. Hyd rotherma l brecciation and other mine raliz ation features are un- deformed. Three discr ete time periods show IOCG miner alizat ion in close temporal spatial association with sedimentary- hosted copp er de posits. The first took place aro u nd Witvlei (Namibia) fro m 1108 to 1059 Ma. The second and thir d ocurr ed in the baseme n t to the Zam bian Cop per belt from 882 to 725 Ma and from 607 to 500 Ma. This idea may gener ate a new concept for the origin of sedimentary-hosted cop per and cobalt deposits. table of contents (cont.) vii SHORT TABLE OF CONTENTS Abstr ac t, v Short Table of Contents, vii Detailed Table of Contents, viii Aknowledgements, iii Conc lus i o ns , 395 1. Introduction, 1 2. Methodology, 4 3. Generaliz e d Geolog y of the Greater Lufilian Arc, 21 4. Description of Rocks from the Different Domains, 23 Zambian domains , 24 Hook Granite Batholith, Zambia, 24 West Lusaka/Kafue Flats domain, 61 Kalengwa-Kas empa Area, Zambia, 70 Northwes tern Zambia domain, 83 Kalene Hill area, 84 Introduction to the geolog y of the Domes Region, NW Zambia , 96 Kabompo Dome, 97 Mwombez h i Dome, 104 Solwez i Dome, 115 Conc lus i o ns on entire NW Zambia region , 118 Zambian Copperbe l t , 121 Nchanga Granite, 127 Nchanga mine area, 137 Muliashi Porphyry, 140 Deep borehole, Konkola mine, 144 Chambishi granite, 148 Mufulira granite, 152 Samba deposit, 155 Conc l us i o ns , 158 Namibian Domains, 163 Kamanjab Batholith, 163 Khorixas Inlier, 211 Oas farm, 213 Lofdal farm, 237 Other Small Outcrops in Namibia and Bostwana, 252 Mesopot a m ie, 252 Summas Mountains, 260 Ugab River outcrop s , 262 Okwa River Outcrops , Botswana, 264 Grootfontein Inlier, 265 Environs of Otjiwarongo, 266 Review of observations, 277 Witvlei, Namibia, 281 5. Thorium Content of Granitoids in the Greater Lufilian Arc, 303 6. Geoc hronolog y, 308 New radio m etr i c ages, 308 Geoc hronolog ical database and interpretation, 308 New Re-Os ages from copper mineral iz a t i o n , Zambian Copperb e l t , 312 7. Some Aspects of Anorog en i c Intrus i v e Rocks, 316 Comparis on of batholit h i c granitoid bodies with anorogen ic ring complex clus ters , 317 Comparis on of Lufilian small basic intrus ions with examples from the literatur e, 334 8. Iron Oxide- Copper-Gold Mineraliz at ion in the Greater Lufilian Arc, 337 Some notes on iron oxide-co pp e r - go l d deposits , 337 Iron oxide- copper-gold systems in the Greater Lufilian Arc, 346 Some known IOCG-l i k e deposi ts and prospe c ts , 362 Relation ship between IOCG and sedimentary-hosted Cu mineralization, 391 Sedimentar y-hosted Au mineraliz ation in the Greater Lufilian Arc, 391 Peculiar i t i es of Zambian and Namibia n IOCG systems , 391 Conc l us i o ns , 392 9. Conc lus i o ns , 395 10. Referenc es , 405 Appendices table of contents (cont.) viii DETAILED TABLE OF CONTENTS ABSTRACT, v SHORT TABLE OF CONTENTS, vii DETAILED TABLE OF CONTENTS, viii AKNOWLEDGEMENTS, iii CONCLUSIONS, 395 1. INTRODUCTION, 1 1.1 The Lufilian Arc, 1 1.2 The Project, 1 1.3 Aims of the Project, 1 1.4 Study Areas, 1 1.5 Project Outline, 3 1.5.1 Phase 1, 3 1.5.2 Phase 2, 3 1.5.3 Phase 3, 3 1.5.4 Phase 4, 3 1.5.5 Curren t Status of Projec t, 3 2. METHODOLOGY, 4 2.1 Field Sampling, 4 2.1.1 Definition of Granitoid , 4 2.1.2 Sampling Proc edure, 4 2.1.3 Referenc ing Geolog ical Stations, Recording Information and Sample Labeling, 4 2.1.4 Other Field Activities, 5 2.1.5 Field Equipment Used, 5 2.1.6 Bibliographical Resear ch, 5 2.1.7 Office and Laborator y Work, 5 2.2 Petrologic Nomenclature, 7 2.2.1 Total Alkali Diagram, 7 2.2.2 R1/R2 Cationic Classification, 8 2.2.3 Granitoid Classification, 9 2.2.4 Debon & LeFort Cationic Classification Diagrams, 10 2.2.4.1 Q-P DiagraM, 10 2.2.4.2 A-B Diagram, 10 2.2.4.3 QBF Diagram, 10 2.2.4.4 K-B Diagram, 10 2.2.4.5 Mg*-B Diagram, 10 2.3 Geochemistry, 12 2.3.1 Major Oxide Chemis try, 12 2.3.2 Trace Element and Rare Earth Chemistry, 12 2.3.3 Presentation of Chemic al Data, 12 2.3.4 Geoc hem ic a l Thresho l d Values, 12 2.4 Tectonic Discrimination of Samples, 14 2.4.1 Granitoid s, 14 2.4.1.1 Comprehensive method of Barbarin, 1999, 14 2.4.1.2 Major oxide method of Maniar & Piccoli, 1989, 14 2.4.1.3 Definition of anorogenic granitoids, method of Whalen et al, 1987, 15 2.4.1.4 Trac e element method of Pearce et al, 1984, 17 2.4.1.5 Discrimination of granitoids from collisional environ ments, method of Harris at al, 1986, 17 2.4.1.6 Discussion, 17 2.4.1.7 A Novel Approach, 17 2.4.2 Mafic Rocks, 18 2.4.3 Conven tions to Tabulate Rock Type and Me thods to Evaluate Environment of Emplacemen t for Samples Studied, 18 table of contents (cont.) ix 3 GENERALIZED GEOLOGY OF THE GREATER LUFILIAN ARC, 21 4 DESCRIPTION OF ROCKS FROM THE DIFFERENT DOMAINS, 23 4.1 ZAMBIAN DOMAINS, 24 4.1.1 HOOK GRANITE BA THOLITH, ZAMBIA, 24 4.1.1.1 Introduction, 24 4.1.1.2 Geoc hemis try, 25 4.1.1.3 Geolog ical Units, 36 4.1.1.4 Comparis on of Hook Granitoids with Ring Complexes, 45 4.1.1.4.1 Airborne Geophysical Image and Definition of Ring Complexes, 45 4.1.1.4.2 Comparis on of Hook Granitoids with rocks from Namibia n Mesozoic Ring Comple xe s , 49 4.1.1. 5 E-W Transec t Across the Kafue Park, Zambia, 55 4.1.1.6 Geoc hronolog y and Geolog ical Histor y, 57 4.1.1.7 Environmen t of Emplacement, 59 4.1.1.8 Conc lus i o ns , 59 4.1.1.9 Recomme n da t i o n s , 59 4.1.2 WEST LUSAKA/KAFUE FLATS DOMAIN, ZAMBIA, 61 4.1.2.1 Introduction, 61 4.1.2.2 Geoc hemis try, 61 4.1.2.3 Lusaka Granite, 66 4.1.2.4 Descrip t i o n of main rock types, 66 4.1.2.4. 1 Four rock associat i on , 66 4.1.2.4.2 Granitoid s, 67 4.1.2.4.3 Gabbroids, 67 4.1.2.4.4 Iron oxide bodies, 68 4.1.2.5 Thoriu m content in Kafue Flats area, 68 4.1.2.6 Geoc hronolog y, 68 4.1.2.7 Conc lus i o ns , 68 4.1.3 KALENGWA-KASEMPA AREA, ZAMBIA, 70 4.1.3.1 Introduction, 70 4.1.3.2 Sampling, 71 4.1.3.3 Geoc hemis try, 71 4.1.3.4 Analysis of independent samples by element s , 79 4.1.3.5 Analysis by source area, 80 4.1.3.6 Kalengwa Area, 80 4.1.3.6.1 Samples, 80 4.1.3.6.2 Geoc hronolog y, 81 4.1.3.6.3 Environmen t of emplacement, 81 4.1.3.7 Kasempa Area, 81 4.1.3.7.1 Boreho le MB-34, 81 4.1.3.7.2 Mufwas hi and Chitampa Boreho les, 81 4.1.3.7.3 Geoc hronolog y, 82 4.1.4 NORTHWESTERN ZAMBIA DOMAIN, 83 4.1.4.1 Introduction, 83 4.1.4.2 Kalene Hill Area, 84 4.1.4.2.1 Geoc hemis try, 84 4.1.4.2. 2 Descript i o n of the various groups, 84 4.1.4.2.2.1 Group 1, 84 4.1.4.2.2.2 Group 2, 84 4.1.4.2.2.3 Group 3, 94 4.1.4.2.2.4 Group 4, 94 4.1.4.2.3 Analysis of indepe n d e n t samples by element s , 94 4.1.4.2.4 Geoc hronolog y, 94 4.1.4.2.5 Environmen t of emplacement, 95 4.1.4.2. 6 Conc lusi o ns , 95 table of contents (cont.) x 4.1.4.3 Introduction to the geology of the Domes Region, NW Zambia, 96 4.1.4.4 Kabompo Dome, 97 4.1.4.4.1 Introduction, 97 4.1.4.4. 2 Descript i o n of sample s collected in the field, 97 4.1.4.4. 2 . 1 Samples L-028 and L-029, 97 4.1.4.4.2.2 Sample L-030, 98 4.1.4.4. 2 . 3 Samples L-047 and L-048, 100 4.1.4.4 . 3 Conc lus i o ns , 103 4.1.4.5 Mwombezhi Dome, 104 4.1.4.5.1 Introduction, 104 4.1.4.5. 2 Lumwana copper mineraliz ation, 104 4.1.4.5.3 Mafic volcan ics from Shilenda, 106 4.1.4.5.4 Chitungulu sodalite syenite, 107 4.1.4.5.4.1 Introduction, 107 4.1.4.5.4.2 Sampling, 107 4.1.4.5.4.3 Description of the rocks, 107 4.1.4.5.4.4 Weathe ring , jointing and pr oblematic structures for mining, 107 4.1.4.5.4.5 Geoc hemis try, 110 4.1.4.5.4.6 Environmen t of emplacement, 113 4.1.4.5.4.7 Geoc hronolog y, 114 4.1.4.5. 4 . 8 Conc lusi o ns , 114 4.1.4.6 Solwezi Dome, 115 4.1.4.6.1 Introduction, 115 4.1.4.6.2 Sampling, 115 4.1.4.6.3 Samples from the Solwezi Dome, 115 4.1.4.6.4 Geoc hronolog y, 116 4.1.4.6.5 Samples from East of Solwez i, 118 4.1.4.6 . 6 Conc lus i o ns , 118 4.1.4.7 Conclusions on the entire NW Zambia Region, 118 4.1.5 ZAMBIAN COPPERBELT, 121 4.1.5.1 Introduction, 121 4.1.5.2 Nchanga Granite, 127 4.1.5.2.1 Introduction, 127 4.1.5.2.2 Sampling, 127 4.1.5.2.3 Main rock types, 128 4.1.5.2.4 Samples P-28 and P-29, 128 4.1.5.2.5 Samples from Chiwempa la Hill, 130 4.1.5.2 . 6 Gray?s quarry, 131 4.1.5.2 . 7 Various dikes, 132 4.1.5.2.8 Geoc hemis try, 132 4.1.5.2.9 Anorogenic charac te r of the Nchanga Granite, 135 4.1.5.2 . 1 0 Conc lus i o ns , 136 4.1.5.3 Nchanga mine area, 137 4.1.5.3.1 Introduction, 137 4.1.5.3.2 Comparis on of gabbroid rocks,138 4.1.5.3 . 3 Nchanga lamproph y r e dike, 138 4.1.5.3.4 Samples with spec ial character, 139 4.1.5.3.5 Geoc hronolog y, 139 4.1.5.3 . 6 Conc lus i o ns , 139 4.1.5.4 Muliashi Porphyry, 140 4.1.5.4.1 Introduction, 140 4.1.5.4.2 Sampling and compos ition of samples, 140 4.1.5.4. 3 Descript i o n of samples, 141 4.1.5.4.4 Geoc hronolog y, 141 4.1.5.4.5 Discussion on the Muliashi Porphyr y and its correla t i v e s , 141 4.1.5.5 Deep borehole, Konkola mine, 144 4.1.5.6 Chambishi Granite, 148 4.1.5.6.1 Introduction, 148 4.1.5.6.2 Geoc hemis try, 148 4.1.5.6 . 3 Chambis h i gabbroid rocks, 150 4.1.5.6.4 Geoc hronolog y, 151 4.1.5.6.5 Environmen t of emplacement, 151 4.1.5.6.6 Conc lusion, 151 table of contents (cont.) xi 4.1.5.7 Mufulira Granite, 152 4.1.5.7.1 Introduction, 152 4.1.5.7.2 Sample description and geochemistr y, 152 4.1.5.7.3 Geoc hronolog y, 153 4.1.5.7.4 Discussion, 153 4.1.5.8 Samba Deposit, 155 4.1.5.8.1 Introduction, 155 4.1.5.8.2 Sampling and geochemis try, 155 4.1.5.8.3 Geoc hronolog y, 157 4.1.5.8.4 Discussion, 157 4.1.5.9 Conclusions on granitoids from the Zambian Copperbelt, 158 4.1.5.9.1 General conclusions, 158 4.1.5.9 . 2 Tectonic envir on m ent of emplacemen t, 158 4.1.5.9.3 Mineralization, 158 4.1.5.9.4 Lithologic correlation, 159 4.1.5.9. 5 Stratigr a ph i c relations , 159 4.2 NAMIBIAN DOMAINS, 163 4.2.1 KAMANJAB BATHOLITH, 163 4.2.1.1 Introduction, 163 4.2.1.2 Geoc hemis try, 164 4.2.1.3 Main Rock Suites, 173 4.2.1.3.1 Examples of rock suites , 173 4.2.1.3.1.1 Suite B, 173 4.2.1.3.1.2 Suite E, 173 4.2.1.3.1.3 Suite G, 174 4.2.1.3.1.4 Suite H, 174 4.2.1.3.1.5 Suite J, 177 4.2.1.3.1.6 Suite K, 177 4.2.1.3.1.7 Suite M, 177 4.2.1.4 Sample grouping, 179 4.2.1.4.1 Quartz monzon ites, 179 4.2.1.4.2 Alkali granites, 181 4.2.1.4.3 Granites, 182 4.2.1.4.4 Syenites, 183 4.2.1.4 . 5 Gabbroi d rocks, 183 4.2.1.4 . 6 Rocks that co uld not be classif i ed into above groups, 184 4.2.1.5 Volcanic rocks, 184 4.2.1.6 Environmen t of emplacement, 200 4.2.1.7 Evidence of magma mixing -mag ma mingling, 200 4.2.1.8 Granitoid s sampled by Tom Clifford , 201 4.2.1.9 Geoc hronolog y, 201 4.2.1.1 0 Some copper- m i n er a l iz e d syst ems in the Kamanjab Batholith, 206 4.2.1.11 Discussion, 208 4.2.1.12 Gelbingen farm, 209 4.2.2 KHORIXAS INLIER, 211 4.2.2.1 Introduction, 211 4.2.2.2 OAS FARM, 213 4.2.2.2.1 Introduction, 213 4.2.2.2.2 4-km long N-S trans ec t across Oas Syenite, 213 4.2.2.2.3 Geoc hemis try, 219 4.2.2.2. 4 Zinc enrichme n t , 229 4.2.2.2.5 Quartz ite from Oas farm that might host mineraliz ation,235 4.2.2.2.6 Geoc hronolog y, 235 4.2.2.2.7 Environmen t of emplacement, 236 4.2.2.2 . 8 Conc lus i o ns , 236 table of contents (cont.) xii 4.2.2.3 LOFDAL FARM, 237 4.2.2.3.1 Introduction, 237 4.2.2.3.2 Geoc hemis try, 237 4.2.2.3.3 Descripti on of outcrop s from the Lofdal farm, 238 4.2.2.3.3.1 Dissolution of s ilicates in granitoids, 238 4.2.2.3.3.2 Carbonatite di kes and iron oxide-c o pp e r - g o l d mineral iz a t i o n , 241 4.2.2. 3 . 3 . 3 Cross sectio n throug h se ries of ultramafic dikes, 244 4.2.2.3.3.4 Magnetite- cemented, polymi c t i c hydr oth e r ma l breccia that makes diatre me , 245 4.2.2.3.3.5 Abandoned Lofdal mine, 247 4.2.2.3.3.6 Carbon a t i t e dikes, 248 4.2.2.3.3.6.1 Introduction, 248 4.2.2.3.3.6.2 Geoc hemis try, 248 4.2.2.3. 3 . 6 . 3 Economic mineraliz a t i on in carbonat i t e dikes, 248 4.2.2.3.3.6.4 High-hea t production pr oper t i e s in some of the dikes, 249 4.2.2.3.4 Environmen t of emplacement, 250 4.2.2.3.5 Geoc hronolog y, 251 4.2.2.3 . 6 Conc lus i o ns , 251 4.2.3 OTHER SMALL OUTCROPS IN NAMIBIA AND BOTSWANA, 252 4.2.3.1 Introduction, 252 4.2.3.2 Mesopotamie, 252 4.2.3.2.1 Introduction, 252 4.2.3.2.2 Sampling and geochemis ty, 252 4.2.3.2.3 Environmen t of emplacement, 252 4.2.3.2.4 Geoc hronolog y, 259 4.2.3.2.5 Economic geology, 259 4.2.3.3 Summas Mountains, 260 4.2.3.3.1 Sampling and geochemis try, 260 4.2.3.3.2 Geoc hronolog y, 261 4.2.3.4 Ugab River outcrops, 262 4.2.3.4.1 Sampling and geochemis try, 262 4.2.3.4.2 Geoc hronolog y, 263 4.2.3.5 Okwa River Outcrops, Botswana, 264 4.2.3.6 Grootfontein Inlier, 265 4.2.3.6.1 Sampling and geochemis try, 265 4.2.3.6.2 Geoc hronolog y, 265 4.2.3.7 Environs of Otjiwarongo, Namibia, 266 4.2.3.7.1 Introduction, 266 4.2.3.7.2 Field description of main outrcrops, 266 4.2.3.7.3 Pegmat i t i c rocks, 270 4.2.3.7.4 Geoc hemis try, 273 4.2.3.7.5 Otjiwarongo Batholith, 274 4.2.3.7.6 Environmen t of emplacement, 274 4.2.3.7.7 Geoc hronolog y, 274 4.2.3.7.8 Discussion, 274 4.2.3.8 Review of observations from Mesopo tamie, Summas Mountains, Ugab River, Okwa River, Grootfontein Inlier and Otjiwarongo outcrops, 277 4.2.4 WITVLEI, NAMIBIA, 281 4 . 2 . 4 . 1 Introduc c io n , 281 4.2.4.2 Field observati o n s , 281 4.2.4.3 Description of the OP-1 borehole, Okatjepuiko Projec t, 284 4.2.4.4 Geoc hemis try, 284 4.2.4.5 Environmen t of emplacement, 291 4.2.4.6 Geoc hronolog y, 291 4.2.4.7 Other events of the same age in the region, 292 4.2.4.8 Evidence of iron oxide-copper-gold mineralization and definition of a mineralized belt, 292 4.2.4.9 Conc lus i o ns , 293 table of contents (cont.) xiii 5 THORIUM CONTENT OF GRANITOIDS IN THE GREATER LUFILIAN ARC, 303 5.1 Introduction, 303 5.2 High Thoriu m samples , 303 5.3 Values for high-heat generating gran itoids, 305 6 GEOCHRONOLOGY, 308 6.1 Introduction, 308 6.2 New radiometric ages, 308 6.3 Geochronological Database and Interpretation, 308 6.3.1 Event diagrams, 309 6.3.2 Compilation of event diagrams, 309 6.4 New Re-Os Ages from Copper Mineralization, Zambian Copperbelt, 312 6 . 4 . 1 Basic data, 312 6.4.2 Discussion, 312 6.4.3 Conc lus i o ns , 314 7 SOME ASPECTS OF ANOROGENIC INTRUSIVE ROCKS, 316 7.1 Intoduction, 316 7.2 Comparison of batholithic granitoid bodies with anorogenic ring complex clusters, 317 7.2.1 Introduction, 317 7.2.2 Nuba Mountains, Sudan, 318 7.2.3 Central Nigeria ring complexe s , 319 7.2.4 Kanye-Gaborone ring complexes, Botswana , 323 7.2.5 Comparis on of the three ring complex cluster s , 324 7.2.6 Model for the origin of batholithic-size granitoi d bodies in anoroge nic environ m en t s , 326 7.2.7 Ring complex clusters in the Greater Lufilian Arc, 329 7.2.8 Conc lus i o ns , 333 7.3 Comparison of Lufilian small basic intrusio ns with examples from the literature, 334 8 IRON OXIDE-COPPER-GOLD MINERALIZ ATION IN THE GREATER LUFILIAN ARC, 337 8.1 Introduction, 337 8.2 Some notes on iron oxide-copper-gold deposits, 337 8.3 Iron oxide-copper-gold systems in the Greater Lufilian Arc, 346 8.3.1 Relation ship between granitoids and iron oxides, 346 8.3.2 Iron oxide bodies, 349 8.3.3 Breccias , 351 8.3.4 Structural control, 353 8.3.4.1 Rock fractur in g to cont rol IOCG mineraliz ation, 353 8.3.4.2 E-W Structures, 354 8.3.4.3 Planar features of iron oxide bodies, 354 8.3.5 Particular hydr othermal alteration featur es , 357 8.3.5.1 Tourmaline alteration, 357 8.3.5.2 Quartz pods, 357 8.3.5.2.1 Description of QP, 357 8.3.5.2. 2 Four rock associat i on , 359 8.3.5.2. 3 Particles enclosed in QP, 359 8.3.5.2.4 Studies that can be done on QP, 360 8.3.5.2.5 Practical applications of QP, 360 8.3.5. 2 . 6 Hypoth es is about the origin of QP, 360 8.4 Some known IOCG-like deposits and prospects, 362 8 . 4 . 1 Namib ia n depos i ts and prospe c ts , 362 8.4.1.1 Okatjepuiko Prospect, Witvlei, 362 8.4.1.2 Kombat mine, Otavi Mountains, 363 8.4.1.3 Otjikoto gold deposit, 366 8.4.1.4 Mesopotamie farm, 366 8.4.1.4.1 Copper Valley mineraliz ation on the NW portion of Mesopo tamie 504, 367 8.4.1.4.2 Kruger?s deposit on the NW portion of Mesopotamie 504, 368 8.4.1.4.3 Mineralizati on on the NE portion of Mesopotamie 504, 369 8.4.2 Zambian deposit s and pros pec t s , 370 8.4.2.1 Evidence of IOCG mineral iz a t i o n under the Copper b e lt , 370 table of contents (cont.) xiv 8 . 4 . 2 . 2 Dunr obin gold mine, 370 8.4.2.3 Nampundwe pyrite mine, 374 8.4.2.4 Kasempa Region Pros pe cts , 374 8.4.2. 5 IOCG pros pec t s and mines ar ound the Hook Granite Batholith, 375 8.4.2.6 Kalengwa copper-silver mine, 377 8.4.3 Other Lufulian Arc IOCG prospect s and deposits , 379 8.4.3.1 Quartz ite-hosted deposits, Gelbingen farm, Namibia, 379 8.4.3.2 Deposits associated to alkali n e rocks and carbon a t i t e s , 383 8.4.3.3 IOCG Mineralization in t he Democratic Republic of Congo, 388 8.4.3.4 Active exploration in projec ts in the Greater Lufilian Arc, 390 8.5 Relationship between IOCG and sedimentary-hosted Cu mineralization, 391 8.6 Sedimentary-hosted Au mineralization in the Greater Lufilian Arc, 391 8.7 Peculiarities of Zambian and Namibian IOCG systems, 391 8.8 Conclusions, 392 9 CONCLUSIONS, 395 9.1 Main Granitoid Terranes in the Greater Lufilian Arc, 395 9.2 Polycyclic Geological Histor y, 395 9.3 Rock Types, 395 9.3.1 Mafic, Ultramafic and Alkaline Rocks, 398 9.3.2 Rock Associations in Anorogenic Environments, 398 9.3.3 Quartz Pods, 399 9.3.4 Iron Oxide Bodies, 399 9.3.5 Round-Pe b b le Hydroth e r ma l Breccia s , 399 9.4 Ring Complex Clus ters, 399 9.5 Tectonic Environment of Emplacement, 399 9.6 High Thorium, 400 9.7 Correlation of Granitoids, 400 9.8 Main Findings in Specific Domain s, 400 9.8.1 Hook Granite Batholith, Zambia, 400 9.8.2 Nchanga Granite, Zambia, 400 9.8.3 Kamanjab Batholith, Namibia, 400 9.8.5 New Tempor al Cons train to Katangan Sedimentation, 401 9.8.6 Khorixas Inlier-Kamanjab Batholith, 401 9.8.7 Long-Lived Frac tures, 401 9.9 Metallogeny, 401 9.9.1 Metallogenic Epoc hs , 401 9.9.2 Iron Oxide-Copper-Gold Mineralization, 404 9.9.3 Association of Sedimentar y-Hosted Copp er Mineralization with IOCG Mineralization, 404 10 REFERENCES, 404-428 10 APPENDICES (Paging in the Appendices volume is independent from the rest of the text) A Sample Maps, 127 B TAS Diagram for Suites of the Kamanjab Batholith, Namibia, 165 C Geoc hemis try Database, 1 D Geograph ic Coordin a t es of Samples Collect e d and Geologic a l Station s , 25 E Geochr onology Database, 41 F Geochron ological Event Diagrams , 67 G Tectonic Environent of Emplacement for Samples, 95 H Partial Transcription of Field Notes, 183 I Other Information, 222 J Raw Data for New Geoch r o no l o g y , 237 K Geochr ono l o g ic a l Correla t i o n Diagram s , 257 list of figures (cont.) xv LIST OF FIGURES 1.1 Definition of the study area area and te ctonic framew or k of Southern Africa, 2 2.1 TAS diagram modified by Middlemost, 1994, 1997, 7 2.2 Comparis on of the total alkali versus silica diagrams proposed by Middlemost, 1994 and by Wils on , 1989, 8 2.3 R1/R2 diagram of De La Roche et al, 1980, 9 2.4 The Q-P diagram, 11 2.5 The A-B diagram, 11 2.6 The QBF diagram, 11 2.7 The K*-B diagram, 11 2.8 The Mg*- B diagram, 11 3.1 Schematic structural map of Gondwana, 21 4.1 General map of the Hook Granite Batholith, 24 4.2 Correla t i o n diagrams betwee n silica and the major oxides for sample s from the Hook Granite Batholith, Zambia, 26 4.3 Enlargement of TAS diagram for Hook Granite Batholith, 28 4.4 TAS diagram for Hook Granite Batholith, 29 4.5 Enlargement of R1/R2 diagram for Hook Granite Batholith, 30 4.6 R1/R2 diagram for Hook Granite Batholith, 31 4.7 Type I, Logarithmic major oxide plot, Hook Granite Batholith, 32 4.8 Type II, Logarithmic major oxide plo t, Hook Granite Batholith, 33 4.9 Type III, Logarithmic major oxide plo t, Hook Granite Batholith, 33 4.10 Type IV, Logarithmic major oxide plot, Hook Granite Batholith, 33 4.11 Type VII, Logarithmic major oxide pl ot, Hook Granite Batholith, 34 4.12 Type IX, Logarithmic major oxide plot, Hook Granite Batholith, 34 4.13 Type X, Logarithmic major oxide plot, Hook Granite Batholith, 35 4.14 Type XI, Logarithmic major oxide plot, Hook Granite Batholith, 35 4.15 Compilation of geology for the Hook Granite Batholith, 38 4.16 Structural interpretation of Zambian geology based on aeromagnetic data, 46 4.17 Sanabozi proc es sed airborne geophysical image, Hook Granite Batholith, Namibia overlain by samples collected, 47 4.18 Anorog e n ic ring struct ur es that can be ident ifi e d in the Sanabozi geophysic a l image, Hook Granite Batholith, Zambia, 48 4.20 Logarit h m ic major oxide plot to compare Namibia n granito i d ring complex es with sample s from the Hook Granite Batholith, 52 4.21 R1/R2 diagram for Hook Granite Batholith compared to other anorogen ic ring comp le xe s , 53 4.21A TAS diagram comparin g Hook Granite Batholi t h with anoroge n ic ring comple x e s , 54 4.22 TAS diagram for samples collected along the E-W transect , Hook Granite Batholit h , 56 4.23 Hypothetical granitoid ring complex clus te r and transec t across it, 57 4.24 Schematic repres entation of the various event s that gave rise to the curren t geology of the Hook Granite Batholith, 58 4.1.2.1 TAS diagram West Lusaka-Kafue Flats, Zambia, 63 4.1.2.2 R1R2 diagram , West Lusaka - Ka f u e Flats, Zambia , 64 4.1.2.3 Geolog ical map of the Lusaka Granite, 66 4.1.2.4 Photogr a p hs of slabs from red- alt e r e d grani toids in the Kafue Flats area, Zambia, 67 4.1.3.1 Geolog i c a l interpr e t a t i o n of airbor n e magneti c image for northwes te r n Zambia, 70 4.1.3.2 TAS diagram Kalengwa-Kas empa Area, Zambia, 73 4.1.3.3 R1R2 diagram, Kalengwa-Kasempa Area, Zambia, 74 4.1.3.4 Q-B diagram, Kalengwa-Kasempa Area, Zambia, 75 4.1.3.5 Q-P diagram, Kalengwa-Kasempa Area, Zambia, 76 4.1.3.6 K-B diagram, Kalengwa-Kas empa Area, Zambia, 77 4.1.3.7 Mg-Fe- B diagram, Kalengwa-Kas empa Area, Zambia, 78 4.1.3.8 Photos of red- altered, subvol c an i c porphyr i t i c grani t o id s that were dated; borehole MB- 34, Chitampa, Kasempa area, Zambia, 82 list of figures (cont.) xvi 4.1.4.1 TAS diagram NW Zambia, 86 4.1.4.2 R1R2 diagram , NW Zambia , 87 4.1.4.3 Q-B diagram, NW Zambia, 88 4.1.4.4 Q-P diagram, NW Zambia, 89 4.1.4.5 K-B diagram, NW Zambia, 90 4.1.4.6 Mg-Fe- B diagram, NW Zambia, 92 4.1.4.7 General iz e d geolog i c a l map of the domes region in Zambia, 96 4.1.4.8 Genera l aspect of the outcro p where sa mple s L-029 and L-030 were collec t ed , 98 4.1.4.9 Main aspects of the outcrop wher e sample L-030 was collected, 98 4.1.4.10 Detail of the foliation and mineral banding of the rock that intersec t at around 5-8 degrees, 99 4.1.4.11 Simpli f i e d region a l geolog y and interpr e te d strati gr ap hic relati on s of the souther n site of the the Kabompo Dome, 102 4.1.4.12 Geolog ical map with location of sample L-047, Kabompo Dome, Zambia, 101 4.1.4.13 Photogr a p hs of slabs, samples L-047* and L-048, 100 4.1.4.14 Cross section of the Malundw e Cu deposit at Lumwana , Zambia, 104 4.1.4.15 Photogr a p hs of hand samples and slabs fr om the Shilenda mafic volcan ics, 106 4.1.4.16 Rough map of sodalite syenite quarry, NW Zambia , 108 4.1.4.17 Photog r a p hs of slabbe d syenit e s from the Ch itungulu sodalite syenite quarry, Zambia, 109 4.1.4.18 TAS diagram sodalite syenite quarry, NW Zambia , 111 4.1.4.19 R1R2 diagram , sodalit e syenite quarry, NW Zambia, 112 4.1.4.20 Major oxide logari t hmi c plot for samples from the Chitungulu sodalite syenite quarry, 114 4.1.4.21 intrusive relationships between the different fa cies of sodalite syenites observed at the quarry, 109 4.1.4.22 Geolog i c a l map and cross sections to locate boreho l es from the environ s of the Kansan shi deposit, Solwes i, Zambia, 117 4.1.4.23 Photogr a p hs of slabs from the sample s that make L-063, 118 4.1.5.1 TAS diagram Basement to the Copperbelt, Zambia, 122 4.1.5.2 R1R2 diagram, Basement to the Copperbe l t , Zambia, 123 4.1.5.3 A-B diagram, Basement to the Copperbelt, Zambia, 124 4.1.5.4 K-B diagram, Basement to the Copperbelt, Zambia, 125 4.1.5.5 Mg-Fe- B diagram, Basement to the Copperbe lt, Zambia, 126 4.1.5.6 W-E geolog ic a l cross sectio n of undergr ound exposure of the Nchanga Granite, 127 4.1.5.7 Geolog i c a l cross sections through the Nchanga Granite , 130 4.1.5.8 Geolog ical map of the Nchanga Granite, 131 4.1.5.9 Photograph of Nchanga Granite inselberg at the Chiwempala Hill, Zambia, 129 4.1.5.10 Logarith m ic scale plot of major oxides to compar e Nchanga Granite with Nigerian and Namibia n granito i d ring complex e s , 133 4.1.5.11 Logarit h m ic scale plot of minor elements and rare earths to compare Nchanga Granite with Nigerian and Namibian granitoid ring complexes, 134 4.1.5.12 Second logarith m i c scale plot of minor elements and rare earths to compare Nchanga Granite with Nigeria n and Namibia n granito i d ring complex e s , 134 4.1.5.13 WSW-ENE Schematic geological cross secti on throgh the Nchanga Granite along the Nchanga mine, Zambia, 138 4.1.5.14 Main features of the Muliashi Por phyry as observed on outcrops, 142 4.1.5.15 Photographs of slabs from the Muliashi Po rphyry, basement to the Copperbe lt, Zambia, 143 4.1.5.16 Surface geological map of the Konkola Dome and Nchanga Area, Zambia, 145 4.1.5.17 Stratigraphic column of explorator y Konk ola Deep Borehole, Zambia , 146 4.1.5.18 Geolog ical map of the Chambishi-Nkana basin, Zambia , 149 4.1.5.19 Stratig r a ph y of drillho l e into Chambis h i gabbros and ganophy r es , 150 4.1.5.20 Undergr ou n d cross sectio n of the Mufuli r a or ebody in relation to the basement highs, 152 4.1.5.21 Geolog ical map of the Mufulira mine environs, Zambia , 153 list of figures (cont.) xvii 4.1.5.22 Cross section of the basemen t of the Mufulir a mine area, 154 4.1.5.23 Generaliz e d geolog ic a l map of the Samba copper deposit in the basement to the Copperbelt, Zambia, 156 4.1.5.24 Eastern borehole - c on t r o l l ed geol og ical cross section, Samba copper deposit, Zambia, 156 4.1.5.25 Western borehol e - c on t r o l l ed geol og ical cross section, Samba copper deposit, Zambia, 156 4.1.5.26 Main stratig r ap h i c relatio ns h i p s betwee n ro ck units in the main Copperbe lt area, Zambia, 159 4.2.1.1 Entire TAS diagram Kamanjab Batholith, Namibia, 167 4.2.1.2 Enlargement of main portion , TAS diagram Kamanjab Batholith, Namibia, 168 4.2.1.3 Entire R1R2 diagram Kamanjab Batholith, Namibia, 169 4.2.1.4 Enlargement of main portion , R1R2 diagram Kamanjab Batholith, Namibia, 170 4.2.1.5 Correla t i o n diagrams betwee n silica and the major oxides for sample s from the Kamanjab Batholith, Namibia, 174 4.2.1.6 General iz e d location of dated samples and geochem ic a l suites in the Kamanja b Batholith, Namibia,175 4.2.1.7 Logarithmic scale plot of major oxides for Quar tzmo nzonite Group, Kamanjab Batholith, Namibia, 185 4.2.1.8 Logarithmic scale plot of major oxides for Alkali Granite Group, Kamanjab Batholith, Namibia, 186 4.2.1.9 Logarithmic scale plot of major oxides fo r Granite Group, Kamanjab Batholith, Namibia, 187 4.2.1.10 Logarithmic scale plot of major oxides for Syenite Group, Kamanjab Batholith, Namibia, 188 4.2.1.11 Logarith m ic scale plot of major oxides for Gabbroid Group, Kamanjab Batholith, Namibia, 189 4.2.1.12 Logarith m ic scale plot of major oxides for Unclassi f i ed Group, Kamanjab Batholith , Namibia, 190 4.2.1.13 Logarit h m ic scale plot of trace elements and rare earths for Quartzm o n z o n i t e Group, Kamanjab Batholith, Namibia, 190 4.2.1.14 Logarith m ic scale plot of trace elements and rare earths for Alkali Granite Group , Kamanjab Batholith, Namibia, 191 4.2.1.15 Logarit h m ic scale plot of trace elements and rare earths for Granite Group, Kamanja b Batholith, Namibia, 192 4.2.1.16 Logarith m ic scale plot of trace elements and rare earths for Syenite Group, Kamanjab Batholith, Namibia, 193 4.2.1.17 Logarit h m ic scale plot of trace elements and rare earths for Gabbroi d Group, Kamanjab Batholith, Namibia, 194 4.2.1.18 Logarit h m ic scale plot of trace elements and rare earths for Unclass i f i e d Group, Kamanjab Batholith, Namibia, 195 4.2.1.19 Photos of samples from Kamanjab Suite G, 178 4.2.1.20 Photos of samples from Kamanjab Batholith Suite J, 178 4.2.1.21 Photos of rocks with ?fuzzy? texture, Kamanjab Batholith, 177 4.2.2.1 Recona issanc e map of a syenite ring complex clus ter in the Oas farm, Namibia - Main portion of the N-S transect across the Oas Mountains, 215 4.2.2.2 TAS diagram Khorixas Inlier, Namibia, 220 4.2.2.3 Enlargement of main portion , TAS diagram Khorixas Inlier, Namibia, 221 4.2.2.4 R1R2 diagram, Khorixas Inlier, Namibia, 222 4.2.2.5 Enlargement of main portion , R1R2 diagram, Khorixas Inlier, Namibia, 223 4.2.2.6 Q-P diagram, Khorixas Inlier, Namibia, 224 4.2.2.7 Enlargement of main portion , Q-P diagram, Khorixas Inlier, Namibia, 225 4.2.2.8 Mg-Fe- B diagram, Khorixas Inlier, Namibia, 226 4.2.2.9 QBF diagram, Khorixas Inlier, Namibia, 227 4.2.2.10 Logarith m ic major oxide plot for the Syenite s A and Syenites B groups in the Oas farm, Loftal farm and Ojtiwarongo environs, Namibia, 232 list of figures (cont.) xviii 4.2.2.11 Logarit h m ic trace element plot for the Sy enite s A and Syenite s B groups in the Oas farm, Loftal farm and Ojtiwarongo envir on s, Namibia, 232 4.2.2.12 Field relations h i ps of minerali z e d quartzit e s at the Oas farm, Namibia, 235 4.2.2.13 Generalized map of the Lofdal farm showing geological stations, 239 4.2.2.14 Map of geolog ical stations and sampling, Lofdal farm, Namibia, 240 4.2.2.15 Cross secti o n throu g h mafic and ultra m af ic dikes, Lofda l farm, Namibia, 244 4.2.2.16 Photograph of a slabbed carbonatite dike from the Lofdal farm, Namibia, 241 4.2.2.17 Photogr a p h of a carbona t i t e dike with subpar allel internal zoning and magnetite, 242 4.2.2.18 Clos e-up view of a magnetite-rich massive carbonatite body, Lofdal farm, Namibia, 243 4.2.2.19 Photogra p h of two subparal l e l carbona t i t e dikes, 243 4.2.2.20 Sample map, carbonatite diatreme at Lofdal farm, Namibia, 246 4.2.2.21 Large fans of elongated amphibole crys tals in an ultramafic dike, Lofdal farm, Namibia, 247 4.2.2.22 Major oxide logarit hmi c plot of carbona t ite samples, Lofdal farm, Namibia, 249 4.2.3.1 TAS diagram of the Ugab River-Summas Mountains-Okwa River-Grootfontein Inlier, Namibia and Botswan a , 254 4.2.3.2 R1R2 diagram of the Ugab River-Summas Mountains-Okwa River-Grootfontein Inlier, Namibia and Botswan a , 255 4.2.3.3 Sample map of the Mesopo tamie farm, Namibia, 257 4.2.3.4 Map of geolog ical stations and sampling, Mesopotamie farm, Namibia, 258 4.2.3.5 TAS diagram Otjiwarongo-Grootfontein Inlier, Namibia, 267 4.2.3.6 R1R2 diagram, Otjiwarong o - Gr oo t f o n t e i n Inlier, Namibia, 268 4.2.3.7 Enlargement of main portion , R1R2 diagram, Otjiwar ongo-Grootfontein Inlier, Namibia, 269 4.2.3.8 Photograph of granitoid inselbergs on t he road Okahand j a - O t j i w ar on g o , Namibia, 266 4.2.3.9 Photogr a p hs of slabs from sample s L807 and L-811, 272 4.2.3.10 Photogra p hs of granitic pegmatit e s fr om the Otjiwarongo Batholith, 272 4.2.4.1 TAS diagram Okatjepuiko, Witvlei, Namibia, 289 4.2.4.2 R1R2 diagram, Okatjepu iko, Witvlei, Namibia, 286 4.2.4.3 QBF diagram, Okatjepuiko, Witvlei, Namibia, 287 4.2.4.4 Map of geolog ical stations and sampling at t he Okatjepuiko site, Witvlei, Namibia, 289 4.2.4.5 Logarithmic major oxide plot, granitoid samples, Ok atjepuiko prospect, Witvlei, Namibia, 290 4.2.4.6 Logarithmic trace element plot, granitoid samples, Okatjepuiko pros pect, Witvlei, Namibia, 290 4.2.4.7 Photo 1. Trap rock breccias from 18.2- 22 .0 m; borehole OP-1, Okatjepuiko, Witvlei, Namibia. 4.2.4.8 Photo 2. Enlargement with detail at 19.77 m; borehole OP-1, Okatjepuiko 4.2.4.9 Photo 3. Volcanic rocks with vacuoles and dense veinlet network, borehole OP-1 4.2.4.10 Photo 4. Close-up of Fig 4.2.4.8. Details of pink zeolites (?) and very thin white veinlets; borehole OP-1 4.2.4.11 Photo 5. Beginning of hydrotherma l breccia t i o n , 33-34 m; borehole OP-1 4.2.4.12 Photo 6. Close-up of photo 5, c entered on letter M; borehole OP-1 4.2.4.13 Photo 7. Breccia with abundant chlorite t hat fills open spac es and veinlets, after 34m; borehol e OP-1 4.2.4.14 Photo 8. 4 core fragments, marked with different alteration types; borehole OP-1 4.2.4.15 Photo 9. Beginning of the pink granitoid 54-57 m; borehole OP-1 4.2.4.16 Photo 10. Clos e-up of photo 9, on t he pink granitoid; borehole OP-1 4.2.4.17 Photo 11. Breccia with angular fragmen ts of volcanic rock (68, 69 and 70 m); borehol e OP-1 4.2.4.18 Photo 12. Intrusive rock in the middle li ne of core, surrou n de d by dark volcan i c trap rocks; borehole OP-1 4.2.4.19 Photo 13. Core showing angular fragment s of pink granitoi d within dark gray trap rock, 73-75 m; borehole OP-1 4.2.4.20 Photo 14. Core fragmen t s from 79-82 m; borehole OP-1 list of figures (cont.) xix 4.2.4.21 Slabs of strong ly hematitized polymictic hy droth er m a l breccias from Samples L-644 and L-645 6.4.1 Re-Os ages calcula t e d by Joaqu?n Ruiz and collabo rators at the University of Arizona, 313 6.4.2 Event diagram for three copper mineraliz i n g period s in the Greater Lufilian Arc, 315 7.1 Schematic cross section of the Wonji Fault Belt: an example of a tectomagmataic belt in a continental rift, 316 7.2 Alkaline intr us ions of the SW Nuba Mountains, 319 7.3 Event diagram for intrus ions from the SW Nuba mountains, Sudan, 318 7.4 Sketch map of cluster of anoroge n ic ring comple x e s in centra l Nigeria , 321 7.5 Event diagram graph for ring complex es in Central Nigeria , 322 7.6 Botsalano ring complex and other possible ring intr usions in the Gaborone-Kanye igneous terrane, Botswana and South Africa, 323 7.7 Event diagram for Gaboron e anoroge n ic ring complex cluster, Botswana/South Africa, 324 7.8 Scheme of what might have taken place to produce one of the granito i d ring complex clus ters identified in the Greater Lufilian Arc, 272 7.9 Comparis on of event diagrams from three anorogen ic ring complex clusters , 325 7.10 Comparis on of the outlines of various ring complex clusters , 328 7.11 Event diagram of Anorogenic Complex Clus te r period s in the Greate r Lufili a n Arc, 330 7.12 Comparis on of event diagrams from various anorogenic ring comple x clusters from the Greater Lufilian Arc, 331 7.13 Sketch map of basalt, trachyte and phonolite plug s of the Filiya area in eastern Nigeria, 334 8.1 Cartoon to illustrate the development pr ocess of an iron oxide- copper-gold system, 337 8.2 Generalized geolog ical map of the Salobo Deposit, Caraj?s, Brazil, 338 8.3 Simplified geoche mical log of borehole ALM-FD 09, from the Alem?o deposit, Caraj?s, Brazil, 340 8.4 Examples of hydrothermal alteration zonation in IOCG deposits formed in volcanic and plutonic host rocks, 341 8.5 Examples of hydrothermal alteration zonation in IOCG deposits formed in sedimentary sequ e nc es , 341 8.6 Geolog ical Map of the Kamanjab Batholith, Namibia, 344 8.7 Iron oxide- coper-gold prospects and deposits, Greater Lufilian Arc, 345 8.8 Quartz bodies, gabbros, felsic gr anitoids and iron oxide bodies that outcrop together east of Solwes i, Zambia, 347 8.9 Quartz body and metamo r p h os e d gabbros that outcrop together to the norteas t of Mwinilunga, Zambia, 347 8.10 Young gabbroic bodies that intersec t all rock types to the northeas t of Solwes i, Zambia, 348 8.11 Quartz bodies , gabbros and felsic granito i d s bodies that outcrop togethe r east of Solwes i, Zambia, 348 8.12 Hill of massive magnetite that outcr ops west of Lusaka, Zambia, 348 8.13 Magnetite ?dis ease? in a felsic granitoid t hat is very light pink when fresh, 350 8.14 Hematite ?disease? that overpr ints a polymicti c hydrothe r ma l breccia, 350 8.15 Progressive ?red-rock? hydr othermal alte rat i o n in round-p eb b l e hydroth e r ma l breccia , 351 8.16 Typical features of polymictic, r ound-pebble hydrothermal breccia, 352 8.17 Aspect of poly-br ecc i a t e d polymic t i c ro und-pe b b le hydroth er m a l breccia , 352 8.18 Typical angular stockwork mineralization in a foliated granitoid host rock, 353 8.19 Typical irregular stockwork mineralizati on in a felsic non-foliated granitoid, 353 8.20 Schematic geological section across the s outheast margin of Kasumbalesa Hill, Zambia, 355 8.21 Stratiform body of magnetite in the Kasempa area of Zambia, 356 8.22 Cross section of stratif o r m body of magn etite at the Kantonga IOCG deposit, Zambia, 356 list of figures (cont.) xx 8 . 2 3 Quartz pod outcrops observed in the Greater Lufilian Arc, Zambia and Namibia, 358 8.24 Types of quartz pod outcrop s observ e d during field work, Greater Lufilian Arc Granitoid Projec t, 357 8.25 Sediment ar y bedding and/or foliatio n that bends around quartz pods , 359 8.26 Various featur es of iron oxides in quartz pods of the Lufilia n Arc, 361 8.27 Schemati c diagram to show proc ess of quartz pod formatio n , 360 8.29 Geolog ical map of the Witvlei site, and loca tion of the Okatjepuiko IOCG pros pect, 362 8.30 Typical mineralization at the Kombat Cu mine, Namibia, 365 8.31 Diagram taken from Deane (1995) to reinterpr e t origin of the Kombat mine, Namibia, 364 8.32 Undergr ou n d map that show s core of iron oxide bordered by copper mineraliz ation at the Kombat Mine, Namibia, 365 8.33 Simplified geological map of the Otjikoto gold deposit, Namibia, 366 8.34 Mineralized quartz pod with magnetite and chalcopyrite, 367 8.35 Minerali z e d samples from the Copper Vallei mi ne, Mesopotamie farm, Khorixas Inlier, Namibia, 368 8.36 Minerali z e d quartz-m ag n e t ite - s u l f i de veins at the Dunr obin gold mine, Zambia, 371 8.37 Progressive hydrothermal alteration ar ound minera l iz ed quartz - ma gn e t i t e - s u l f i d e veinlets at the Dunr obin gold mine, Zambia, 372 8.38 Conc en tr i c iron oxide banding around minera lized veinlets at the Dunr obin gold mine, Zambia, 373 8.39 Explanation diagram for Fig 8.37, 371 8.40 Geolog ical map around the Lusaka West area, Zambia, 374 8.41 Geolog ical Map NW of Mumbwa, Hook Gr anite Batholith Province, Zambia, 375 8.42 Generalized geolog y of the Kitumba prospe ct, Kafue Flats, Zambia , 377 8.43 Cross section and map of the Kalengw a mine open pit, Zambia, 378 8.44 Angular hydroth e r ma l breccias and the subvolc a nic, porph yritic, rhyolitic intrusive that is respon s ib l e for their format i o n , 379 8.45 Another aspec t of hydrothermal breccias cemented by massive magnetite from the Gelbingen farm, Namibia, 380 8.46 Sulfide - be a r in g hydrothe r m a l breccia - ve in cemented by magnetite that intrudes quartz i t e s , 380 8.47 Three clos e- up aspects of the mineral iz ed breccia s from the Gelbing e n farm, Namibia , 381 8.48 Another aspec t of sulfide- bearing hydrot h e r ma l breccia cemente d by magneti t e that intrud es quartz i t e s , 381 8.49 Network of Sulfide-be ar ing magnetite veins that form a stockwork in Pan African felsic granitoid s , 382 8.50 Aspect s of hydrot h er m a l brecci as associ ated to a diatreme body 450 m by 150 m in outcrop, 383 8.51 Another aspec t of hydrothermal brecci as cemented by massive magnetite, 384 8.52 Sulfide-bearing magnetite-hematite veins associated to ultramafic dikes, 385 8.54 Slab of magnetite-cemented angular polymic t i c hydroth e r ma l breccia , 385 8.55 Another aspect of round-pebble hydr othe rm a l breccias cemented by magnetit e , 386 8.56 Dense packing in round-pebble hydrothermal breccias associa t e d to IOCG systems in the Lufilian Arc, 386 8.57 Angular fragment s in a magnetite - c eme n t ed hydrothe rmal breccia from an IOCG mineralized body, 388 8.58 IOCG Mineraliz e d Frac tur e System, norther n Namibia, 387 8.59 General gravime t r i c map overlai n by selecte d samples and metal values , Tevrede property, north western Kamanjab batholith, Namibia, 390 9.1 Distrib u t i o n of rock types and compar a t ive co mpos ition of rock alkalinity in the Greater Lufilian Arc, 397 9.2 Composi t i on of the samples collect ed in the Greater Lufilia n Arc, 398 list of tables (cont.) xxi LIST OF TABLES 2.1 Laborat or i es wher e chemic a l analysis were carried out, 6 2.2 Threshold or notch values used in the Great er Lufilian Arc granitoid project for various elements and oxides, 13 2.3 Synthet i c table show ing the relatio ns h ips between main granitic petrogenetic types, their origins, and the geodynamic environment, 15 2.4 Princip a l mineral og i c a l , petrogr a p h ic a l and ch emical features of the main types of granitoid s , 15 2.5 Review of the main methodologies to stud y the tectonic environ ment of emplacement of granitoi d rocks, 16 2.6 Acronyms used to shor ten rock names (after the use of Debon & LeFort, 1983), 19 2.7 Acronyms for environment of emplacement te rms, diagrams of Maniar & Piccoli, 1989, 19 2.8 Acronyms for environment of emplac e me n t terms of mafic rocks, 19 2.9 Acronyms for environment of emplacement te rms, diagrams of Harris et al, 1986, 20 4.1 Geolog ic a l Domains sampled during the Greater Lufilian Arc Granitoi d Projec t, 25 4.1.1 Statistics of rock types in the suite of sa mples from the Hook Granite Batholith, 36 4.2 Groups of samples from the Hook Granite Batholith, based on major oxide chemis try and logarit h mic plots, 27 4.3 High Zn samples from the Hook Granite Batholith, Zambia, 27 4.4 Correla t i o n of mapped units for the Hook Gr anite Batholith, from published 1:100 ,000 geolog i c a l sheets , 37 4.5 Hook Granite Batholith rock types and environment of emplacement, 39 4.6 Chemic a l analyse s of Namibia n Mesozoic anoroge n ic comple x e s , 50 4.7 Rock group s from Namib i an Mesoz o ic anorog e n ic grani t o i d compl ex e s , 50 4.8 Comparative chemic al analysis from gran ite anorogenic ring comple x e s Hook Granite Batholith samples, 51 4.9 Analys i s of samples along E-W transec t acro ss the Hook Granite Batholith, Zambia, 55 4.10 Samples collect e d along the E-W transec t through the Kafue Park, Hook Granite Batholith, 55 4.11 List of samples sorted by rock type based on maps /field observations, Hook Granite Batholith, Zambia, 41 4.12 Samples from the E-W transect through the Kafue Park, Hook Granite Batholith, and corres po n de nc e with ring complexes from Fig SUCH and geologic a l map units, 56 4.13 Hook Granite samples that show similariti es with granitoid samples from Nigerian, Namib ia n and Corsic a n anorog e n ic ring comple x e s , 50 4.14 Radiom e t r ic ages for the Hook Granit e Bat holith published by Hans on et al, 1993, 57 4.1.2.1 Chemic al Analysis of samples from the West Lusaka-Kafue Flats Area, Zambia, 62 4.1.2.2 Rock types from the West Lusak a-Kafue Flats area, Zambia, 62 4.1.2.3 Basic geoc hem i s t r y and environ m en t of emplac e me n t for sample s from the West Lusaka-Kafue Flats, Zambia, 65 4.1.2.4 Statistics of rock types in samples from West Lusaka and Kafue Flats, Zambia, 65 4.1.2.5 Analysis of gossanous massive iron oxi de bodies , West Lusaka - Ka f u e Flats area, Zambia, 68 4.1.2.6 Samples with high Th values from the Kafue Flats, Zambia, 69 4.1.3.1 Chemic al Analysis of samples from the Kalengwa-Kas empa Area, Zambia, 72 4.1.3.2 Rock type statisti c s , sample s from Kalengwa and Kasempa region, Zambia, 71 4.1.3.3 Suites of samples from Kalengw a / K a s emp a and project i o n on various geoc hemi c a l diagrams, 79 4.1.3.4 Rock name, basic geochem i s t r y and environ m en t of emplac e me n t for sample s from the Kalengwa and Kasempa region , Zambia, 79 4.1.3.5 Chemic al Analisis , Kasempa Area, Zambia, 82 4.1.4.1 Roc k type statis tic s , from Northwes tern Zambia, 83 4.1.4.2 Partial roc k type statis tic s , from Northwes tern Zambia, 83 4.1.4.3 Chemic al Analysis of samples from the Kalene Hill Area, NW Zambia, 85 list of tables (cont.) xxii 4.1.4.4 Rock type statist i c s , from Kalene Hill samples , NW Zambia, 84 4.1.4.5 Samples from Kalene Hill sorted by groups and geochemi s tr y , 93 4.1.4.6 Kalene Hill groups of samples and their projec tion on various geochemical diagrams, 93 4.1.4.7 Rock name, basic geochem i s t r y and environ m en t of emplac e me n t for sample s from the Kabompo Dome, NW Zambia, 97 4.1.4.8 Resour c e s and Reserv e s at the Lumwan a Distri c t , Zambia , 105 4.1.4.9 Chemic al Analysis of the sodalite syenite quarry, Zambia, 110 4.1.4.10 Chemic a l char ac t er of sample s from the Sodalite Syenite Quarry, Zambia, 113 4.1.4.11 Tectonic envir onment of emplacemen t fo r sodalit e syenite quarry, Zambia, 113 4.1.4.12 Chemic al Analysis of samples from the Solwes i Dome, Zambia, 115 4.1.4.13 Rock name, basic geochem i s t r y and environ m en t of emplac e me n t for sample s from the Solwes i Dome, NW Zambia, 116 4.1.5.1 Statistics of rock types, basement to the Copperbe lt, Zambia, 121 4.1.5.2 Statistics of rock types, Nchanga Granite, Zambia, 128 4.1.5.3 Rock name, basic geochem i s t r y and environ m en t of emplac e me n t for sample s from the Nchanga Granite, Zambia, 128 4.1.5.4 Exchange in values for Na and K in chemical analysis of sample X-34, 132 4.1.5.5 Chemic a l analysi s of sample s from the Nchanga Gr anite and others in the basement to the Zambian Copperbelt, 132 4.1.5.6 Comparis on of chemical data from anorogenic ring complexes and the Nchanga Granite, 135 4.1.5.7 Borehole samples collected in the envir ons of the Nchanga open pit mine, Zambia, 112 4.1.5.8 Rock name and main geochem i c a l para meters of samples from the Nchanga mine, 112 4.1.5.9 Chemic a l analysi s from the Nchanga Mine environ s , 112 4.1.5.10 New SHRIMP U-Pb ages from the Copperbe l t area, Zambia, 139 4.1.5.11 Chemic al analysis of sample s from the Muliashi Porphyry, Basement to the Copperbelt, Zambia, 140 4.1.5.12 Chemic a l char act er is t i c s and environ m en t of emplacement for Muliashi Porphyry samples, Zambia, 141 4.1.5.13 Statistics of rock types, Muliashi Porphyry, Zambia, 140 4.1.5.14 Chemic al Analysis of samples from the deep borehole, Konkola mine, Zambia, 144 4.1.5.15 Data from borehole samples, Konkola Deep boreho le, Zambia, 144 4.1.5.16 Simplified log of exploratory Konkola Deep Borehole, Zambia, 146 4.1.5.17 Geolog ical history interpreted from the Konkola deep borehole, Zambia, 147 4.1.5.18 Chemic al analysis of sample s from the Chambish i copper mine envir ons , Zambia, 148 4.1.5.19 Statistics of rock types, Chambishi granite, Zambia, 148 4.1.5.20 Chemic a l char ac t er and enviro n m en t of emplac e me n t for sample s in the Chambis h i mine environs, Zambia, 150 4.1.5.21 Chemic a l analysi s of sample s from the ba sement to the Mufulira copper mine, Zambia, 152 4.1.5.22 Main details of analysed samples from the Samba copper deposit, basement to the Copperbelt, Zambia, 157 4.1.5.23 Regional correlat i o n of dated Paleopro te r o zoic granitoids in the Greater Lufilian Arc, 160 4.1.5.24 Original data, additional samples from the lit erature on Copperbe lt granitoids, Zambia, 161 4.1.5.25 Chemic a l char ac t er is t i c s and environ m en t of emplaceme n t for samples in the Basement to the Copperbelt, Zambia, 162 4.2.1.1 Chemic al Analysis, Kamanjab Batholith Area, Namibia, 165 4.2.1.2 Statistics of rock types, Kamanjab Batholith, Namibia, 173 4.2.1.3 Brief descrip tion of analysed sample s, Kamanjab Batholith, Namibia, 171 4.2.1.4 Kamanjab Batholith rock suites that are made by two or more rock types, 176 4.2.1.5 Chemic al Analysis of the Group of Quar tzmonzonites, Kamanjab Batholith, 180 4.2.1.6 Chemic al Analysis of the Group of Alkali Granites, Kamanjab Batholith, 181 4.2.1.7 Chemic al Analysis of the Group of Granites, Kamanjab Batholith, 182 list of tables (cont.) xxiii 4.2.1.8 Chemic al Analysis of the Group of Syenites, Kamanjab Batholith, 183 4.2.1.9 Chemic al Analysis of the Group of Gabbroids, Kamanjab Batholith, 183 4.2.1.10 Chemic al Analysis of the Group of uncla ssified samples, Kamanjab Batholith, 184 4.2.1.11 Comparis on of volcanic and plutonic rock types in the Kamanjab Batholit h , 184 4.2.1.12 Groups of samples from the Kamanjab Batholith based on chemical similarity, 198 4.2.1.13 Kamanjab rock suites with samples of non-an or o g en ic or subduct io n a l charact er , 200 4.2.1.14 Chemic al Analysis, Sample s analysed by C lifford, 1969; Kamanjab Batholith, Namibia, 201 4.2.1.15 Granitoid samples from the Kamanjab Batholith that were dated, 202 4.2.1.16 Hypothetic al correlation of the dated samp les, Kamanjab Batholith and Grootfontein inlier, Namibia, 203 4.2.1.17 Tentative correlation of t he various rock units in the Suites from the Kamanjab Batholith. Namibia, 204 4.2.1.18 Location of samples and geologic a l stations on the Kamanjab Batholith, Namibia, 205 4.2.1.19 Rock suites that show miner a l iz a tio n or hy drothermal alteration; Kamanjab Batholith, sorted by rock suite letter, 207 4.2.1.20 Compilation of data from mineraliz ed suites, Kamanjab Batholith, 208 4.2.1.21 Regional correlation of Paleoproterozoic Gr anitoids in the Greater Lufilian Arc, 210 4.2.2.1 Statistics of rock types, Khorixas Inlier, Namibia, 211 4.2.2.2 Comparis on of samples from the Khorix as Inlier and nearby Summas Mountain s , Namibia, 212 4.2.2.3 Chemic al Analysis of Samples from the Oas Farm, Namibia, 213 4.2.2.4 Main features of small syenitoid circular bodies found at the Oas farm, Namibia, 217 4.2.2.5 High heat produc in g rocks in the Oas fa rm, Namibia; estimated at 750Ma, 214 4.2.2.6 Statistics of rock types, Oas farm, Namibia, 219 4.2.2.7 Sample grouping, Oas farm, Namibia, 228 4.2.2.8 Correla t i o n matrix of sample s from the Oas ring comple x e s using the isoc on diagram and visual comparis on , 229 4.2.2.9 Comparis on of sample groups from various Namibia n regions , 233 4.2.2.10 Groups of sample s from various Namibia n regions , 230 4.2.2.11 Samples form the Oas farm ring comple x cluster that were dated , 235 4.2.2.12 Statistics of rock types, Lofdal farm, Namibia, 237 4.2.2.13 Chemic al Analysis of Samples from the Lofdal Farm, Namibia, 238 4.2.2.14 Main feature s of cross sect ion across mafic, ultramafic and carbon a ti t i c dikes, Lofdal farm, Namibia, 245 4.2.2.15 High heat produc in g rocks in the Lofdal farm, Namibia; estimated at 750Ma, 249 4.2.2.16 Chemis try of carbonatites and di kes, Lofdal farm, Namibia, 250 4.2.3.1 Chemic a l analysi s of sample s from the Mesopot a m i e farm, Namibia, 253 4.2.3.2 Chemic a l analysi s of sample s from the Summas Mountai n s , Namibia , 260 4.2.3. 3 Rock types and environ ment of emplacement for the Summas Mountains , Namibia, 260 4.2.3.4 Chemic al Analysis, Ugab River, Namibia, 262 4.2.3.5 Rock types and environ m en t of emplac eme n t for the Ugab River, Namibia, 262 4.2.3.6 Chemic al Analysis, Okwa River, Botswana, 264 4.2.3.7 Rock types and environ m en t of emplac eme n t for the Okwa River area, Botswana , 264 4.2.3.8 Chemic al Analysis, Grootfontein Inlier, Namibia, 265 4.2.3.9 Rock types and environ m en t of emplaceme n t for the Grootfontein Inlier, Namibia, 265 4.2.3.10 Chemic al Analysis, Otjiwar ongo environs, Namibia, 271 4.2.3.11 Chemic al Analysis, Otjiwar ongo pegmatites, Namibia, 270 4.2.3.12 Main details of samples from pegmatit ic granitoids , Otjiwarongo batholith, Namibia, 272 4.2.3.13 Statistics of rock types, Otjiw ar o n go environs , Namibia , 273 4.2.3.14 Rocks from differe n t regions that displa y very simiar major oxide and trace elemen t chemis try, 273 4.2.3.15 Tentative correlation table fo r samples from the environ s of Otjiwar on g o , Namibia, 274 4.2.3.16 Rock types and environ m en t of emplaceme n t for the environs of Otjiwarongo, Namibia, 275 list of tables (cont.) xxiv 4.2.3.17 Rock types and environ m en t of emplaceme n t for several Namibia n domains , 276 4.2.3.18 Groups of rocks from the Ugab-Okwa Domain compared with others in Namibia, 279 4.2.4.1 Descrip t i o n of OP-1 Borehol e , Ok atjepu iko, Project, Namibia, 283 4.2.4.2 Samples collecte d from borehole OP-1, Okatjepu ik o , Namibia, 284 4.2.4.3 Chemic al Analysis, Okatjepuiko, Witvlei, Namibia, 284 4.2.4.4 Statistics of rock types, Okatjepuiko envir ons, Witvlei, Namibia, 288 4.2.4.5 Comparis on of samples from the Okatjepuiko area, Namibia, 288 4.2.4.6 Chemis try of granitoid s from the Okatjepuiko Pros pect, Namibia, 290 5.1 High Thoriu m Values from Greater Lufilia n Arc Granito i d s , 303 5.2 Samples with simila r chemic a l signat ur e as Th-rich samples from the Kafue Flats, Zambia, 305 5.3 Heat product io n values for various high-hea t produc ing granitoid s , 306 5.4 High heat production capacity of Greater Lufilia n Arc intrusi v e rocks calc ula t e d at the time of emplac emen t, 307 6.1 New radio m etr i c ages, Great e r Lufili a n Arc - sorted by age, 310 6.2 New radiom etr i c ages, Greate r Lufili a n Arc - sorted by sample numbe r , 311 6.3 Events of magmatism identified in the Greater Lufilian Arc based on the new radiome t r ic ages obtain ed , 308 6.4 Events associated with three main copper mi neral iz i ng periods in the Greater Lufilia n Arc, 315 7.1 Radiome t r ic (Rb-Sr) ages from ring complex e s , SW Nuba Mountai ns , Sudan, 318 7.2 Radiom e t r ic (Rb-Sr ) ages from Nigeria n ring comple x e s , 322 7.3 Chemis t r y of biotite granites from Nigeria n anoroge n ic ring complex e s , 323 7.4 Geoc hro n o log i c a l data availab l e for Gaboron e anoroge n ic ring complex clus ter , Botswana and South Africa, 324 7.5 Compilation of ages from various ring complex clus ters in the Greater Lufilian Arc, 330 7.6 Compilat i o n of Anorogen i c Comple x Clus ter Periods in the Greater Lufilian Arc, 329 7.7 Geoc hronolog ical data from various ring comple x clus ters leveled to a common age, for compar is on , 332 8.1 Data for some iron oxide-c o p p er - g o l d deposit s , 343 8.2 Details of selecte d IOCG deposit s and pr ospects, Greater Lufilian Arc, Africa, 342 8.3 Discrete periods of iron oxide-co pp er - go l d mi neralization that took plac e in the Greater Lufilian Arc, 393 9.1 Rock type statis t i c s of all samples analys ed from the Greater Lufilian Arc, 396 9.2 Number of samples from each rock type for domains of the Greater Lufilian Arc, 396 9.3 Percent a ge s of each rock type for domai ns of the Greater Lufilian Arc, 397 9.4 Main metallog e n ic events observ ed - Greater Lufilian Arc, 402 9.5 Simplifi e d classific a t i o n of metallog en i c events in the Greater Lufilian Arc, 403 9.6 Periods of iron oxide-coppe r-gold mineraliz a t i on in the Greater Lufilian Arc, 404 list of appendices (cont.) xxv APPENDICES (all page numbers in Appendices volume) Abbreviated Table of Contents for the Appendices A Sample Maps, 120 B TAS Diagram for Suites of the Kamanjab Batholith, Namibia, 160 C Geoc hemis try Database, 1 D Geograph i c Coor dina t e s of Samples Collected and Geolog ic a l Stations , 25 E Geochronology Database, 41 F Geochronological Event Diagrams, 67 G Tectonic Environent of Emplacement for Samples, 95 H Partial Transcription of Field Notes, 183 I Other Information, 222 J Raw Data for New Geoc hr on o l o g y , 237 K Geoc hro n o log i c a l Correl a t io n Diagram s , 257 A SAMPLE MAPS M1 Key for Zambian Sample Maps, 121 M2 Sample map, Hook Granite Batholith, Zambia over 1:1'000,000 geological map, 122 M3 Sample map, Hook Granite Batholith, Zambia over 1:100,000 geologic a l sheets, 123 M4 Enlarged sample map, Hook Granite Bat holith, Zambia over 1:100,000 geological sheets , M5 Enlargement of sample, Hook Granite Batholith, northern portion, 124 M6 Enlargement of sample, Hook Granite Batholith, southern portion, 125 M7 Sample map of the Kafue Flats area, Zambia, 126 M8 Sample map, Kalengwa mine environ s, Zambia, 127 M9 Sample map, Kasempa environs, Zambia , 128 M10 Sample map, Kalene Hill and Kabompo Dome, NW Zambia, 129 M11 Sample map of Kalene Hill and environ s, NW Zambia , 130 M12 Sample map, Domes Area, Zambia, 131 M13 Sample map, Kabompo and Mwombezhi Domes, Zambia, 132 M14 Sample map SE of Mwinilunga, 133 M15 Sample map, Solwesi Dome environs, Zambia, 13 M16 Sample map of the Nchanga Granite, Zambia, 135 M17 Sample map of the Chambishi-Mufulira Area, Zambia, 136 M18 Sample map of the Serenje area, Zambia, 137 M19 Key for Namibian Sample Maps, 138 M20 Sample map of the Khorixas inlier and the Mesopotamie farm, Namibia, 139 M21 Sample map of the Oas and Lofdal fa rms, Khorixas Inlier, Namibia, 140 M22 Sample map of the Summas Mountains and Ugab River, Namibia, 141 M23 Sample map, Otjiwaron g o environs , Namibia, 142 M24 Clos e-up of sample map, Otjiw aro n go environs , Namibia, 143 M25 Sample map, Otavi Mountains, Namibia, 144 M26 Sample map, Witvlei environs, Namibia, 145 M27 Key for Kamanjab Batholith sample maps , Namibia, 146 M28 K-14 portion of sample map, Kamanjab Batholith, Namibia, 148 M29 K-15 portion of sample map, Kamanjab Batholith, Namibia, 149 M30 K-16 portion of sample map, Kamanjab Batholith, Namibia, 150 M31 K-17 portion of sample map, Kamanjab Batholith, Namibia, 151 M32 K-18 portion of sample map, Kamanjab Batholith, Namibia, 152 M33 K-19 portion of sample map, Kamanjab Batholith, Namibia, 153 M34 K-20 portion of sample map, Kamanjab Batholith, Namibia, 154 M35 K-21 portion of sample map, Kamanjab Batholith, Namibia, 155 M36 K-22 portion of sample map, Kamanjab Batholith, Namibia, 156 M37 K-23 portion of sample map, Kamanjab Batholith, Namibia, 157 M38 K-24 portion of sample map, Kamanjab Batholith, Namibia, 158 list of appendices (cont.) xxvi M 3 9 K-25 portion of sample map, Kamanjab Batholith, Namibia, 159 B TAS DIAGRAM FOR SUITES OF THE KAMANJAB BATHOLITH, NAMIBIA F 1 Suite A, 160 F2 Suite B, 160 F3 Suite C, 161 F4 Suite D, 161 F5 Suite E, 162 F6 Suite F, 162 F7 Suite G, 163 F8 Suite H, 163 F9 Suite I, 164 F10 Suite J, 164 F11 Suite K, 165 F12 Suite L, 165 F13 Suite M, 166 F14 Suite N, 166 F15 Suite P, 167 F16 Suite Q, 167 C GEOCHEMISTRY A1 Chemic al analysis of sample s from t he Greater Lufilian Arc sorted by region, 1 A2 West Lusaka-Kafue Flats, Zambia, 1 A3 Hook Granite Batholith, Zambia, 2 A4 Serenje, Zambia, 3 A5 Kalengwa-Kas empa Area, Zambia, 4 A6 Northw es tern Zambia Region Zambia , 5 A7 Kalene Hill, Archean rocks, Paleopr o t e r oz o ic Group 2, Paleopr o t e r oz o ic Group 3, Paleoproterozoic Group 4, Other sample s, 5 A7.1 Kabompo Dome, 5 A7.2 Solwesi Dome, 6 A7.3 Mwombez h i Dome, 6 A7.4 Sodalite Syenite Quarry, 6 A7.5 Shilenda, 6 A8 Basement to the Copperbelt, Zambia, 6 A8.1 Muliashi Porphyry, 6 A8.2 Chambish i mine area, 7 A8.3 Samba copper prospect, 7 A8.4 Nchanga Granite, 7 A8.5 Nchanga mine, 7 A8.6 Mufulira Granite, 7 A8.7 Other, 7 A9 Kamanjab Batholith, 8 A10 Felsic volcan ics, Namibia; Ugab River, Namibia; Okwa River, Botswana; Summas Mountains , Namibia, 10 A11 Oas farm, Namibia, 11 A12 Lofdal farm, Namibia; Mesopotamie farm, Namibia; other alkaline and gabbroic rocks, Khorixas , Namibia, 12 A13 Otjiwarongo environs, Namibia; Groo tfont ein Inlier, Otavi Mountains, Namibia; Okatjepuiko, Witvlei, Namibia, 13 A14 Spitskoppe complexes, Namibia; Erongo comple x, Namibia; Brandberg complex, Namibia ; Nigeri a n ring comple x e s , 14 A15 Chemical analysis from the Greater Lufilian Arc sorted by number, 15 list of appendices (cont.) xxvii D GEOGRAPHIC COORDINATES OF SAMPLES COLLECTED A16 Zambian sample s located on UTM zone 35, 24 A17 Zambian samples located using latitude and longitude (WGS84), 29 A18 Namibian samples that are located in UTM zone 33 (Schwartzeck), 30 A19 Namibian samples that are located in UTM zone 34, (Schwartzeck), 34 A20 Namibian samples that are located using latitude and longitude coordina t es (Schw ar t z eck) , 35 E GEOCHRONOLOGY A21 Compila t i o n of radiome t r ic ages, Greater Lufilia n Arc ? sorted by chronol og i c a l order, 38 A22 Compila t i o n of radiome t r ic ages, Greater Lufili a n Arc ? sorted by region and sites, 46 ZAMBIA A22.1 Hook Granite Batholith, Zambia, 46 A22.2 Northwes tern Zambia, Domes Area, 46 A22.3 Solwesi Dome Area, Zambia, 46 A22.4 Western Lusaka-Kafue Flats Area, Zambia, 46 A22.5 Kalengwa-Kas empa Area, Zambia, 47 A22.6 Mkus hi-Seren je Area, Zambia, 47 A22.7 Copperbelt region, Zambia , 47 A22.8 Mufulira Area, Zambia, 48 A22.9 Nchanga Area, Zambia, 48 A22.10 All Basement to the Copperbelt, Zambia (Compilation of Groups), 48 A22.11 Choma-Kalomo Batholith, Zambia, 48 A22.12 Irumde Belt, Zambia, 49 A22.113 Luangwa Valley, Zambia, 49 A22.14 Other Zambia, 50 NAMIBIA A22.15 True Kamanjab Batholith, Namibia, 50 A22.16 Khorixas Inlier, Namibia, 50 A22.17 All Kamanjab Area, Namibia, 51 A22.18 Witvlei Area and possible correlatives in the region, 51 A22.19 Central Namibia, 53 A22.20 Northe rnmost Namibia, 53 A22.21 Southernmost Namibia, 53 A22.22 Kaokoveld, Namibia, 53 A22.23 Rehoboth Inlier, Namibia, 54 A22.24 Namibr an d - Sa s r ie m Area, Namibia , 54 A22.25 Namaqua Metamor ph i c Complex , Namibia , 54 A22.26 ?Kibara n? rocks of Namibia, 55 A22.27 Other Namibia , 55 A22.28 Other countrie s relevant to Lufilian Arc projec t, 55 A22.29 All Zambia (compilation of all Zambian ages), 56 A22.30 All Namibia (compilation of all ages from the country), 60 F EVENT DIAGRAMS ZAMBIA A23 Hook Granite Batholith, Zambia, 63 A24 NW Zambia, 64 A25 West Lusaka-Kafue Flats Area, Zambia, 65 A26 Environs of the Nchanga Mine, Zambia, 66 A27 Basement to the main Copperbe lt, Zambia, 67 A28 Environs of the Mufulira Area, Zambia, 68 A29 All basement to the Copperbelt, Zambia, 69 list of appendices (cont.) xxviii A30 Luangwa Valley, Zambia, 70 A31 Mkus hi-Seren je Area, Zambia, 71 A32 Choma-Kalomo Batholith, Zambia, 72 A33 Irumide Belt, Zambia, 73 A34 Other Zambian reporte d ages, 74 A35 All Zambian radiome tr i c ages, 75 NAMIBIA A36 Kaokoland Area, Namibia, 76 A37 Entire Kamanjab region, Namibia, 77 A38 Khorixas Inlier, Namibia, 78 A39 True Kamanjab Batholith, Namibia, 79 A40 Comparative event diagram for Khorixas In lier and Kamanjab Batholith, Namibia, 80 A41 Central Namibian Area, 81 A42 Namaqua Metamor ph i c Complex , Namibia , 82 A43 Witvlei Area and correlatives in the Greater Lufilian Arc, 83 A44 So-called ?Kibaran -Age ? rocks, Namibia, 84 A45 Southernmost portion of Namibia, 85 A46 Namibr an d - Sa s r ie m Area, Namibia , 86 A47 Rehoboth Inlier, Namibia, 87 A48 All Namibi a n radiome t r ic ages, 88 A49 Radiom e t r ic ages of other countr i es that are related to the Greater Lufilian Arc., 89 G TECTONIC ENVIRONMENT OF EMPLACEMENT A50 Tectonic envir onme n t of emplacem en t for sa mples from the Greater Lufilian Arc, 90 A51 Results of determination for environment of emplace me n t of granito id s based on methodology of Maniar & Piccoli, 1989, 96 A52 Result s of determ i na t i o n for anorog e n ic charac t er of granit o i ds based on the Whalen et al, 1987 plots, 102 A53 Results of determination for environment of emplace me n t of granito id s based on methodology of Pearce et al, 1984, 107 A54 Discrim i n a t i on of granito i ds followin g procedure of Harris et al, 1986, 112 A55 Results of determination for environment of emplace me n t of granito id s based on methodology of Batchelor & Bowden, 1985, 116 A56 Tectonic envir on me n t of mafic roc ks, Greater Lufilian Arc projec t, 117 H PARTIAL TRANSCRIPTION OF FIELD NOTES ZAMBIA A57 Field notes taken along E-W transec t of the Hook Granite Batholith, 168 A58 Abbrevia t ed descrip t i o n of samples collecte d in the Hook Granite Batholith by Pepper, 2001, 170 A59 Comment s from publis h ed Zambian geologi c a l su rvey reports and maps on iron oxide bodies , quartz pods, associa t e d granito id s and round- p e bb l e hydr oth e r m a l brec cia s , 172 A60 Sample description and field relationships in the West Lusaka-Kafue Flats Area, Zambia, 173 A60.1 Quartz pods, 173 A60.2 Granito id s , 173 A60.3 Gabbroi ds , 174 A60.4 Iron oxide bodies, 175 A60.5 Contac t metamorphic rocks, 175 A61 Descriptions of samples from the Kale ng wa Area, Zambia by Pepper, 2001, 176 A62 Descriptions of samples collected in the field, Kalene Hill Area, NW Zambia , 178 A63 Field descriptions of sample s L-032 to L-034, Kabompo dome, NW Zambia, 1798 A64 Petrography of the Chitungulu sodalite sy enites, Mwombezhi Dome, NW Zambia, 180 list of appendices (cont.) xxix NAMIBIA A64 Field notes for a few suites of Cu-mineralized rocks in the Kamanjab Batholith, Namibia, 182 A65.1 Suite G, 182 A65.2 Suite H, 182 A65.3 Suite M, 183 A65.4 Suite N, 184 A66 Field notes on the N-S transect through the Oas Farm, Namibia, 185 A67 Field notes from the Lofdal farm, Namibia, 194 A67.1 Cross section through series of ultramaf ic dikes, Lofda l farm, Namibia, 197 A67.2 Magnetite- cemented, polymictic hydr otherma l breccia that makes a diatre me , 198 A68 Partial field notes collected at the Mesopo tamie farm, Namibia, 200 A69 Field notes , Ugab River, Namibia, 201 A70 Field notes , Okwa River, Botswana, 204 A71 Field notes Grootfontein Inlier, Namibia, 205 A72 Field notes from Okatjepuiko, Witvlei, Namibia, 206 I OTHER A73 Persons interviewed for preparation of fieldwork, during fieldwork, and when proc es s in g inform a t i o n , 208 A74 Rock names of samples from the Greater Lufilian Arc Granitoi d project, 209 A75 Experiment to test quality of chemic al laborator y, 214 A76 Heat production capa city of intrusive roc ks from the Greater Lufilian Arc at the time of their emplacement, 216 J RAW DATA FOR NEW GEOCHRONOLOGY A77.1 Raw data obtaine d for SHRIMP II U-Pb dating at the Australian National Univer sity, Canberra , 221 A77.2 Raw data and proc es s in g for zircon dating using U-Pb laser- a b l a t io n ICP-MS techniq u e , 225 A78 CONCORDIA DIAGRAMS A78.1 Sample L-030, 227 A78.2 Sample L-047, 227 A78.3 Sample L-075, 228 A78.4 Sample L-158, 228 A78.5 Sample L-160, 229 A78.6 Sample L-207, 229 A78.7 Sample L-213 Conc or d i a diagra m for high U zircons + rims , 230 A78.8 Sample L-213 Conc or di a diagram for cores and rims, 230 A78.9 Sample L-638 Conc or d i a diagram for all zircons includ i n g xenocrys t s , 231 A78.10 Sample L-638 Conc or dia diagram for main clus ter of zircons, 231 A78.11 Sample L-688 Conc or di a diagram for all zircons, 232 A78.12 Sample L-688 Histog ram of all 12 ages in main clus ter, 232 A78.13 Sample L-693, 233 A78.14 Sample L-868, 233 A78.15 Sample L-855 Conc or di a diagram for all zircons, 234 A78.16 Sample L-855 Conc or dia diagram for main clus ter of ages, 234 A78.17 Sample L-943 Conc or di a diagram for all zircons, 235 A78.18 Sample L-943 Conc or dia diagram for main clus ter of zircons, 235 A78.19 Sample L-969, 236 A78.20 Sample L-993, 236 A78.21 Sample L-1013 first, 237 A78.22 Sample L-1013 second, 237 A78.23 Sample L-1043 concord ia diagram for older group of zircons , 238 A78.24 Sample L-1043 concordia diagram fo r younger group of zircons , 238 list of appendices (cont.) xxx A78.25 Sample L-1043 concord ia diagram for all zircons 2, 239 A78.26 Sample L-1043 concord ia diagram for all zircons 1, 239 K GEOCHRONOLOGICAL CORRELATION DIAGRAMS A79 Correlation of dated events, Zambian locations, 240 A80 Correlation of dated events, Namibian locations, 241 A81 Correlation of dated events, Greater Lufilian Arc, 242 A82 Correlation of dated events, Greater Lufili an Arc, first portion (3000 to 1400 Ma), 243 A83 Correlation of dated events, Greater Lufili an Arc, second portion (1400 to 0 Ma), 244 1. INTRODUCTION This documen t reports observ a t i on s , findin gs and conclu s i o s of the resear c h projec t entitled ?Geoche m is t r y , Geoc hronology and Metallogeny of Pre- Katangan and Post -Kat ang a n Granito i ds in the Greater Lufilia n Arc, Zambia and Namibia?. It is pres ented to the School of Geo scie nc e s of the Science Faculty of the Univer s it y of the Witwatersrand, and constitutes the thesis for the Ph.D. degree in Geolog y at that institution. 1.1 The Lufilian Arc The Lufilian Arc of South-Central Africa is defined as the curvilinear belt of Neoproterozoic Katangan sedimen t s that was deforme d during the Pan African orog eny in Zambia and the Democra t ic Republic of the Congo. Those two countrie s contain the vast stratifo rm Katanga copper-cobalt ores, as well as the epigene tic polymeta l l i c (Pb, Zn, Cu-Au, and U) ores of the re gion . The Katang an sequen c es were deposi t e d over a lengthy period of Neoprote r oz o ic time that extended from around 880 Ma (Lower Roan) to less than 590 Ma (Upper Kunde lu n gu ) . That interva l coincid es with the Cryogenian Period , or so-called ?Snowball Earth? . The Lufilia n Arc also compris es a dominan tl y Paleopr o t er o z o ic basement of deformed gr an itoids, and a diverse suite of Pan-Afri c a n granito i d s that intrude the Katangan sequences. Although the Lufilian Arc p er se , occurs essentially in Zambia and the Democratic Republic of Congo, it is evident that tectonized corr ela t i v e s of the tectonos tra t i g r a ph i c Ka tangan entitity extend westwards, beneath Karoo and Kalahari cover in Botswana , into Angola and northern Namibia. The wester n extension of this arc has only been spor ad ically studied. At the time of starting this projec t, there was an urgent need to address that deficit, especially since it is clear that minerali z a tio n also extends into Angola and Namibia . The Greater Lufilian Arc covers that large area, as shown on Fig 1.1. 1.2 The Project This projec t was structur ed by Professor Laurenc e Robb of the Universi ty of the Witwatersrand in late 2001. It was designed to study the pre- and post-Ka t a ng a n granito id s that comprise the Greater Lufilian Arc. Its main purpo se was to provide insights into the metallo g en ic chara c t er i s ti c s and poten t i a l of the whole belt. Three South African- based mining companies were interested in the project and joined to fund and support it. These were Anglo American Corporation, AngloVaal and BHPBilliton. Granitoid s were selected fo r study because they repr es en t rock types that c ould potentially provide a great deal of information about the orogenic proc es ses involved in the formation of the Greater Lufilian Arc. They were also likely to be implicated in many of the ore forming proc es ses in the belt. Given that three mining companies were involved in funding this collaborative resear ch project, a study of granitoid ev oluti o n and metallo g en y was cons idere d to be the best way to avoid compromising any of the individual corpor ate strategic initiatives that might otherwis e have arisen in a project aimed at studyin g specifi c explora ti o n targets or deposit s . 1.3 Aims of the Project The main aims of the study of granitoids in the Greater Lufilian Arc were: 1. To evaluate geological relationships of intrusiv es relative to the Katangan, emplacemen t style and depths of intrusion. 2. To study the role of granitoids in Katangan orogenesis and mineralization. 3. To define the geochemis try of the granitoids in order to identify th eir tectonic setting and metallogenic affinities . 4. To study the age of the princi pa l events and evolution of the belt. 5. To improve geologic a l understan d i ng of late granite intrus ions in the arc . 6. To assess whether the iron oxide-co p pe r - g o l d mineral deposi t model pertains to the region. 7. To impr ove the metallo g en i c models for the belt in or der to assist in explor a t i on of know n areas, and areas covered by Karoo and Kalahari sediments in eastern Angola, northea s t Namibia and Botswan a . 1.4 Study Areas The project was cons tra in e d to areas with reas ona b l y good surface exposure, that allowed for adequate repres entative sampling and definite geological control. Main fieldwor k was conc en t r a te d in two broad region s: NW Zambia and northern Namibia (Fig 1.1) . 2 Fig 1.1 Definition of the study area area and tectonic framework of southern Africa. Th e Greater Lufilian Arc covers the northern part of Namibia and wes tern pa rt of Zambia, as indicated in gray. Fieldw ork was carried out in the two boxed areas. Zambia lies jus t in the center of the map; Namibia on the lower left. B orders of t h e t w o countries were enhanced for referenc e. Note that the Greater Lufilian Arc, limited by the covers significant portions of t h e Democratic Republic of Congo, Angola, Botswana, Zambia and Namibia. LA = Lufilian Arc, DB = Damara Belt, KaB = Kaoko Belt, ZB = Zambezi Belt, IB = Irumide Belt, BB = Bangweulu Block, CKB = Choma-Kalomo Block. Figure slightly modified from (Hanson, 2000). 3 1.5 Project Outline The project was subdivi de d into three discret e phases. Each of them defined by a specific task, budget and delivery date. They each were followed by a report summar izi n g the results to the fundin g partie s . Th e follow i ng three phases define d the projec t ? s objectives and deliverables up to June, 2003: 1.5.1 Phase 1 ? April to November 2002. Geological Charac teristics of Pre- and Post-Katangan Granitoids. The main objecti v e of this phase was to collect a r epr esentative suite of sample s from both study areas and provide definiti v e geologic a l controls for the sample s . Fieldw ork began after carryi ng out a prelim ina r y literature survey and review of informat io n . Much of the phase was dedicat ed to field work. Specific objec tives of the phase included: ? To collect samples repr esen t i n g the composit i on a l va riety in each of the major pre- and post-Katangan granitoid bodies in the two study areas. ? To establish geological relationships of the grani toid s to the Katangan sequence and its correlatives. ? To collate information relating to the known mineral deposits in and adjacent to these gr anitoid bodies . 1.5.2 Phase 2 ? December 2002 to May 2003. Petrogr a ph i c and Geoc hem ic a l Charact er i z a t i o n of Pre- and Post-K a t a ng an Granit o id s . The main objecti v e of this phase was the petrogr ap h ic and geochem i c a l char ac t e r i z a t i o n of the sample suite collected in Phase 1. It was a laboratory-based phase t hat entailed slabbing of all granito i ds , and prepara tio n of thin and polished/thin sections of a repres en tative co llection of the sample suite. A subset of the samples was analys ed for major oxide s , trac e eleme n t s and rare earth elements at various laborat or i es . Specific objec tives included: ? To obtain major and trace element analysis by XRF techniques. ? To evaluate the rare earth conten t of some samples using various techniqu es . ? To proc ess and interpr e t petrogr a ph i c and geochem ic a l informa t i on from the samples . 1.5.3 Phase 3 ? June to September 2003. High Precis ion U- Pb Zircon Geochronolog y of Pre- and Post- Katangan Granitoids. The main objectiv e was to provide accurate and prec is e age dates for each major granitoid unit identified during the previo u s two stages . Zircons separa t ed from select samples were sent to two geochr o n o lo gi c a l labora t o r ie s in Austra l ia and Canada . 1.5.4 Phase 4 ? October 2003 to January 2005. Ellaboration of the Ph.D. thesis . The main object i v e was to compil e , proc es s and interp re t all the informat i o n obtained during the previous three phases . It was an office - b as e d phase wher e most of the diagra ms were draw n, many referen c es were review e d , and the thesis was struct ured. Specia l attention was given to compil a t i o n of geochr o n o lo gi c a l informat i on from the Greater Lufilian Arc and to interpre tation of the tectonic environment of emplacement of the various rocks analys ed . Several presen t a t i o ns were made at interna t i on a l and South African geolog i c a l confer e nc es to ventila t e some of the ideas and interac t with other resear ch e r s , espe cially in the field of iron oxide-copper-gold mineralization (Lobo-Gu e r r er o , 2004a; Lobo-Gue r r e ro, 2003; Lobo-Guer rero, 2004b; Lobo- Guerrero, 2004c; Lobo-Guerrero, 2004d; Lobo-Guer rero, 2004e; Lobo-Guer rero S., 2003). 1.5.5 Current status of project A total of 1500 samples were collected in the field; 351 were analysed. 157 chemical analysis were compiled from various well-d oc u m en t e d sources , to reach a total of 508 samples analysed in the database. 38 new zircon U-Pb ages were produced : 10 of them by laser-ab l ation ICP-MS techniques at the Memorial University of Newfound l a n d , Canada, by Marc Poujol and his rese ar ch group; and 28 by SHRIMP II at the National University of Australia (ANU) by Richar d Armstron g and his researc h group. Major samplin g domains of the Lufilia n Arc Granitoi d Projec t will be grouped and described in the followi ng pages. Main findin gs on geoche m i s tr y , petrol o g y and geo chro n o lo gy of the rocks sampled will be exposed for the third time. Future work to be carried out in spec if i c projec t s and on-go i n g work will also be describ e d . 4 2 METHODOLOGY 2.1 FIELD SAMPLING 2.1.1 Definition of Granitoid The term ?granit o i d ? was loosely used during field samplin g , to include all felsic to interme d ia t e plutonic rocks. That field classific a t i o n included all syenites and foid-b ea r in g rocks, as well as diorit es and carbona t i t e s . Ocassi o na l l y such ?grani t oi d s ? were intima t e l y associ a t e d with small gabbro ic bodies . This was noted very early in the projec t, in northwestern Zambia. Once that the granito i d - ga b br o i d associ a t i o n was establ is h ed , mafic rocks that occurred with the ?granit o i ds ? were also sampled. Some areas had very little to no r ock outcrop, so any in situ gabbroid or granit o i d exposed on the surf ac e was sample d . Gabbros from regiona l Mesozo ic dike swarms (Kar oo) were not sampled . 2.1.2 Sampling Procedure Most of the samples were taken from the surfac e. The fres hest samples were collected and only the best of that group were select e d for chemic a l analys is and dating. Samples were generall y only collecte d along the main roads. At most, they come from a few hundred meters away from the main road network. For these reas ons , samples collect e d have a bias : they come from the best outcrops available along the main roads in each of the regions . Rocks t hat did not outcrop well were selected out of the project. A very small number of foot transects was done at spec ial sites. Core fr om many locali t i es was also observ ed and sample d , especia l l y in areas with no outcrop . Trans ec t s were made acros s the intru s ive bodies of the Greater Lufilian Ar c, with represe n t ati v e samplin g of the main outcrops along roads or near them. Inform a t i o n on granito i ds was primari l y based on publis h ed maps and literatur e. Interviews with key persons , mainly geolog is t s from various geolog i c a l surveys , mining companies , universities and consulting firms, helped to define which particular regions deserved more attentio n . Most intervi e w s were recorded on tape and later transcribed. A list of the persons interviewed is pres ented in the Appendix. Pre-Katangan and Post-Katangan granitoid rocks were selected for sa mpling based on their location, repr es entativity, foliation, deforma tion and compos ition. Sampli ng was carried out in areas that had little recent geolog ic a l work. For example, geochemis t r y and geochr on o l o g y of granit o i d rocks in some parts of Namibia has been studied in detail during the last ten years (Becker & Brandenburg, 1997; Becker , Diedric hs , Hansen, & Weber, 2000; Becker & Sc hreiber, 2002; McDermott, Harris , & Hawkesworth, 2 000; McDermott & Hawkesworth, 1990; Seth, 1999; Seth, Armstrong, Brandt, Villa, & Kramers, 2003; Seth et al., 1998; Seth, Okrusch, Wilde, & Hoffmann, 2000). T hose areas were not conside r e d for sampli n g . In contra s t , most of the Zambian graniti c rocks do not have any recent studies , apart from general 1:200,0 00 , and 1:100,0 00 scale mapping of the Mwinilu n ga area (Key & De Waele, 2003; Key & Banda, 2000; Key et al., 2002; Key et al., 2000; Key et al., 2001), and work done on the Irumi de and Kibaran belts by (De Waele, Fitzsim o ns, & Nemc hin, 2004; De Waele & Tembo, 2000; De Waele, Tembo, & Wingate, 2001; De Waele, Wingate, & Mapani, 2002). On most occassi o ns , samplin g routes were first travers e d one way in order to locate all possibl e outcrops with GPS waypoin t s ; the most favorab l e outcrop s were sampled on the way back. The general approac h for sampling was to collect fresh, represen tative spec imens of all the differe n t facies of intrus i v e rocks within a given area. For example, if a well-e xp o s e d outcrop had a granit e gneiss intrud ed by a medium- g r a in e d tonalite and a series of uniform gabbroids , homogeneo u s sa mples of all three rocks were select e d . Choice fell on the least altered, with the minimium of veins and xeno liths. In principle, all sample s for chemical analysis and dating were chosen to be approximately 1? to 2? kilo gr ams in weight. Ideally, every specimen had fresh, trimmed surfaces on all faces. 2.1.3 Referencing Geological Stations, Recording Information and Sample Labeling All sampling stations were located on a map and t heir GPS coodina t es were recorde d . Dependi ng on the region , publis hed 1:100,00 0 geologic a l maps had lati tude and longitude , or UTM based coor dina t e s . The same coor dinates, projection systems and datums of th e maps were used for GPS location of stations. Coor d i na t e s and refer e nce syste ms for all sample collec t i o n sites, and most geolog ic a l obs ervat i on stations have been listed on Tables A16 to A20 in the Appendix. T he table is brok en down into groups , to accoun t for the various coordin a t e systems and datums used. Sample locations have been plotted on the maps that come with this doc ument. 5 When possible, the following observations were recor ded on each outcrop: station number, sample number, GPS coordina t e s , macrosc o p ic field descri p t i on , stru ctur al relations, contacts, foliation, alteration and mineralization. Other information recorded on the field notebook was type of outcrop, its environs and general physiog r ap h y. The sample, if any, was then placed in a heavy plastic bag along with a cardboar d tag labeled on both sides with a waterp r o o f marker . The plas ti c bag was also labeled on both sides. Its upper portion was cut with a knife and then tied with a square knot to keep the spec imen from getting out. Batches of sample s were temporar i l y stored in warehous es and mining comp an y facilities until the moment of driving them to Johannesburg. 2.1.4 Other Field Activities Although sampling for granitoid rocks was the main objec tive of the project, several other aspects of the geolog y were observed . Namely, structur al featur es , mineralization produc ed by some of the granit o i d rocks, and hydrothe r m a l alteratio n around granitoi d bodies. Apart from granitoid s and gabbroid s , other rocks sample d includ e : volcan ic rocks, iron oxide bodies , quartz pods 1 , ma fic and ultramafic dikes, carbonatites , and mineral i z e d zones associa t e d (or potentia l l y associa t ed ) with granito i d s . 2.1.5 Field Equipment Used The main equipment used for fieldw ork was: 10X magni fying glass, HCl bottle, steel scratcher, field magnet, GPS, 4 megapixel high-resolution digital camera, Brunt o n compas s , large sledge hamme r , 1 kilogr a m steel hammer with modifi e d long handle , steel chisse l , portab l e computer and field notebook. A steel pan was also carried along for samplin g gravity concent r a t es . Four wheel drive vehicles were used for all fieldwo r k . Most field mapping and sampling activiti e s were based on moving tent camps. Small hotels were used to sleep at the main towns and cities . Ninety percent of the fieldwork was done singlehandedly. 2.1.6 Bibliographical Research Before going to the field, basic cartog r ap h i c and bibl io g r ap h ic resea r c h on granit o i d s , struc t ura l geolo g y and mineral deposit s of the Lufilia n Arc was carried out. Th is resear ch was done at the various libarie s of the University of the Witwater srand, t he Geolog i c a l Survey Organiz a t i o n in Lusaka, the Zambian Chamber of Mines in Kalulus h i , the Geologic a l Survey of Namibia in Windho ek , and the Geolog ic a l Survey of South Africa in Pretor ia. Some published papers and internal r eport s from the funding mining compan i es were also reviewed. Most of the bibliographical resear ch on Zambia was carrie d out at librar ie s of the University of the Witwaters r and , the main Johannes b ur g Public Libr ar y, and the library of BHPBilli t o n in Johanne s bu r g . 2.1.7 Office and Laboratory Work Once back in Johann es bu r g , prepar a t i o n of sample s b egan. First of all, field notes and draw ings were reviewed and updated. Lists of sample coordina t es we re assemb l ed and prelim in a r y sample databas es were put together. These included field name of rock, site, coordinates , type of sample collected , and research to be done on each partic u l ar sample . Granit o i d samples were prepar e d first, and other samples of minera l iz e d material, iron oxides, volcanic and sedimentary rocks were saved for later evaluation. After assemb lin g the databa s es , rock specim en s were prepar e d in the follow in g manner : They were organiz e d by sample number , later they were slabbed using a 40 cm diamete r circular diamond blade. The largest possi b le slabs were kept as counter - s a m p l es . Weath e r e d or otherwis e altered portions of the sample s were sawed off. All of the slabbed surfac es were photographed wet or dry, to obtain the maximum contrast. Repres entative slabs of all samples were labeled and stored for future referenc e. Thin and thin-polis hed petrogr ap h ic al section s were made of select ed sample s. The remainder of the rocks were carefull y crus hed and then ground to a medium sand size for zircon- p i c king. Standard dense media separation, as well as magnetic separat i o n procedu r es were used at the EGRI-HA L 2 laboratories to concentrate zircon s and other minerals of interest . Mineral separates were kept for further referenc e . If grinding for zircon-p i c k i ng was not to be carried out, cr ushe d sample s were quarter e d , and a repres en t at i v e portion was finely ground. Samples were labeled and sent to the chemic al laboratory of the School of Geoscie nc es for XRF chemi c a l analy s is of major oxi des and some trac e elemen t s as indica t e d on Table 2.1. 1 T h e infor ma l term ?quar tz pod? will be used to indica te massive quartz bodies that occur through ou t the work area as round outcro ps of milky to sugary quartz in circ ular to sub-circular outcrops that range from a few meters in diameter to one kilomete r in diamete r (See Chapter SUCH). 2 EGRI-H A L stands for Econo m i c Geolo g y Resear c h Institute-Hugh Alsopp Labor atory of the School of Geoscie nc es , Univer s i t y of the Witwatersrand. 6 Part of the trace elements and rare earths were an alysed by ICPOES at the Chemis try Department of the University of the Witwater srand and ot hers were analys ed by ICPMS at the University of Capetown. Table 2.1 indicat e s which elements were analyse d where and what their detec ti o n limits were. All samples , count e r s a mp le s , slabs and thin secti o ns were filed and stored. They are currently k ept at the Departme n t of Geos c ie nc es . All results for iron oxides were given as total iron oxides, expr essed in Fe2O3. Several of the sample s from the literat u r e had both FeO and Fe2O3 and were kept as such in the geoch e m ica l datab as e . Never t he l es s , for comparis on purpos es , total iron oxide expres s e d as Fe2O3 was used. Table 2.1 Laboratories where chemical analysis were carried out, with threshold values and detection limits where available. Element /Cation Laboratory Type of Analysis Detection Limit Notch Element Laboratory Type of Analysis Detection Limit Notch S i O 2 SGWits XRF 50.00 U UCT 20 TiO2 SGWit s XRF 1.00 T h SGWit s XRF 15 37 Ti O 2 SGWits XRF 0.10% 1 . 0 0 T h UCT ICPMS 37 Al2 O 3 SGWit s XRF 15.50 S c SGWit s XRF 10 20 F e 2 O 3 SGWit s XRF 6.00 P b UCT ICPMS 20 MnO SGWit s XRF 0.150 S m SCWit s ICPOE S 50 MgO SGWit s XRF 2.00 S m UCT ICPMS 50 CaO SGWit s XRF 5.00 N d SCWit s ICPOE S 50 Na2 O SGWit s XRF 4.90 P r UCT ICPMS 15 K2O SGWit s XRF 5.50 C e SGWit s XRF 12 175 P 2 O5 SGWit s XRF 0.30 C e UCT ICPMS 175 LOI SGWits Differ e n c e 2.00 La SGWits XRF 12 95 T o t a l SGWit s La UCT ICPMS 95 Rb SGWit s XRF 3 200 C s UCT ICPMS 3 Rb UCT ICPMS 200 Hf SCWit s ICPOE S 10 Sr SGWit s XRF 3 400 H f UCT ICPMS 10 Sr UCT ICPMS 400 Ta SCWit s ICPOE S 120 Y SGWit s XRF 3 60 Ta UCT ICPMS 120 Y UCT ICPMS 60 Eu SCWit s ICPOE S 4 Zr SGWit s XRF 8 360 E u UCT ICPMS 4 Zr UCT ICPMS 360 Gd SCWit s ICPOE S 30 Nb SGWit s XRF 3 40 Gd UCT ICPMS 30 Nb UCT ICPMS 40 Tb SCWit s ICPOE S 5 Co SGWit s XRF 6 30 Tb UCT ICPMS 5 Ni SGWit s XRF 6 16 D y UCT ICPMS 20 Cu SGWit s XRF 6 25 Ho UCT ICPMS 3 Zn SGWits XRF 6 85 E r UCT ICPMS 9 Ga SGWit s XRF 9 26 Tm UCT ICPMS 35.5 V SGWi t s XRF 12 10 0 Yb SCWi t s ICPOE S 7.5 Cr SGWit s XRF 12 100 Yb UCT ICPMS 7.5 Ba SGWit s XRF 20 130 0 L u SCWit s ICPOE S 1.6 U SGWit s XRF 6 20 Lu UCT ICPMS 1.6 NOTES S G W i t s = Labora t o r y of the Schoo l of Geo sc i e n c e s , Unive r s i t y of the Witwa t e rs r a n d SCWit s = Schoo l of Chemi s t r y, Unive r s i t y of th e Witwa t e rs r a n d UCT =Univer s i t y of Capeto wn No anal ys is were perform e d for H2O+ and H2O-, SO2, F, Cl, CO2. Anal ys i s for Mo, Sn, W, Ge, Be, Li, As and Se we r e not ca rri e d ou t durin g the proje c t . Sampl e s with s uch anal ys i s we r e obtai n e d from exter n a l sourc e s . 7 2.2 PETROLOGIC NOMENCLATURE Samples were first classifie d macros cop i c a l l y in the field using the bare eye and a 10X hand lens. In general, that prelimin ar y classification included main color, grain size, foliatio n , fres hnes s , basic colors of principa l rock cons titu e n ts , degree of observab le hydrothermal alteration and mineralization constituents. Typical descrip t i o ns were ?fine- gra i n e d , pink plagioc l as e porphy r y ? , ?medium - gr a i ne d gray granito i d with blue quar tz ?eyes? ? , ?dar k brow n, very fine-gr a in e d gabbro with diss eminated cubic vugs after probable sulfides?, and ?well- foliated coarse-grained red porphyritic granitoid with pink plagio c l as e pheno c r ys t s (2.5 cm aver ag e long dimens ion) and biotite in the foliation planes?. Two differ e n t proc edu r es were used to give proper petrol og i c names to sample s collec t e d for the projec t , based on their major oxide chemical a nalysis. These will be discussed below. 2.2.1 Total Alkali Diagram The modified version of the IUGS Total Alkali versus Silica diagram pres ent ed by (Middle mos t , 1994b) is a comprehens iv e and widely accepted standard for plutonic rock nomencl a t ur e. It builds upon the total alkali versus silica (TAS) diagram to name volcan ic rocks s uggested by the IUGS Subc ommission for Igneous Rock Nomencla t u r e (LeMaitr e et al., 2002 and several other ear lier versions). The diagram is made by plotting SiO 2 weight percenta g es on the abcis sa versus the sum of Na 2 O and K 2 O on the ordinate (Fig 2.1). Middlemo s t , 1997 sugges ts that three si gma isoplet hs should be used to s eparat e the subalka l i n e , midalkal i n e and alkaline magmatic lineages. The sigma index wa s devis ed by Rittmann, 1957, and is equal to: Equation 1 ?Rocks of the subalk a l i ne suite have sigma values less than 2.5; sigma values between 2.5 and 10 define the midalka l i n e suite; wher eas sigma values in the range 10 to 25 separat e the alkalin e suite.? (Middle mo s t , ? index = (Na2O + K2O) 2/(SiO2 ? 43) 8 1 9 9 7) . He furthe r adds that igneous rocks with sigma values that are greater than 25 or negativ e ?should be regarde d as spec ial rocks with chemica l compos i t i on s that set them apar t from the normal igneous rocks? (Middlemos t, 1997, p. 46). Both the modified TAS diagr a m for pluto n ic rocks and t he sigma isople t h s just described will be used throughout this document. All plutonic rock names , as well as the alkalinity suites are show n on Fig 2.1. Fig 2.2 Comparison of the total alkali versus silica diagrams proposed by Middlemost, 1994 and by Wilson, 1989. Both diagrams were plotted at the same scale, to compare the various fields o f each metho d. Note that the fields of granites, syenites and foid sy enites in Middlemo s t ?s diagram than in Wilson ?s diagram. Many fresh samples from the Greater Lufili an Arc plotted o u t side of t h e Wilson diagram. The TAS diagram described by Cox, Bell, & Pankhurst, 1979 and later modified by Wilson, 1989 to include plutonic rocks is not very practic a l and will not be used her e. Its rock names are signific an t l y differen t from the Middlemost TAS diagram, as show n on Fig 2.2. 2.2.2 R1/R2 Cationic Classification Classific a t i o n of plutonic rocks only based on total cont en t of potash , soda and silic a is an oversim p l i f i c ati o n . Other classi f ic a t i o n proc edu r es use variou s relati o ns of most major oxides that defi ne intrus i v e rocks. Perhaps the most used multioxide methodology to classi f y igneo us rocks was devis ed by the Frenc h resea r c h group let by Henry De la Roche (De la Roche, Leter r i er , Gandclau d e , & Marchal , 1980). Common spread s h e e t applic ations and drafting softwar e, make it very simple to apply De la Roche?s method for batch plotting of geoche m ic a l analys is . The method separa t es igneous rocks into at least 28 groups using eight cations (SiO 2 , Na 2 O, K 2 O, FeO 3 , TiO 2, CaO, MgO and Al 2 O 3 ) to classify the rocks. Parame te r s R1 and R2 are calculat e d from millicat i on i c values and plotted against each other. Values for R1 and R2 are calc ulated as follows: Equations 2 The R1/R 2 nomenc l a t ur e devised by De la Roche and co -wor k er s is the most descr iptive of the chemic al- b a s e d rock nomenc la t ur es availabl e . The facts that it der ives from a range multiple cations and that it spans all types of intrusiv e rocks, makes it a robust system to classif y igneous rocks from the Greater Lufilia n Arc Granitoid Project. Fig 2.3 illustrates the limits between various rock types and the names used. R1 = 4Si ? 11 (Na + K) ? 2 (Fe + Ti) R2 = 6 Ca + 2 Mg + Al 9 2.2.3 Granitoid Classification Charac t e r iz a tio n of the differ e n t types of granit o id s was one of the main tasks of this researc h project . The granite family, composed by granodior ite, quartz monzonite, monz on ite and true granite (sensu modified TAS diagram of Middlemost, 1994b) confor ms a very signifi cant portion of the rocks sampled for the Lufilian projec t . The same group of rocks includ es the fields of alkali granite, granite , granodior ite, tonalite, quartz monzoni t e and monzoni t e , accordin g to the R1/R2 diagram of De la Roche et al., 1980. Differen t names for the same rock spec imen ts turn out, because each proce du r e is based on a contras t i ng relation of major oxide values. The system ati c s of method s propos ed by (De la Roche et al., 1980) and by Middlemost, 1994b and Middlemo s t , 1997 were consider ed to be more repr es en t a t ive of the various rock types and were selected for 1 0 n o m e nc l a t ur e and discuss i o ns of variou s petro l og ic a l as pec t s in this repor t. All sampl e s with chemic a l analysis were evaluated with the TAS and R1/R2 methodol og i e s . Table A74 in the Append i x pres en t s result s of the nomenclature. The triangular modal diagrams devised by the IU GS Subcomm i s s io n on nomenc l a t ur e of igneous rocks (LeMaitre et al., 2002) offer yet another solution to the complex issue of naming rocks. They were not used for this projec t due to the amount of samples and the lack of precis ion of those methods for comparative purpo se s . 2.2.4 Debon & LeFort Cationic Classification Diagrams Several of the diagrams presented by Debon & Le Fort, 1988 are useful for rock discrimination and geochem ic a l evaluat i o n . The authors devis ed ways to standa r d is e descri p t i o n of some geochem i c a l parame t e r s includ i n g : quartz conten t , al umina index, color index, alkali ratio, relation ship of quartz -dark mineral s - a lk al i e s , sodium versus potassi u m content , and magnesiu m versus iron content. The main cation ic parameters are calc ulated in terms of millications and he lp to produce specially designed plots. The way to calculate these parameters in described clearly in Debon & Le Fort, 1988 and Debon & LeFort, 1983. The main equation s for each parame t e r are listed below . Q is an empiri c estima t e of the rock?s quartz / ( qu a r tz + feldspa r s + muscovi t e ) proport i o ns in volume percent ag es . P is the alkali ratio. The A parameter is the classic a l alumina index. B is directl y proport i on a l to the weight conten t of dark minerals in common graniti c rocks. F is proportional to the weight content of feldspars + muscovite. Equations 3 The diagrams devis ed by Debon & LeFort will be used ex tens ively through the projec t to compare suites of sample s, evaluate their hydr other m a l al terati o n , and define geochemi c a l trends. 1. The Q-P diagram (Fig 2.4), origina l ly designe d to name the co mmon pluton ic rocks, is useful to evaluate rock assoc ia t i o n s , geochemi c a l trend s , and some types of hydrotherma l alteration. The twelve ?standard? plutonic rock types, as defined by Debon & LeFort, 1983 are plotted in the middle of the fields. 2. The A-B diagram (Fig 2.5) separat e s peralum i no u s minerals and rocks from metalum ino u s minerals and rocks. It also helps to identify some of the char ac teristic rock-fo r min g minerals . The plot is sensib l e to subtle hydrothermal alteration. 3. The QBF diagram (Fig 2.6) is useful to help define geoc hemi c a l trends of igneous rocks, and aids in distinction of different magmatic associations. 4. The K*-B diagram (Fig 2.7) is useful to help establ i s h sodic, sodi c -p o tas s ic or potass i c char ac te r of rock s , as well as to classify their color index into leucocratic, suble uc oc r ati c and mesoc r a t ic . This plot is sensib l e to subtle hydr othermal alteration. It also helps to define geochemic al trends of igneous rocks. 5. The Mg*-B diagram (Fig 2.8) has a central line made by joinin g the averag e values for granite, adamellite, granodi or i t e , tonalit e quartz dior ite and gabbro, as de fined by Debon & LeFort, 1983. The diagram helps to distingu i s h between common, magnesi a n and ferrife r o us associations. It is sensib le to some hydr othermal alterati o ns related to iron oxide-co p pe r gold systems. The variou s diagrams define d by Debon & LeFort, 1983 were used extensively during the Gr eater Lufilian Arc Granito id Projec t . Result s from the A-B, K*-B and Mg*-B diagra ms helped to produc e detaile d rock names. The basic rock type name was never theless given by the TAS diagr am modified by Middlemos t, 1994b. Q = Si/3- ( K+N a+ 2C a /3 ) P = K-(Na +Ca ) A = Al-(K+N a+ 2 Ca) B = Fe+Mg +T i F = 555-( Q + B) K* = K/(Na+ K) Mg* = Mg/(Fe+Mg) 1 1 1 2 2.3 GEOCHEMISTRY 2.3.1 Major Oxide Chemistry The major oxide geoc hem is t r y of sample s from the Lufili an Arc region will be described using the modified TAS diagram of Middlemost, 1994a; and Middlemost, 1997 and the R1/R2 classification of plutonic rocks by De la Roche et al., 1980. Since most of the rocks sampl ed fall within the granite field, the 2.5 sigma isopleth was used to separat e subalka l in e from midalka l i n e rocks in the modifie d TAS diagram . It was also used to break the field of granites into alkali granite s from granites on the same diagram. Each suite of analysed rock sample s was evaluated statistically in terms of their al kalinity using the modified TAS diagram and the sigma isoplet h s . All individual sample s from the Greater Lufilian Arc gran itoid project were first given the R1-R2 basic rock name. Later the methods of Debon & Le Fort, 1988 and Debon & LeFort, 1983 were used to establish their aluminos i t y , color, sodic-po t a s s ic and ferriferous -magnesian parame ters. Results of this classification are listed in each of the chapters that describe the sampling domains . Suites of rocks were studied using the logarithmic diagram of their major oxides. That diagram was found useful to compare the entire major ox ide chemis try of samples. It helps to visually evaluate the similarity or dissimilarity of groups of rocks, and will be extensively used throughout this document. 2.3.2 Trace Element and Rare Earth Chemistry Trac e elemen t geochemi s t r y of samples is included in the main geochemic a l databases (Tables A15 and A1 to A14). In many cases, trace elemen t s and rare eart h s were used to defin e geoch e m ic a l signa t u r es in groups of rocks. Those signatu r e s helped to search for samp le s with simila r chemis t r y within the databa s e . Logari t h m ic plots of trace elemen ts and ra re earths proved to be very useful in visual comparis on of rock suites . Normaliz e d logarit hmi c geoche m i c a l plots or ?spider - d i a gr ams? were not found prac tical to compar e the vast range of rock types and large number of samples from t he Greater Lufilian Arc. The wide variety of elemen ts used and normal i z i ng standa r ds select ed for plots in num er ous publications, made it extremely difficult to use a standa r d iz ed proc e du r e . Normal iz e d logari t hmi c trac e elemen t plots were certai nl y used in the evaluati on of several domains and sub- domains . Nevertheless, results obtained from those analyses were meaning l es s . Now that the geograph ic a l , geochem ic a l and geoc hr on o l o g ic a l aspects of the do mains and sub- doma i ns have been identifi e d , more detailed evaluation of the geochemic al database comp iled can be done. That escapes the scope of this projec t. Trac e elemen t and rare earth data have proved to be ke y in the definition of environment of emplac ement. They will be used in a new project to compare samples from the Greate r Lufilian Arc with a database of almost 4000 geochem ic a l analysis from granito i ds in well-identified geotectonic environ m e n ts . Neural web geostatistical analysis and specially des igned software will be applied, as des cribed under Novel Approach section below. 2.3.3 Presentation of Chemical Data Chemical analyses were compiled into a main database that is listed on Table A15 in the Appendix. The databas e was then broken into main samplin g domain s, and a few domains were further subdivided, as show n on Tables A1 to A14. The entire range of chemica l analyses is included in the list of Tables A1 to A15. Geoc hemic al tables in the main text of the documen t have been reduce d and simpli f i e d . 2.3.4 Geochemical Threshold Values To assist in visual evaluat io n of t he geoc hem ic a l data, thresho l d or notch values were defined for each of the elemen ts . Thresh o l d values were based on informa t ion from the entire database, and in general terms epres en t the upper ten percent of the data. Elements that were only analys e d in a small group of samples do not have a defined thresho l d . The values chos en were arbitrar y , and were used for interpre t a t i o n purposes only. Two notc h values were used for silic a : a lower li mit of 50% and an upper limit of 76%. All values above the notches were highlighted in yellow on the geochemical tables . That type of labeling helped to rapidly identif y pattern s and geochem i c a l signatures in the database. 1 3 T h e first line of most geoche m ic a l tables includ es the not ch values for easy referen c e . Table 2.2 lists the notch values used. Any values highlighted were cons ide r ed anomalo us . They are cons ide r e d to be higher than aver age or relatively enric hed. For example, any sample with a loss on ignit i o n over 2% was cons i der e d anomalo us . Likewis e , samples with bariu m cotent over 1300 ppm or thoriu m above 37 ppm. Table 2.2 Threshold or notch values used in the Greater Lufilian Arc granitoid project for various elements and oxides Sample Notch Sample Notch Sample Notch Sample Notch S i O 2 50.00 Rb 200 Ba 1300 Ta 120 TiO2 1.00 Sr 400 U 20 As 100 Al2O3 15.50 Y 60 Th 37 Eu 4 Fe2O3 6.00 Zr 360 Sc 20 Gd 30 MnO 0.15 Nb 40 Pb 20 Tb 5 MgO 2.00 Co 30 Sm 50 D y 20 CaO 5.00 Ni 16 Nd 50 Ho 3 Na2O 4.90 Cu 25 Pr 15 Er 9 K2O 5.50 Zn 85 Ce 175 Tm 35.5 P2O5 0.30 Ga 26 La 95 Yb 7.5 LOI 2.00 V 100 Cs 3 Lu 1.6 Cr 100 Hf 10 1 4 2.4 TECTONIC DISCRIMINATION OF SAMPLES By far, the most difficult task of the Lufilian Arc granitoid project was to define the environment of emplac e me n t of the various rock sample s . Establ is he d method s for that purpos e failed to produc e meanin g f u l resul ts for the major i ty of the sampl e s collec te d . A co mpletely different approach to the problem was finally tried and it produce d signific a n t results . The next two se ctions describe the proc edures followed to study the environment of emplacement in granitoids and mafic rocks. 2.4.1 Granitoids 2.4.1.1 Comprehensive Method of Barbarin, 1999 After reviewing more than twelve different classifica tio n schemes to define the environm e n t of emplac eme n t for granitoi d rocks, the proc edur e devised by Barb ari n , 1990 and Barbar i n , 1999 was found to be the most compreh e ns iv e and univers a l method of evaluat i o n . Tabl es 2.3, 2.4 and 2.5 show the basic enviro n me n t s and the main parameters of the granitoid s produced by each. Table 2.3 Synthetic table showing the relationships between main granitic petrogenetic types, their origins, and the geodynamic environment . (After Barbarin, 1999) GRANITOID TYPES ORIGIN GEODYNAMIC ENVIRONMENT Muscovit e - b ea r i n g Peralumi n o us Grani t o id s MPG C o rd i er i t e - bea r i n g Peralum i n o us Grani t o id s CPG CRUSTAL ORIGIN Peralumin o us Granitoi ds CONTINENTAL COLLISION K - r i c h Calc-alk a l i ne Granito i d s (High K - Low Ca) LCG TRANSITIONAL REGIMES A m p h i o b le - be a r i ng Calc-al k a l i ne Grani t o id s (Low K - High Ca) ACG MIXED ORIGIN (Crus t + Mantl e ) Metaluminous and Calc- Alkaline Granitoids Arc Tholei i t i c Granit o id s ATG SUBDUCTION M i d - Oc ea n Ridge Tholeii t i c Grani t o id s RTG Peralk ali n e and Alkaline Granito i ds PAG MANTLE ORIGIN Tholeiitic, Alkaline and Peralk a l i n e Granit o i ds OCEANIC SPREADING OR CONTINENTAL DOMING AND RIFTING Four main methods to determin e environm e n t of empl acemen t were followed: the major oxide system of Maniar & Piccoli, 1989; the definition of anorogenic grani toids by Whalen, Currie, & Chappell, 1987; the trace element method of Pearce, 1996 and Pearce, Harris, & Ti ndle, 1984; and the discrimination of granitoids from collisi o n a l environ m en t s , Method of Harris, Pear ce, & Tindle, 1986. The methods and main results will be briefly discussed in the next paragraphs. Various other methods were tried , but did not produ c e pract i c a l results (among them, Sylve s ter, 1989 and Batchelor & Bowden, 1985). Barbarin?s method was used to solve incoherences fr om results of other methods. Neverthe l ess , many sample s from the collec t i on produc e incong r ue n t results . It is expected that applicati o n of the vario us physi c a l , chemic al and mineralogical par ameters presented by Barbarin will in time provide more precise environments of emplacement for the granitoids collected in the Lufilian Arc. 2.4.1.2 Major Oxide Method of Maniar & Piccoli, 1989 Maniar & Piccoli, 1989 developed a simple and strai ghtforwar d proc edure to classify the environ ment of emplac e me n t of granito i d rocks based on major oxide chemical analysis . This enabled most of the rock sample s from the Lufilian Arc to be evaluated. After careful processing of all samples t hat fit the classification scheme, results were color-coded and are listed on Table A51. 1 5 Table 2.4 Principal mineralogical, petrographical and chemical features of the main types of granitoids. (After Barbarin, 1999) [M.E.=microgranu lar enclaves . O= absent; X=rare or low; XX=comm o n or medium; XXX=abundant or high.] MINERALS MPG CPG KCG ACG RTG PAG Biotit e X XXX XXX XX X XX Muscovit e XXX X X O O X Cordierite O XX O O O O Sill.- A nd. O X O O O O Amphibole O O X XXX XXX Alk.amph. Pyro xene O O O XX XXX Alk.pyr. Apatit e XXX XXX XX XX XX XX Zircon X XX XXX XXX XXX XXX Monazit e X X O O O O Garnet XX X O O O X Tourmaline XXX XX O O O O Allanite O X XX XX X XX Titanite O O XX XXX X X Ilmenite X X X X X XX Magnetit e O O X XX XX XX Plag An% 0-20 15-40 15-30 20-50 20-50 0-10 PETROGRAPHY P e t r o g r a p h ic Types Leucogranites (gran i t es ) (Leucogr a n i t e s ) Granites Granodiorit es (Qz diorit es ) (Leucogr a n i t e s ) Granites Granodiorit es Qz diorit e s (Granit e s ) Granodiorit es Tonalites Gabbros Plagi o g r a n it es Trondjemites Tonalites Gabbros Alk. Granites Alk. Syen i t es Syeni t e s Granites (Gabbros ) (Anor t ho s it es ) Associated Rocks Metamorphic O Migmatites Anate xi t e s O O O O Volca n ic O O Acid lavas ("Tuff s" ) Andes it es & dacit e s Olivine-bearing Tholeii t es Alkal i n e lavas Mafic O Qz diorit es (Vaugnerit es ) Qz diorit es Gabbros (Appinites) Gabbros (in large amounts) Gabbros (in large amounts) Gabbros (in large amounts) Enclaves X enol i t hs X O-X X X X X Restit es X XXX X O O O Fels ic M.E. X O-X X X X X Mafic M.E. O X XX XXX XXX X Diffe r en t i at i o n Process e s frac t i o na l crys t a l l iz a ti o n frac t i o na l crys ta l l iz a t i o n or restite unmixing F r a c t i on a l crys t a l l iz a ti o n and magma mixing strong frac tio n a l crys t a l l iz a ti o n and magma mixing extreme frac t i o na l crys t a l l iz a ti o n extreme frac t i o na l crys t a l l iz a ti o n and subs olidus interac t i o n s CHEMISTRY Alumina Index A ?CNK CNK>A>NK A ? NK A/KCN (molar) ?1 <1 alkaline Al2O3 XXX XXX XX XX XX X CaO X X XX XXX XX X Na2O XX XX XX XX XXX XXX K2O XX XXX XXX XX X XXX FeOt+MgO+MnO X XX XX XXX XX XX Fe3+/(FeOt + MgO) X X XX XXX XXX XX 87Sr/ 8 6S r 0.706 to 0.760 >0.70 8 0.706 to 0.712 0.706 to 0.708 ? 0. 704 0.704 to 0.712 End -4 to -17 -6 to -9 -4 to ?9 - - delta 18O permil +10 to +14 +10 to +13 +5 to +10 - - delta 34 S permil -12 to +2 +5 to +20 - - 2.4.1.3 Definition of Anorogenic Granitoids, Method of Whalen et al, 1987 Whalen et al., 1987 devis ed a series of geochemi c a l di agrams to discrim in a t e samples that formed in anorogenic environments. The diagrams us e Ga/Al, various major element ratios and Y, Ce, Nb and Zr. Many of the diagrams use the most commonly analysed element s, and that allowed a large number of the samples to be processed in numerous diagrams. A bit of interpre t a t i o n from results was requir ed. A single ?anorogenic? signat u r e was not accepte d , but only repetitive results from the various diagr ams. Similarly, single ?non- ano r o g en i c ? results were not cons ider e d valid. Table A52 lis ts results of the various plots; the last column of the table indica t es interpr et e d result s co ming from more than one of the plots. 1 6 1 7 2.4.1.4 Trace Element Method of Pearce et al, 1984 The experie nc e using tectoni c discrim in a t i o n diagram s devis ed by Pearce, 1996 and Pearce et al., 1984 for granito id rocks of the Greater Lufilia n Arc was unsati s f ac t or y . ?Anorog e n ic ? results from the Whalen et al., 1987 plots were not validat e d by the proc edu r e s of P earce et al., 1984. In most cases , sample s could be plotted on two different diagrams (Nb vs Y and Rb vs Y+ Nb), but results were not coherent . When more than two diagrams were used, coheren t results seldom came out. In fact, many times the so-called Pear ce plots contradict themselves . Table A53 in the Appendix lists the results of all four di agrams . Coheren t results are marked in the last column and a blank space was left when no conc lus i v e results t hat could be used were obt ained from the plots. When two or three of the four diagrams produc ed a similar environ m e nt of emplaceme n t , that was indicate d by a code lik e W2/4, W3/4 or O3/4. Once all the informat i on was proc es se d, and sinc e most of the results were not completely compatible, the databas e was sorted to extract as much informa t i o n from it as possible . Similar results were grouped in order to establis h ?Pearce-plot rock families? . After testing the method in severa l sites, no signific ant results were achieved. The meaning of the ?rock families? was not validated by other field observ ati o n s . A simila r proc e du r e was tried by groupi n g simil a r resul t s from t he (Whalen et al., 1987) plot s . Resul t s were sorte d and grouped into ?Whalen-plo t rock families?. These were not significant either. A very thoroug h review of the Rb vs (Y+Nb) discri mination diagram of Pearce et al, 1984 was publis hed by Forster, Tischendorf, & Trumbull, 1997. It shows that m any granitoids defy the classification schemes devised by Pearce et al., 1984. Geodynamic envir onmen t of formation of many granitoid types does not fit well. In fact, incorre c t envir on me n t s are interpr e t e d in many cases. Many ambigu i t i e s and mis-cl ass i f i c at i o n s aris e when the sample suites come from complex polyphyas e oroge ny that mixes sour ce rocks from different tectonic provenance. Continental arcs and collisional settings that can be clos ely associated in space and time with extensi on a l regimes are especia l l y prone to misinterpr etation using the Pear ce et al., 1984 diagrams . In addition to that, differentiation can produ ce compos itional trends that cros s field boundaries, especially the ?Volcanic Arc Grantiod? and ?Within-Plate Granitoid? field boundary. 2.4.1.5 Discrimination of Granitoids from Collisional Environments, Method of Harris et al, 1986 Harris et al., 1986 develope d a systemati c proc edu r e to evaluate the granitoids from collisional environmen ts. Such environments of emplacement co uld not be identif i e d using the discrim i na t i o n proc ed ur e s of Pearce et al., 1984 and Pearce, 1996. A problem of the Harris? met hodol o gy is that it requires tantalum and halfnium , two elements not commonly analysed for all samples. Basic data and results from the three main plots are listed on Table A54 in the Appendi x . No true collisio n a l gr anito id s were positiv e l y identif i e d . Neverth e le s s , several within- p l a t e and volcanic - arc granitoids were identified. 2.4.1.6 Discussion Table A50 in the Appendix compiles results from six di fferen t methods used to evaluate the environm e n t of emplac e me n t of the various rocks. Coheren t results fr om colums 2, 3 and 4 were marked in red. Incoher e n t results were marked in light yellow. Additional color c oding is indica t e d at the end of the table. The overall interpretation of results from tectonic environment of emplacem ent for the granitoid s of the Lufilian Arc Granito id Project was not conclu s i v e for a large propor t i o n of the samples . Most of the methods to evaluate te ctonic environment of emplacement for granito i d s were develop e d for large batches of samples from the same lo cation. Samples from the Greater Luf ilian Arc come from many different sites . Few speci m en s of simil a r rocks were collec t e d and analyz ed at each site, and in most cases only a single one. That makes interpretation of tectonic discrimination diagrams more difficult. For all the proc edur es of tectonic discrimination, samples were initially treated as single entities and not in cluster form. 2.4.1.7 A Novel Approach Forster et al, 1997 compiled a substantial database of publis hed geochemical information from suites of granitoids from all over the world that have r easonably well established environments of formation. The database includes some major oxides, trace elements and rare earths. At t he time of writing, the author is collaborating with Juan Pablo Lacassie, from the University of Johannesburg, to use Forster?s updated database with neural web geostatistical analysis and specially desi gned software to compare the chemistr y of problematic samples from the present Greater Lufilian Arc study. Lacassie has been using the methods for sedimentary provenance analysis (Lacassie, Roser, Ruiz del Solar, & Herve, 2004). Prelimi nary results of this approach to evaluate samples from 1 8 the Greater Lufilian Arc have been very encouraging, but will not be included in this document. That approach demands a lot of computer processing power, but has prov ed to be the best way to evaluate the environment of emplacement for gran itoid igneous rocks. A complete re-evaluation of the environ ment for ea ch of the granito i ds analyse d will be carried out and pres ented in a public ation after the Ph.D. thesis . 2.4.2 Mafic Rocks As indicat e d in previou s chapte r s , many of the samplin g sites had only gabbro ic rock outcrop s , and in most locati on s mafic and fels ic intrus i v e rocks were intima t e ly associated. Although very few of the mafic rocks collected for the Lufilian Arc Granitoid Projec t were ba salts, they were all analysed following methods devised to discriminate tecton ic environmen t of emplac ement fo r mafic volc a n ic rocks . Prec is e l y the same approa c h was made by Kampunzu , Tembo, Matheis, Kapenda , & Huntsman-Mapila, 2000 and Tembo, 1995 to study Katangan mafic igneous rocks of the Democratic Rep ublic of Congo and Zambia. In general terms, the followi ng procedu r e was followed : All mafic and ultramafic rocks from the suite of samples colle cted during fieldwork in the Greater Lufilian Arc were separa te d based on their major oxide chemis t r y . Carbonat i t ic rocks were taken out of the group before furth e r stud ies . Mafic sampl e s were sele c te d base d on the R1-R2 and modified TAS diagrams. Later the systematics of Winchester & Floyd, 1977 was applie d to name the vario us ro cks. Most of the sample s were certainly not basalts. Some of them turned out to be ultrama f i c and lamproph y r i c ; but that was discove r e d later in the process. Once that was done, discri mination diagrams to evaluate environment of emplacement of mafic volc anic rocks devised by Meschede, 1986; Pearce & Cann, 1973; Wood, 1980; and Shervais, 1982 were used. Each of the proc edur e s was completed independ en t l y from the others, in order to compar e results. Interpretations from all results are listed on Table A53 in the Appendi x . No singl e sample plots the same on all four of the tectonic discrimin a t i o n diagrams devised by (Pearce & Cann, 1973). Accordin g to Pearce & Cann, 1973 only rocks with CaO+MgO values between 12 and 20 should be evalua t e d in their classif i c a t i o n . The proc edu r e s that follow includ e a wider range of rocks. On Table A56, sample s that fall out of that range were highli g h t e d in pink; thes e ar e 33, and accoun t for 37.1% of the sample s identi f i e d as ?mafic rocks?. The process of tect on i c discri m i na t i o n was never t h ele s s fo llowed for all of the sample s, and results are presen ted on Table A56 in the Appendix. They are also included on tables in each of the chapters from the domains. 2.4.3 Conventions to Tabulate Rock Type and Methods to Evaluate Environment of Emplacement for Samples Studied A l l chapter s that describ e rock domains in this documen t contain review tables such as that of Table 2.5. Comple te tables are include d in Appendi x G. The first column contain s the sample number . The second , the rock name as respectively indicated by the TAS diagram s of Middlemost and the IUGS for plutonic or volcanic rocks . The third column shows the rock type class ificati o n of Debon & LeFort. Table 2.6 lists acronyms used to shorten the detailed rock names, after using the various diagrams defined by Debon & LeFort, 1983. Table 2.5 Review of sample main characteristics and potential environment of emplacement obtained by traditional methods 1 2 3 4 5 6 7 8 9 10 Methods to Evaluate Environment of Emplacement Sample Rock Name Debon & LeFort Rock Type Classification Maniar & Piccoli Whalen Pierce Mafic Rb/10HfTa Rb/30HfTa Nb-Ta L-012A quartzmonzonite metaiv mesoKMg IAG+CAG A O-W 1-1 L-079 Granite metaiv mesoNaKFe O-W 1-1 L-353 quartzmonzonite metav mesoNaKFe A W L-354 Granodiorit e peraiii mesoNaKFe A W 1 9 Table 2.6 Acronyms used to shorten rock names (after the use of Debon & LeFort, 1983) Convention Meaning Debon-LeFort Diagram p e r a peral u m i n o u s field meta metal u m i n o u s field i,ii, i i i locat i o n s in the peral u m i n o u s field iv,v, v i locat i o n s in the metal u m i n o u s field A-B Diagram (Fi g 2.5) leuc o leuc o c r a t i c fiel d suble u c o suble u c o c r a t i c field meso meso c ra t i c fiel d Na sodi c fiel d Na-K sodi c - p o t a s s i c fiel d P Pota s s i c K*-B Diagra m (Fi g 2.7) Mg Magne s i a n Fe Ferri fe rous Mg*-B Diagra m (Fig 2.8) Column s 4 to 10 of Table 2.5 pres ent the environment s of emplacement identified for each rock sample, according to seven different method s described in the previous pages. The fourth column shows results of the major oxide method devised by Maniar & Piccoli, 1989. Table 2.7 lists t he acronyms used for environment of emplac eme n t terms deduced after using the various diagrams defined by Maniar & Piccoli, 1989. Table 2.7 Acronyms for environment of emplacement term, diagrams of Maniar & Piccoli, 1989 Acronym Meaning P O G Post-O r o g e n i c Granit o i d IAG+CA G Island Arc Granit o i d + Conti n e n t a l Arc Grani t o i d CEUG Conti n e n t a l Epeir o g e n i c Uplif t Gra ni t o i d RRG Rift-Re l a t e d Gra nito i d OP Ocean i c Plagi o g r a n i t e CCG Conti n e n t a l Colli s i o n Grani t o i d CCG-I A G - C A G Impos i b l e to define bet we e n these three types CEUG-R R G CEUG near the margin with RR G RRG-CEU G RRG near the m argin with CEU G The fifth column pres en ts results of the method to identify anorogenic granitoids by Whalen et al, 1987. C o l u mn 6 of Table 2.5 pres e n ts resul ts of the Pearc e et al, 1984 trace element method to identify environm e n t of emplacement for granitoids. Column 7 pres en ts res ults of the vario us metho ds to discriminate the tectonic environment of emplacement for the mafic rocks (Mes c h ede, 1986; Pearce & Cann, 1973; Wood, 1980; and Shervais , 1982). Table 2.8 lists the acronyms used for the environme n t of emplacemen t of mafic rocks. Table 2.8 Acronyms for environment of emplacement terms of mafic rocks Acronym Meaning M o r Mid-Oc e a n Ridg e Basalt Emor E-T yp e Mid- O c e a n Ridge Basal t Wpab With i n - P l a t e Alkal i n e Basa l t Vab Volc a n i c Arc Basal t Wpt Withi n - P l a t e Thole i i t e ? Unkno wn Envir o n m e n t - Or + And 2 0 C o l u mn s 8 to 10 show resul t s of the proce d ur e defin e d by Harris et al, 1986 for granit o i ds from collis io n a l environm e n ts . Table 2.9 lists acrony ms used by the authors for the envi ro n me n t of emplac e m en t of such granit o id s . Table 2.9 Acronyms for environment of emplacement terms, diagrams of Harris et al, 1986 Acronym Meaning W P With i n -P l a t e Gran i t o i d s VA Volk a n i c Arc Gran i t o i d s II Type II Coll i s i o n a l Gran i t o i d s VA- Plot s in Volca n ic Arc Fiel d but migh t be Colli s i o n a l Gran i t o i d WP- Plots in Withi n - P la t e Field but mig ht be Colli s i o n a l Grani t o i d OF Oceanic Floor Gr anito i d 2 1 3 GENERALIZED GEOLOGY OF THE LUFILIAN ARC The Greater Lufilian Arc is one of many Pan African orogenic belts. Thes e mobile belts are an importa n t component of the African geology and developed ext ensively throughout the continent. They formed during a series of orogen ic cycles over a period of 500 million years (approximately 950 to 450 Ma), to produc e the Africa n sector of the Gondwan a supe rcon t i ne n t (Fig 1.1). Diverse orogenic styles in the belts range from major contine n t a l collis i on (Moz amb i qu e Belt) throug h t he closur e of small oceanic trac ts (Damar a Belt) to major accretio n a r y belts of island arcs and microc on t i n e n t s (Nubian Shield) (Foster et al., 2001). Orogenic evolution was very diverse through space and time du ring Pan African times. That makes correla t i on of strati gr a ph i c sequenc es , intrus i v e , metamo r p h ic and tecton ic events between the differ e n t terran es comple x and, in some cases, irrelevant (Foster et al., 2001). The Lufilian Arc of southern Africa is composed by a Meso- to Neo-Proterozoic rift basi n that ceased to exist after closure of the basin during th e Pan-African orogeny at approximate l y 500 Ma (Kampun z u & Cailteau x , 1999). It is made by the extensio n of the Pan African Katanga fold belt westward into the Damara fold belt (Figs 1.1 and 3.1). Superf i c i a l cover of Mesozo ic rocks conform e d by Karoo deposit s and Kalahar i sand masks the central portion in NE Namibia, Bots wana, Angola and SW Zambia (Fig 1.1). A geological recons t r uc t i on map of Gondwan a terrain s is shown on Fig 3.1. Note the Lufilian Arc emplac ed between the Congo Craton and the Kapvaal Craton in the southwes t e r n part of Africa. As shown, similar belts border craton s throughout most of Africa, in parts of east ern South Americ a and India. Note the location of the Caraj?s province in Brazil, wher e major IOCG deposits are know n to exist (Table 8.1). Fig 3.1 Schematic structural map of Gondwana. T his map show s location of the Gr eater Lufilian Arc rough ly in the middl e, indicated with a rectangle. It is ma de by the exte n sion of the Katanga fold b elt into the Damara fold b elt, and lies betw een the C ong o and Kaapval cratons. Like other Pan-African fol d belts, the Gr eater Lufilian Arc was formed during th e amalgamation of continental t erranes to conform Go ndwana. The prolific mineral province of Caraj?s in Brazil, off th e eastern b order of the Guapor? Cr aton, is indicated by a smaller rectangle. Note similarities among both locations. T hey lie in b etw een Archean cratons and w ere formed d uring collisions . Als o n ote the extens e portions of Africa and So uth America that have similar tectonic features. IOCG mineralization is prospective in most of that area. Figure s lightly mo dified from Tromp ette, 199 4. 2 2 T h e Damara sequenc e of rocks (Namibi a ) and the Ka tangan sedimentary sequence (Democratic Republic of Congo and Zambia) were deposi t e d during the opening of an ocean (Miller, 1983; Martin & Eder, 1983; Hoffmann, 1990; and Porada, 1989). Katangan rocks host t he Copper be l t world- c l as s copper and Co depos i t s (Mende ls o h n , 1961; Unrug, 1988; Kampunz u & Cailt eaux, 1999; Miller, 1994; Sweeney & Binda, 1994; and Singer, 1995). Rocks of the Damara Orogen cover half of northe r n Na mibia. They are made by a thin N-S coastal branch and a thick NE-tren d i ng branch. The second one ha s been divided into a number of contras t i n g tecton os t r a t i gr a p h ic zones (Mille r , 1983a; Miller , 1994; Mille r , 2002). ?The struct ure and tecton oth e r m a l history of the northea s t arm of the orogen have been explaine d in terms of a plate- te c t o n ic model based on the pres ence of paired metamorphic belts; extensive calc-alk ali granite intrus i ons ; an assyme tr i c struc ture ; an intensely thrusted southe rn margin; and basic and ultr a b as ic igneo us rocks occur r i n g in assoc ia t i o n with a high-pressure, schis tose flycsh.? (Foster et al, 2001, p. B-16). The Lufili a n Arc se ns u s tricto (bas ic al l y the Pan-Afr ic a n Katang an belt in Zambia and the D.R. Congo) has been intensive l y studied since the beginnin g of the twent ieth century when mining in the Central African Copperb e l t began. The Katangan Supergr o up basical l y cons is ts of a series of basal continen t a l and shallow marine silicic la s t i c s and carbona t e s ; thes e are overlai n by marine shales , dolomi t e s and sandst on es ; in turn they are overlain by black shales and carbonates. Abundant volcanic mate rial is intercalated with most of the units . Crus tal attenuat i o n and rifting of the MesoPr ot e r o z oic Rodinia Supercon t i n e n t lead to contine n t a l break-u p and to the formation of an ocean basin. Pre-rift mi dalkaline granitoid magmatism, syn-rift continental sedimentation, rift-related bimodal tholeiitic volcanism , and granite emplac emen t took place during 890 to 850 Ma. The early rift basin s were filled by continental clas tics; later by shallo w marine clastics and platfo rm carbonates; and tholeiitic basalts within a succession of oceanic silicicl as t i c s and carbonat e rocks. Thick diamict i t es with interbed s of banded iron formati on a nd impure sandston es were interca l a t ed by rift-re l a t ed ocean ic volcan i c rocks . A short- l i v e d subduc t i o n of part of the oceani c basin began by 640 Ma (Tembo & Porada, 2002) before the closure of the Katanga-Damara basi n . It was followe d by contine n t a l collisi on around 550 Ma, widespr ea d , NE-tren d i ng thrusti n g , emplace me n t of anoroge n i c granito i d s , and contine n t a l- s c a l e shearin g . The cons idera b l e thrusti ng and shearin g that took plac e during contine n t a l collis io n makes strati g r ap h i c correlation of the Katanga Supergroup difficult. The importa n c e of halok ines is in the evolution of the region is very signific an t and is just beginn in g to be understood . Signific an t revision s to the stratigr a p hy are being made (Cailteaux, 1995; Master et al, 2003). Midalkaline magmatism took place during the rifting phase. Bimodal midalka lin e magmatism and vulcan i s m occurred during the opening of the Katanga- D am a r a ba sin . Wides pr e ad midal k a l in e magma t i s m occur r ed after clos ur e of the basin; subalk a line magmatis m, during a shor t-lived subduction-related event; and later anorogenic midalkaline magmatism, during epeirogenic upli ft and post orogenic collaps e that took place after clos ure of the basin. Igneous massifs like the Lusaka pluton, Hook Granite Batho lith, Kamanjab Batholith, Khorixas Inlier and Otjiwaro n g o Batholit h are examples of granitoid bodies formed by those proc esses (Figs 4.1 and 4.2). Rocks in the massif s have a wide petrogr a p h i c variabil i t y ; they range from alkali granites throug h quartmo nz o n it e s , granite s , syenites , diorite s and granodi o r ites into carbonatites. Some of those granitoids are high-heat producers, with elevated Th, K and/or U conten t (Phillips, 1958a; Phillips, 1958b and Griffiths, 1978). Abundant small gabb roic intrus ions ac companied midalkaline magmatis m throughout. 2 3 4 DESCRIPTION OF ROCKS FROM THE DIFFERENT DOMAINS Samples collect e d for the Greater Lufilia n Arc Granito i d Projec t were grouped for preliminar y evaluation into geograph i c a l domains with apparen t l y similar geolog i c a l char ac t e r is t i c s . The domain s were establ is h ed as a means to pres ent the information in this Ph.D. thes is. Thes e are listed on Table 4.1. The maps of Figs M1 and M19 (prese n te d in the Append ic es Volume ) show their ge neral location . A few of the domains sampled will not be describe d in this documen t . These are marked by an asteris k on Table 4.1. Samples from those domain s were incomp le tely analysed, or did not contain granito id s . The next chapter will describ e main charac t er i s ti c s of rocks from each domain, following the same arbitrary order of Table 4.1. Table 4.1 Geographical-Geological Domains sam pled during the Greater Lufilian Arc Granitoid Project. T h es e domains were establis he d for descripti v e purposes . They are geograp h ic a l entitie s as shown on Figs M1 and M19. (Domains marked with an asterisk did not contain granito i d s , or their sample s have not been fully studied at the time of writing this document.) ZAMBIAN DOMAINS NAMIBIAN DOMAINS Hook Granite Batholith Kamanjab Batholith West Lusaka-Kafue Fl ats Khorixas Inlier Kalengw a- K as e m pa Area Oas farm NW Zambia Lofdal farm Kalene Hill Area Mesopo tamie farm Kabompo Dome Several outcrops south of Khorixas Inlier Mwombezhi Dome Ugab River Area Solwezi Dome Summas Mountains Sodalite Nepheline Syenite Quarry Grootfontein Inlier Main Zambian Copperbelt Area Otjiwarongo Environs Nchanga Mine Area Okwa River, Botswana Nchanga Granite Muliashi Porphyry Other domains sampled but not included in this document Deep Borehole, Konk ola Mine *Okatjepuiko, Witvlei Chambishi Granite *Gelbingen Farm Mufulira Granite *Sesfontein Area Samba Copper Pros pect *Otavi Mountains Other domains sampled but not included *Tshoosha / K a l k f o n t e i n , Botswana *Serenje Area *Mkushi Area *Bwana Mkubwa Area 2 4 4.1 ZAMBIAN DOMAINS 4.1.1 HOOK GRANITE BATHOLITH, ZAMBIA 4.1.1.1 Introduction The Hook Granite Batholith is located in wester n Zambia, as indicated on the map of Fig M1, in the Appendix. Its name is derived from a rectangu la r turn that the Kaf ue River makes through the granitic massif. Part of the turn is control l e d by a N-S frac tur e zone on its way south and southeas t into the Zambez i River (Fig 4.1). It fulfills the definition of batholith becaus e it is ?a type of area, where indivi d u a l pluton s are so numer o us as to overlap or intersec t one an other? (Hall, 187, p. 93). Fig 4.1 General map of the Hook Granite Batholith. N o t e t h e angular turns that the Kafue river does around the batholith. Also n o t e t he road that crosse s the batholith from east to wes t from Mumb wa. A sampling transect was done along that road. The roughly triangular shape of t h e batholith will be discussed o n chapter 7. Pink indicates granitoid rocks of th e H oo k Granite; brown, Mesozoic Karoo rocks; light green, Katangan sediments; orange, me ta-sediments; y e l lo w , allu vial and cover; dott e d orange, Kalahari sand. The b lack squares indicate 1:10 0 , 0 0 0 g eo l ogical map sheet s p u b lished b y t h e Zambian Geolo gical Survey. S mall dots with sy mb o l s indiate various mineral deposits and oc currences. Yel l ow s hapes are gold d ep osits; red, copper deposits; brown, iron; gray, uranium; purple bo wtie s are kimberlites; b l ue , e vaporites; green, industrial minerals. Specific deposits will not b e di scussed here. Notice that the SW port ion of the batholith, west of the Kafue River, does n o t have any mineral occurrences. Ge o l og y is very similar, but it is less well studied. Taken from 1:2,00 0 , 0 0 0 g eo l o gical and mineral occurrence map of Zambia, 1994. Surprisi ng l y little is know n about this importa n t Za mbian batholit h . The publis hed 1:100,000 geolog ic a l maps are less than reconais s a nc e grade, but cons tit u t e a formidab le amount of work, given the lack of outcrop , access and infrastr uc t u r e (Philli ps , 1958; Simpson , 1962; Cikin, 1971; Cikin, 1972; Page, 1974; Abel, 1976; and Griffi t h s , 1978). The geolog i c a l map sheets publis h ed by the various authors are show n by large black squares on Fig. 4.1. Report s accomp a ny the maps incl uded in the figure. They deal mainly with petrography of the various mappab l e units, and contai n genera l descri ptions of mineral deposits, hydrothermal alteration 2 5 features , structures, and stratigr a phic units that cover and were intruded by the batholith. Geolog ical compila t i o n work and geochro no l o g y of the batholith was published by Hans on et al, 1993. Attempts to evaluate geoc hemis try of the Hook Granite have be en carried out by Pepper, 2000 and Goagoseb, 2004. In additio n to the previous l y listed documen t s , reports about mineraliz a t i o n on and around the batholit h have been published by Hitzman, 2001; Nisbet, Cooke, Richards, & Williams , 2000; and Nisbet, 2004b. Fig 4.1 shows the main know n minera l deposi t s and occurr e n c e s . Structural geology of the intrus ive body is not well describ e d or mapped in the public l y - a va i l a b l e geolog i c a l lit er ature. Many of the feat ure s observed during field work for this Ph.D. projec t have never been described in the literature. This account will first describe the c hemis try of sample s collected in the batholith; next comes a discussion on problems faced with mapped geologic a l units; that will be fo llowed by evidence of circular complexes in the Hook Granite; and an E-W sampling transect through t he batho li t h; the rest of the chapter will be comple t e d by comments on geochrono logy, geological history and envir onment of emplacement of the Hook granitoids. 4.1.1.2 Geochemistry One-hund r e d- a n d- f o ur samples were collect ed from the ma in Hook Granite Batholith in an effort to produce a repr es e n t a t i ve spread . Ninete e n sample s were collec t e d in the field. Forty-four samples were selected from the collect i o n of the Zambian Geologic al Survey in Lusak a, and located as best as possibl e accordi n g to the author?s descrip t i o ns and field notes, with help of 1:50,00 0 and 1:100,0 00 topogra p h ic maps. Major oxide chemic al analysis of thirty-t h r e e samples X-43 to X-74 were taken directl y from Griffit h s , 1978, and located according to the author?s description and field notes. Finally, eight, reas onab ly well studied and located sample s were recovere d (Pepper, 2000). Most of the samples clus ter from 69 to 77% silica. In general terms, geoc hemistry of the batholith shows the following trends (Fig 4.2): There is a negative correlation of silica with titanium dioxide, alumina, total iron oxide, magnesia , lime and P 2 O 5 ; a positiv e correl a t i o n was observ ed between silica and potash. Manganes e oxide and soda do not correl a t e . The trends are wide and qu ite complex, as shown. As will be explaine d in a later portion of this chapter , each of the trends is made of numero us linear trends that come from differ e n t types of graniti c rocks from ring complexe s , and are unrelat ed to each other. Fig 4.3 is a clos e- up of a modified TAS diagr am show ing the wide variety of granitoid rocks that occ ur in the main batholith. Fig 4.4 shows the en tire suite of samples on the modifi ed TAS diagram. Fig 4.5 illustrate s the same samples on the R1/R 2 diagram . The statis t i c s of Table 4.1.1 were obtaine d from the TAS diagram of sample s from the batholith. Only samples that plotted inside the diagram were consider ed . Table 4.1.1 Statistics of rock types in the su ite of samples from the Hook Granite Batholith The fifth column (Granitoids) is the sum of underlined rock types. Group Rock type number % Granitoids Groups a l k a l i grani t e 26 29.21 Q u a r t z m o n z o n i t e 20 22.47 S ye n i t e 7 7.87 M o n z o n i t e 5 5.62 71 . 6 0 Monzo d i o r i t e 3 3.37 M o n z o g a b b r o 1 1.12 Midalkaline Rocks a l k a l i gabbr o 2 2.25 71.91 Granite 16 17.98 G r a n o d i o r i t e 7 7.87 28 . 4 0 Gabb ro-di o ri te 1 1.12 Subalkaline Rocks Gabb ro 1 1.12 28.09 Total 8 9 1 0 0 . 0 0 1 0 0 . 0 0 100.00 65% of the granitoid s fall within the midalkaline field, while 26% of them fall in the subalkaline field. All midalkaline rocks make 72% of the samples, 28% of them are subalka l in e . None are alkaline . This is significant, especially when 22.5% of the rocks are quartz monzonites. The R1/R2 plot for the Hook Granite (Fig 4.5) show s a large range of rock types. Fig 4.6 pr esen t s the entire R1/R 2 diagra m with all the sample s that were studied for the batholith. 2 6 M a n y of the sample s from X-46 to P-40ii are enric hed in K 2 O (Table A3). Many of the samples from L-181 to L-345 to L-465 are enrich ed in Fe 2 O 3 . Most of the Hook Granite sample s have very high conten t s of Nd, Pr. Ce and La are also high. Fig 4.2 Correlation diagrams between silica and the major oxides for samples from the Hook Granite Batholith, Zambia . All values are in percentage . Samples P-57 and P-50 are anomalou s l y enriche d in many LREE, Nb and K 2 O. P-39 to P-41 have high conten ts of Rb, Y, Nb, Ga and Co. These are all featur es of anorogenic granites. All samples from the Hook Granite were compare d with each other using the logarith m ic plot of major oxides. Thirteen discrete groups were identified, and they ar e listed on Table 4.2. 27 samples could not be allocat e d to any of the groups. Main features of each of the group s is also inclu de d on the table. Rock groups that show 2 7 similarities with groups of rocks from the Kamanjab Batholith 1 in Namibia ar e indicated with an asterisk (See Table 4.2) . The geochem ic a l diagram s of Figs 4. 3 and 4.5 show that the gr oups behave as indepe n de n t chemical entities. Logarithmic major oxide plots of the various groups are shown on Figs 4.7 to 4.14. Part of the samples from the batholi t h are enric he d in copper. Ring comple x e s 2 with high Cu are underli ne d of Fig 4.18 (A, E, O, K and P). Chemistr y of all t he samples is show n on Table A3 in the Appendi x . Table 4.2 Groups of samples from the Hook Granite Batholith, based on major oxide chemistry and logarithmic plots . * = group that was also in the Kamanjab Batho lith. Table 4.5 presents f urther details on th e rock groups. Sub-chapter 4.1.1.3 describes geological units. Group # samples Characteristics Rock Type I * 13 high Fe,Mg , M n l ow Si,K sye ni t e , quart z m o n z o n i t e , grano d i o r i t e , s yeni t e , ton al i t e II* 9 high Mg,P, M n low Si gabbr o i d s III* 6 Orde r = K,Na, Fe, C a , M g , T i granite , alkal i grani t e IV* 6 Orde r = K,Na, Fe , C a , T i , M g granit e , alkali granit e , quartz s yeni t e VII 9 high K, order = K,Fe,N a , C a , M g granit e , gra nod i o ri t e VIII IX 4 Orde r = K,Fe, Na , C a , T i , M g quartz s yenit e , gr anit e , quartz m o n z o n i t e X 10 Orde r = K,Fe, Na , C a , T i , M g granit e , qua rtz m o n z o n i t e XI 8 Orde r = K,Fe, Ca , N a , T i , M g alkali granit e , granit e XII XIII Another group of sample s from the Hook Granite was f ound to have high Zn values. Thes e are listed on Table 4.3. A few ring comple xes 2 contain them. Three of the complexe s with high Zn values have gabbroic ring dikes: K, AC and AL. Only a few of the sample s from T able 4.3 come from the center of the ring comple xe s , these are: L-433, L-437. Table 4.3 High Zn samples from the Hook Granite Batholith, Zambia F or location of ring complexes , s e e Fig 4.18 . Sample Ring complex Rock type (sensu TAS) Rock type (sensu Dela Roche, 1980) General rock type Position within ring dike L - 1 8 1 ? Gabb ro Saturat e d olivine gabbro Gabb roi d L-347 K Gabb ro Gabb ro Gabb roid Nucleus L-403 O Quartzmonzonite Quartz mo nzo n i t e Grani t o i d Rim L-406 O Gabb ro Alkali gabbro Gabb roi d Rim L-410 E Gran odi o r i t e Granite Granito i d Rim L-433 Q Monzodi o r i t e Syeno ga bbro Gabb roi d Nucleus L-437 P Monzo n i t e Syeno diori t e Syeni t o i d Nucle u s L-440 AC Monzoga b b r o Gabb ro- d i o r i t e Gabb roi d Rim L-441 K Quartzm o n z o n i t e Quartz mo nzo n i t e Grani t o i d Rim L-444 AQ Monzodi o r i t e Gabb ro- d i o r i t e Gabb roi d L-459 ? Diorite Tonali t e Granit o i d L-463 AL Gabb ro Gabb ro-diorite Gabb roid Rim L-464 AL Out of plot, foid Foid- r i c h rock Foid- r i c h s yeni t o i d Rim L-465 AL Out of plot, foid Foid- r i c h rock Foid- r i c h s yeni t o i d Rim 1 The Kamanjab Batholith of Namibia is discussed in section 4.2.1 of this documen t. 2 Relationship of the Hook Granite Batholith with ano rog en i c ring comple x es will be explai n ed in sub-cha p te r s 4.1.1.4 and 4.1.1.5. Fig 4.18 shows t he main ring complex e s that have been identified in the batholith. 4 5 5 0 5 5 6 0 6 5 7 0 7 5 8 0 SiO2% 3 4 5 6 7 8 9 1 0 1 1 1 2 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM Hook Granite Batholith, Zambia; Lufilian G.P. (Based on Middlemost, 1994, 1997) S a m p l e s P e t r o gr a p h ic fie l d s L i n e / S c a t t e r Pl o t 17 L-012 L-012A L-079 L-237 L-23839 L-242 L-248 L-248-LG L-249 L-257 L-259 L-259-B L-263 L-341 L-343 L-344 L-345 L-346 L-347 L-348 L-349 L-352 L-353 L-354 L-355 L-402 L-403 L-405 L-406 L-407 L-408 L-409 L-410 L-433 L-434 L-435 L-436 L-437 L-438 L-439 L-440 L-441 L-442 L-443 L-444 X-43 X-44 X-45 X-46 X-47 X-48 X-49 X-50 X-51 X-52 X-53 X-54 X-55 X-56 X-57 X-58 X-59 X-60 X-61 X-62 X-63 X-64 X-65 X-66 X-67 X-68 X-69 X-70 X-71 X-72 X-73 X-74 X-75 P-39 P-46 P-50 P-53 P-58 P-40i P-40ii L-207 L-208 L-209 L-210 L-212 L-213 L-214 L-215 L-217 L-218 L-222 L-223 L-224 L-416 L-458 L-459 L-460 L-461 L-462 L-463 L-466 L-467 X-90I II IV VII Fig 4 .3 Notes: Re d do ts * in d i c a t e s a m p l e s fro m ro ck gro u p XI. O t h e r as p e c t s d e sc r i b e d in tex t. XI* 5 1 0 1 5 2 0 2 5 3 0 3 5 4 0 4 5 5 0 5 5 6 0 6 5 7 0 7 5 8 0 SiO2% 0 1 2 3 4 5 6 7 8 9 1 0 1 1 1 2 1 3 1 4 1 5 1 6 1 7 1 8 1 9 2 0 2 1 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM Hook Granite Batholith, Zambia; Lufilian G.P. (Based on Middlemost, 1994, 199 7 ) S am pl es P etr o gr a ph ic fie ld s L-012 L-012A L-079 L-237 L-23839 L-242 L-248 L-248-LG L-249 L-257 L-259 L-259-BL-263 L-341 L-343 L-344 L-345 L-346 L-347 L-348 L-349 L-352 L-353 L-354 L-355 L-402 L-403 L-405 L-406 L-407 L-408 L-409 L-410 L-411 L-433 L-434 L-435 L-436 L-437 L-438 L-439 L-440 L-441 L-442 L-443 L-444 X-43 X-44 X-45 X-46 X-47 X-48 X-49 X-50 X-51 X-52 X-53 X-54 X-55 X-56 X-57 X-58 X-59 X-60 X-61 X-62 X-63 X-64 X-65 X-66 X-67 X-68 X-69 X-70 X-71 X-72 X-73 X-74 X-75 P-39 P-46 P-50 P-53 P-57 P-58 P-40i P-40ii L-207L-208 L-209 L-210 L-212 L-213 L-214 L-215 L-217 L-218 L-222 L-223 L-224 L-416 L-458 L-459 L-460 L-461 L-462 L-463 L-466 L-467 X-90 Fig 4 .4 Note: T h e ce n t r a l clu s t e r o f s a m p l e s on th e gr a n i t e a n d q ua r t z m o n z o n i t e fi el d s is be tte r s h o w n on Fi g 4. 3 . 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti) 5 0 0 L-012 L-012A L-079 L-237 L-23839 L-242 L-248 L-248-LG L-249 L-257 L-259 L-259-B L-263 L-345 L-346 L-348 L-349 L-352 L-353 L-354 L-355 L-402 L-403 L-408 L-409 L-410 L-434 L-435 L-436 L-439 L-441 L-442 L-443 X-43 X-44 X-45 X-46 X-47 X-48 X-49 X-50 X-51 X-52 X-53 X-54 X-55 X-56 X-57 X-58 X-59 X-60 X-61 X-62 X-63 X-64 X-65 X-66 X-67 X-68 X-69 X-70 X-71 X-72 X-73 X-75 P-39 P-46 P-50 P-53 P-58 P-40i P-40ii I IV VII XI R1R2 PLUTONIC ROCK CLASSIFICATION Hook Granite batholith, Zambia: Lufilian G.P. (After De la Roche et al, 1980) Fig 4 .5 - 5 0 0 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti) 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 R 2 = 6C a +2M g +A l L-012L-012A L-079 L-237L-23839 L-242 L-248 L-248-LG L-249 L-257 L-259 L-259-B L-263 L-341 L-343 L-344 L-345 L-346 L-347 L-348 L-349 L-352 L-353 L-354 L-355 L-402 L-403 L-405 L-406 L-407 L-408L-409 L-410 L-433 L-434 L-435 L-436 L-437 L-438 L-439 L-440 L-441 L-442 L-443 L-444 X-43 X-44 X-45 X-46 X-47 X-48 X-49 X-50 X-51 X-52 X 53 X-54 X-55 X-56 X-57 X-58 X 9 X-60 X-61 X-62 X-63 X-64 X-65X-66 X-67X-68 X-69 X-70 X-71X-72 X-73 X-74 X-75 P-39 P 46 P-50 P 53P-57 P-58 P-40i P-40ii L-411 R1R2 PLUTONIC ROCK CLASSIFICATION Hook Granite batholith, Zambia: Lufilian G.P. (After De la Roche et al, 1980) P e t r o g r a p h i c fi e l d s S a m p l e s Fig 4 .6 Note: T h e ce n tr a l cl u s t e r o f s am p l e s o n th e g ra n i t e a nd q u a r t z m o n z o n i t e f i e l d s is be t t e r sh o w n on F ig 4. 5 . 3 2 3 3 3 4 3 5 3 6 4.1.1.3 Geological Units Geolog ic a l units from eac h of the eight publis h ed 1: 100,000 , half-deg r ee by half-deg r ee geolog ic a l map sheets were correla t e d on Table 4.4. They were correl a t e d from one map to the next to produc e a series of discret e map units. Several units cannot correla t e well, due to varying litholog i e s and mapping strateg ie s of the various authors. In fact, many of the contac ts between litholog ic units run along map borders. Some roads that can now be used to traverse through the Hook Gr anite Batholith were not available at the time of mapping . For that reas on , many of the outcrops ope ned during the constr uc t i o n of the roads have not been include d in the origina l mapping . This produce d many new mappab l e units. Exampl e s of such outcro ps lie along the E-W road from Mumbwa to eastern Zambia, acro ss the Kafue Nationa l Park. Twelve samples were analysed from the most relevant outcrops along the road, and geology along that transec t does not coincid e with the 1:100,0 0 0 geologic a l map sh eets (for example on Sheet 1426SE). For lack of a better system, the mapping units from each map sheet were corre la t e d with those used by Hans on et al, 1993. Results of that process are shown on the map of Fi g 4.15 and on Table 4.4. As seen on Table 4.11, there is a wide variability in the chemis try of the samples . This may be due to imprope r selecti on of the mapping units, to a large variability in the mapping units, or both. Careful evaluation indicated that in some cases, units Nos. 8 and 1 (from Table 4.4) coul d be grouped. In others , units 9 and 1 could be groupe d . Unit 12 could be grouped with unit 2, unit 9 with 3, and unit 13 with 1. After findin g out that mappin g units were not coheren t with the geochemis try and field observations , a new approach to group all available sample s by chemis try was tried out. All samples from the Hook Granite Batholi t h with chemica l analysis were grouped using major oxide values and logarit hm i c plots. This is explained on Table 4.5. And later, rocks with similar c hemis try were mapped as ?units?. The main faults and some lithologic a l contacts were kept as limits betw een map units, and new polygonal limits were produced betwee n contra s t i ng map units. This exercis e had no t been complet e d , when the conc ep t of a ring complex clus ter for the batholit h was devised. The scope of this projec t did not include remapp i ng of the Hook Granite Batholit h , but in the opinion of the author, mapped units are not adequate and a major re-mappi n g effort is needed. 3 7 3 8 3 9 Table 4.5 Hook Granite Batholith ro ck types and environment of emplacement ( s ee acronym description on s ection 2.4.3 . ) Sample Rock Name Debon & LeFort Maniar & Piccoli Whalen Pierce Mafic Rb/10HfTa Rb/30HfTa Nb-Ta Type I L - 0 1 2 quartz syenite IAG+CAG A VA- III INW -INV L-012A quartzmonzonite metaiv mesoKMg IAG+CAG A O-W 1-1 L-079 granite metaiv mesoNaKFe O-W 1-1 L-353 quartzmonzonite metav mesoNaKFe A W L-354 granodiorit e peraiii mesoNaKFe A W L-403 quartzmonzonite metaiv mesoNaKFe CEUG A W P-58 gran i t e meta i v meso NaFe VA- III INV- I NW X-45* granite metaiv mesoNaKF e X-52* granite metaiv mesoNaKF e X-56 granodiorit e metaiv mesoNaKFe IAG+CAG X-57 granodiorit e metaiv mesoKFe X-63* quartzmonzonite metaiv mesoNaFe X-73* granite metaiv mesoNaFe Type VII L-237 granite peraiii mesoKFe CEUG A O-W 1-1 L-238 granodiorit e metaiv mesoKFe CEUG-RRG A O3/4 OUTU L-239 granite metaiv mesoKFe A O-W 1-1 L-249 granite peraiii mesoNaKFe A O3/4 OUTU L-352 granite metaiv mesoNaKFe CEUG A O-W 1-1 L-434 granodiorit e peraii mesoKFe RRG-CEUG A X-58* granit e peraii i subleuc oK F e X-67 granite peraii mesoKFe Type IV L-259 granite metaiv, peraiii subleucoKFe A W L-408* granite metaiv mesoNaKFe CEUG A W L-435 quartz syenite metaiv mesoKFe CEUG A O-W 1-1 L-439 alkali granite metaiv mesoNaKFe RRG A W L-467 alkali granite metav leucoNaFe RRG-CEUG A P-53* granit e metav subleuc o K Fe CEUG VA- II INV-INW Type IX L-346 granite metaiv mesoKFe RRG-CEUG A O-W 1-1 L-348 granodiorit e metav mesoNaFe A V1/2 P-40ii quartz syenite metav mesoNaKFe CEUG VA- III INW -INV X-68 granite peraii subleuco K F e Type X L-461 granite peraii leucoKFe POG ?N L-462 granite peraiii subleucoKFe POG N X-53* granit e peraii i subleuc oK F e X-55 granite peraiii subleuc oK F e X-59* quartzmonzonite metav mesoNaFe X-61* granite peraii subleucoNaKFe CCG-IAG-CAG X-66* granite peraiii mesoNaKFe IAG+CAG X-70 granite perai leuc oKFe CCG X-75 granite perai mesoNaFe Type XI L-248-LG granite perai leuc oNaFe POG A O-W 1-1 L-257 granite metaiv subleucoNaKFe POG A O-W 2-2 WP WP OUTU L-355 granite peraiii subleucoKFe CEUG A O-W 1-1 L-436* granite metav subleucoNaFe RRG A O-W 1-1 L-439* alkali granite metaiv mesoNaKFe RRG A W L-466 granite metav leucoNaFe A P-39* alkali granite metav subleucoNaFe CEUG VA- VA- INW -INV P-40i granite metav leucoNaFe VA- VA INV Type III L-409* granite metaiv mesoNaFe CEUG-RRG A O-W 1-1 L-458 alkali granite metaiv leucoKF e A O-W 1-1 L-461 granite peraii leucoKFe POG ?N L-462 granite peraiii subleucoKFe POG N P-50* granite metav subleucoNaFe CEUG VA- III OUT D-I NW X-60* granite metaiv mesoKFe (Continued on the next page) 4 0 Table 4.5 Hook Granite Batholith rock types and environment of emplacement (continues from previous page) Sample Rock Name Debon & LeFort Maniar & Piccoli Whalen Pierce Mafic Rb/10HfTa Rb/30HfTa Nb-Ta Type II L-347 melteigite metav mesoNaMg A V vab L-405 sat olivine gabbro metaiv mesoNaFe IAG+CAG N V Emor L-406 alkali gabbro metav mesoNaFe A V Emor L-433 syeno gabbro metav mesoNaFe A O-W 1- 1 wpt L-438 monzogabbro metav mesoNaMg IAG+CAG A O-W 1- 1 Wpab L-440 gabbro-diorit e metaiv mesoNaFe A O-W 1- 1 Wpab L-444 gabbro-diorit e metaiv mesoNaFe RRG N? V1/2 Emor L-463 gabbro-diorit e metaiv mesoNaFe A V wpt Type Unclassified L - 2 4 1 origin A O-W 2-2 VA- III INW -INV L-242 granodiorit e peraii mesoKFe A V L-248 granodiorit e peraiii mesoNaFe A W L-259-B* granite metaiv subleucoKFe RRG A W L-263 quartzmonzonite metav subleucoKMg IAG+CAG A O-W 2-2 OUTU L-341 monzonite metavi mesoNaFe OP A V1/2 L-343 gabbro-diorit e metav mesoNaFe A S1/2 L-344 monzonite metav mesoNaFe A V1/2 L-345 quartz syenite metaiv mesoKFe CEUG-RRG A O-W 1-1 L-349 quartzmonzonite metav subleucoNaFe A W L-402 granodiorit e metaiv mesoNaFe CEUG-RRG A W L-407 gabbro-diorit e metav mesoNaFe A W wpt+ vab L-410 granite peraii mesoKFe CEUG A L-411 carbonat it e metavi mesoKMg L-437 syeno diorite metav mesoNaFe CEUG A O-W 1- 1 wpab+ wpt L-441* quartzmonzonite metaiv mesoNaKFe RRG A W L-442 alkali granite peraiii subleucoKFe RRG A O-W 1-1 L-443 peraiii mesoKFe CEUG A O-W 1-1 L-459 tonalit e metaiv mesoNaFe A L-460 granite metaiv mesoNaFe A L-464 foid out of plot metaiv mesoKFe CEUG V L-465 foid out of plot peraiii mesoKFe CEUG A V P-46* alkali granite metav mesoKFe CEUG VA- VA- INW -INV P-50 granite metav subleucoNaFe CEUG VA- III OUTD-INW P - 5 7 * nepheli n e syenite metavi subleuc o N aF e VA- VA- INW -INV X-43 granite peraii subleucoKMg CCG-IAG-CAG X-44 granite perai mesoKMg X-46 granite peraiii leucoNaMg IAG+CAG X-47 granite peraiii leucoKMg X-48 granite metaiv leucoNaMg IAG+CAG X-49 syenite peraii leucoNaF e O-W 1-1 X-51 nepheline syenite metav mesoNaKFe O3/4 X-54 granodiorit e metav subleucoKMg X-62 quartz syenite metaiv mesoKFe X-64 tonalit e metaiv mesoNaFe IAG+CAG X-65 granite peraiii leucoNaKMg X-69 alkali granite peraii mesoKFe X-71 granite peraii subleuco K F e X-72 alkali granite peraiii mesoKFe X-74 syeno-diorite metavi mesoNaMg Table 4.11 List of Sample Sorted by Rock Type Based on Maps/Field Observations 6 Sample SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu L-212 67.27 0.40 15.94 2.89 0.00 0.00 0.15 0.81 4.44 7.04 0.03 0.71 99.69 149.0 117.0 51.0 336.0 49.0 8 <6 32 17 22 <12 <12 503 8.00 79.0 <10 250 130 L-213 66.68 0.36 17.40 3.03 0.00 0.00 0.08 0.23 6.87 4.87 0.03 0.60 100.17 73.0 193.0 27.0 596.0 39.0 8 6 18 22 25 22 <12 762 12.00 163.0 <10 4.4 42.1 69.13 137 20 16.48 39.14 0.663 0.7 0.8 L-214 66.63 0.39 17.62 1.54 0.00 0.03 0.00 0.24 7.68 3.92 0.06 0.63 98.74 65.0 167.0 24.0 662.0 77.0 <6 12 20 15 25 19 81 657 7.00 104.0 <10 181 89 L-215 70.53 0.23 16.82 0.65 0.00 0.00 0.00 0.15 10.32 0.19 0.03 0.36 99.30 7.0 72.0 15.0 443.0 23.0 6 7 6 9 27 <12 <12 71 <6 193.0 <10 18 <12 L-217 73.54 0.39 10.80 3.98 0.00 0.09 3.40 1.35 0.64 2.97 0.15 2.41 99.72 124.0 48.0 10.0 128.0 10.0 86 17 8 43 13 67 502 805 <6 <15 11 6.8 28.2 53.20 89 30 58.60 0.8 L-218 66.30 0.52 15.92 4.64 0.00 0.00 0.49 2.01 4.79 5.43 0.11 0.21 100.42 202.0 344.0 46.0 601.0 53.0 8 <6 6 30 22 15 16 793 8.00 99.0 <10 16.7 74.6 264.5 342 1 35 7.513 65.38 1.450 2.1 1.1 L-260 L-395 L-411 8.09 0.09 0.85 0.57 0.00 0.02 4.72 43.80 0.04 0.35 0.16 41.87 100.56 6.0 87.0 4.0 17.0 3.0 <6 <6 <6 16 <9 <12 <12 23 <6 <15 45 12 <12 L-460 74.38 0.43 11.58 4.11 0.00 0.03 0.62 1.86 3.67 2.33 0.12 0.34 99.47 68.0 482.0 13.0 632.0 7.0 8 9 19 63 18 22 14 596 <6 20.0 <10 197 102 L-466 73.93 0.13 12.78 1.65 0.00 0.03 0.08 0.98 4.27 4.50 0.03 0.30 98.68 351.0 83.0 31.0 75.0 39.0 <6 <6 15 21 24 <12 14 225 <6 23.0 <10 57 27 L-467 70.78 0.25 13.75 2.33 0.00 0.02 0.18 0.87 4.53 5.45 0.08 0.50 98.74 145.0 1046.0 29.0 208.0 18.0 7 10 12 30 22 16 <12 2676 <6 67.0 <10 224 130 7 4HD 115 72.98 0.13 14.41 0.10 1.05 0.04 0.42 1.03 4.45 4.57 0.07 0.79 100.04 4HD 117 78.16 0.15 11.55 0.00 0.86 0.02 0.70 0.41 2.45 6.08 0.40 0.18 100.96 4HD 190 75.50 0.31 12.40 1.50 0.60 0.03 0.40 0.60 3.10 5.60 0.04 0.94 101.02 4HD200 67.00 0.75 14.20 1.10 4.00 0.07 1.30 2.40 2.80 5.10 0.22 1.34 100.28 4HD202 71.10 0.28 14.50 1.20 1.10 0.03 0.29 1.10 3.40 6.30 0.07 0.93 100.30 4HD 203 69.70 0.52 14.20 1.00 2.40 0.07 0.60 1.70 4.80 5.50 0.14 0.77 101.40 8 39 72.16 0.28 12.57 3.40 0.00 0.08 0.12 1.17 4.67 5.57 0.11 0.17 100.13 404.0 43.0 109.0 309.0 59.0 56 4 <3 12 29 <4 5 182 19.00 71.0 4 11.0 21.4 114.1 33.00 290 145 2.00 10.00 2.50 <1 12 0.80 19.40 3.10 18.30 3.60 9.20 34.4 7.30 1.10 40i 76.05 0.26 11.74 2.15 0.00 0.08 0.13 1.54 4.06 4.05 0.07 0.07 100.13 150.0 92.0 48.0 335.0 27.0 61 12 <3 26 26 <4 9 309 6.00 20.0 2 8.0 9.3 45.6 11.90 98 51 1. 00 11.00 1.30 2 8 1.50 8.80 1.40 8.30 1.70 5.00 35.3 5.00 0.80 9 57 62.19 0.36 13.11 2.44 0.00 0.05 0.26 0.86 15.42 5.52 0.06 0.21 100.27 225.0 45.0 375.0 404.0 48.0 63 21 <3 1 24 <4 <4 286 10.00 51.0 6 5.0 79.0 499.4 133.60 7 35 579 2.00 11.00 2.60 <1 5 7.60 80.50 10.00 55.60 11.10 28.9 35.9 21.4 3.30 L-235 L-236 L-237 70.85 0.37 13.24 4.02 0.00 0.00 0.52 1.36 2.51 5.44 0.11 0.40 98.83 151.0 276.0 74.0 194.0 24.0 8 6 25 16 18 28 <12 815 <6 26.0 <10 273 148 L-238 70.04 0.46 14.22 4.47 0.00 0.00 0.70 2.13 3.09 4.42 0.17 0.45 100.16 110.0 399.0 59.0 238.0 26.0 8 <6 28 19 19 37 27 647 <6 27.0 12 15.0 50.8 105.6 130 44 6 7.75 1.313 3.4 1.28 L-239 70.02 0.51 13.56 3.71 0.00 0.00 0.67 1.50 2.89 6.16 0.15 0.74 99.92 156.0 260.0 58.0 240.0 27.0 7 <6 9 18 18 33 15 747 6.00 24.0 <10 130 67 L-240 L-254 L-257 73.62 0.26 13.30 1.97 0.00 0.00 0.15 1.23 3.67 5.29 0.05 0.55 100.10 214.0 117.0 53.0 208.0 25.0 6 <6 <6 13 22 <12 14 321 16.00 74.0 <10 113.8 43.0 114.8 192 66 5.363 26.34 0.663 4.0 1.18 L-258 L-259 69.45 0.42 15.44 2.77 0.00 0.00 0.29 1.80 3.10 6.11 0.07 0.59 100.05 174.0 199.0 72.0 402.0 47.0 7 <6 <6 21 20 13 26 911 7.00 21.0 11 113 58 L-259-B 73.83 0.30 12.91 2.80 0.00 0.00 0.17 1.01 3.55 5.35 0.04 0.44 100.42 204.0 118.0 214.0 292.0 39.0 <6 <6 12 28 20 <12 15 617 10.00 29.0 <10 277 209 L-345 62.53 0.76 14.29 8.20 0.00 0.05 0.77 1.46 2.52 7.65 0.20 0.40 98.83 210.0 366.0 61.0 494.0 18.0 7 11 19 27 23 67 24 1440 6.00 <15 <10 174 94 10 L-219 L-406 46.64 2.48 13.15 14.14 0.00 0.23 6.55 10.17 3.29 0.80 0.26 1.09 98.80 11.0 282.0 38.0 180.0 17.0 43 73 80 104 18 374 106 118 <6 <15 37 29 18 L-416 52.44 0.65 15.34 8.63 0.00 0.15 7.28 12.42 2.55 0.73 0.07 0.20 100.46 6.0 126.0 17.0 41.0 5.0 34 72 94 84 17 195 217 43 6.00 <15 42 <12 <12 L-433 51.23 2.42 14.76 11.92 0.00 0.16 4.74 8.16 3.82 2.33 0.42 0.59 100.55 71.0 396.0 44.0 261.0 22.0 28 11 45 99 20 275 62 384 7.00 <15 27 96 52 L-434 69.24 0.53 13.96 4.52 0.00 0.06 0.74 1.98 1.92 4.77 0.13 1.32 99.17 149.0 247.0 8.0 411.0 7.0 8 9 25 35 16 19 18 869 <6 <15 30 18 <12 L-437 55.61 1.95 14.33 9.89 0.00 0.14 2.79 5.09 3.77 4.40 0.52 0.58 99.07 113.0 395.0 52.0 404.0 32.0 21 8 121 132 22 144 21 736 <6 <15 18 111 56 L-438 53.44 1.57 14.02 8.54 0.00 0.13 5.89 7.86 3.34 3.75 0.49 0.76 99.79 171.0 402.0 43.0 390.0 31.0 27 77 43 71 19 163 250 592 7.00 22.0 22 99 55 L-440 51.34 2.12 14.48 11.82 0.00 0.15 4.77 7.19 3.18 2.19 0.48 0.89 98.61 74.0 395.0 39.0 348.0 19.0 32 29 27 99 21 244 101 373 <6 <15 29 56 29 L-444 52.77 2.43 15.66 11.98 0.00 0.17 3.98 7.06 3.24 1.98 0.56 0.22 100.05 43.0 404.0 41.0 170.0 21.0 33 14 27 108 21 245 54 396 6.00 <15 33 67 36 L-463 48.36 2.43 14.19 14.79 0.00 0.19 7.26 7.68 2.85 1.01 0.40 -0.53 98.63 25.0 255.0 38.0 193.0 15.0 39 11 16 153 21 133 94 285 <6 <15 30 30 18 L-464 5.46 0.07 0.00 77.5 0.00 0.08 0.50 6.09 0.10 0.52 0.06 3.16 93.53 14.0 13.0 16.0 17.0 3.0 25 185 184 122 <9 34 <12 142 29.00 <15 37 <12 <12 11 Sample SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu L-465 14.01 0.58 2.56 64.7 0.00 0.03 0.70 0.17 0.06 0.43 0.12 12.85 96.25 25.0 76.0 9.0 129.0 17.0 13 85 143 102 11 127 <12 694 24.00 <15 36 <12 <12 Gabbro Iron oxides Syenite K felds migmatite Ca-enriched porphyroblast gt Older qz porph 12 50 71.53 0.25 12.60 3.26 0.00 0.10 0.30 1.66 4.55 4.88 0.21 0.14 99.34 376.0 66.0 163.0 312.0 107.0 40 16 <3 30 27 <4 4 314 62.00 256.0 3 23.0 54.3 334.8 100.20 899 505 4.00 9.00 3.20 1 8 1.20 39.60 6.00 32.20 6.20 16.3 5.70 11.40 1.60 5HC303 74.82 0.11 13.65 0.38 0.65 0.01 0.50 0.98 3.57 5.35 0.03 0.58 100.63 5HC307 72.86 0.30 14.37 0.79 2.66 0.04 0.54 0.93 3.98 5.25 0.09 0.72 102.53 5HC317 70.30 0.38 13.88 0.60 3.27 0.07 0.45 1.17 2.29 5.90 0.14 0.84 99.29 5HC445 74.17 0.21 12.86 0.00 1.80 0.04 0.33 0.49 1.94 5.91 0.10 0.50 98.35 13 L-344 61.49 1.13 15.69 3.77 0.00 0.07 1.27 6.94 5.64 1.83 0.40 0.98 99.21 47.0 555.0 126.0 485.0 41.0 10 <6 13 25 27 44 22 577 6.00 24.0 15 209 107 L-349 67.98 0.35 13.65 3.38 0.00 0.07 0.35 2.69 4.47 4.97 0.13 0.82 98.86 108.0 423.0 55.0 230.0 32.0 7 11 24 16 19 21 16 590 <6 23.0 <10 106 50 L-353 64.23 0.92 13.89 5.97 0.00 0.04 1.34 3.73 3.62 5.05 0.24 0.49 99.52 120.0 400.0 152.0 404.0 20.0 10 <6 67 24 21 36 19 606 6.00 20.0 12 141 73 L-436 73.93 0.27 12.03 2.68 0.00 0.04 0.17 1.02 4.15 4.81 0.06 0.39 99.55 235.0 74.0 45.0 303.0 31.0 <6 <6 10 21 21 <12 <12 195 26.00 99.0 <10 223 114 14 L-013 L-014 16 L-439 70.07 0.33 12.99 4.06 0.00 0.02 0.22 0.77 4.27 5.46 0.05 0.62 98.86 243.0 66.0 90.0 572.0 46.0 <6 3 21 16 25 <12 <12 163 19.00 90.0 <10 237 124 18 L-410 67.74 0.44 12.99 8.55 0.00 0.02 0.88 0.29 0.17 4.34 0.09 3.18 98.69 233.0 16.0 25.0 177.0 33.0 9 9 489 218 17 51 14 187 7.00 32.0 <10 147 80 20 5HC485 67.24 0.73 14.52 2.90 2.30 0.03 0.95 2.17 4.44 3.53 0.26 0.00 99.07 21 4HD133 73.41 0.14 13.97 0.16 1.08 0.05 0.37 1.05 4.41 4.44 0.35 0.59 100.02 4HD182 71.79 0.23 14.21 0.31 2.26 0.05 0.37 1.06 3.40 5.64 0.12 0.98 100.42 4HD205 71.10 0.38 13.60 1.10 2.50 0.06 0.42 1.50 3.50 5.50 0.08 1.27 101.01 4HD41 71.74 0.27 14.47 0.32 1.73 0.05 0.42 1.62 3.44 4.65 0.24 0.55 99.50 53 73.18 0.24 13.04 2.62 0.00 0.07 0.22 0.95 3.78 5.92 0.12 0.09 100.14 421.0 59.0 54.0 179.0 48.0 71 19 <3 <1 24 <4 24 209 21.00 43.0 2 11.0 5.6 25.7 8.00 78 44 6 .00 6.00 2.50 6 6 0.80 6.00 1.10 6.70 1.50 4.70 31.8 4.80 0.80 5HC455 70.61 0.33 14.72 1.41 0.86 0.02 0.55 0.54 2.17 7.33 0.18 0.73 99.45 28 L-265 L-354 64.83 0.81 14.83 6.19 0.00 0.07 1.46 2.45 3.15 4.06 0.20 0.95 99.00 138.0 207.0 77.0 435.0 25.0 11 17 115 78 20 71 22 977 <6 22.0 12 156 82 29 L-404 30 L-253 31 4HD48 61.07 0.80 16.53 1.03 5.61 0.16 0.56 2.97 3.75 6.03 0.14 0.84 99.49 32 L-224 62.03 0.58 13.42 15.02 0.00 0.00 0.62 0.07 0.24 5.69 0.11 2.33 100.13 261.0 103.0 35.0 301.0 28.0 9 8 <6 21 24 76 16 1065 8.00 19.0 <10 120 65 L-225 33 Sample SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu L-255 L-256 Fine-to medium-grained biotite quartz monzonite Post-tectonic qz porph Post-tectonic adamellite Grey to pink fm-g homogeneous biotite g Qz-Tourmaline and Qz veins Qz feldspar porph Younger porphyritic K granite Grey porphyroblastic gt Rapakivi gt Aegirine-augite gt 3-9 41 42 44 45 46 71.17 0.38 12.62 4.35 0.00 0.12 0.20 0.81 3.59 6.89 0.07 0.16 100.20 398.0 65.0 89.0 257.0 53.0 48 4 <3 45 27 <4 9 387 10.00 46.0 1 11.0 16.9 93.1 25.70 217 11 0 3.00 11.00 2.80 26 28 1.40 15.50 2.40 14.00 2.80 7.90 4.90 7.40 1.10 40i 76.05 0.26 11.74 2.15 0.00 0.08 0.13 1.54 4.06 4.05 0.07 0.07 100.13 150.0 92.0 48.0 335.0 27.0 61 12 <3 26 26 <4 9 309 6.00 20.0 2 8.0 9.3 45.6 11.90 98 51 1. 00 11.00 1.30 2 8 1.50 8.80 1.40 8.30 1.70 5.00 35.3 5.00 0.80 40ii 68.86 0.55 13.67 4.56 0.00 0.12 0.33 1.82 4.52 5.77 0.12 0.19 100.32 195.0 110.0 77.0 391.0 52.0 53 14 <3 53 27 11 19 503 <2 15.0 5 10.0 15.9 78.8 20.00 157 71 1.00 11.00 3.30 <1 22 2.00 14.40 2.40 14.20 2.80 7.50 34.9 6.40 1.00 L-441 62.98 1.11 14.13 7.49 0.00 0.12 0.99 2.75 3.71 5.30 0.35 0.46 99.39 180.0 226.0 74.0 414.0 46.0 10 <6 13 88 24 28 <12 893 6.00 19.0 12 187 98 9-1 L-250 L-251 L-252 L-261 L-079 67.09 0.80 14.65 4.99 0.00 0.07 1.21 2.40 3.35 4.98 0.19 0.83 100.56 165.0 216.0 40.0 332.0 24.0 14 12 41 45 0 68 40 1291 0.00 0.0 0 0 0 L-139 75.60 0.09 11.88 1.50 0.00 0.03 0.62 0.14 1.61 7.87 0.01 0.79 100.14 399.0 17.0 40.0 75.0 41.0 10 7 55 34 23 14 47 769 <6 26.0 <10 42 12 L-175 74.72 0.41 12.60 2.96 0.00 0.00 0.41 1.08 2.71 4.60 0.09 0.32 99.90 221.0 63.0 45.0 229.0 29.0 9 7 31 31 15 28 17 541 <6 25.0 <10 5.9 30.1 47.8 153 19 41.58 0.263 1.30 0.84 L-181 49.82 1.08 15.86 11.33 0.00 0.16 6.30 11.28 2.94 0.24 0.06 0.86 99.94 7.0 157.0 29.0 62.0 8.0 34 30 57 94 16 293 35 <22 <6 <15 35 <12 <12 L-195 61.25 0.38 15.84 8.67 0.00 0.09 0.04 2.35 5.66 5.03 0.09 0.51 99.91 89.0 130.0 115.0 1054 80.0 <6 <6 10 71 40 13 <12 2151 8.00 <15 <10 15.8 44.1 74.25 118 25 145.1 3.888 1.463 7.50 2.20 L-199 10.3 786.7 42.2 533.6 46.6 399 8.85 38.7 5.6 20.0 137.1 35.6 288 95 0.67 10.8 2.65 5.38 12.6 1.58 9.10 1.61 4.24 0.59 3.76 0.53 L-207 75.03 0.07 13.63 0.68 0.00 0.00 0.00 0.11 4.32 6.27 0.01 0.26 100.39 123.0 182.0 12.0 432.0 6.0 8 6 10 13 0 <12 13 557 0.00 0.0 0 4.575 0 2 19.10 0.225 0.62 5 0.44 L-208 74.23 0.05 13.85 0.87 0.00 0.03 0.00 0.12 4.36 6.13 0.05 0.24 99.93 137.0 178.0 12.0 431.0 33.0 <6 <6 14 10 25 <12 238 517 9.00 132.0 <10 35 20 L-209 46.78 1.81 16.06 9.69 0.00 0.05 7.51 11.46 2.34 1.91 0.57 0.60 98.79 53.0 1592.0 27.0 111.0 17.0 36 42 29 52 19 243 50 1437 <6 <15 27 113 61 L-210 66.74 0.43 17.99 3.52 0.00 0.00 0.29 0.69 9.58 0.09 0.14 0.39 99.87 4.0 275.0 30.0 474.0 36.0 6 7 143 13 22 28 <12 83 7.00 74.0 <10 372 223 L-211 L-229 L-230 L-231 L-242 76.03 0.29 10.81 5.91 0.00 0.01 2.03 0.21 0.57 1.96 0.11 1.21 99.14 42.0 228.0 33.0 256.0 11.0 14 18 8 12 38 87 309 617 7.00 <15 29 148 112 L-259 69.45 0.42 15.44 2.77 0.00 0.00 0.29 1.80 3.10 6.11 0.07 0.59 100.05 174.0 199.0 72.0 402.0 47.0 7 <6 <6 21 20 13 26 911 7.00 21.0 11 113 58 L-259-B 73.83 0.30 12.91 2.80 0.00 0.00 0.17 1.01 3.55 5.35 0.04 0.44 100.42 204.0 118.0 214.0 292.0 39.0 <6 <6 12 28 20 <12 15 617 10.00 29.0 <10 277 209 L-263 67.90 0.54 13.93 2.49 0.00 0.00 0.71 3.88 3.29 5.55 0.27 0.54 99.13 83.0 640.0 51.0 244.0 26.0 7 <6 23 15 20 34 16 920 <6 19.0 10 118.9 46.7 91.5 118 32 29. 10 1.813 2.86 1.06 L-402 68.46 0.60 13.71 5.64 0.00 0.04 0.43 2.96 4.94 1.14 0.11 0.82 98.85 70.0 286.0 178.0 602.0 44.0 7 10 12 29 22 25 20 272 6.00 21.0 12 178 107 L-458 72.83 0.09 13.43 1.35 0.00 0.02 0.00 0.20 3.52 6.94 0.03 0.37 98.78 277.0 30.0 72.0 45.0 13.0 <6 <6 9 11 18 <12 13 129 8.00 <15 <10 38 42 L-459 61.30 0.79 13.54 9.09 0.00 0.13 3.38 5.88 3.02 1.16 0.10 0.63 99.02 87.0 204.0 22.0 81.0 8.0 26 40 111 107 19 181 57 287 <6 <15 23 54 30 L-461 71.85 0.20 14.11 1.77 0.00 0.02 0.26 1.01 3.45 5.34 0.06 0.70 98.77 178.0 241.0 14.0 65.0 10.0 <6 <6 30 36 18 <12 13 1222 <6 15.0 <10 43 21 L-462 72.04 0.34 13.78 2.58 0.00 0.02 0.38 1.21 3.18 5.19 0.04 0.37 99.13 114.0 630.0 5.0 95.0 11.0 <6 <6 11 32 17 25 <12 3607 <6 16.0 <10 61 25 Older qz porphyry Grey Qz-felds porph 4 5 4.1.1.4 Comparison of Hook Granitoids with Ring Complexes Some portions of the Hook Granite Batholith may hav e formed by the amalga mat i o n of granito i d anorogen ic ring complexes. Several supporting facts to this hypothesis will be pres ented in the next pages. 4.1.1.4.1 Airborne Geophysical Im age and Definition of Ring Complexes The aeromagn e t i c interpre ta t i o n of Zambian geolog y publ is he d by Nisbet et al., 2000, and shown on Fig 4.16, illustrates many circular features. Th e Hook Granite lies roughly in the c enter of the figure. These circular features probabl y are annular complexe s that make the batholith. Part of the original geophysical image is show n on Fig 4.17. The image is basically a digital blend of airborne magnetometry and radiome t r y with other electro m ag n et i c informa t i on . It is based on the Sanaboz i TMI geophysical database used by Equinox Limited for mineral explora t i o n in Zambia. White repr es en t s high magnetic values . A pseudo-topography of magnetic values has been illumina ted from the NW to enhance perception of relief. Fig 18 is a transparent overlay on Fig 4.17. It shows an interpretation of the geology around the Hook Granite Batholit h , based on the geophysi c a l image just describe d and other information published by (Nisbet et al., 2000 and Nisbet , 2004b) . The variou s ring comple x es ar e labeled in the figure for easy reference. The majori t y of the rock samples obtain e d come from ri ng dikes. Severa l granit o i d s were collec t e d from a granit e ring dike of complex A: L-436, L-348 , L-349 , L-343 and they conta i n high Cu. L-352 was collect ed from further inside the same ring complex . Other samples that seem to come from potent i a l ring dikes are: L-404, L-403, and L-406 (comple x O, high Cu); L-263, L-408 (M ); L-258 and L-359 (L); L-441 and L-257 (K high Cu); L-435 (P high Cu); P-40ii (Q); P-39 and other (R); P- 42 (AA); L-440 (AC); L-442 (AF); L-254 and L-257 (J); L- 410 (E?); X-74 (AD); and L-216 (AN). L-406 is a gabbr o, and it probab l y comes from a gabbroi c ring dike. See Table 4.12. A few of the rock specime ns come from intrusio ns al ong major structur es . Sample s P-46, X-59, X-50 and X-66 probably were emplaced along one of the main N-S-tren d in g fracture zones that are well defined on the geophy s ic a l image (Figs 4.17 and 4.18). L-348 also se ems to have been collected on granitoi ds extruded along that frac tu r e zone. P-044, P-045, X-44 were collec te d along or very near another impor tan t N-S fracture . The granitoids could have been emplac ed at an earlier time and were later exposed by displacement of the faults . Differe n t i a l erosion generat e s a samplin g bias in grani to i ds from the Hook Granite . Rocks that stand out topographically tend to be sampled; valley-forming granito ids remain unsamp led. Fig 4.16 show s that very few of the rock specimens collecte d come from the nucleus of ring complexes. These are: L-352 (A high Cu); L- 264, L-265 (M); L-347 (K high Cu); L-433 (Q); P-40i (R ); L-262, P-58, L-261, L-26 0, L-259 (L); L-255 and L- 256 (J); L-014 (C); L253, P-57 (K high Cu); L-437 (P high Cu); L-433, L- 40ii (AQ); L-013, L-407 (E with high Cu). The granitoids that lie in between ring complexes probably came from older ring complexes. Most of the Th - rich rocks are of that type (See section 4.1.1.2 on geochemis ty). They probably formed in an earlier generati o n of intrusio ns , and later were overprin t e d by newer granitoi d ring comple xe s . An interes t i ng group of well-lo c a t e d sample s is P-39, L-40i, P-40ii. These come from the rims of ring comple x e s Q and R. Many structu r e s pres en t on the geophys i c a l image of Fig 4.17 (and mapped on Fig 4.18) do not corres p on d with those mapped on the publishe d geologic a l sheets. Most N-S structur es and WSW-EN E struc t u r es are evident on the geophys ic al image and were not descri be d or mapped in the publis h e d geology . The ring structu r e s are not even hi nted. Ther e is not enough outcrop to map structu r e or geolog y adequat e ly at 1:100,000 scale. A lensoid N-S fault structure that is present on the map by Hanson et al, 1993 (and on the Zambian Geolog i c a l Survey maps) shows up well on the geophys i cal image (wes ternmost portion of Figs 4.17 and 4.18). A few sample s (P-50, P-46 and others) were collect ed from the middle of the fault duplex. That fault is the same very long N-S fracture that is evident on t he geophysical image, connects the Hook Granite to the Kasemp a area to the north (Figs 4.18 and 4.16), and seem s to be the site of emplac e me n t of massiv e iron oxide bodies and iron oxide-c opper-gold mineralization. 4 6 4 7 4 8 Fig 4.18. Anorogenic ring structures that can be identi fied in the Sanabozi geophysical image, Hook Granite Batholith, Zambia. T hick lines are fractures. T hin lines are ge ophysical ring lineaments. T he letters serve to designate the various ring structures. Based on interpretation of Fig 4.17 with input from Fig 4.16 and Nisbet, 2 00 4a and Nisbet, 20 04b. T he letter of compl exes with high copper content are und er lined. Stars indicate ring complex es dated by Hanson et al, 199 3. The south-western half of the Hook Gr anit e (the part that lies west of the Kafue River) seems to have been down-fa u l t ed along the same N-S structu r e , and is now le ss-well exposed. That same fault control s the N-S deflection of the Kafue River across the Hook Granite Batholith. Maybe the textural change show n by the geophys ic a l image is due to differe n t data sour ces or a di fferent scale of coverage of geophysical information. Some of the mapped syenite bodies that lie to the northea st and east of the main Hook Granite Batholith (Fig 4.1) seem to be isolated from it. They intrude Ka tangan metasediments, have been called ?outliers? or ?satellites? of the batholith, and could be younger or older than the main batholith . Samples L-207 a nd L-213 , from some of the satelli te bodies, were dated during this projec t . Their ages are very simila r to ages publis hed by Hans on et al, 1993 for the Hook Granite. That implie s that the satellite bodies are isolated ring complexe s , apo phy s is of ring comple x es that did not outcrop, or portions of the main batholith that are partially covered by fluvial deposits. The image of Nisb et presen t s an explan a t i on for such intrus i v e bodies (Fig 4.17). L-213 sampled a syenito id that produce d one of the strongest magnetic anomalies in the environs of the Hook Granite . It will be discussed in detail below. The geology mapped by the Zambian Geological Survey and published on reports (Phillips, 1958; Simpson, 1962; Cikin, 1971; Cikin, 1972; Page, 1974; Abel, 1976; and Griffit h s , 1978) does not bear any resemblan c e with the geophysic a l interpre t a t i o n published by Nis bet, 2004a and Nisbet, 2004b. Field observat i on s along the E-W transect do not relate to the publishe d geologi cal map sheets either. The same can be said of some of the struct ur e s mapped . The map publis h ed by Hanson et al, 1993 is just a compilat i o n of older 1:100,0 0 0 geological map sheets. It does not relate to field observations or to the geophysical interpreta tions. 4 9 When syenites and quartz syenites from the Hook Granite are plotted on the publishe d maps, these seem to be spread out in no particular location. Some of them are even related to the granite bodies. Gabbroic bodies are also widely distrib u t e d through ou t . These ar e common feature s in anorogen i c ring complexe s . 4.1.1.4.2 Comparison of Hook granitoids wi th rocks from Namibian Mesozoic ring complexes A review of literat u r e on Mesozoic Namibia n anor ogen i c complex es show ed that the Erongo and Brandber g comple x e s , two of the countri e ? s larger ring complexe s are exclusiv e l y made of gr anites. Fig 4.19 shows their location on a simplifi e d geologi c a l map. Brandbe r g measur es 25 x 30 km. If several bodies of that size were to overprint each other, a batholithic-size body of granit e would result. This would happen if the granitic bodies would occur with the dens ity of the Sudane s e Nuba Mounta i ns (See chapte r 7). Two smalle r Namibia n anorog en i c granit i c comple x e s are Klein Spitsk o p p e and Gr oss Spitzkoppe. Chemical analyses from the four Namibia n complex e s are listed on Table 4.6. Neoprot er oz o ic granitic ring comple x e s from norther n Mali studied by Liegeois & Black, 1987 have equivalent compositions and dimens ions . Simple evalua tion was carried out to define the general chemistry of the four mentioned Namibian granitic comp le xe s . This was later comp ar e d with granitoids from the Hook Granite Batholith. Based on the R1/R2 diagram of De la Roche et al, 1980, samples from the Namibian anorogenic complexes may be grouped into five sets (A to E), as indicate d on Table 4.7 and presen te d on Fig 4.5. Major oxide chemistry is very similar betwee n sample s X-97, X-98, X-99, X-100 and X-101 (G roups A, D and E); and between samples X-92, X-93, X-94, X-95 and X-96 (Groups B and C). These make two sets of comparable rocks. Several partic ular geochemical featur es were observ e d in the chemica l analysi s from Namibia n Mesozoic anorogen i c granite ring complex e s (Table 4.2). Among ot hers, the samples contain high potash, Rb, Y, Nb, and Zr, and low Sr. When thos e signa tu r es were compare d with all samples from the Hook Granite , 10 sample s produ ce a good match. Thes e are listed on Table 4.8. A particu l a r minor element signatur e is common in rocks from the Nigeria n ring comple x e s , Namibia n granite anorogen i c complex es and those of the Hook Granite Batho lith. All three groups have high values for Rb, Y, Nb, Th, Pb, Ce, La, and low values for Sr and Zr (Table 4.8). If anomalou s enric hment in Rb, Y, Nb, Th and Pb (all of them at the same time) is assumed to be the chemic al signature of some anoroge nic granitoid ring complexes, then ro cks with that signature from any provinc e could have been formed as anorog en i c granit e ring complexes. A search for rocks with similar chemic a l signat u r e in the entire Greater Lufili a n Arc sa mple database shows that only a few suites of rocks have similar signatures. There is no match for the major oxide chemis t r y from Nigeria n granito i d complex e s with the Hook Granite . Namibia n rocks correla t e much better. Certain samples from the Hook Granite display very similar chemis t r y to the Mesozoic Namibian granitoid ring comple xe s , as shown on Table 4.8 and Fig 4.20. Samples cons id er e d to come from anorog e n ic ring co mplexes are L-259B, L-408 , L-409, L-436, L-439, L-441, P-39, P-46, P-53, P-57, and P-58 (Table 4.8) . Others cons idered to be of the same origin due to major oxide similarities were X-43, X-45, X-52, X-58, X-59, X-60, X-61, X-63, X-66 and X-73. Unfortunately the last group of sample s was not analyse d for trace elemen t s or rare ea rths. Fig 4.20 illustrates the similarity of their major oxide compos i t i o n . Ther e is a remarkab l e correl a t ion between the samples, and they all probably originated as anorog e n ic ring compl ex e s . On the modified TAS diagram, several groups of samples fr om the Hook Granite Batholit h display simila ri tie s with rocks from suites of anorog e n ic ring comple x e s (Fig 4.21) The TAS diagr a m inclu d es rocks from comple xe s such as Pan-Afri c a n and Evisa granitoi d s of Nigeria , and others of Corsic a . Nchanga Granite sample s were also plotted for comparison. Part of the samples with similar ities to the ring complexes are direct l y associ a t e d with the rock gr oups identif i e d for the Hook Granite . The Nchanga Granite also display s clos e associati o n with some Nigeri a n ARC rocks. Result s are listed on Table 4.13. Further m or e , a midalk a l in e linear trend of rocks has been observed on the TAS diagram for the Hook Granite Batholith (Fig. 4.21). The trend seems to be a spec ial featur e of a portion of the Hook Granite batholith, but its relevanc e is not yet well understood. Samples that make the trend have been listed on Table 4.13. 5 0 Table 4.6 Chemical analyses of Namibian Mesozoic anorogenic complexes From Harris & le Roex, 2002, pgs. 10 and 26. Numbers refer to Lufilia n Arc databas e . # Sample SiO2 TiO2 Al2O3 FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total Notch 50.00 1.00 15.50 6. 0 0 0 . 1 5 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2.00 Spitzkoppe Complexes X - 9 2 CH9308 76.99 0.10 11.73 2. 0 6 0 . 0 2 0 . 0 8 0 . 7 4 3 . 0 3 5 . 2 3 0 . 0 2 0.52 100.52 X - 9 3 CH9309 76.04 0.04 12.83 1. 5 7 0 . 0 2 0 . 0 4 0 . 6 2 3 . 8 9 4 . 9 3 0 . 0 1 0.46 100.45 X - 9 4 CH9310 75.67 0.04 12.94 1. 7 1 0 . 0 2 0 . 0 5 0 . 6 5 4 . 0 5 4 . 8 4 0 . 0 2 0.45 100.44 X - 9 5 SMER11 69.75 0.51 12.55 5. 7 7 0 . 0 8 0 . 1 1 2 . 3 0 2 . 5 5 6 . 2 9 0 . 0 9 1.38 101.38 Erongo Complex X - 9 6 ERG 76.26 0.07 13.30 1.4 3 0 . 0 3 0 . 0 6 0 . 4 3 3 . 0 8 5 . 0 7 0 . 2 6 - 99.99 Brandberg Complex X - 9 7 CH9301 74.98 0.16 10.39 5. 0 6 0 . 0 7 0 . 0 6 0 . 1 6 4 . 4 3 4 . 6 9 0 . 0 0 0.66 100.66 X - 9 8 CH9302 71.34 0.48 13.14 4. 7 1 0 . 1 1 0 . 2 3 0 . 9 1 3 . 4 5 5 . 5 3 0 . 1 1 0.98 100.99 X - 9 9 CH9306 71.05 0.45 13.09 4. 3 8 0 . 1 1 0 . 3 0 1 . 4 6 3 . 4 6 5 . 6 0 0 . 1 0 0.49 100.49 X - 1 0 0 CH9307 70.25 0.50 13.51 4. 3 7 0 . 1 1 0 . 3 8 1 . 5 2 3 . 5 8 5 . 6 6 0 . 1 1 0.28 100.27 X - 1 0 1 CH9401 69.97 0.55 13.70 4. 6 5 0 . 1 1 0 . 3 0 1 . 8 8 3 . 5 9 5 . 1 5 0 . 1 1 0.56 100.57 # Sample Rb Sr Y Zr Nb Ni Cu Zn V Cr Ba Sc Ce La Na+K Notch 200 400 60 360 40 1 6 2 5 8 5 1 0 0 1 0 0 1 3 0 0 2 0 175 95 Spitzkoppe Complexes X - 9 2 CH9308 473 14 157 196 1 4 1 3 3 4 4 2 7 7 5 2 148 84 8.3 X-93 CH9309 604 2 208 112 88 2 3 5 8 6 2 9 1 63 26 8.8 X-94 CH9310 620 1 214 128 83 4 4 4 5 2 7 2 - 54 21 8.9 X-9 5 SMER11 243 81 68 474 24 - - - - - 1 0 5 1 1 0 162 77 8.8 Erongo Complex X - 9 6 ERG 637 25 155 60 26 1 0 2 3 8 7 6 6 8.2 Brandberg Complex X - 9 7 CH9301 1241 18 438 537 9 5 1 4 459 207 9.1 X-98 CH9302 211 111 66 483 56 8 5 6 134 64 9 X-99 CH9306 210 112 110 455 5 3 8 0 7 163 85 9.1 X-100 CH9307 209 111 78 505 61 8 0 8 144 66 9.2 X-101 CH9401 188 132 73 472 51 112 54 8.7 Table 4.7 Rock groups from Namibian Mesozoic anorogenic granitoid complexes and comparison with samples from the Hook Granite Batholith, Zambia B a s e d on R1/R 2 diagram and chemica l data from Table 4.5. See plots on Fig 4.21. Site/Group A B C D E S p i t s k o p p e X-95 X-93, X-94 X-92 Erongo X-96 Brandber g X-99, X-100 , X-1 01 X-98 X-97 Hook Granit e Bat hol i t h P-40ii , P-50, L-4 08 L-139 L-458 P-39, P-46, L-259B, L-436 L-442, L -443 Table 4.13 Hook Granite samples that show sim ilarities with granitoid samples from Nigerian, Namibian and Corsican anorogenic ring complexes. U nd erlined samples are memb ers of t h e H o o k Granite Batholith rock group indicated on third column . All data was obtained from TAS diagram of Fig 4.21. Anorogenic ring complexes Sample numbers from Hook Granite Batholith Hook Granite Batholith Rock Group Y o u n g Nigeri a n , Namibia n and Cors ic a n ARC X-46, L-257, L-436 , L-355 , L-259 B , X-43, L-46, X-66, L-442, X-90, X-65, X-55, L-248-LG , P-40i XII N a m i b ia n Mesozoic ARC L-238, L-239, X-72, L-408, X-68, X-75, X-60 PanAfr i c an Nigeri an black and white granito id s L-343, L-354 , L-341, L-403 , X-63 , L-079 , X-52 , L-263, L-348 , X-45 , P-58 , X-73 , X-57 , X-56 I Hook Granite midalkal in e linear trend L-213, L-212, L-214, X-49, L-012, L-012A, L-345, X-62, X-74, L-437, L- 402, L-438, L-433, L-209 Nchanga Granite rocks that are similar to Nigeri a n ARC L-151, L-154, L-153, L-162, X-43, X- 36; also to a minor extent: P-29, X- 35 and X-37 5 1 Table 4.8 Comparative chemical analysis from granite anoroge nic ring complexes Hook Granite Batholith samples. (Boxes in yellow are anomalous values) (complete trac e element analysis on Table A3 in Appendix) Anorogenic Granite Complexes, Nigeria Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 F eO MnO MgO CaO Na2O K2O P2O 5 LOI T otal Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h Sc Pb Sm Nd Pr Ce La Cs Hf T a As Se Eu Gd T b D y Ho Er Tm Yb Lu AMN 24 72.6 0 0.29 14.1 0.90 1.73 0.07 0.43 1.01 3.36 5.74 0.07 0.47 100. 74 185 100 63 246 57 61 9 362 27 22 144 59 6 B34 76.0 0 0.10 11.7 0.37 0.89 0.02 0.09 0.83 3.78 5.77 0.04 0.24 99.8 7 574 4 115 141 158 60 12 39 40 74 114 64 5 DR11 76.7 0 0.14 13.4 0.00 1.16 0.03 0.05 0.33 4.41 3.58 0.02 0.34 100. 12 966 0 87 81 119 103 4 0 61 47 149 88 9 DW 1 78.0 3 0.06 12.1 0.33 0.89 0.01 0.09 0.52 4.59 3.56 0.01 0.42 100. 65 389 22 356 207 205 77 0 71 42 16 275 169 10 FG5 77.4 4 0.08 12.0 0.37 0.87 0.02 0.07 0.49 3.89 4.45 0.01 0.34 100. 02 347 3 189 161 148 42 0 43 39 27 117 64 8 JON147 73.2 0 0.18 14.2 0.67 1.19 0.02 0.08 0.73 3.45 5.32 0.03 0.98 100. 03 296 38 227 330 118 126 0 264 41 38 251 218 8 KD12 76.5 0 0.10 12.8 0.35 0.84 0.02 0.07 0.46 4.17 4.39 0.01 0.34 100. 08 283 4 144 147 96 48 0 4 36 41 62 27 6 MD33 3 75.4 0 0.10 13.3 0.01 0.96 0.02 0.04 0.34 4.26 4.53 0.01 0.20 99.2 0 620 0 139 129 78 9 68 0 0 66 70 79 28 9 NG208 75.7 0 0.20 13.2 1.48 0.01 0.03 0.09 0.44 3.41 5.10 0.01 0.66 100. 31 318 29 75 186 80 70 2 151 63 57 156 83 7 PAN 112 73.9 0 0.15 14.9 0.43 0.80 0.02 0.67 0.43 3.98 5.17 0.02 0.61 101. 06 192 28 117 234 88 0 80 25 22 195 189 7 RN75 75.9 0 0.11 12.9 0.33 1.05 0.05 0.02 0.24 3.91 4.31 0.01 0.88 99.6 6 979 15 696 399 214 120 376 0 109 111 56 296 234 28 T15A 74.3 0 0.08 11.7 0.33 0.89 0.02 0.01 0.26 3.88 4.59 0.01 0.64 96.7 5 502 1 86 166 132 7 61 3 0 69 37 153 166 7 Mesozoic Anorogenic Granite Complexes, Namibia Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 F eO MnO MgO CaO Na2O K2O P2O 5 LOI T otal Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h Sc Pb Sm Nd Pr Ce La Cs Hf T a As Se Eu Gd T b D y Ho Er Tm Yb Lu X-100 70.2 5 0.5 13.5 4.37 0.11 0.38 1.52 3.58 5.66 0.11 0.28 209 111 78 505 61 808 144 66 X-101 69.9 7 0.55 13.7 4.65 0.11 0.3 1.88 3.59 5.15 0.11 0.56 188 132 73 472 51 112 54 X-92 76.9 9 0.1 11.7 2.06 0.02 0.08 0.74 3.03 5.23 0.02 0.52 473 14 157 196 141 3 3 44 2 7 75 2 148 84 X-93 76.0 4 0.04 12.8 1.57 0.02 0.04 0.62 3.89 4.93 0.01 0.46 604 2 208 112 88 2 3 58 6 2 9 1 63 26 X-94 75.6 7 0.04 12.9 1.71 0.02 0.05 0.65 4.05 4.84 0.02 0.45 620 1 214 128 83 4 4 45 2 7 2 - 54 21 X-95 69.7 5 0.51 12.6 5.77 0.08 0.11 2.3 2.55 6.29 0.09 1.38 243 81 68 474 24 - - - - - 1051 10 162 77 X-96 76.2 6 0.07 13.3 1.43 0.03 0.06 0.43 3.08 5.07 0.26 - 637 25 155 60 26 10 2 38 76 6 X-97 74.9 8 0.16 10.4 5.06 0.07 0.06 0.16 4.43 4.69 0 0.66 1241 18 438 537 95 14 459 207 X-98 71.3 4 0.48 13.1 4.71 0.11 0.23 0.91 3.45 5.53 0.11 0.98 211 111 66 483 56 856 134 64 X-99 71.0 5 0.45 13.1 4.38 0.11 0.3 1.46 3.46 5.6 0.1 0.49 210 112 110 455 53 807 163 85 Samples from Hook Granite that are similar to ring complex granites Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 F eO MnO MgO CaO Na2O K2O P2O 5 LOI T otal Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h Sc Pb Sm Nd Pr Ce La Cs Hf T a As Se Eu Gd T b D y Ho Er Tm Yb Lu L-259- B 73.8 3 0.30 12.9 2.80 0.00 0.17 1.01 3.55 5.35 0.04 0.44 100. 42 204 118 214 292 39 <6 <6 12 28 20 <12 15 617 10 29 <10 277 209 L-408 70.2 6 0.33 13.6 3.87 0.05 0.26 1.23 3.49 5.24 0.07 0.43 98.8 2 241 95 104 348 33 7 6 15 34 23 <12 13 483 12 32 <10 241 121 L-409 69.3 6 0.41 14.8 3.25 0.02 0.49 1.13 4.47 5.43 0.10 0.44 99.8 6 206 151 43 313 32 6 <6 10 16 19 25 12 677 13 53 <10 120 60 L-436 73.9 3 0.27 12.0 2.68 0.04 0.17 1.02 4.15 4.81 0.06 0.39 99.5 5 235 74 45 303 31 <6 <6 10 21 21 <12 <12 195 26 99 <10 223 114 L-439 70.0 7 0.33 13.0 4.06 0.02 0.22 0.77 4.27 5.46 0.05 0.62 98.8 6 243 66 90 572 46 <6 3 21 16 25 <12 <12 163 19 90 <10 237 124 9.73 L- 441 62.9 8 1.11 14.1 7.49 0.12 0.99 2.75 3.71 5.30 0.35 0.46 99.3 9 180 226 74 414 46 10 <6 13 88 24 28 <12 893 6 19 12 187 98 P-39 72.1 6 0.28 12.6 3.40 0.08 0.12 1.17 4.67 5.57 0.11 0.17 100. 13 404 43 109 309 59 56 4 <3 12 29 <4 5 182 19 71 4 11 21 114 33 290 145 2 10 3 <1 12 1 19 3 18 4 9 34 7 1 P-46 71.1 7 0.38 12.6 4.35 0.12 0.20 0.81 3.59 6.89 0.07 0.16 100. 20 398 65 89 257 53 48 4 <3 45 27 <4 9 387 10 46 1 11 17 93 26 217 110 3 11 3 26 28 1 16 2 14 3 8 5 7 1 P-50 71.5 3 0.25 12.6 3.26 0.10 0.30 1.66 4.55 4.88 0.21 0.14 99.3 4 376 66 163 312 107 40 16 <3 30 27 <4 4 314 62 256 3 23 54 335 100 899 505 4 9 3 1 8 1 40 6 32 6 16 6 11 2 P-53 73.1 8 0.24 13.0 2.62 0.07 0.22 0.95 3.78 5.92 0.12 0.09 100. 14 421 59 54 179 48 71 19 <3 <1 24 <4 24 209 21 43 2 11 6 26 8 78 44 6 6 3 6 6 1 6 1 7 2 5 32 5 1 P-57 62.1 9 0.36 13.1 2.44 0.05 0.26 0.86 15.4 2 5.52 0.06 0.21 100. 27 225 45 375 404 48 63 21 <3 1 24 <4 <4 286 10 51 6 5 79 499 134 735 579 2 11 3 <1 5 8 81 10 56 11 29 36 21 3 P-58 67.7 6 0.79 13.5 6.83 0.17 1.40 2.21 3.78 4.27 0.18 0.25 100. 85 210 189 66 223 30 77 4 21 72 26 45 12 680 4 24 8 12 10 51 13 107 53 5 6 2 1 30 2 10 2 9 2 5 33 4 1 X-45 68.4 1 0.69 14.5 4.60 0.08 1.29 2.07 3.47 4.63 0.25 X - 52 67.1 7 0.72 14.6 4.81 0.07 1.20 2.05 3.59 5.30 0.20 X - 53 71.7 9 0.23 14.2 2.57 0.05 0.37 1.06 3.40 5.64 0.12 X - 58 71.1 0 0.28 14.5 2.30 0.03 0.29 1.10 3.40 6.30 0.07 X - 59 69.7 0 0.52 14.2 3.40 0.07 0.60 1.70 4.80 5.50 0.14 X - 60 71.1 0 0.38 13.6 3.60 0.06 0.42 1.50 3.50 5.50 0.08 X - 61 71.7 4 0.27 14.5 2.05 0.05 0.42 1.62 3.44 4.65 0.24 X - 63 64.7 7 0.89 15.3 5.55 0.08 1.45 2.54 3.83 4.30 0.27 X - 66 72.8 6 0.30 14.4 3.45 0.04 0.54 0.93 3.98 5.25 0.09 X - 73 67.2 4 0.73 14.5 5.20 0.03 0.95 2.17 4.44 3.53 0.26 5 2 Fig 4.20 Logarithmic major oxide plot to compar e Namibian granitoid ring complexes with samples from the Hook Granite Batholith. Fe Ot represents total iron oxides. Samples on the left come from the Nigeri a n comple x e s ; the other are from the Hook Granit e. The ten sample s from the right lack trac e elemen t analysis . In conc lu s io n, the chemis tr y of granit o id s from the Mesozo ic anoroge n ic comple x e s from Namibi a is quite similar in trace element and major oxide geochemis tr y to some samples from the Hook Granite. These are shown on Table 4.8. A 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 Na+K) -2(Fe+Ti) 5 0 0 R1R2 Plutonic Rock Classification Diagram Hook Granite Batholith compared to other ARC Greater Lufilian Arc Granitoid Project (Di agr am afte r Dela Roche et al , 198 0) P e tr o g ra p hic fie ld s M e s oz o i c Nam i b i an ARC Y o un ge r Nige r i a n ARC N c ha ng a Gran it e, Zam bia H o o k Gra ni t e Bath o l i t h , Zamb i a E D C B Fig 4 .21 N o t e : S m a l l c o lo r e d p o l y g o n s ref e r to gro u p s of gra n i t o i d s , b a s e d o n Me s o z o i c Na m ib i a n rin g c om p l e x e s (s e e te x t ) . 4 5 5 0 5 5 6 0 6 5 7 0 7 5 8 0 SiO2% 3 4 5 6 7 8 9 1 0 1 1 1 2 1 3 N a 2 O % + K 2 O % L-207 L-208 L-209 L-210 L-212 L-213 L-214 L-215 L-217 L-218 L-222 L-223 L-224 L-416 L-458 L-459 L-460 L-461 L-462 L-463 L-466 L-467 X-90 L-012 L-012A L-079 L-237 L-23839 L-248 L-248-LG L-249 L-257 L-259 L-259-BL-263 L-341 L-343 L-344 L-345 L-346 L-347 L-348 L-349 L-352 L-353 L-354 L-355 L-402 L-403 L-405 L-406 L-407 L-408 L-409 L-410 L-433 L-434 L-435 L-436 L-437 L-438 L-439 L-440 L-441 L-442 L-443 L-444 X-43 X-44 X-45 X-46 X-47 X-48 X-49 X-50 X-51 X-52 X-53 X-54 X-55 X-56 X-57 X-58 X-59 X-60 X-61 X-62 X-63 X-64 X-65 X-66 X-67 X-68 X-69 X-70 X-71 X-72 X-73 X-74 X-75 P-39 P-46 P-50 P-53 P-58 P-40i P-40ii TOTAL ALKALI vs SILICA DIAGRAM Hook Granite Batholith, Zambia; Lufilian G.P. (Based on Middlemost, 1994, 1997 ) N am i bi a n ARC P et r ogr a phi c fiel ds Y ou ng ARC, Nig er i a, Afri ca H oo k Grani t e Bat hol i t h, Zam b i a, Afr i ca N ch an ga Gran i te , Zambi a , Afr ic a E vi sa ARC, Cor s ic a, Med it e rr an ea n S hi r a ARC , Nige ri a , Afr ic a P an Af ri c an AR C, Nig er i a, Afr i ca Midalkaline linear trend Fig 4 .21a Fig 4.21a 5 5 4.1.1.5 E-W transect across the Kafue Park, Zambia A well-paved road runs E-W across the Hook Granite Ba tholi t h in the Kafue Nationa l Park (Figs 4.1 and M2 to M5, in Appendix). Since most of the rest of the bat holi t h lacks good infrast r u c t u r e , detaile d samplin g was carried out along that main road. Outcrop is sparse along the transec t , rarely of good quality . In most cases, relati o ns h ip s betwee n the various types of rocks identif i e d was not clear. A total of 57 outcrops were visited along the 90 kilomet er transec t ; each outcrop was located using a GPS. Only repr es e n t a t ive outcrops were fully descri bed and sampled . Thirty sample s were collec ted, twelve of them were analysed and they are liste d on Table 4.9. Differ en c e s based on grain size, main co ns tit u e n ts and foliati on helped to name and group them in the field. At least five differen t generati o n s of gran itoids were identified along the transect. Part of the rocks contain more xenoliths than others. Hydr othermal bre ccia t i o n , minor mineral i z a t i on and tourmalinization were observed in a few plac es . A summary of main field obser vat i o ns along the transect is included in Append ix A57. Table 4.9 Analysis of samples along E-W transect across the Hook Granite Batholith, Zambia ( X = samples collect e d in the field; P = samples by Pepper, 1999; Z = from Zambian Geological Survey. (complete elemental on Table A3, in the Appendix) Sam ple # SiO 2 T iO 2 Al2O 3 Fe2O 3 MnO MgO CaO Na2O K2O P2O 5 Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h L-237 X VII 71.9 9 0.38 13.4 5 4.08 0 0.53 1.38 2.55 5.53 0.11 151 276 74 194 24 8 6 25 16 18 28 <12 815 <6 26 L- 238 X VII 70.2 5 0.46 14.2 6 4.48 0 0.7 2.14 3.1 4.43 0.17 110 399 59 238 26 8 <6 28 19 19 37 27 647 <6 27 L- 239 X 70.6 1 0.51 13.6 7 3.74 0 0.68 1.51 2.91 6.21 0.15 156 260 58 240 27 7 <6 9 18 18 33 15 747 6 24 L- 241 X 0 0 0 0 0 0 0 0 0 156 229 55 174 24 0 0 0 0 0 0 594 0 0 L- 242 X 77.6 4 0.3 11.0 4 6.03 0.01 2.07 0.21 0.58 2 0.11 42 228 33 256 11 14 18 8 12 38 87 309 617 7 <15 L-248 X 65.3 4 0.92 15.5 7 6.43 0 2.78 3.54 3.01 2.13 0.26 126 300 54 205 42 15 15 13 28 25 109 39 271 6 <15 L-248- l g X XI 76.7 3 0.14 13.2 6 0.92 0 0.04 0.66 3.71 4.49 0.04 121 314 48 206 20 9 7 8 16 19 35 25 745 <6 27 L- 249 X VII 71.3 0.43 14.2 4 3.55 0 0.76 1.99 3.04 4.56 0.14 123 309 49 211 23 8 7 8 16 19 45 21 716 <6 20 L- 257 X 73.9 6 0.26 13.3 6 1.98 0 0.15 1.24 3.69 5.31 0.05 214 117 53 208 25 6 <6 <6 13 22 <12 14 321 16 74 L- 259 X XI 69.8 3 0.42 15.5 3 2.79 0 0.29 1.81 3.12 6.14 0.07 174 199 72 402 47 7 <6 <6 21 20 13 26 911 7 21 L- 259- b X 73.8 6 0.3 12.9 2 2.8 0 0.17 1.01 3.55 5.35 0.04 204 118 214 292 39 <6 <6 12 28 20 <12 15 617 10 29 L- 263 X C 68.8 9 0.55 14.1 3 2.53 0 0.72 3.94 3.34 5.63 0.27 83 640 51 244 26 7 <6 23 15 20 34 16 920 <6 19 L- 354 Z 66.1 2 0.83 15.1 2 6.31 0.07 1.49 2.5 3.21 4.14 0.2 138 207 77 435 25 11 17 115 78 20 71 22 977 <6 22 L- 403 Z 64.3 3 0.68 14.6 7 7.89 0.06 1.14 3.14 3.51 4.4 0.16 119 277 83 762 25 9 9 196 89 25 19 19 1054 8 17 L- 405 Z II 52.9 9 1.24 16.3 3 10.1 9 0.11 5.39 9.13 3.36 1.1 0.15 23 882 24 121 14 37 72 30 53 17 220 35 226 <6 <15 L-406 Z II 47.7 3 2.54 13.4 6 14.4 7 0.24 6.7 3.37 0.82 0.27 11 282 38 180 17 43 73 80 18 374 106 118 <6 <15 L-408 Z IV 71.4 1 0.34 13.8 1 3.93 0.05 0.26 1.25 3.55 5.33 0.07 241 95 104 348 33 7 6 15 34 23 <12 13 483 12 32 P- 58 P I1 67.1 9 0.78 13.3 5 6.77 0.17 1.39 2.19 3.75 4.23 0.18 210 189 66 223 30 77 4 21 72 26 45 12 680 4 24 If the transect is cons ider ed to be representative of t he main batho li t h , it consist s of granites and minor grano- diorite that correspond to the map units listed on Tabl e 4.4. From the TAS diagram of Fig 4.22, one might conc lud e that there are six distinc t rock types in t he batholith. After processing data of the transec t , geology observ e d in the outcrop s was not coher ent with the map units indicated on Table 4.4. Map units did not make any geolog ical sens e. Table 4.10 shows the ways in whic h samples from the transec t can be groupe d . Table 4.10 Samples collected along the E-W transect through the Kafue Park, Hook Granite Batholith ( U nd er l i n e d samples were anayse d . ) Map units are correla t e d on Table 4.12. Map Unit (Table 4.5) Map sheet Sample Numbers O 1426SW +1426 S E L-235, L-236, L-2 37 , L-238 , L-239 , L-240, L -250, L -251, L-252, L-254, P-57 , L- 257 , L-25 8, L-25 9 , L-354 , L-261, L-263 N 1426SW L-241 , L -245, L -246, L-244, L-248 , L-249 , L-247 L 1426SW L-253, L-255, L-2 56 H 1426SW L-260 A 1426S W L-262 , P- 58 B 1426SE L-405 , L-403 Unide n t i f i e d 1426S E L-406 , L-408 The E-W trans ec t along the Kafue National Park intersected complexes J (4), K (2), L (8), M (4), and O (2) (See Table 4.12). In all cases except for ring complex K, both rim and nucleus were sampled (Fig 4.17 an d Table 4.12). Some portions of the ring complexes c onta in anomal o us coppe r , and part of them are also enric hed in zinc , as show n. Outc rops are scatte red around and they lack continuity to enable proper geolog ical mapping to be done. In the field, it is virtua lly impossible to establish that one is looking at ring comple x e s , because the various relation s of rocks exposed do not provid e clues . Fig 4.23 illustrates a hypothetical case of a ring complex cluster. Somethin g similar might ha ve been the case of the Hook Granite Batholith. The hypothetical transe c t across the series of ring complexe s produ ces a lithological variation that is difficult to interpret withou t having the map of the ring complexes. Several such detailed traver ses may help in understanding the geology and interpreting the geolog ical history of the rock mass if. 5 6 Fig 4.22 Total alkali versus silica diagram for sa mples collected along the E-W transect through the Kafue Park, Hook Granite Batholith, Zambia. See more details in tex t. 4.1.1.6 Geochronology and Geological History Hans on et al, 1993 compiled the geology of the Hook Gr anite Batholith and dated what they considered were the main geological events of the batholith. Table 4.13 lists their ages and Fig 4.15 illustr a t es the positi o n of sample s dated. UTM coor din a t e s of the samles have been included on Table 4.4. Other ages availabl e for the Hook Granite and its environ s are listed on Table A22.1 in the Appendix. Thes e ages were plotted on the event diagram of Fig A23 (Appendix) . Based on that di agram, the time span for emplacement of the Hook Granite Batholith is 40 million year s (from 570 to 530 Ma ). See also Table 4.13 with correlation of the various geolog i c a l map sheets and their geologi c a l units . Table 4.14 Radiometric ages for the Hook Granite Batholith published by Hanson et al, 1993. All information was ex tracted from the original publication. Coordinates of the sample s are listed on Table 4.4. Ring complex l ocation is shown on Fig 4.18. Sample Age (Ma) Rock type Ring complexes dated H - 1 559?18 Deforme d , fine- to medium- g r a i n e d granite V H-2 566?5 Deform e d megac r ys t i c granit e V H-3 538?1. 5 Rh yoli t e dike within Katang a n pe ndan t R H-4 533?3 Post- t e c t o n i c megac r ys t i c grani t e P? H-5 551?1 9 Rh yol i t e intru s i o n in Mwem b e z h i Dislo c a t i o n AJ Hans on and co-workers define six different intrusive events for the batholit h . There might be younger ones, sinc e they did not date any of the syenitic bodies , which seem to have come later, accordin g to recent field observat i o ns . Intrusiv es dated around 750 Ma might hav e been precur sors to the main Hook Granite event. 5 7 Table 4.12 Samples from the E-W transect through the Kafue Park, Hook Granite Batholith, and correspondence with ring complexes from Fig 4.18 and geological map units of Table 4.4 ( X = samples collecte d in the field; P= samples by Pepper, 1999; Z=from Zambian Geolog ical Survey. Underli ne d samples have chemic a l analysi s . The last two columns indicate high Cu or Zn values.) Samples Source Chemical rock type New unit (Table 4.5) Map unit (Table 4.5) Map sheet Ring complex (Fig 4.6) Position Rock type (sensu TAS) Cu Zn L-254 X 9 O 1426SW J n u c l e u s Grani t e L-255 X L 1426SW r i m Granite L-256 X L 1426SW n u c l e u s Grani t e L-257 X XI 9 O 1426SW r i m Granite L-253 X L 1426SW K n u c l e u s Quart z po d P-57 P uncla s s i fi e d 9 O 1426S W n u c l e u s Grani t e X L-258 X 9 O 1426SW L n u c l e u s Grani t e L-259 X XI 9 O 1426SW n u c l e u s Grani t e L-259B X Uncla s s i fi e d 9 O 1426S W n u c l e u s Grani t e L-260 X 3 H 1426SW n u c l e u s lt bn granit e L-261 X 9 O 1426SW n u c l e u s Grani t o i d + c p X L-262 X 1426SE n u c l e u s grani t o i d + c p + p y X L-354 Z I 9 O 1426SW rim Gran odiorite X L-433 Z II 1426SW r i m Syenoga b b r o X X L-263 X Uncla s s i fi e d 9 O 1426S W M r i m folia t e d grani t o i d L-264 X 1 B 1426SE n u c l e u s folia t e d grani t o i d L-265 X ? 1426SE n u c l e u s bn grani t o i d L-408 Z IV ? 1426SE r i m Granite L-403 Z VII 1 B 1426SE O r i m Quart z m o n z o n i t e X X L-406 Z II ? 1426SE rim alkal i gabbr o X X P-58 Z II 1426SE nucleu s Grani t e L-235 X 9 O 1426SW Un i d e n t i f i e d granit o i d L-236 X 9 O 1426SW Un i d e n t i f i e d Hornfe l s L-237 X VII 9 O 1426SW Un i d e n t i f i e d Granit e X L-238 X VII 9 O 1426SW Un i d e n t i f i e d Gran od i o r i t e L-239 X VII 9 O 1426SW Un i d e n t i f i e d granit e L-240 X 9 O 1426SW Un i d e n t i f i e d granit o i d L-241 X Uncla s s i fi e d 2 N 1426S W Un i d e n t i f i e d Foido l i t e L-244 X 2 N 1426SW Un i d e n t i f i e d pink grani t o i d L-245 X 2 N 1426SW Un i d e n t i f i e d pink grani t o i d L-246 X 2 N 1426SW Un i d e n t i f i e d gra y granit o i d L-247 X 2 N 1426SW Un i d e n t i f i e d foliat e d grani t o i d L-248 X Uncla s s i fi e d 2 N 1426S W Un i d e n t i f i e d Gran od i o r i t e L-248L G X XI 1426SW Un i d e n t i f i e d grani t o i d L-249 X VII 2 N 1426SW Un i d e n t i f i e d Granit e L-250 X 9 O 1426SW Un i d e n t i f i e d granit o i d L-251 X 9 O 1426SW Un i d e n t i f i e d granit o i d L-252 X 9 O 1426SW Un i d e n t i f i e d granit o i d L-405 Z II 1 B 1426SE Un i d e n t i f i e d s. oliv. Gabbr o X 5 8 Fig 4.23 Hypothetical granitoid ring co mplex cluster and transect across it. N o tice that if a series of five different ge nerations of granitoid ring complex s tructures intrude and intersect each other, a complex assembly of igneous lithologies can form. Each of the s eparate intrusive ev en t s ( A t o E ) was made of a few ring complexe s widely s pread in the ar ea. In the hypothetical case, each generation of ring complex es has a uniform litholog y . A chance orientation for a geological transect along X- Y results in the g e o l og y s ho w n. I n t erpretation of t hat geolog y based on th e single transect is quite complex, es pecially if the outcrop density is not good. Compare with Fig 4.18. H a ns on et al, 1993 dated sample s that come from various granite ring comple x e s . Ring Complex V had samp le s H-1 inside and H-2 on the rim; both could be dating the same event. H-5 is located on the rim of ring AJ; no samples from this projec t were collected there. H-5 was said to be a rhyolite intrusio n into the Mwembez h i Disloc a t i o n ; that sample dates at leas t one of the intrusiv e ev ents that took place along that major struc tu re . H-3 comes from the same site as L-40i and both lie on the rim of ring R. accordi ng to Hans on et al, 1993, H-3 c om e s from a rhyolite dike within a Katangan pendant. H-4 could come from the rim of not very well defined complex P. A tentative geological history for the Hook Granite Batholith may be established out of interpreting its geoph y s ic a l image with the radio m e t r ic ages publis he d by Ha ns on et al, 1993. Four distinct events of faulting can be establis h ed , and using cros s-c uttin g relations h ips of the various ring comple x e s , the sequenc e of events illustr a t e d on Fig 4.24 turns out. Note that avail a b l e rock dating does not includ e a large portio n of the plutons on Fig 4.24. If ring complex es AO and AQ were dated geochronologically, the geological history of the batholit h would be much better cons train e d . These two seem to be the oldest and younges t ring comple xe s , based on data availabl e . The basement to the oldest granite complex es is also made by granito i ds ; these rocks are probably the oldest in the batholith and have not been given names.Timing of the structural evolution could also be defined precis ely by dating ring comple xes that ar e younger and older than the faults. 5 9 Fig 4.24 Schematic representation of the various events that gave rise to the current geology of the Hook Granite Batholith. Each letter represents the emplacement of a single granitoid ring complex. Time advances upward. The diagram is based on cross-cutting relationships ob s erved in interpreted ge op hy sical images (Fig 4.18). Four distinct generations of faulting are recognized, and they help to es tablish the order of emp lacement. O n l y e v en t s j oined b y b lack lines have dire ct sequential order. For example, V is older than T, that is older than O. Nevertheless, the temporal rela tionship between V , F , B A and I has not established. U n derlined ring complex es could b e dated to refine ge o l o gical history of the H oo k Granite Batholith. As previous ly discus sed, IOCG mineralization took pl ace along various N-S faults. The age of those events in uncertain, but probably younger than 532 Ma. If the bathol i t h was made by amalga m ati o n of anorog e n ic granitoi d ring complexe s , geochron o l o g ic a l studies of Hanson et al, 1993 are not repr esentative of the entire Hook Granite; especially for the pr e- tectonism granito id phas es . The geologic a l model on whic h they based their observ a t i o n s and geochr o n o lo gi c al deductions was partially wrong. There mi gh t be signif i c a n t change s in the pictur e if more ring comple x es were dated. Case studies from other similar size, ring comp lex clusters, such as those in the Nuba mountains of Sudan and in central Nigeria show that the main intrus iv e event is pre- dated and post-dated by various other anorog en i c intrus i on s (Sectio n 7.2). The model here pres e n ted for the Hook Granite could be refine d by dating rocks of ring comple x e s AQ, AC, AS, AG, U, BD, and AO. These are underlined on Fig 4.23. The new information would produc e a much better cons tra in e d geologic a l history of the batholi t h . Dating comple x e s AF, AC, A, L and E would provide a good geochronological gras p on the timing of the N-S faults, and could help to cons tra i n the age of at least one of the IOCG mineralizing events. 6 0 4.1.1.7 Environment of Emplacement At least the samples listed on Table 4.8 formed in intr a- pl a t e anorogen i c rift environm e n ts , by compa r is on with sample s from anorogen i c ring complex es in Sudan, Namibi a and Nigeria. All other samples that come from some of the ring complex e s mapped on Fig 4.18 probabl y have a simila r origin. The last phases of rift magmatism in the batholith seem to have taken place in clos e temporal association with tectonism. Table 4.5 shows that granitoids in groups IV, VII and IX form ed as continen t a l epeiroge n ic uplift granitoi ds , in an anorogen i c environm e n t . Part of the samples indica t e a post orogen ic enviro nm e n t of emplac eme n t . Associated gabbroid rocks formed in continental extensional environments. The environment of emplacement of all samples from the batholit h will be refined us ing the automat e d process of compari s o n describ ed in section 2.4. 4.1.1.8 Conclusions We can conc lude that information currently availabl e on geophysics, geochronology, rock distribu tion and geochemis t r y from the Hook Granite Batholit h fit quite we ll with an intracontinen tal, anorogenic, ring complex clus ter origin. A series of ring complexes roughly centered on the same place for a period of at least forty million years could very well have produced a body of the size of the curren t Hook Granit e. More than fifty individual ring complexes have been identified. The Hook Granite Batholith is mainly made of midalk a l in e granito i d s . Alkali granites , quartzm o nz on i t e s and granites make up 70% of all samples . Rock composi t i o n varies widely from one ring complex to the next, and also within individ u a l ring comple x e s . The suite of 10 4 samples collec t e d from the bathol i t h has been grouped into eight main types, but 40% of them do not classify into those groups. A 90 kilomete r E-W transect across the batholit h samp led five different ring complexes and proved that publis hed geological maps do not repr es ent the reality. Many features of iron oxide- copper-gold mineralization were identified in the batholith. Some of them include massive iron oxide bodies , red-altered intrusives , rou nd- pe b b le hydro t h er m a l brecc i a t i o n , gold, copper , zinc and silver occurren c e s and some old mines. Several of the samples analysed carry coppe r enrichm e nt . Zinc values are high in a few granites and syenites , as we ll as in most of the gabbroi ds analyse d . Zinc-ri c h samples come from at least nine different ring complexes. 4.1.1.9 Recommendations There is so little outcrop in the Hook Granite area, that field mapping on its own is not enough to understand the geology. Airborne geophysics should be used to guide and help interpre t the field observat i o ns . Good geolog i c a l maps of the Hook Granite Batholi t h could be made by going back to the original field maps and using the outlines of the outcrops . If only mapped real data is re-inte r pr e t e d with the airborne geophys i c s , a reas onab l e geologic a l map may be produce d . All of the samples collect e d by Zambian Geologic a l Survey geolog i s ts should be prec is e l y located on topogra phic a l maps , using the origina l field notebook s . Many of these samples have alread y been analys e d during the Lufilian Arc granitoid project. Such samples can be used to re-map the entire area. All samples collect ed during the mapping of the Hook Granite could be precis ely located with a few days of office work at the Zambian Geolog ical Survey. Once their precise location is know n, well-selected samples could be dated to complet e the proces s . Wher ev er new roads or ways of access are availabl e , additiona l samplin g and mapping could be carried out to complet e those portion s of the maps. The entir e projec t could be completed in two month?s time by the Zambian Geological Survey, and should not be expensive to execute. 6 1 4.1.2 WEST LUSAKA AND KAFUE FLATS REGION, ZAMBIA 4.1.2.1 Introduction This portion of Zambia is know n to have various co ppe r occur r e nc es assoc i a t e d to iron oxide bodies that outcrop as prominen t hills (See Fig 8.12). The Nampundw e pyrite mine 1 is locate d in the West Lusaka region , while the Dunrob in and Matala gold mines, the Lewis- Ma r i e coppe r mines, and the Kitumb a and Kanton ga copper deposits, occur to the north of the Kafue Fl ats area. Shimyoka , another mineraliz e d domain where various mineral deposits have been sought for in the last decade, lies just south of the Kafue Flats area. As illustra t ed on Figs 8.40 and M7, Cu, Zn, Au and Fe occurren c e s are know n througho u t this zone. 4.1.2.2 Geochemistry T w e n t y nine chemic a l analys e s of sample s confor m the database of Table 4.1.2.1. The Zambian Geolog ical Survey provided L-416 an d L-458 to L-467 , analys is for X-90 (labeled ?Lusak a Granit e ? ) comes from Simpson, Drysdall, & Lambert, 1963, p. 25; the remai n d in g sevent e e n sample s were collec t e d during field work by the author . The rocks analys e d can be groupe d in to six discrete types, as shown on Figs 4.1.2.1 and 4.1.2.2. These are listed on Table 4.1.2.2. Fig 8.12 (brought in from Chapter 12) Hill of massive magnetite that outcrops west of Lusaka, Zambia . As show n here, massive iron oxide bodies in this par t of the L ufilian Arc produce t h ese inte resting geo morphol ogical features. T hey stand o ut up to 120 meters abov e the average flat plateau. In t he foreground, rolling hills are syenitic intrusive bo dies. Small gabbroic bodies are also fou nd in the environs. A bun dant hydrothermal breccias with su lfide mineralization occur here too. T h e West Lusaka and Kafue Flats region has very abun dan t small gabbroic bodies (group D); never th e le s s , these were not sampled as often, and few of the ones collected were analys ed. Group F is made of single sample L-217 ; it contains abnormally high Cr, anoma lous Mg, Pr, Co and Ni, and very low Na and Al. At the time of collect i o n the rock was thought to be a red syenite, but its chemist r y indicat e s granodio r i t i c composit i on . Group G is made of hydrothe r ma l l y altered granites that plot as granodior ite-diorite on the TAS diagram (Fig 4.1.2.1). Samples L-222 , L-223 a nd L-224 contain anomalou s iron oxide, high loss on ignition, abnormal l y high Rb and Ce and low Mn, Ca and Na. In addition, two samples of massive iron oxide were collec te d ( L-464 and L-465 ). The pattern of multiple compos itional fields re-occur s here, and is fully recognized. Four contrasting rock types that occur together . Granites B probably are t he host rock, and alkali granit es A, syenit e s C and gabbros D were intrude d into them, giving rise to the large iron oxide bodies and sulfidation in the region. Quartz pods are also quite common in some parts, especia l l y around L-175 . 1 The Nampund w e pyrite mine was pr eviously called King Edward mine. 6 2 Table 4.1.2.1 Chemical Anal ysis of samples from the West Lusaka-Kafue Flats Area, Zambia ( C omp l e t e elementa l analysis on Table A2, Appendix ) Sample SiO2 TiO2 Al2O3 FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total Notch 50.00 1.00 15.50 6 . 0 0 0 . 1 5 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2 . 0 0 Notch 50.00 1.00 15.50 6 . 0 0 0 . 1 5 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2 . 0 0 L-175 74.72 0.41 12.60 2. 96 0 . 0 0 0 . 4 1 1 . 0 8 2 . 7 1 4 . 6 0 0 . 0 9 0 . 3 2 99.90 L-181 49.82 1.08 15.86 1 1 . 3 3 0 . 1 6 6 . 3 0 1 1 . 2 8 2 . 9 4 0 . 2 4 0 . 0 6 0 . 8 6 99.94 L-195 61.25 0.38 15.84 8 . 6 7 0 . 0 9 0 . 0 4 2 . 3 5 5 . 6 6 5 . 0 3 0 . 0 9 0 . 5 1 99.91 L-207 75.03 0.07 13.63 0. 68 0 . 0 0 0 . 0 0 0 . 1 1 4 . 3 2 6 . 2 7 0 . 0 1 0 . 2 6 100.39 L-208 74.23 0.05 13.85 0. 87 0 . 0 3 0 . 0 0 0 . 1 2 4 . 3 6 6 . 1 3 0 . 0 5 0 . 2 4 99.93 L-209 46.78 1.81 16.06 1 1 . 3 3 0 . 0 5 7 . 5 1 1 1 . 4 6 2 . 3 4 1 . 9 1 0 . 5 7 0 . 6 0 98.79 L-210 66.74 0.43 17.99 3 . 5 2 0 . 0 0 0 . 2 9 0 . 6 9 9 . 5 8 0 . 0 9 0 . 1 4 0 . 3 9 99.87 L-212 67.27 0.40 15.94 2 . 8 9 0 . 0 0 0 . 1 5 0 . 8 1 4 . 4 4 7 . 0 4 0 . 0 3 0 . 7 1 99.69 L-213 66.68 0.36 17.40 3 . 0 3 0 . 0 0 0 . 0 8 0 . 2 3 6 . 8 7 4 . 8 7 0 . 0 3 0 . 6 0 100.17 L-214 66.63 0.39 17.62 1 . 5 4 0 . 0 3 0 . 0 0 0 . 2 4 7 . 6 8 3 . 9 2 0 . 0 6 0 . 6 3 98.74 L-215 70.53 0.23 16.82 0 . 6 5 0 . 0 0 0 . 0 0 0 . 1 5 1 0 . 3 2 0 . 1 9 0 . 0 3 0 . 3 6 99.30 L-217 73.54 0.39 10.80 3 . 9 8 0 . 0 9 3 . 4 0 1 . 3 5 0 . 6 4 2 . 9 7 0 . 1 5 2 . 4 1 99.72 L-218 66.30 0.52 15.92 4 . 6 4 0 . 0 0 0 . 4 9 2 . 0 1 4 . 7 9 5 . 4 3 0 . 1 1 0 . 2 1 100.42 L-222 64.17 0.57 13.11 1 3 . 7 2 0 . 0 0 0 . 8 0 0 . 0 8 0 . 1 5 4 . 7 4 0 . 1 2 2 . 4 6 99.94 L-223 66.79 0.57 14.12 1 0 . 1 6 0 . 0 0 0 . 7 9 0 . 0 8 0 . 1 7 5 . 2 0 0 . 1 0 2 . 4 9 100.48 L-224 62.03 0.58 13.42 1 5 . 0 2 0 . 0 0 0 . 6 2 0 . 0 7 0 . 2 4 5 . 6 9 0 . 1 1 2 . 3 3 100.13 L-416 52.44 0.65 15.34 8 . 6 3 0 . 1 5 7 . 2 8 1 2 . 4 2 2 . 5 5 0 . 7 3 0 . 0 7 0 . 2 0 100.46 L-458 72.83 0.09 13.43 1. 35 0 . 0 2 0 . 0 0 0 . 2 0 3 . 5 2 6 . 9 4 0 . 0 3 0 . 3 7 98.78 L-459 61.30 0.79 13.54 9 . 0 9 0 . 1 3 3 . 3 8 5 . 8 8 3 . 0 2 1 . 1 6 0 . 1 0 0 . 6 3 99.02 L-460 74.38 0.43 11.58 4. 11 0 . 0 3 0 . 6 2 1 . 8 6 3 . 6 7 2 . 3 3 0 . 1 2 0 . 3 4 99.47 L-461 71.85 0.20 14.11 1. 77 0 . 0 2 0 . 2 6 1 . 0 1 3 . 4 5 5 . 3 4 0 . 0 6 0 . 7 0 98.77 L-462 72.04 0.34 13.78 2. 58 0 . 0 2 0 . 3 8 1 . 2 1 3 . 1 8 5 . 1 9 0 . 0 4 0 . 3 7 99.13 L-463 48.36 2.43 14.19 1 4 . 7 9 0 . 1 9 7 . 2 6 7 . 6 8 2 . 8 5 1 . 0 1 0 . 4 0 - 0 . 5 3 98.63 L-464 5.46 0.07 0.00 77 . 4 9 0 . 0 8 0 . 5 0 6 . 0 9 0 . 1 0 0 . 5 2 0 . 0 6 3 . 1 6 93.53 L-465 14.01 0.58 2.56 64 . 7 4 0 . 0 3 0 . 7 0 0 . 1 7 0 . 0 6 0 . 4 3 0 . 1 2 1 2 . 8 5 96.25 L-466 73.93 0.13 12.78 1. 65 0 . 0 3 0 . 0 8 0 . 9 8 4 . 2 7 4 . 5 0 0 . 0 3 0 . 3 0 98.68 L-467 70.78 0.25 13.75 2. 33 0 . 0 2 0 . 1 8 0 . 8 7 4 . 5 3 5 . 4 5 0 . 0 8 0 . 5 0 98.74 X-90 73.62 0.31 12.90 2. 2 1 0 . 0 5 0 . 4 2 1 . 1 3 3 . 3 7 5 . 9 0 0 . 1 0 0 . 4 4 100.45 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Sm Nd Pr Ce La Hf Ta Eu Gd Yb Lu Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 50 50 15 175 95 10 120 4.0 30 7.5 1.6 L-175 221 63 45 229 29 9 7 31 31 15 28 17 541 <6 25 <10 6 30 48 153 19 42 0.3 1.3 0.8 L-181 7 157 29 62 8 34 30 57 94 16 293 35 <22 <6 <15 35 <12 <12 L-195 89 130 115 1054 80 <6 <6 10 71 40 13 <12 2151 8 <15 <10 16 44 74 118 25 145 3.9 1. 5 7 . 5 2 . 2 L-199 10 787 42 534 47 399 9 39 20 137 36 288 95 11 3 5.4 13 3. 8 0 . 5 L-207 123 182 12 432 6 8 6 10 13 0 <12 13 557 0 0 0 5 0 2 19 0.2 0. 6 0.4 L-208 137 178 12 431 33 <6 <6 14 10 25 <12 238 517 9 132 <10 35 20 L-209 53 1592 27 111 17 36 42 29 52 19 243 50 1437 <6 <15 27 113 61 L-210 4 275 30 474 36 6 7 143 13 22 28 <12 83 7 74 <10 372 223 L-212 149 117 51 336 49 8 <6 32 17 22 <12 <12 503 8 79 <10 250 130 L-213 73 193 27 596 39 8 6 18 22 25 22 <12 762 12 163 <10 4 42 69 137 20 16 39 0.7 0.7 0. 8 L-214 65 167 24 662 77 <6 12 20 15 25 19 81 657 7 104 <10 181 89 L-215 7 72 15 443 23 6 7 6 9 27 <12 <12 71 <6 193 <10 18 <12 L-217 124 48 10 128 10 86 17 8 43 13 67 502 805 <6 <15 11 7 28 53 89 30 59 0.8 L-218 202 344 46 601 53 8 <6 6 30 22 15 16 793 8 99 <10 17 75 265 342 135 8 65 1.5 2.1 1.1 L-222 304 122 69 275 30 <6 7 <6 22 29 79 18 499 7 20 11 220 121 L-223 312 122 77 270 28 <6 <6 <6 27 28 68 18 468 8 21 <10 2 1 20 250 2 166 1.0 L-224 261 103 35 301 28 9 8 <6 21 24 76 16 1065 8 19 <10 120 65 L-416 6 126 17 41 5 34 72 94 84 17 195 217 43 6 <15 42 <12 <12 L-458 277 30 72 45 13 <6 <6 9 11 18 <12 13 129 8 <15 <10 38 42 L-459 87 204 22 81 8 26 40 111 107 19 181 57 287 <6 <15 23 54 30 L-460 68 482 13 632 7 8 9 19 63 18 22 14 596 <6 20 <10 197 102 L-461 178 241 14 65 10 <6 <6 30 36 18 <12 13 1222 <6 15 <10 43 21 L-462 114 630 5 95 11 <6 <6 11 32 17 25 <12 3607 <6 16 <10 61 25 L-463 25 255 38 193 15 39 11 16 153 21 133 94 285 <6 <15 30 30 18 L-464 14 13 16 17 3 25 185 184 122 <9 34 <12 142 29 <15 37 <12 <12 L-465 25 76 9 129 17 13 85 143 102 11 127 <12 694 24 <15 36 <12 <12 L-466 351 83 31 75 39 <6 <6 15 21 24 <12 14 225 <6 23 <10 57 27 L-467 145 1046 29 208 18 7 10 12 30 22 16 <12 2676 <6 67 <10 224 130 Table 4.1.2.2 Rock types from the West Lusaka-Kafue Flats area, Zambia Rock type Group Samples a l k a l i gran i t e s A L - 2 0 7 * , L-208, L- 458, L-46 7 Grani t e s B L-175, L -460, L -461, L-462, L-460 , X-90 sye ni t e s and qua rt z syeni t e s C L - 1 9 5 , L-210, L-2 12, L-213*, L-21 4, L-215, L-218 Gabb ro s D L-181, L -209, L -416, L-436, L-463 , X-11 Tonali t e E L-459 Anoma l o u s gran o d i o r i t e F L-217 Hydr oth e r m a l l y altered granite G L - 2 2 2 , L-223, L-2 24 4 5 5 0 5 5 6 0 6 5 7 0 7 5 SiO2% 3 4 5 6 7 8 9 1 0 1 1 1 2 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM W Lusaka-Kafue Flats, Zambia; Lufilian G.P. (Based on Middlemost, 1994, 1997) S a m p le s P e tr o g r a p hi c fiel d s L - 1 7 5 L - 1 8 1 L - 1 9 5 L - 2 0 7 L - 2 0 8 L - 2 0 9 L - 2 1 0 L - 2 1 2 L - 2 1 3 L - 2 1 4 L - 2 1 5 L - 2 1 7 L - 2 1 8 L - 2 2 2 L - 2 2 3 L - 2 2 4 L - 4 1 6 L - 4 5 8 L - 4 5 9 L - 4 6 0 L - 4 6 1 L - 4 6 2 L - 4 6 3 L - 4 6 6 L - 4 6 7 X - 9 0 C A B G D E H Fig 4.1.2.1 - 5 0 0 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti) 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 R 2 = 6C a +2M g +A l L-175 L-181 L-195 L-207L-208 L-209 L-210 L-212 L-213L-214 L-215 L-217 L-218 L-222 L-223 L-224 L-416 458 L-459 L-460 L-461 L-462 L-463 L-464 L-465 L-466L-467 X-11 X-90 R1R2 PLUTONIC ROCK CLASSIFICATION West Lusaka-Kafue Flats Area, Zambia; Lufilian G.P. (After De la Roche et al, 1980) Pe t r o gr aph ic fie ld s Sa m pl es C F H G B A C C Fig 4.1.2.2 6 5 Table 4.1.2.3 Basic geochemistry and environm ent of emplacement for samples from the West Lusaka-Kafue Flats, Zambia ( S e e acronym descrip t i o n on section 2.4.3.) Sample Rock Name Debon & LeFort Maniar & Piccoli Whalen Pearce Mafic Rb/10H fTa Rb/30HfTa Nb-Ta L-175 Granite Peraii subleucoKFe POG A O3/4 OUTU L-181 Saturated olivine gabbro Metav mesoNaFe IAG+CAG N V emor L-195 Syenite Metav mesoNaFe CEUG A O-W 2-2 OUTU L-1 9 9 Syenite O 2/4 WP WP INW L-207* alkali granite Metav leucoNaKFe ? L-208 alkali granite Metaiv leucoNaKFe A L-209 alkali gabbro Metav mesoNaFe N emor L-210 Syenite Peraiii mesoNaFe OP A V1/2 L-212 quartz syenite Metaiv subleucoKFe CEUG A O-W 1-1 L-213* Syenite Peraiii subleucoKFe CEUG A O3/4 WP WP OUTU L-214 Syenite Peraiii leucoNaFe A W L-215 Syenite Metav leucoNaFe A V L-217 Granodiorit e Peraii subleucoKMg N? O2/3 OUTU L-218 quartz syenite Metaiv mesoNaFe CEUG A O3/4 WP WP OUTU L-22 2 alkali granite Peraii subleucoK F e CEUG A O-W 1-1 L-223 Granite Peraii mesoKFe CEUG A O2/3 OUTU L-224 alkali granite Peraii mesoKFe CEUG A O-W 1-1 wpab L-416 Gabbro norit e Metav mesoNaMg L-458 alkali granite Metaiv leucoKF e A O-W 1-1 L-459 Tonalite Metaiv metaNaFe A L-460 Granite Metaiv mesoNaFe A L-461 Granite Peraii leucoKFe POG ?N L-462 Granite Peraiii subleucoKFe POG N L-463 Gabbro-diorite Metaiv mesoNaFe A V wpt L-464 mass. iron oxide Metaiv mesoKFe CEUG V L-465 mass. iron oxide Peraiii mesoKFe CEUG A V L-466 Granite Metaiv leucoNaFe A L-467 alkali granite Metaiv leucoNaFe RRG-CEUG A X-11 Metav subleuc o K Fe X-90 Granit e Metaiv subleuc o K Fe 65% of the granitoids from the West Lusaka/K a f u e Flats region fall within the midalkal i n e field, while 35% of them fall in the subalkaline field (Table 4.1.2.4). All mi dalkaline rocks make 60% of the samples, 40% of them are subalka l in e . Table 4.1.2.4 Statistics of rock types in sam ples from West Lusaka and Kafue Flats, Zambia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type number % Granitoids Groups A l k a l i gran i t e 7 25.93 Q u a r t z m o n z o n i t e 2 7.41 S ye n i t e 4 14.81 6 5 . 0 0 Monzog a b b r o 1 3.70 Midalkaline Rocks A l k a l i gabbr o 2 7.41 59.26 Granite 4 14.81 Gr a n o d i o r i t e 3 11.11 3 5 . 0 0 Diorit e 2 7.41 Gabb ro-di o ri te 1 3.70 Subalkaline Rocks Gabb ro 1 3.70 40.74 Total 2 7 1 0 0 . 0 0 1 0 0 . 0 0 100.00 We will now proceed to describe the Lusaka Granite, continu e descri b in g the main rock types in the West Lusaka and Kafue Flats region, and discus s the high thorium cont en t of Kafue Flats rocks. 6 6 Fig 4.1.2.3 Geological map of the Lusaka Granite. Taken from T hieme, 1968. Not e location of sample L-175 . 4.1.2.3 Lusaka Granite The Lusaka Granit e is an elonga t e d stock that intrudes into slight ly folded and metamorphosed Katang a limestone s , and silicicla s t ic s . It has a drop- lik e shape, as shown on Fig 4.1.2.3 . L-175 comes from an outc r op of the Lusaka Granite, a coarse-grained, foliated, pi nk peral u mi n o us subleuc oc r a t ic potas s ic ferri f er ou s granite with abundan t coarse biotite , and quar tz porph yr ob l a s ts in ellipso i ds . The main foliati o n at the samplin g site was 120/37?S, with lineati o n s along the in tersec t i o n with 125/37 ?N . Outcrops are generall y flat, and follow horizon t a l planes of foliat i o n . Many quartz pods occur around L-175 . The pluton is cons ider ed to have formed at approximately 820 Ma. Thieme, 1968 states that X-90 is a representative sample from the Lusaka Granite and it is a metalumin ous subleucocratic potassic ferriferous granite. Tables 4.1.2.1 and 4.1.2.3 shows that it differers from L-175 , which was the most represen tative roc k in the outcrops vis ited. As discussed by Thieme, 1968 #38, the center of the granite is unfolia ted, and it grades into strong ly gneisso s e rocks towards the eastern and western boundar ie s (Fig 4.1.2.3) . Foliation is parallel to the boundar ie s . ?The interna l structu r e s of the pluton sugges t a combinati o n of internal intrusiv e forces and external regional defor mat io n during the waning phases of the Lufilian orogeny.? Additional referenc es on the Lusaka Granite are: DeSwardt & Si mpson, 1972; Drysdall & Garrard, 1964; Snelling, Johnson, & Drysdall , 1972. The environme n t of emplaceme n t of L-175 and X-90 is not easy to interpret based on the two chemical analyses available. Whalen plots indicate anorogenic origin , and the Maniar & Picolli method indicates a post orogenic origin . A working hypothes i s for the Lusaka Granite is that is formed as a single anoroge n ic granite ring complex; it was later deformed. 4.1.2.4 Description of Main Rock Types 4.1.2.4.1 Four Rock Association Small bodies of red-altered granitoids, gabbros, iron ox ide bodies and quart z pods occur toget h e r in the West Lusaka-Kafue Flats area. These four rock featur es are associ a t ed with iron oxide- c o pp er - gold minera l iz a ti o n throughout the Greater Lufilian Arc. In this case, the f our-roc k association is hosted by Katangan carbonates of the Lusaka Formati o n (marked light blue on Fig 8. 40). Hydrothermal brec ciation and coarse-grain sodic alteration (scapolitization) in the carbona t e s are common l y observ e d arou nd the four-rock association. Both syenit es and alkali granite s are closely relate d to gabbro ids. At times, the features of mineraliz ation and alterati o n resemble skar n. Descriptions of all the granitoids, gabbroids, ir on ox ide bodies and quartz pods collec t e d during fieldw o r k in the West Lusaka/ K a f u e Flats area are include d in A ppendix 60. They have been grouped by rock type for 6 7 d e s c r ip t i o n purpos es , but these rocks generall y occur in cl ose associa t i o n in the field. Discus s io ns on their field relations, geochemistry, environmen t of emplacem e n t and other geolog ic al data are were also include d there. 4.1.2.4.2 Granitoids Samples L-207* a nd L-213* are good repres en t a t i v e s of the red-alte r e d granito i d s and were dated. Both of them contain miarolitic cavities; t hese are eviden ce of boiling that to ok place during rock format i o n . Degassification from magma, or boiling, is a very importa n t clue for mineral i zation; in other parts of the same magma chamber , rocks might have experi enced violent hydrothermal explos io n s . This observat i o n is relevant for mineral exploration. L-207* , a red, metalu m i n ou s leuc oc r a t i c sodic- p o t ass s ic fe rriferous alkali granite from West Lusaka, comes from a series of granitoid s that are intimately asso cia t e d with small gabbro ic bodies (See photog r a p h on Fig 4.1.2.4). L-213* is a red, peraluminous subleucocratic potassic ferriferous syenite with small miarolitic cavities and dissemin a t e d spec ula r hematit e (Fig 4.1.2.4) . Th is sample has eviden c e of intens e hydr oth er m a l alteration, probably due to its high thor iu m content a nd heat produc t i o n capacit y . Chapte r 5 commen t s about thorium-related heat pr oduction capacity in greater detail . The rock also contain s anomal o us Pr, Zr, Na 2 O and Al 2 O 3 . Both L-207* and L-213* were dated; their geochrono logy is discus sed on subc hapter 4.1.2.6. Fig 4.1.2.4 Photographs of sl abs from red-altered granitoids in the Kafue Flats area, Zambia . A comes from sample L-207 ; B, from L-208 ; C, from L-213 ; D from L-215 . Notice the abundant, large miarolitic cavities in A and B. Part of them have been filled by q uartz , others are empty. C and D display abundant, but s maller miarolitic cavities. Mo s t o f t h e cavities in C and D are empty . Samples o f A and C were dated. Se e m ore details in the text. All scales in millimeters. Part of the granitoid s in the Kafue Flats displa y di ssemin a t io n s of specular hematite and others are intersected by abundant specularite veinlets. The majori ty of the granitoid s are anorogenic, and formed in a continen t a l epeirog e n ic uplift environ me n t , as shown on T able 4.1.2.3. Most granito id s from the suite are enric hed in the light rare elements. 4.1.2.4.3 Gabbroids M a n y gabbros outcrop in the West Lusaka/ K a f u e Flats region. Only a few of these abundant gabbroid rock outcrops were analysed. They contain significant metal mineralization and ma y be source for copper, zinc and 6 8 other ec onomic metallic enr ichment in the region. Some occur as small isolat e d bodi es that intersect any type of rock, as dikes or sills with various granito i ds , or as gabbro only ring comple x e s . The Appendi x includ es descrip t i o ns of the main samples observe d and studied . 4.1.2.4.4 Iron Oxide Bodies Massive bodies of magnetite and/or hematite are ho sted by Katangan limeston e s and dolos ton es . Sometime s the entire soil is made of only magnetite sand and gravel. Pa rt of the iron oxide bodies contain sulfides and/or gossans after various sulfides. They may contain meta ls beside s Fe, includin g Cu, Mn and others (See Table 4.1.2.1). Although gold and silver were not analysed, t hey could be pres ent in economic concentr a t i o ns . Many of the iron oxide bodies overprint breccioid text ures . It is common to see hydrothermal breccias flooded by coarse, metallic hematite or magnetite. There generally is a relict igneous texture in some of the iron oxide bodies . This may be due to progress i v e overprin t i n g and replac ement of the silicates by iron oxides. L-464 and L-465 , two samples from massive iron oxide bodies associa t e d to a gabbroic ring comple x in th e Kafue Flats area were analysed (Table 4.1.2.1) . Fig M7 show s their location . The rocks are extremely vuggy; before being leached, their vugs containe d copper , nickel and zinc sulfides , among other metals. That elemental enrichment is an evi dence of IOCG-type mineraliz ation. Table 4.1.2.5 Analysis of gossanous massive iron oxide bodies, West Lusaka-Kafue Flats area, Zambia S a m p l e S i O 2 TiO2 Al2O3 Fe 2 O 3 M n O M g O Ca O N a 2 O K 2 O P 2 O 5 LOI Total Notch 50.00 1.00 15.50 6. 0 0 0 . 1 5 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2.00 L-464 5.46 0.07 0.00 77. 4 9 0 . 0 8 0 . 5 0 6 . 0 9 0 . 1 0 0 . 5 2 0 . 0 6 3.16 93.53 L-465 14.01 0.58 2.56 64. 7 4 0 . 0 3 0 . 7 0 0 . 1 7 0 . 0 6 0 . 4 3 0 . 1 2 12.85 96.25 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Ce Notch 200 400 60 360 40 30 16 2 5 8 5 2 6 1 0 0 1 0 0 1 3 0 0 2 0 37 20 175 L-464 14 13 16 17 3 25 185 1 8 4 1 2 2 < 9 3 4 < 1 2 1 4 2 2 9 <15 37 <12 L-465 25 76 9 129 17 13 85 1 4 3 1 0 2 1 1 1 2 7 < 1 2 6 9 4 2 4 <15 36 <12 4.1.2.5 Thorium content in Kafue Flats Area S o m e syenites and quartz syenites from the Kafue Flats area contain extrem ely high values of thorium. These are listed on Table 4.1.2. 1 . That Th enrichm en t is more than ten times the average value for most granito i d s in Zambia and Namibia ; such values are among the highes t in sample s collec t e d during the Greater Lufili a n Arc granit o id projec t . Abunda nc e of Th in an igneous rock enables it to act as a long-lived heat engine. This can generate and focus hydrothe r ma l fluid flow for a long time. It possibly is a key ingredie n t for the occurren c e of iron oxide-c op p e r - go l d mineral iz a t i on . Chapter 5 contains more information on high thorium content of granitoid s in the Greater Lufilian Arc. Sample L-257 from the Hook Granite , and several others listed on Table 5.1, also contain anomalo us thorium and are related to granitoids in the Kafue Flats. Samples L-212 a nd L-218 contain much more potassium than normal, and their soda content is far lower than the rest of the high-Th samp les listed on Table 4.1.2.6 . 4.1.2.6 Geochronology Z i r c o n conc en t r a t e s from sample L-207* gave a zircon U-Pb SHRIMP II age of 538.2?3.3 Ma. Sample L-213* gave a SHRIMP II age of 550?25 Ma; several xenocrys ti c zircons were dated at 1872?14 Ma (Table A22.4) . Both of the young ages could represen t the same intrusive event, given the error overla p . The large error in age for L-213* could be due to intense hydroth er m a l alterat i o n due to the rock?s extraor d in a r y Th content . 4.1.2.7 Conclusions T h e granitoi ds and gabbroid s from the West Lusaka ? Kafue Flats region formed in an anoroge n ic uplift envir o nm e n t . There is a clos e assoc ia t i o n of gabbr o i ds with red-alter e d granitoi d s , bodies of massive iron oxide and quartz pods. Gabbroid s of various ages and origin s intersec t the rest of the rock types in the region. High thorium conten t in many of the granitoi d s induced and maintain e d a long-liv e d flow of hydroth er m a l fluids 6 9 i n the region . Severa l large iron oxide- c o pp e r - go l d pros pec t s are known in the area, and there is very good potential to find new, large, economic , iron oxi de-copp e r gold minerali z a t i o n in the region. Table 4.1.2.6 Samples with high Th values from the Kafue Flats, Zambia Samples contain high values in alumina, soda, Zr, Nb, Ce, La and low values for lime. Note the extraordinary heat capacity of these rocks at the time of emplac ement. Any valu e of heat capacity above 4 is anomalous. Sample Rock Name SiO2 Al2O3 Fe 2 O 3 Ca O N a 2 O K 2 O L O I Total Y Zr Nb Cu Ga L-19 9 Syenit e 42 534 47 L-210 Syenite 66.74 17.99 3. 5 2 0 . 7 0 9 . 5 8 0 . 1 0 0 . 3 9 9 9 . 8 7 3 0 474 36 143 22 L-212 Quartz s yenite 67.27 15.94 2. 8 9 0 . 8 0 4 . 4 4 7 . 0 0 0 . 7 1 9 9 . 6 9 5 1 336 49 32 22 L-21 3 * Syenit e 66.68 17.4 3. 0 3 0 . 2 0 6 . 8 7 4 . 9 0 0 . 6 0 1 0 0 . 2 2 7 596 39 18 25 L-214 Syenite 66.63 17.62 1. 5 4 0 . 2 0 7 . 6 8 3 . 9 0 0 . 6 3 9 8 . 7 4 2 4 662 77 20 25 L-215 Syenite 70.53 16.82 0. 6 5 0 . 2 0 1 0 . 3 0 . 2 0 0 . 3 6 9 9 . 3 0 1 5 443 23 6 27 L-218 Quartz s yenite 66.30 15.92 4. 6 4 2 . 0 0 4 . 7 9 5 . 4 0 0 . 2 1 1 0 0 . 4 4 6 601 53 6 22 Sampl e Z n U Th Sm Nd Pr Ce La Cs Hf Eu G d Yb L u H e a t Capaci t y L-199 9 39 20 137 36 2 8 8 9 5 1 1 1 5 1 3 4 1 2 . 9 2 4 L-210 13 7 74 372 223 5 . 3 2 5 L-212 17 8 79 250 130 6 . 5 6 L-213* 22 12 163 4 42 69 13 7 2 0 1 7 1 1 1 1 2 . 2 1 1 L-214 15 7 104 181 89 7. 8 7 3 L-215 9 <6 193 18 <12 13 . 4 4 9 L-218 30 8 99 17 75 265 3 4 2 1 3 5 8 1 2 1 7 . 7 4 3 7 0 4.1.3 KALENGWA-KASEMPA AREA, ZAMBIA 4.1.3.1 Introduction The Kalengwa and Kasempa areas lie in the Northwes t e r n Province of Zambia (Figs M1, M8 and M9). They occur in the same geographical area, their geology is comparab le , and have similar general charact er i s t i c s ; for these reas ons , they have been gr oupe d togeth er for discus s ion . The area may be reache d by road from the Copper belt, through Solwesi into Kasempa. Access from Mumbwa in the south is possible, but the roads are in bad shape. It lies halfway between the Hook Gr anite batholith and the border with the Democratic Republic of Congo. The region is underl a in by Katanga n silici c la s t ic s an d carbonates. Thes e in turn are covered by Mesozoic sedime n t s and recent sands. The Katang a n sedimen t s were intrud e d by variou s midalk a l in e granit o i ds and gabbro i ds . These have been groupe d by some resear c h ers into anorog en i c ring comple x es . Ther e are very few outcro ps in the Kasemp a and Kaleng w a areas. Outcrops of granitoids are especia lly scarce. The geophys ic a l image of Fig 4.1.3. 1 shows that the Kalengwa - K a s e mp a area is made up of several large ring structur es . Kalengw a has at least four ring stru ctu r es with a diameter of 15 km and one with 25 km diameter . It is center ed in another ring structure with diameter of 55 km; se veral smaller rings structu r e s are also eviden t. The Kasempa area is made by of such structur es with diameters around 20 km, some with diamet er of 10-15 km, and one with 50 km diamet e r ; severa l smalle r ring structu r es are also pres en t . Some very large magnetic anomali e s like at Chitamp a and Kametet e are evident in geophys ic a l images of this region (Nisbet, Cooke, Richards , & Williams, 2000; Nisbet, 2004a and Nisbet, 2004b). See also Fig. 4.16. Fig 4.1.3.1 Geological interpretation of ai rborne magnetic image for northwestern Zambia. N o t e t h e abundant circular features that are represented in m any parts of the figure. Also n o t e t h e N - S- trending structures that exten d f or hundreds of kilometers. The Kalengwa and Kasempa areas are dominated by large annular structures that are considered to b e anorogenic ring complex es . Same color coding as ex plained for Fig 4.17, which is located in the red rectagle. Extracted from Nisbet, 2004b. 7 1 The Kaleng w a mine is conside r ed by many to be one of the major exponen t s of iron oxide-copper-gold deposits in Zambia. It was one of the most profitable copper deposits in the country, and paid for its own infrastr uc t u r e in a remote locatio n , separat e d from th e rest of the main Copper b el t . Few reports on the deposit are publicly available today. Hydr other m a l brecciati o n , as well as gabbroid rocks seem to have played important roles in the formation of the original depo si t . Most of the mined copper minerals were enriche d by supergen e concentr a t i on ; copper oxides and few sulfid es were found near the surface. Ther e is more information about the Kalengwa mine in section 8.4.2.6. The Kasempa area has been explor ed for its copper and gold potential sinc e the early twentieth centur y by various mining compan i es . Numero us prospec t s and miner al occurren c e s are known from the distric t . Many borehol es drilled in the region are kept at the Kalulu s h i coreshed . Both the Kalengw a and Kasempa areas have significant potential for iron oxide-copper-gold mineraliz ation. 4.1.3.2 Sampling Althoug h the road from Kasempa to Mumbwa was traver s e d du ring fieldwor k for this project, there is very little outcrop and no samples were collected. All samples were obtained from indirect sources. A total of 27 chemic al analysis were collecte d (Table 4.1.3.1) ; 18 were chemic al analysis from previous reports, and 9 were physica l samples from borehol es and outcrop s visited by other resear cher s. More details on the samples will be given for each sectio n . 4.1.3.3 Geochemistry Samples from the Kalengw a - Ka s e m p a region fall within the midalka l i ne and alkaline fields as show n on Fig 4.1.3.2. Midalkaline and alkaline rocks dominate as seen on Table 4.1.3.2. This is probably related to the ring comple x composit i on . 82% of the granitoi d s from t he Kalengwa-Kasempa region fall within the midalkaline field while the rest are subalkaline. All midalkaline ro cks make 64% of the samples, 29% are alkaline and 7%, subalkaline. Table 4.1.3.2 Rock type statistics, sampl es from Kalengwa and Kasempa region, Zambia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type number % Granitoids Groups a l k a l i gran i t e 2 7.14 q u a r t z m o n z o n i t e 3 10.71 s ye n i t e 2 7.14 m o n z o n i t e 2 7.14 81 . 8 2 monzo d i o r i t e 3 10.7 1 m o n z o g a b b r o 3 10.71 Midalkaline Rocks a l k a l i gabbr o 3 10.7 1 64.29 granite 1 3.57Subalkaline Rocks g r a n o d i o r i t e 1 3.57 18 . 1 8 7.14 foid monzo - d i o r i t e 1 3 . 5 7Alkaline Rocks f o i d gabbro 7 25.00 28.57 Total 2 8 1 0 0 . 0 0 1 0 0 . 0 0 100.00 Geoc hemis try from Kalengwa and Kasempa will be discus sed jointly. The TAS diagram (Fig 4.1.3.2 ) show s a wide spread di strib u t i on of rock chemist r y that spans the entire midalkaline field in at least five discrete clus ters (Table 4.1.3.2). Most rocks from the Kalengwa area fall in the mid-alk a l i ne field except for L-322 , L-321 and the foid-bearing rocks of the Ka sempa area. Most rocks display evidence of hydrothermal alteration, especially L-321 . The differen t geochem ic a l diagram s (F igs 4.1.3.2 to 4.1.3.7) helped to establi s h seven main geoche m ic a l suites of contra s t i ng rock types in the Kalengw a- K a s e m pa area (See Table 4.1.3.3). This variety of rock types is a featur e observed in several other mineralized area s of the Greater Lufilian Arc. Rocks that fall in the general gabbr oid field have extremel y differen t chemistr i e s. Some of them are intrus ive and others effusive rocks. Thes e observat i o ns are common in anorogen i c mafic, midalkal i n e and alkaline ring complexe s . 7 2 Table 4.1.3.1 Chemical Analysis of sampl es from the Kalengwa-Kasempa Area, Zambia ( C omp l e t e elementa l analysis on Table A5, Appendix ) Sample SiO2 TiO2 Al2O3 Fe2O3 MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Notch 50.00 1.00 15. 5 0 6.00 0.15 2. 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 30 2.00 200 400 60 360 40 30 16 L-139 75.60 0.09 11.88 1. 50 0.03 0. 6 2 0 . 1 4 1 . 6 1 7 . 8 7 0 . 0 1 0 . 7 9 1 0 0 . 1 4 399 17 40 75 41 10 7 L-313 54.29 1.67 13 . 4 7 10.37 0.06 5. 0 7 4 . 9 2 4 . 5 5 0 . 8 0 0 . 6 7 4.40 100.27 21 164 89 445 40 14 12 L-314 43.72 7.81 12 . 7 3 11.28 0.08 6. 6 8 7 . 0 1 3 . 3 8 0 . 3 6 0 . 6 4 6.73 100.42 14 77 56 25 36 20 19 L-318 47.28 3.04 15 . 3 1 7.93 0.04 6. 8 6 1 3 . 8 5 4 . 1 8 0 . 5 6 0.38 0.96 100.39 9 154 37 163 27 23 53 L-32 1 71.94 0.71 9.67 11.04 0.03 3. 4 3 0 . 3 0 0 . 6 8 0 . 0 5 0 . 1 2 2.40 100.37 6 81 59 242 18 96 18 L-322 70.45 0.74 13.65 5. 38 0.02 0. 4 8 0 . 0 8 0 . 1 3 7.57 0.08 1.74 100.32 168 30 37 264 30 12 7 L-323 67.04 0.81 14.1 5 7.57 0.02 0. 5 2 0 . 1 9 0 . 1 7 8.21 0.17 1.61 100.46 173 29 37 302 35 26 9 L-324 62.05 0.97 14.5 0 7.90 0.06 1. 4 3 1 . 7 1 3 . 8 5 6 . 2 9 0 . 2 9 1 . 2 5 1 0 0 . 3 0 1 1 2 230 57 362 35 20 16 L-325 60.42 1.15 16. 9 8 11.07 0.02 0. 9 1 0 . 0 6 0 . 0 8 6 . 7 5 0 . 2 9 2 . 8 2 1 0 0 . 5 5 227 37 346 372 31 28 13 P-13 65.76 0.82 14.6 7 5.87 0.10 1. 0 0 2 . 4 0 5 . 7 7 3 . 8 9 0 . 2 4 0 . 2 1 100.52 90 301 45 157 30 70 11 P-17 64.11 0.97 14.2 9 7.35 0.08 0. 8 0 2 . 4 3 3 . 9 5 5.62 0.26 0.18 99.86 107 372 54 327 32 84 16 P-25 51.44 2.40 20. 3 8 8.73 0.71 3. 9 1 5 . 2 8 6 . 4 2 1 . 7 1 0.38 0.12 100.72 55 348 24 107 14 33 6 P-26 76.20 0.13 11.5 8 0.93 0.05 <. 1 0.25 10 . 5 1 0 . 0 3 0 . 0 3 0 . 0 8 9 9 . 7 1 7 15 170 705 243 39 4 X -76 55.35 1.48 14 . 6 3 10.86 0.10 4. 4 3 2 . 4 3 0 . 9 1 7 . 3 4 0 . 5 0 1 . 6 5 9 9 . 6 9 209 199 56 591 28 13 11 X -77 61.50 1.10 15. 1 5 7.30 0.11 1. 5 8 2 . 8 1 4 . 3 9 5 . 0 7 0.34 1.21 100.59 182 313 48 339 34 15 <9 X-78 51.81 3.13 15. 0 6 11.46 0.06 7. 5 3 1 . 0 0 3 . 0 2 4 . 4 8 0 . 3 3 2.67 100.54 137 109 32 290 46 25 102 X - 79 48.31 4.07 11 . 3 8 9.92 0.21 9. 9 2 5 . 9 0 2 . 5 8 1 . 1 4 0 . 5 7 6.34 100.34 18 234 32 358 44 47 70 X -80 45.03 3.27 13 . 5 3 16.29 0.09 6. 0 4 5 . 0 5 5 . 1 4 3 . 3 2 0 . 5 3 2.13 100.41 97 112 48 325 55 24 81 X -81 46.37 3.96 13 . 4 6 15.27 0.05 6. 2 0 4 . 8 8 4 . 9 1 2 . 9 6 0.54 1.92 100.52 103 94 55 302 48 17 88 X -82 48.60 1.56 13 . 7 1 18.47 0.08 2. 0 2 5 . 0 7 7 . 3 8 1 . 0 5 0 . 8 1 1 . 5 2 1 0 0 . 2 6 3 2 122 61 567 84 <9 10 X -83 46.07 2.56 14 . 2 0 17.60 0.15 5. 9 7 5 . 8 4 3 . 6 0 3 . 2 0 0.32 0.85 100.37 88 105 27 177 32 17 44 X -84 46.07 3.95 12 . 3 0 12.67 0.06 3. 4 4 8 . 5 6 5 . 4 9 0 . 8 7 0 . 9 1 6.14 100.47 27 106 59 444 89 11 11 X -85 47.35 2.56 14 . 0 8 13.25 0.14 7. 2 9 8 . 2 2 4 . 2 1 0 . 6 1 0 . 3 2 2.54 100.58 21 287 26 173 37 36 69 X -86 45.88 3.96 12 . 7 2 16.75 0.25 5. 6 1 7 . 1 9 3 . 7 8 1 . 4 6 0 . 3 1 2.23 100.14 37 319 33 201 40 14 36 X -87 46.09 2.86 13 . 8 0 14.33 0.23 6. 9 8 7 . 0 7 4 . 9 0 0 . 3 2 0 . 4 1 3.05 100.06 13 344 31 208 42 18 50 X -88 45.24 2.00 14 . 3 7 11.55 0.11 10 . 9 7 4 . 1 1 2 . 7 2 5 . 2 4 0 . 2 0 3.85 100.37 147 69 25 131 21 35 201 X - 89 46.20 3.57 8. 6 8 14.36 0.18 11 . 4 2 6 . 0 7 4 . 3 0 2 . 7 0 0.67 1.85 100.01 56 337 36 223 53 37 30 Sample Cu Zn Ga V Cr Ba U Th Sc Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Notch 25 85 26 100 100 1300 20 37 20 50 50 15 175 95 3 10 120 100 4.0 30 5.0 20 3 9 36 7.5 1.6 L-139 55 34 23 14 47 769 <6 26 <10 42 12 L-313 42 39 23 102 21 104 7 <15 36 139 75 L-314 28 49 18 438 50 60 <6 <15 55 27 16 L-318 9 22 19 258 99 20 <6 <15 30 68 33 L-321 16 30 15 157 95 65 <6 <15 12 102 61 L-322 13 35 21 49 33 498 <6 27 <10 171 74 L-323 17 28 20 58 32 525 <6 30 <10 153 71 L-324 62 121 21 96 27 1004 13 48 11 190 74 L-325 55 48 26 114 <12 508 6 27 <10 1460 819 P-13 <3 4 23 55 22 787 10 56 7 10 59 17 1 5 3 8 0 < 1 9 3 1 3 5 2 . 1 9. 5 1.3 8 2 5 35 4.6 0 . 8 P-17 63 23 24 103 11 782 11 48 10 12 64 17 136 47 1 8 2 3 88 2.4 11.7 1.5 9 2 5 36 5 . 0 0. 8 P-25 40 13 24 98 90 120 <2 2 20 4 15 3 22 9 1 2 1 12 1 0 7 1 . 7 4. 5 0.7 4 1 2 34 2. 1 0 . 3 P-26 <3 <1 68 <4 24 22 6 76 1 7 15 3 24 8 <1 3 1 5 1 7 0. 7 1 1 . 8 3.3 28 7 21 36 2 3 . 0 3 . 4 X - 76 295 50 139 <9 1379 X-77 7 47 92 11 1189 X-78 20 100 415 117 118 X-79 35 146 458 74 75 X-80 12 23 327 142 141 X-81 7 22 324 135 148 X-82 777 47 58 <9 233 X-83 102 44 325 79 384 X-84 26 59 138 <9 152 X-85 11 182 318 36 127 X-86 124 167 522 <9 303 X-87 9 134 315 23 119 X-88 <2 168 326 515 112 X-89 7 228 474 9 155 0 4 5 5 0 5 5 6 0 6 5 7 0 7 5 SiO2% 1 2 3 4 5 6 7 8 9 1 0 1 1 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM Kalengwa-Kasempa Area, Zambia; Lufilian G.P. (Based on Middlemost, 1994, 1997) S a m p l e s P e t ro g r a p h i c fiel d s L-139 L-313 L-314 L-318 L-321 L-322 L-323 L-324 L-325 P-13 P-17 P-25 P-26 X-76 X-77 X-78 X-79 X-80 X-81 X-82 X-83 X-84 X-85 X-86X-87 X-88 X-89 Fig 4.1.3.2 - 5 0 0 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti) 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 R 2 = 6C a +2M g +A l L-139 L-313 L-314 L-318 L-321 L-322 L-323 L-324 L-325 P-13P-17 P-25 P-26 X-76 X-77 X-78 X-79 X-80 X-81 X-82 X-83 X-84 X-85 X-86 X-87 X-88 X-89 R1R2 PLUTONIC ROCK CLASSIFICATION Kalengwa-Kasempa Area, Zambia; Lufilian G.P. (After De la Roche et al, 1980) P e t r o g r a p h i c fi e l d s S a m p l e s Fig 4.1.3.3 1 0. 8 0. 6 0 .4 0 . 2 0 K/(Na+K) 0 100 200 300 400 500 B = F et + M g + T i L -1 3 9 L -3 1 3 L -3 1 4 L -3 1 8 L - 32 1 L -3 2 2 L - 32 3 L -3 2 4 L -3 2 5 P -1 3 P - 1 7 P - 25 P -2 6 X -7 6 X -7 7 X -7 8 X -7 9 X - 8 0 X -8 1 X - 82 X -8 3 X -8 4 X - 85 X - 86 X - 87 X -8 8 X -8 9 K-B Diagram (After Debon & LeFort, 1994) Kalengwa-Kasempa Area, Zambia; Lufilian Arc Granitoid Project Fig 4.1.3.4 - 5 0 0 5 0 1 0 0 1 5 0 2 0 0 2 5 0 3 0 0 3 5 0 Q=S i/3- (K +N a+2 C a/3) Q-P Plutonic Classification ( Af t e r De b o n & L e F o r t , 1 9 8 3 ) Kalengwa-Kasempa Area, Zm, Lufilian Arc Granitoid Project Pe trographic Fields Reference rocks Sa mples - 4 0 0 - 3 5 0 - 3 0 0 - 2 5 0 - 2 0 0 - 1 5 0 - 1 0 0 - 5 0 0 5 0 1 0 0 1 5 0 2 P=K-(Na+Ca) L - 1 3 9 L - 3 1 3 L - 3 1 4 L - 3 1 8 L - 3 2 1 L - 3 2 2 L - 3 2 3 L - 3 2 4 L - 3 2 5 P - 1 3 P - 1 7 P - 2 5 P - 2 6 X - 7 6 X - 7 7 X - 7 8 X - 7 9 X - 8 0 X - 8 1 X - 8 2 X - 8 3 X - 8 4 X - 8 5 X - 8 6 X - 8 7 X - 8 8 X - 8 9 Fig 4.1.3.5 0 250 500 -250 0 L -13 9 L-3 13 L-3 14 L -31 8 L-3 21 L-3 22 L- 323 L-3 24 L- 325 P -1 3 P -17 P -25 P - 26 X -76 X -77 X - 78 X - 79 X -80 X - 81 X -82 X - 83 X - 84 X - 85 X -86 X - 87 X -8 8 X -89 A-B Diagram ( A f t e r Deb o n & LeF o r t , 199 4 ) Kalengwa-Kasempa Area, Zambia; Greater Lufilian Arc Granitoid Project Fig 4.1.3.6 0 1 0 0 2 0 0 3 0 0 4 0 0 5 0 0 0 0 . 1 0 . 2 0 . 3 0 . 4 0 . 5 0 . 6 0 . 7 B K 16b B K 19a B K 1a B K 1b B K 1 c B K 24a B K 27a L -13 9 L-3 13 L- 314 L- 318 L- 321 L- 322 L -32 3 L-3 24 L-3 25 P - 13 P -17 P - 25 P - 26 X -7 6 X -7 7 X -7 8 X - 79 X - 80 X - 81 X - 82 X - 83 X -8 4 X - 85 X -86 X - 87 X - 88 X -89 Mg-Fe-B Diagram ( A f t e r Deb on & LeFo r t , 199 4 ) Kalengwa-Kasempa Area, Zambia; Lufilian Arc Granitoid Project Fig 4.1.3.7 7 9 As shown on Table 4.1.3.3, samples from the Kalengwa/Kas empa area can be grouped into six main suites and others made by single samples . The diagrams proposed by Debon & Le Fort, 1988 and Debon & LeFort, 1983 are very useful for evaluating the tr ends of the differe n t suites. Thes e are also include d on Table 4.1.3.4 . A few samples that are signifi c a n t l y differe n t were plac ed on their own suites (6 to 8). These do not fall on any of the other trends. Suite 1 produced well-defined trends of differentiation. L-314 from Kalen gw a seems to follow the same pattern and was grouped with that suite. Table 4.1.3.3 Suites of samples from Kalengwa/Kasempa and pr ojection on various geochemical diagrams Suite Lithology AB MgB KB QB QP TAS R1-R2 Samples 1 F o i d gabbr o i d s or esse xi t e s Trend Trend Tr e n d Cluster Cl u s t e r Cluster X-80, X-81, X-82 , X-83, X-84, X-85, L-31 4 2 Granite Cluster Trend Trend Trend spread Cluster L-139, L -322, L -3 23, L-325 3 Q u a r t z s yenite Cluster Cluster Tr e n d Tr end Cluste r Cl u s t e r P-13, P-17, X-77 and L-324 4 Gabb roid Trend Trend Cluster Trend Trend Cluster L-313, X- 79 5 N o n - f o i d gab broi d s Trend Long trend Cluste r Trend Cluster Cl u s t e r X-86, X-87 6 G a b b r o i d Trend Se p a r a t e Tr e n d Distan t C l u s t e r Di s t a n t X-79, X-88, X-89 6 Lamproph yr e Na Na Na Na Na na Na L-318 7 A l t e r e d grano di o r i t e Na Na Na Na Na Na Na L-321 8 Q u a r t z s yenite Na Na Na Na Na Na Na P-26 9 Q u a r t z mo nzo n i t e - s ye n i t e near near near near near Near X-76, X-78 Table 4.1.3.4 Rock name, basic geoche mistry and environment of emplacement for samples from the Kalengwa and Kasempa region, Zambia (See acronym descript i on on section 2.4.3.) Sample Rock Name Debon & LeFort Maniar & Piccoli Whalen Pearce Mafic Rb/10H fTa Rb/30HfTa Nb-Ta L-139 Granite peraiii leucoKMg A L-313 Monzodiorit e metaiv mesoNaFe L-314 Syeno gabbro metaiv mesoNaFe L-318 Theralite metav mesoNaMg L-321 Granodiorit e (altere d) peraii mesoNaFe OP A V1/2 L-322 Alkali granite peraii mesoKFe RRG A O-W 1-1 L-323 Alkali granite peraii mesoKFe RRG A O-W 1-1 L-324 quartz syenite metaiv mesoKFe RRG-CEUG A W L-325 Granite peraii mesoKFe RRG A W P-13 quartz syenite metav mesoNaFe VA- WP INW P-17 quartz syenite metaiv mesoNaKF e VA- WP INW P-25 Essexit e metai v mesoNaFe IAG+CAG Wpab V A - III-W P INV P-26 quartz syenite metavi leucoNaFe OF WP OUTD X -76 quartz syenite peraiii mesoKFe RRG O-W 1-1 W pab X-77 Quartzmonz onite metaiv mesoNaFe RRG O-W 1-1 W pab X-78 Syenite peraiii mesoNaKFe A Wpab X-79 gabbro-diorit e metaiv mesoNaFe A V1/2 Wpab X-80 nepheline syenite metaiv mesoNaFe RRG A W Wpab X-81 Esse xit e meta i v meso NaFe RRG A W Wpab X-82 nepheline syenite metav mesoNaFe RRG A V1/2 Wpab X-83 syeno diorite metaiv mesoNaFe RRG N Wpab X-84 essexit e Meta v meso NaFe A V1/2 Wpab X-85 syeno gabbro metaiv mesoNaFe N V1/2 Wpab X-86 syeno diorite metaiv mesoNaFe RRG N V1/2 Wpab X-87 syeno gabbro metaiv mesoNaFe N V1/2 Wpab X-88 essexite metaiv mesoKFe N Wpab X-89 essexit e meta i v meso NaFe N W Wpab 4.1.3.4 Analysis of Independent Samples by Elements L-321 seems to have been subjec t to Na 2 O, Al 2 O 3 and K 2 O depletion, and MgO, Co, Ni, V and Fe 2 O 3 enric hme n t by hydrother ma l alterati on . L-322 to L-325 come from a similar region and they all show eviden c e 8 0 o f potass i c altera t i o n . Conver s e l y , potassiu m is very low in L-313 , L-314 , L-318 , L-321 and P-26 . Note the signific a n t enrichm e n t in copper show n by some rocks of this suite ( L-313 , L-324 , L-325 , P-17 a nd P-25) . Cobalt is high in L- 321 and in P-13 , P-17 , P-25 and P-26 . Vanadium is high in L-311 , L-313 , L-314 , L-318 , L- 321 , L-325 , and P-17 . P-26 , an altered quartz syenite is extreme l y enric hed in Na, contain s high Th and is enriche d in multipl e metals: Y, Zr, Nb, Co. Before being altered and mineralized , the rock might have been like P-13 or P-17 (See original description by Pepper, 2000 in Appendix A61). P-26 is also enriched in Hf and in the heavy rare earths Dy, Ho, Er, Tm, Yb and Lu. Samples P-13 and P-17 are enriched in Nd and Pr. The suites of quartz syenite s and granit e s all are high-hea t producers. Although L-139 is not very enric hed in Th, maybe other gr anitoids from the MB-34 borehole might be; the rest of the elements for that sample have an incipi e n t Th-ass o c ia t e d signat u r e . P-25 , L-311 , L-313 , L-314 and L-318 are enriched in Sc. Potash is highly enriched in L-322 , L-323 , L-324 and L-325 . This is evident in Table 4.1.3.1. L-325 is very enric hed in Ce and La and probably also in the other LREE. L-324 , P-13 and P-17 are very similar in many ways. X-86 and X-87 is simila r to L-318 in the TAS diagram; that is not true in the R1/R 2 diagram . The last sample probaby has been hydrothe rmally altered. X-76 seems to be similar to L-324 ; that is true in both R1/R2 and in the TAS diagrams (Figs 4.1.3.2 and 4.1.3.3) . X-76 , X-77 , X-78 , L-324 , P-13 and P-17 seem to have very similar chemis try on the R1R2 diagram, but they sepa rate into two discrete clus ters on the TAS diagram. X- 76 , and X-78 behave indepen d en t l y from the rest, especia l l y on the Debon & Le Fort diagra ms (Figs 4.1.3.4 to 4.1.3.7). 4.1.3.5 Analysis by Source Area L-321 , L-322 , L-323 and L-324 c o m e from the ?meta-ga b br o? , or ?albite- c h lorite rock? that is as sociated to the Kalengwa deposit (See Fig 8.43). Their chemis try is very different: L-321 is a peralum i n o us mesocra t i c sodic ferriferous altered granodiorite; L-322 and L-323 ar e peralu mino u s mes ocr atic potas s ic ferr ifer o us alkali granites ; and L-324 is a metalum i n ou s mesocr a t i c potass i c ferri ferous quartz syenite. The four samples seem to have been part of the same body of rock; their varying chemis try is probably due to differential hydroth er m a l alterat i on and/or origina l chemic a l dispar ity. The rocks formed in a rift-rela ted environmen t, as show n on Table 4.1.3.4. L-322 and L-323 are probaby the leas t altered rocks from which L-321 , L-324 and L-325 could have been hydroth er m a l ly altered . The origina l rock may have had a comple tely differen t composit i on altogeth er . X-80 , X-81 , X-82 , X-83 , X-84 an d X-88 are all similar and form a cluster of foid gabbros or essexites. P-25 is similar to this group. X-79 , X-85 , X-86 an d X-87 are non-fo id gabbro i ds . X-76 , X-77 and X-78 ar e syenit o id s . Thus, the suite of samples from boreho l e s in the Kasemp a area has at leas t three contras t i n g chemis tr i e s . See Table 4.1.3.3. Note that the KB and MgB diagrams (Figs 4.1.3. 6 and 4.1.3. 7 ) group all these rocks in a particular trend. Rock sampl es L-318 , L-319 , L-320 and P-13 go together in the Kalengwa Ndenda granitoid area. This proves that the Ndenda region has at leas t those two types of contras t i ng rocks. Thes e are metalum in o us mesocra t ic sodic ferrif e r ou s quartz syenit e ( P-13 ) and metalu m i nou s mesocr a t i c sodic magnes ic theral i t e ( L-318 ) Samples P-14 , P-16 , P-17 and L-313 come from the same region. They also have contrasting chemis try. L- 313 is a monzodiorite, while P-17 is a metalu m ino u s mesocr ati c sodic- p o t as s ic ferrif er ou s quartz syenit e . Samples X-87 and X-86 are simila r to X-88 in the R1/R2 and TAS diagrams. They are syeno-diorite and syeno-gab br o, and probably contain high Th values. L-324 , P-13 , P-17 and P-26 are all high heat producing granito id s . Mafic and ultram a f i c litholog i e s were observ ed in boreholes CHIT-8, K-1 and RK N 719 and RKN 801. Studies of those borehol es will not be include d in this documen t . 4.1.3.6 Kalengwa 4.1.3.6.1 Samples C h e m is t r y of intrusiv e rocks collecte d around the Kalengwa deposit is very important for exploration and to gain insight on its possibl e environm ent of formation. A total of thirt een sample s from the Kalengwa area were 8 1 o b t a i n ed from various source s . Sample s L-312 to L-326 were collected in the field by Mr. Jon Woodhead, exploration geolog ist at the Kitwe office of A ngloAmerican Corpor ation (Woodhead, J., personal commun ic a t io n , 2002). Samples P-13 , P-17 , P-25 an d P-26 were colle c t ed and proc es s ed by (Pepp e r , 2000) . An abstract of Pepper?s descriptions and observati o ns on the samples is include d in Appendix A61. 4.1.3.6.2 Geochronology There is no publis h e d radiom e t r ic age on rocks from the Kalengw a area. The age of intrus i v e rocks has to be younger than the silici c la s tic and carbon a t e sequenc e s t hat host them. The age of the sedime n t a r y rocks is not know n either , and only loose lithos t r a t i g r a ph i c co rrelations have been attemp ted (Berbelea c et al., 1979; Evans, 2004 (estima t e d ) ; Jannek e r , 2002 and William s , 1997). If the hypothesis of common origin for the Kasempa and Kalengwa intrusiv e rocks is true, then the anoroge n i c complexe s that formed at Kalengw a around 750 Ma. 4.1.3.6.3 Environment of Emplacement A l l the granito i d s from the Kalengw a area formed in anorogenic environments, and possibly as rift-related granit o id s as shown on Table 4.1.3. 4 . All of the ga bbro id rocks formed as within - p l a t e alkali basalts . This inform a t i on , added to the numero us large ring struct u r e s from the map produce d by (Nisbet et al., 2000) makes a strong case in favor of midalk a l i n e anorogen i c ring complexes that intruded Katangan sediments are the most probable environment of emplacement. 4.1.3.7 KASEMPA AREA A total of fifteen samples from the Kas empa area were studied for this projec t. All came from boreho les. One came from borehole MB-34 and fourteen from various boreholes drilled by Billiton in the Kasempa area. 4.1.3.7.1 Borehole MB-34 The MB-34 boreho l e was located in the Chitampa area of Kasempa, as indicated on Fig M9. It was drilled to a depth of 1484 feet 2 in the middle of one of the largest magnetic anomal i es of the region , and was comple te d on June 19, 1958. The hole was logged at 1:500 scale at the Kalulushi coreshed. Fifty-four samples for studies of mineraliz ation, hydrothermal alteration and brecciation were collected. The boreho l e has iron oxide - c o pp er - gold miner a l iz a tio n , polymict ic , multi-st a g e, round-pe b b le hydrothe r ma l breccias and variou s types of hydrothermal alterati on including red-rock alte ration, massive magnetite and ?hematite-disease? alteration. Parts of this is disc ussed and illustrated on the c hapter about iron oxide-copper- g o l d minera l iz a t i o n . Results of the resear c h on round- p ebble hydrothermal br eccias, hydr othermal alteration and mineral iz a t i o n will not be include d here. Relativ e l y unalter e d granito i d s were sought for chemica l analysis , and only L-139 was analy s e d from a depth of 1305.3 feet. It is one of severa l subvolc an i c porph yr i t i c , peralum i n o us leucocr a t i c potassi c magnesic granit es respon s ib l e for minera l iz a t i on at the Chitam pa site. Sample L-142 was dated; it comes from the same suite of subvol c an i c porphy r i t i c intrus ive s as L-139 . Zircons from six of the mineralizing granitoids were separ a ted . 4.1.3.7.2 Mufwashi and Chitampa Boreholes Six boreholes were drilled at the Chitampa and Mufw ashi areas of Kasempa by Billiton (Fig M9). The boreho l es were sunk to test iron oxide- c o pp er - gold minera l iz at i o n hosted by Katang an carbon a t es and silicic lastics, and to help define local stratigraphy. A signi ficant part of the boreholes intersected previous ly unidentified diamictites. They were sampled during an un-finis he d M.Sc. project at the University of the Witwa t ers r and (Jann ek er , 2002 and Jannek er , D., per son a l commun ic a t i o n , 2003). Fourte e n samples of intrusi v e rocks were analyse d from borehol es CH5, MUF1, MUF2, MUF3, MUF3 and MUF4. They were added to the geochemical datab as e of this project (A5) . Coor dinates of the boreholes are listed in Appendix A16. Samples X-76 to X-89 come from vario u s mafic and syeni t i c dikes that are intimately associated with the mineralization (Janneker, D., persona l communic a t io n , 2003). 2 The original borehole was measur ed and recovered in feet. 1484 feet are approximately equal to 453 meters . 8 2 Table 4.1.3.5 Chemical Analisis, Kasempa Area, Zambia (complete elemental analysis on Table A5, Appendix) Sam ple Origin al # SiO 2 T iO 2 Al2O 3 Fe2O 3 MnO MgO CaO Na2O K2O P2O 5 LO I T otal Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba X-76 CH5/0 1 55.3 5 1.48 14.6 3 10.8 6 0.10 4.43 2.43 0.91 7.34 0.50 1.65 99.6 9 209 199 56 591 28.0 13 11 295 50 139 <9 1379 X - 77 CH5/0 5 61.5 0 1.10 15.1 5 7.30 0.11 1.58 2.81 4.39 5.07 0.34 1.21 100. 59 182 313 48 339 34.0 15 <9 7 47 92 11 1189 X - 78 MUF 1/1 5 51.8 1 3.13 15.0 6 11.4 6 0.06 7.53 1.00 3.02 4.48 0.33 2.67 100. 54 137 109 32 290 46.0 25 102 20 100 415 117 118 X - 79 MUF 2/0 4 48.3 1 4.07 11.3 8 9.92 0.21 9.92 5.90 2.58 1.14 0.57 6.34 100. 34 18 234 32 358 44.0 47 70 35 146 458 74 75 X - 80 MUF 3/0 2 45.0 3 3.27 13.5 3 16.2 9 0.09 6.04 5.05 5.14 3.32 0.53 2.13 100. 41 97 112 48 325 55.0 24 81 12 23 327 142 141 X - 81 MUF 3/0 3 46.3 7 3.96 13.4 6 15.2 7 0.05 6.20 4.88 4.91 2.96 0.54 1.92 100. 52 103 94 55 302 48.0 17 88 7 22 324 135 148 X - 82 MUF 3/0 9 48.6 0 1.56 13.7 1 18.4 7 0.08 2.02 5.07 7.38 1.05 0.81 1.52 100. 26 32 122 61 567 84.0 <9 10 777 47 58 <9 233 X - 83 MUF 3/1 1 46.0 7 2.56 14.2 0 17.6 0 0.15 5.97 5.84 3.60 3.20 0.32 0.85 100. 37 88 105 27 177 32.0 17 44 102 44 325 79 384 X - 84 MUF 3/1 3 46.0 7 3.95 12.3 0 12.6 7 0.06 3.44 8.56 5.49 0.87 0.91 6.14 100. 47 27 106 59 444 89.0 11 11 26 59 138 <9 152 X - 85 MUF 4/0 1 47.3 5 2.56 14.0 8 13.2 5 0.14 7.29 8.22 4.21 0.61 0.32 2.54 100. 58 21 287 26 173 37.0 36 69 11 182 318 36 127 X - 86 MUF 4/0 2 45.8 8 3.96 12.7 2 16.7 5 0.25 5.61 7.19 3.78 1.46 0.31 2.23 100. 14 37 319 33 201 40.0 14 36 124 167 522 <9 303 X - 87 MUF 4/0 3 46.0 9 2.86 13.8 0 14.3 3 0.23 6.98 7.07 4.90 0.32 0.41 3.05 100. 06 13 344 31 208 42.0 18 50 9 134 315 23 119 X - 88 MUF 4/0 9 45.2 4 2.00 14.3 7 11.5 5 0.11 10.9 7 4.11 2.72 5.24 0.20 3.85 100. 37 147 69 25 131 21.0 35 201 <2 168 326 515 112 X - 89 MUF 4/1 7 46.2 0 3.57 8.68 14.3 6 0.18 11.4 2 6.07 4.30 2.70 0.67 1.85 100. 01 56 337 36 223 53.0 37 30 7 228 474 9 155 L- 139 75.6 0 0.09 11.8 8 1.50 0.03 0.62 0.14 1.61 7.87 0.01 0.79 100. 14 399 17 40 75 41.0 10 7 55 34 23 14 47 769 4.1.3.7.3 Geochronology A zircon conc entrate of L-142 , from borehole MB-34 (1373.5 feet) was dated by U-Pb SHRIMP II at approximately 750 Ma 3 . That is at least one of the ages of empl ace m e n t for ring comple x e s in the Kalengw a - K a s e mp a area, and does not overrul e the presenc e of younger intrusives . Geoc hronology of the Kalengwa- Kasempa area is still in its early stages. L-139 comes from the same borehol e as L-142 (MB-34 ) , and is the same type of subvolc a n ic porph y r i t i c , peralum i n o us leucoc r a t i c potass ic magnes i c granit e (Fig 4.1.3. 8 ) . The normal analys is for environ ment of emplacem ent did not produce any valid results for L-139 . Most probably, the granites were emplaced in an anorogen ic rift-rela ted or continental epeirogenic uplift environment. Fig 4.1.3.8 Photos of red-altere d, subvolcanic porphyritic granitoids that were dated; borehole MB-34, Chitampa, Kasempa area, Zambia . A and B come from sample L-12 9 , and C and D from L-127 . M ore details in the text. Gray material is the s ilicate-sulfide matrix to hy drothermal breccias and stockworks. Mm for scale. 3 750 Ma is a preliminary age. Comple te results have not been produce d by the ANU. 8 3 4.1.4 NORTHWESTERN ZAMBIA DOMAIN 4.1.4.1 Introduction This portio n of northw es te r n Zambia compris es the environ s of Mwinil un g a and Kalene Hill as well as the Domes Area and show n on Figs M1, M10 and M12. It has a la rge areal extent and very little outcrop. It will be subdivided into four ar eas, as follows: Kalene Hill, Kabompo Dome, Momb wezhi Dome, and Solwezi 1 Dome, as illustr a t e d on Figs M1 and 4.1.4.7 . Samples collect ed from each of these areas are described from west to east in the following pages. A spec ial section about a sodalit e syenite quarry is include d with the Mwombe z h i Dome. G r a n i t o id s from northw es t er n Zambia are equall y spr ead between midalkal i n e and subalkal i ne rocks: 45% of all rocks collected come from midalkaline rocks, 36% from subalk aline rocks and 20% from alkaline rocks (Table 4.1.4.1 ) . This domain has the la rger proport i on of subalka l i n e rocks in the Greater Lufilia n Arc granito i d projec t. Table 4.1.4.1 Rock type statistics, from Northwestern Zambia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type Number % Granitoids Groups A l k a l i gran i t e 7 12.50 Q u a r t z m o n z o n i t e 8 14.29 S ye n i t e 2 3.57 M o n z o n i t e 1 1.79 50 . 0 0 Monzo d i o r i t e 1 1.79 M o n z o g a b b r o 1 1.79 Midalkaline Rocks A l k a l i gabbr o 5 8.93 44.64 Granite 10 17.86 G r a n o d i o r i t e 8 14.29 5 0 . 0 0 Diorit e 1 1.79 Subalkaline Rocks Gabb ro 1 1.79 35.71 Foid s yenit e 8 14.29 F o i d gabbr o 2 3.57 Alkaline Rocks Fo i d o l i t e 1 1.79 19.64 Total 56 100.00 1 0 0 . 0 0 100.00 If samples from the sodalite syenite quarry are not cons id er e d , rocks analyse d are still spread out almost equally between midalkal i ne and subalkal i n e rocks. Nevethel es s , a 6.5% of rocks is still alkalin e , as show n on Table 4.1.4.2. A large portion of the samples come from the Kalene Hill area, whic h contain s a signif i c an t number of subalk a l i n e or calc -a lk a l in e rocks. This sh ows that the domain is a mix of several magmatic environments that were active through time. Table 4.1.4.2 Partial rock type statistics, from Northwestern Zambia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type number % Granitoids Groups A l k a l i gran i t e 7 15.22 Q u a r t z m o n z o n i t e 8 17.39 S ye n i t e 1 2.17 M o n z o n i t e 1 2.17 48 . 5 7 Monzo d i o r i t e 1 2.17 M o n z o g a b b r o 1 2.17 Midalkaline Rocks A l k a l i gabbr o 5 10.8 7 52.17 Granite 10 21.74 G r a n o d i o r i t e 8 17.39 5 1 . 4 3 Subalkaline Rocks Gabb ro 1 2.17 41.30 Foid gabbr o 2 4.35Alkaline Rocks Fo i d o l i t e 1 2.17 6.52 Total 46 100.00 1 0 0 . 0 0 100.00 1 Solwez i is a Zambian term with seve ral spellings in use. This document uses Solwez i instead of ?Solwesi?. 8 4 4.1.4.2 Kalene Hill Area, Zambia This northw es t e r n portio n of Zambia border s with the Democratic Republic of Congo to the north and Angola to the west, as indicated on Fig M1. There is very littl e outcrop in the region. Some of the bes t outcrop s were roadcu ts and founda t i on s for bridges over perenn i a l cree ks. The rocks from this part of the Lufilian Arc are mainly granite s, granodior ites, quar tzmonzonites, al kali granites, gabbro and syenite (Figs 4.1.4.2 and 4.1.4.1). Thir ty-one samples make the database of Kal ene Hill, as show n on Table 4.1.4.3. Six samples from the field w ork were analy s ed . 24 rock sampl e s were collect ed during mapping of 1:100,0 0 0 scale geolog i c a l sheets 1124N W , 1023SE and 1024SW (Key & Banda, 2000). Thes e were kindly supplie d by the Zambia n Geolog ical Survey in Lusaka (See Map of Fig M11). Th e origin a l report include s UTM coor di na t e s of all sample s. Renumber ing of samples from Key & Banda, 2000 is listed on Table 4.4.4.5. Detailed field descrip t i o ns of outcrop s and spec imens collected are included in Appendix A62. 4.1.4.2.1 Geochemistry Granitoid s from the Kalene Hill area are equally sp read between the midalkal i ne and subalkal i n e fields. Midalka l i n e and subalka l i ne rocks are evenly spread too, as shown on Table 4.1.4.4. In addition to that, midalkal i n e and subalkal i ne rocks are each brok en into two dominant rock groups. Table 4.1.4.4 Rock type statistics, from Kalene Hill samples, NW Zambia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type number % Granitoids Groups A l k a l i gran i t e 6 20.00 Q u a r t z m o n z o n i t e 7 23.50 S ye n i t e 1 3.33 50 . 0 0 Midalkaline Rocks M o n z o d i o r i t e 1 3.33 50.00 granite 7 23.33 g r a n o d i o r i t e 7 23.33 5 0 . 0 0 Subalkaline Rocks gabbro 1 3.33 50.00 Total 3 0 1 0 0 . 0 0 1 0 0 . 0 0 100.00 Table 4.4.4. 5 groups the various sample s into three map types (fifth column ) , based on the maps and report of Key & Banda, 2000 and Key et al., 2000 Archean rocks were marked with letter A, and Paleoproterozoic rocks were marked with B. Samples that corres po n d with uncer tai n map units have a question mark. 4.1.4.2.2 Description of the Various Groups As seen on Table 4.4.4. 5, rocks from Kalene Hill can be divided at least into four groups , listed below in tentative chronolog ical order. The first group is a suite of Archean rocks made of pink , iron-rich mainly metalum i no us granites and alkalin e granite s (map type A) that was intrude d by mafic dikes and syenite s . It corres po n ds with map unit A and covers a particular area in the NW part of the geolog ic a l map (Fig M11). All rocks in the suite are enriched in Cu and Pr. There is a good correlation of the various oxides agains t silica. Group 2 is a suite of Paleoproterozoic leucocratic to meso cra t i c , sodic to potassic , pink to red granites , alkalin e granite s and granite s that correspo n d to map unit B and were probabl y formed in an anoroge n i c contine n t a l epeirog e n ic uplift environ m en t . More precise definition of the environ ment will not be made here. These are associated with minor mafic intrusio ns. Group 2 samples are enric hed in Pr and K and have low Ca conten t . This group of rocks seems to have emplaced itself at approxim ately 1928 Ma, as indicated by the SHRIMP age of L-030* discus s ed below under the secti o n for the Kabompo Dome. This group plots as a linear trend in the KB, MgB and QBF plots of Debon & LeFor t and as a clus ter on R1R2 and TAS diagrams as illustrated on Figs 4.1.4.1 to 4.1. 4.6 and shown on Table 4.4.4.6 . Unal ter e d member s of the group are all subleucocratic to leucocratic. There is a slight corr ela ti o n when the various oxides are plotted agains t silica. Additional samples from the NW Zambia region that fall into this group are L-030 * , L-060b , L-360 , L-420 an d L-421 . If L-030* a nd L-060 (samples from the Kabompo and Solw ez i Domes, respec ti v e l y ) are included in the group, they are somewhat differen t from the ?average ?. This is probably due to hydrothermal alteration. The group is far from homogene o us (See Fig 4.1.4.5 ) . De tailed geochemis try of samples from Group 2 varies significantly, especially in terms of minor elements. A fe w samples seem to deviat e from the ?avera ge ? cluste r , due to moderat e or strong hydroth er m a l alterat i o n . These includ e L-377 , L-368 , L-366 , and to a minor extent, L-375 , L-360 and L-380 . L-366 is enriched in Fe, Ti, P 2 O 5 Zn, Zr, Ce, La, Eu, Gd, Nd, Pr, Yb and Lu. L-368 is 8 5 enric hed in Mg, Ba, Zr, Ce, La, Mg, Ti and P 2 O 5 . A subgroup of group 2 may be made. It includes L-026 , L- 365 , L-366 , L-368 a n d L-378 . Thes e samples contain high Zn, Fe, Ce, La and Zr in comparis o n with the rest of the suite; in addition, part of these show lo w Ca and deviate from the ?average? composition. Table 4.1.4.3 Chemical Analysis of sampl es from the Kalene Hill Area, NW Zambia ( C omp l e t e elementa l analysis on Table A7, Appendix ) Sample SiO2 TiO2 Al2O3 FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total N o t c h 50.00 1.00 15.50 6 . 0 0 0 . 1 5 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2 . 0 0 Archean rocks L-372 54.14 0.84 17.15 9 . 3 3 0 . 1 2 3 . 2 4 7 . 0 0 4 . 3 1 2 . 2 5 0 . 2 8 1 . 8 5 100.51 L-373 72.41 0.25 14.10 2. 22 0 . 0 3 0 . 4 1 1 . 3 6 3 . 4 9 4 . 2 0 0 . 0 5 0 . 9 3 99.45 L-375 69.92 0.45 12.64 4. 64 0 . 0 7 0 . 3 3 1 . 0 4 3 . 2 7 5 . 8 1 0 . 1 3 0 . 7 7 99.07 L-376 59.71 0.51 17.93 5 . 5 4 0 . 0 9 1 . 1 0 2 . 0 5 6 . 0 7 4 . 9 4 0 . 1 2 0 . 8 3 98.89 Paleoproterozoic rocks L-027 67.24 0.53 15.50 4 . 7 4 0 . 0 9 1 . 3 8 4 . 3 1 3 . 7 5 1 . 7 2 0 . 1 9 1 . 0 2 100.47 L-023 67.01 0.56 14.95 5. 02 0 . 0 7 1 . 8 3 2 . 7 4 3 . 7 1 3 . 6 0 0 . 1 9 0 . 8 0 100.48 L-025 70.60 0.40 13.80 3. 70 0 . 0 5 0 . 7 3 1 . 8 2 3 . 1 9 4 . 8 0 0 . 0 8 0 . 9 6 100.13 L-026 71.92 0.37 13.46 3. 29 0 . 0 4 0 . 6 7 1 . 9 8 3 . 2 3 4 . 5 1 0 . 0 8 0 . 8 2 100.37 L-362 64.93 0.66 14.31 9 . 3 3 0 . 0 7 1 . 3 9 3 . 7 9 3 . 7 2 2 . 1 5 0 . 1 7 1 . 6 6 98.65 L-363 65.30 0.64 15.16 2 . 2 2 0 . 0 9 1 . 2 3 3 . 1 1 3 . 9 5 3 . 3 7 0 . 1 6 1 . 4 9 99.80 L-369 71.39 0.21 13.38 4. 64 0 . 0 3 0 . 4 9 1 . 8 0 4 . 1 0 3 . 8 3 0 . 0 4 1 . 7 4 98.90 L-370 74.09 0.20 12.02 5 . 5 4 0 . 0 3 0 . 2 6 0 . 9 5 4 . 3 2 4 . 0 7 0 . 0 4 0 . 8 8 99.44 L-377 69.88 0.26 12.62 3 . 0 7 0 . 0 4 0 . 2 8 1 . 2 7 5 . 0 6 5 . 4 5 0 . 0 5 1 . 0 1 98.99 L-364 74.42 0.19 11.94 2. 26 0 . 0 2 0 . 4 0 0 . 2 6 3 . 5 4 5 . 0 7 0 . 0 4 0 . 6 8 98.82 L-365 72.12 0.48 12.08 4. 21 0 . 0 4 1 . 2 5 0 . 4 5 2 . 6 4 4 . 8 7 0 . 1 2 1 . 3 3 99.59 L-378 73.20 0.22 12.15 3. 08 0 . 0 4 0 . 2 3 0 . 8 4 3 . 9 5 4 . 1 8 0 . 0 5 0 . 8 4 98.78 L-020 74.44 0.22 12.70 2. 48 0 . 0 5 0 . 2 8 0 . 5 8 3 . 0 3 5 . 8 5 0 . 0 2 0 . 7 5 100.40 L-379 72.89 0.21 12.77 2 . 5 4 0 . 0 3 0 . 4 5 0 . 7 2 6 . 1 2 2 . 9 2 0 . 0 7 0 . 6 2 99.34 Other L-367 72.13 0.48 11.76 4. 45 0 . 0 6 1 . 3 0 3 . 1 7 1 . 6 9 2 . 4 1 0 . 1 3 1 . 7 0 99.28 L-023 67.01 0.56 14.95 5. 02 0 . 0 7 1 . 8 3 2 . 7 4 3 . 7 1 3 . 6 0 0 . 1 9 0 . 8 0 100.48 L-024 48.01 2.10 12.37 1 8 . 9 1 0 . 2 8 4 . 9 3 8 . 7 4 1 . 7 0 0 . 4 3 0 . 1 7 1 . 1 6 98.80 L-357 61.26 0.49 17.43 5 . 3 3 0 . 0 7 1 . 0 8 2 . 8 5 4 . 9 2 3 . 5 9 0 . 2 2 1 . 7 7 99.01 L-358 63.11 0.65 15.74 6 . 2 9 0 . 0 7 1 . 0 4 3 . 8 0 4 . 0 3 2 . 3 1 0 . 1 7 1 . 5 1 98.72 L-359 66.92 0.41 14.63 4. 21 0 . 0 6 0 . 7 9 2 . 3 1 3 . 9 1 4 . 8 4 0 . 1 2 1 . 0 7 99.27 L-360 68.89 0.31 14.44 3. 71 0 . 0 4 0 . 6 0 1 . 2 3 3 . 1 8 6 . 0 2 0 . 0 7 0 . 9 1 99.40 L-361 63.38 0.74 15.35 6 . 0 8 0 . 0 6 1 . 5 7 3 . 8 0 4 . 3 8 2 . 0 6 0 . 2 2 1 . 4 9 99.13 L-366 67.02 0.66 13.23 5 . 7 9 0 . 0 9 0 . 9 0 1 . 7 6 4 . 0 5 4 . 2 8 0 . 1 8 0 . 9 2 98.88 L-368 67.04 0.71 14.00 4. 96 0 . 0 5 1 . 3 2 0 . 9 8 3 . 4 1 4 . 6 4 0 . 1 7 1 . 3 9 98.67 L-371 70.77 0.25 14.56 1. 78 0 . 0 3 0 . 4 0 1 . 3 7 4 . 8 5 4 . 0 6 0 . 0 8 1 . 0 4 99.19 L-374 70.46 0.20 14.58 2 . 2 8 0 . 0 4 0 . 3 1 1 . 7 5 5 . 0 2 3 . 9 2 0 . 0 5 0 . 7 7 99.38 L-380 70.37 0.39 13.41 3. 59 0 . 0 5 0 . 2 7 0 . 9 2 3 . 6 5 5 . 9 4 0 . 0 9 0 . 6 9 99.37 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Sm Nd Pr Ce La Hf Ta Eu Gd Yb Lu Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 50 50 15 175 95 10 120 4.0 30 7.5 1.6 Archean rocks L-372 86 764 11 193 8 20 9 57 116 21 23 18 423 <6 <15 24 135 71 L-373 114 353 31 147 8 6 7 17 28 14 198 12 1215 <6 17 <10 105 15 35 90 10 3 21 0.2 0.6 L-375 140 197 47 365 30 7 11 26 55 18 22 19 1228 <6 21 <10 296 145 L-376 74 419 29 280 27 11 <6 18 58 20 67 <12 1036 <6 <15 <10 174 95 Paleoproterozoic rocks L-027 49 619 21 123 13 7 <6 <6 49 18 68 161 573 <6 <15 12 107 58 L-023 78 376 24 133 13 10 6 <6 44 16 80 219 1283 <6 <15 12 7 50 77 127 44 61 0.7 1.3 1.1 L-025 91 370 11 108 10 6 8 9 71 17 38 42 1390 <6 <15 <10 4 32 47 85 20 25 0.8 0.6 0.8 L-026 85 384 12 392 14 6 7 8 55 16 38 42 1367 <6 <15 <10 97 41 L-362 77 452 35 221 9 9 8 17 93 19 79 22 1523 <6 <15 10 113 61 L-363 119 398 31 202 9 11 6 18 69 20 73 20 1054 <6 <15 <10 82 40 L-369 78 254 51 135 25 <6 6 119 118 16 53 20 789 <6 <15 <10 114 19 57 86 27 23 0.6 1.4 0.7 L-370 279 61 7 195 6 <6 10 10 32 21 16 <12 264 9 52 <10 145 73 L-377 255 69 91 174 17 <6 9 167 109 19 12 19 365 8 45 <10 135 71 L-364 236 34 42 207 10 <6 9 9 23 20 59 23 198 8 44 <10 179 88 L-365 146 81 75 353 24 8 7 24 38 19 <12 15 881 <6 26 <10 212 114 L-378 216 69 79 255 19 <6 10 163 98 19 <12 15 371 6 33 <10 267 135 L-020 226 91 53 228 19 <6 <6 9 64 18 <12 47 553 10 62 <10 11 88 145 286 75 73 3.3 2.7 1.3 L-379 139 54 59 84 27 <6 14 17 15 25 <12 20 133 10 <15 <10 39 18 Other L-367 59 232 237 162 22 10 <6 7 61 15 29 14 1518 <6 <15 <10 80 42 L-023 78 376 24 133 13 10 6 <6 44 16 80 219 1283 <6 <15 12 7 50 77 127 44 61 0.7 1.3 1.1 L-024 16 78 51 140 11 57 66 236 149 22 470 79 108 6 <15 43 14 39 39 25 19 391 2.3 2. 1 L-357 69 568 67 298 29 10 9 36 70 21 <12 12 1645 <6 <15 <10 111 55 L-358 80 492 29 233 13 12 10 479 261 22 58 16 950 <6 <15 14 10 28 69 106 32 98 0.2 0.6 1.1 L-359 120 359 28 192 13 8 8 11 54 22 64 26 1134 <6 <15 10 149 76 L-360 100 369 67 134 15 7 6 9 46 16 40 20 2144 <6 <15 <10 114 57 L-361 118 544 17 246 8 12 15 20 78 21 36 <12 844 <6 <15 12 162 84 L-366 142 188 54 448 19 7 <6 13 86 20 21 12 1082 <6 <15 11 10 139 247 347 139 88 6.1 42 . 5 1 3 . 2 2 . 6 L-368 112 156 18 565 10 10 8 13 61 18 38 15 1652 <6 <15 <10 189 101 L-371 104 650 59 127 23 <6 10 10 38 18 <12 15 1474 <6 <15 <10 110 52 L-374 97 473 10 105 6 <6 <6 9 33 17 17 14 1054 <6 <15 <10 49 23 L-380 177 135 57 365 28 7 10 116 83 18 17 13 1129 <6 18 <10 15 66 188 241 95 1 44 1.5 2. 9 2 . 5 1. 1 5 4 0 4 5 5 0 5 5 6 0 6 5 7 0 7 5 8 SiO2% 2 3 4 5 6 7 8 9 1 0 1 1 1 2 1 3 1 4 1 5 1 6 1 7 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM NW Zambia, Zambia; Lufilian G.P. (Based on Middlemost, 1994, 1997) S a m p l es P e t ro gr ap hi c field s L-372 L-373 L-375 L-376 L-380 L-027 L-023 L-025 L-026 L-362 L-363 L-369 L-370 L-377 L-364 L-365 L-378 L-020 L-379 L-367 3 L-024 L-028 L-029 L-030 L-047 L-049 L-050 L-060a L-060b L-060c L-063 L-064 L-065 L-311 L-357 L-358 L-359 L-360 L-361 L-366 L-368 L-371L-374 L-420 L-421 6 36 36 4 36 3 6 6 3 6 8 3 6 9 3 7 3 7 3 7 7 3 7 8 3 7 9 3 7 3 6 3 3 7 3 8 3 9 3 6 3 6 3 6 7 4 8 9 3 4 7 4 9 6 6 6 4 4 6 3 6 4 6 L-032 L-034L-034A L-036 L-037 L-038 L-039 L-040 L-041 L-044 L-045 L-046 3 2 4 3 L-420 L-369 L-361 L-029 A rc h e a n sa m pl e ( Solwezi Dome Mwombezhi Dome Fig 4.1.4.1 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti) 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 R 2 = 6C a +2M g +A l L-372 L-373 L-375 L-376 L-027 L-023 L-025L-026 L-362 L-363 L-369 L-370 L-377 L-364 L-365L-378 L-020 L-379 L-367 3 L-024 L-028 L-029 L-030 L-047 L-049 L-050 L-060a L-060b L-060c L-063 L-064 L-065 L-311 L-357 L-358 L-359 L-360 L-361 L-366 L-368L-371 L-374 L-380 L-420 L-421 R1R2 PLUTONIC ROCK CLASSIFICATION NW Zambia; Lufilian Ar c Granitoid Project (After De la Roche et al, 1980) P e t r o g r a p h i c fie ld s S a m p l e s 4 3 2 Fig 4.1.4.2 0 0.2 0.4 0.6 K/(Na + K) 0 50 100 150 200 250 300 350 400 450 L - 3 7 2 L - 3 7 3 L - 3 7 4 L - 3 7 5 L - 0 2 0 L - 0 2 5 L - 0 2 6 L - 3 6 4 L - 3 6 5 L - 3 6 6 L - 3 6 8 L - 3 6 9 L - 3 7 0 L - 3 7 1 L - 3 7 7 L - 3 7 8 L - 3 7 9 L - 0 2 3 L - 0 2 7 L - 3 6 3 L - 3 5 7 L - 3 5 8 L - 3 5 9 L - 3 6 1 L - 3 6 2 L - 3 6 7 L - 0 2 4 L - 0 2 8 L - 0 2 9 L - 0 3 0 L - 0 4 7 L - 0 4 9 L - 0 5 0 L - 0 6 0 a L - 0 6 0 b L - 0 6 0 c L - 4 2 0 L - 4 2 1 L - 0 6 3 L - 0 6 4 L - 0 6 5 KB Diagram (After Debon & LeFor t , 1994) NW Zambia; Lufilian Arc Granitoid Project 4 3 2 2 Fig 4.1.4.3 - 1 0 0 - 5 0 0 5 0 1 0 0 1 5 0 2 0 0 2 5 0 Q=S i/3- (K +N a+2 C a/3) Q-P Plutonic Classification ( A f t e r De b o n & LeF o rt , 19 8 3 NW Zambia, Lufilian Arc Granitoid Project Petrographic Fields Reference rocks Sampl es - 4 0 0 - 3 5 0 - 3 0 0 - 2 5 0 - 2 0 0 - 1 5 0 - 1 0 0 - 5 0 0 5 0 1 0 P=K-(Na+Ca) L -3 7 2 L- 3 73 L -3 7 4 L- 3 75 L- 0 20 L- 0 25 L- 0 26 L -3 6 4 L -3 6 5 L -3 6 6 L -3 6 8 L - 36 9 L - 37 0 L -3 7 1 L- 3 77 L -3 7 8 L - 37 9 L -0 2 3 L -0 2 7 L -3 6 3 L - 35 7 L -3 5 8 L -3 5 9 L- 3 61 L -3 6 2 L - 36 7 L -0 2 4 L - 02 8 L- 0 29 L- 0 30 L- 0 47 L -0 4 9 L - 05 0 L- 0 60 a L -0 6 0 b L- 0 60 c L - 42 0 L -4 2 1 L- 0 63 L -0 6 4 L- 0 65 2 4 Fig 4.1.4.4 20 40 60 80 100 120 1 4 -75 -50 -25 0 25 50 L - 3 7 3 L - 3 7 4 L - 3 7 5 L - 0 2 0 L - 0 2 5 L - 0 2 6 L - 3 6 4 L - 3 6 5 L - 3 6 6 L - 3 6 8 L - 3 6 9 L - 3 7 0 L - 3 7 1 L - 3 7 7 L - 3 7 8 L - 3 7 9 L - 0 2 3 L - 0 2 7 L - 3 6 3 L - 3 5 7 L - 3 5 8 L - 3 5 9 L - 3 6 1L - 3 6 2 L - 3 6 7 L - 0 2 9 L - 0 3 0 L - 0 4 7 L - 0 6 0 b L - 4 2 0 L - 4 2 1 A-B Diagram ( A f te r Deb o n & LeF o r t, 199 4 ) NW Zambia; Greater Lufilian Arc Granitoid Project (Central portion. To view en tire diagram, see Fig 4.1.4.5a)) S a m p l e s Fig 4.1.4.5 0 50 100 150 200 250 300 350 400 450 -450 -425 -400 -375 -350 -325 -300 -275 -250 -225 -200 -175 -150 -125 -100 -75 -50 -25 0 25 50 75 L-372 L-373 L-37 4 L-375 L-020 L-025 L-026 L-364 L-365 L-366 L-368 L-36 9 L-370 L-371 L-377 L-37 8 L-379 L-023 L-027 L-363 L-357 L-358 L-359 L-361L-362 L-367 L-024 L-028 L-029 L-030 L-047 L-049 L-050 L-060a L-060b L-060c L-420 L-421 L-063 L-064 L-065 A-B Diagram ( A f t e r De b o n & LeF o r t , 19 9 4 ) NW Zambia; Greater Lufilian Arc Granitoid Project ( c o m p le t e fig u r e ) S a mp les Fig 4.1.4.5a 0 1 0 0 2 0 0 3 0 0 4 0 0 0 . 1 0 . 2 0 . 3 0 . 4 0 . 5 0 . 6 0 . 7 0 . 8 B K 16b B K 19a B K 1 a B K 1b B K 1c B K 24a B K 2 7a L- 372 L- 373 L-3 74 L- 375 L- 020 L- 025 L- 026 L-3 64 L- 365 L- 366 L- 368 L- 369 L- 370 L- 371 L -37 7 L- 378 L-3 79 L- 023 L- 027 L- 363 L- 357 L- 358 L- 359 L -36 1 L-3 62 L- 367 L- 024 L -02 8 L- 029 L-0 30 L- 047 L -04 9 L -05 0 L- 060 a L- 060b L-0 60c L- 420 L-4 21 L- 063 L -06 4 L- 065 2 4 3 Mg-Fe-B Diagram ( A f t e r Deb o n & LeFo r t , 199 4 ) NW Zambia; Lufilian Arc Granitoid Project Fig 4.1.4.6 9 3 Table 4.4.4.5 Samples from Kalene Hill sorted by groups and geochemistry (^ = sample with hydrothermal alteration. * = dated sample. High-heat produc ing rocks are underlined. # = high Cu and Zn content. $ high Cu only. Z = high zinc only. Original sample numbe rs, from Key & Banda, 2000. See acronym descrip t i o n on section 2.4.3.) Group 1 # Rock Type Debon & LeFort Orig # Map type M a n i a r & Pic Whalen Pearce L - 3 7 2 * # Monzo - g a b b r o Metal u m i n o u s iv me socr a t i c Na Fe 3DA100 A IAG+CA G A L-373* Grani t e Peral u m i n o u s ii subl eu c o c r a t i c Na Fe 3DA101 A POG N L-374 Grani t e Metal u m i n o u s v subleu c o c r a t i c Na high Fe 3DA103 ? N L-375$ Grani t e Metal u m i n o u s iv mesoc r a t i c K high Fe 3DA106 A CEUG A O-W1- 1 L-376 Syeni t e Metal u m i n o u s iv mesoc r a t i c Na Fe 3DA10 7 A CEUG A O-W1- 1 L-380 # Alkal i grani t e Metal u m i n o u s iv mesoc r a t i c K high Fe 3DA11 7 A CEUG-R R G A O3/4 Group 2 # Rock Type Debon & LeFort Orig # Map type M a n i a r & Pic Whalen Pearce L-020 Alkal i grani t e Peral u m i n o u s iii subl e u c o c r a t i c K high Fe B POG A O3/4 L-025 ^ Grani t e Peral u m i n o u s iii mesoc r a t i c Na-K Fe B N O3/4 L-026 ^ Granit e Metalu m i n o u s iv mesocr a t i c Na-K Fe B POG A L-360 Grani t e Peral u m i n o u s iii mesoc r a t i c K Fe 3DA04 5 ? CEUG A O-W1- 1 L-364 Alkal i grani t e Peral u m i n o u s iii suble u c o c r a t i c Na-K Fe 3DA06 0 B A L-365 ^ Grani t e Peral u m i n o u s iii mesoc r a t i c K Fe 3DA07 2 B A O-W1- 1 L-366 # Grani t e Metal u m i n o u s iv mesoc r a t i c Na Fe 3DA073 B CEUG-R R G A O-W 2-2 L- 3 6 8 ^ Grani t e Peral u m i n o u s iii mesoc r a t i c Na-K Fe 3DA08 3 ? RRG-CE U G A L-369# Granit e Peralu m i n o u s iv leuc o c r a t i c Na Mg 3DA09 3 B A ? L-370 Grani t e Peral u m i n o u s iv suble u c o c r a t i c Na Fe 3DA097 B CEUG A L-371 Grani t e Metal u m i n o u s iv leuco c r a t i c Na Mg 3DA098 ? POG A O-W1- 1 L-377# Quart z s yeni t e Metal u m i n o u s v suble u c o c r a t i c Na Fe 3DA109 B CEUG A O2/3 L-378 # Grani t e Metal u m i n o u s iv suble u c o c r a t i c Na Fe 3DA11 0 B CEUG- R R G A O-W1- 1 L-379 Alkal i grani t e Metal u m i n o u s v suble u c o c r a t i c Na Fe 3DA11 1 B A O-W1- 1 Group 3 # Rock Type Debon & LeFort Orig # Map type M a n i a r & Pic Whalen Pearce L - 0 2 3 Gran od i o r i t e Metalu m i n o u s iv mesocr a t i c Na Fe L-023 B N O3/4 L-027 Gran o d i o r i t e Metal u m i n o u s iv meso cr a t i c Na Fe L-027 B IAG+CA G N V L-363 Gran o d i o r i t e Metal u m i n o u s iv mesoc r a t i c Na Fe 3DA05 9 B N Group 4 # Rock Type Debon & LeFort Orig # Map type M a n i a r & Pic Whalen Pearce L - 3 5 7 Quart z mo nzo n i t e Peral u m i n o u s iii mesoc r a t i c Na Fe 3DA03 4 ? CEUG A W L-358 # Quart z mo nzo n i t e Metal u m i n o u s iv mesocr a t i c Na Fe 3DA035 ? A O3/4 L-359 Grani t e Metal u m i n o u s iv mesocr a t i c Na Fe 3DA036 ? CEUG A L-361 Quart z mo nzo n i t e Metal u m i n o u s iv mesoc r a t i c Na Fe 3DA05 6 ? A L-362# Gran o d i o r i t e Metal u m i n o u s iv mesoc r a t i c Na Fe 3DA05 8 B A L-367 Gran o d i o r i t e Peral u m i n o u s iii mesoc r a t i c Na-K Fe 3DA08 2 B A W Other Samples # Rock Type Debon & LeFort Orig # Map type M a n i a r & Pic Whalen Pearce L - 0 2 4 # Gabb r o - d i o r i t e Metal u m i n o u s iv meso cr a t i c Na high Fe L-024 B RRG A V2/4 Table 4.1.4.6 Kalene Hill groups of samples a nd their projection on various geochemical diagrams Group # samples AB MgB KB QB QP QBF TAS R1R2 1 6 Disp e r s e Disp e r s e D i s p e r s e D i s p e r s e D i s p e r s e Disp e r s e Disp e r s e 2 1 4 Cluster Trend Long curv y trend Dispe r s e L a r g e clus t e r Elong a t e d clus t e r Cluste r Cluste r 3 3 Trend Trend Trend Dispers e C u r v e Curved trend Curve Curve 4 6 Trend Curv y trend Trend Dispers e D i s p e r s e T r e n d Trend Curv y trend X 1 - - - - - - - - 9 4 Group 3 is a widespr e ad series of three Paleop r o t e r oz o ic , metalum i n o us , sodic, ferrifer o us , black and white granodiorites that could have formed in a magmatic arc environment and corresponds to map unit B. It is enric hed in Al, Pr, and Cr. There is a good correlation of the various oxides agains t silica . This group plots as a trend in the K B and MgB plots of De bon LeFort (Figs 4.1.4.5 and 4.1.4.6 ) . Group 4 is a series of six Paleoproterozoic , mesocratic, sodic, ferrife r o us , black and white granodi or i t e s and quartz m on z on i t e s that formed in an anoroge n ic contine n t al epeirogenic uplift environment and corres ponds to map unit B. It is enriched in Sr, Pr, Te, and has high lo ss on ignition. There is a good correlation of the various oxides agains t silica. This group plots as a linear trend in the Debon & LeFort K vs B and Mg vs B diagr ams (Figs 4.1.4. 5 and 4.1.4. 6) . Rock groups 3 and 4 occur in clos e associ a t i o n . L-359 seems to be hydrot h er m a l ly altered , as a variatio n from group 2 ro cks by the intrus ion of group 4 rocks ( L-358 ). 4.1.4.2.3 Analysis of Independent Samples by Elements All the sample s from the Kalene Hill area that were anal yzed for Pr are enriched in that element. There is no valid explanation for that fact yet. High heat produc in g granite s (due to high Th) are L-020 , L-364 , L-370 , and L-377 . Several samples from the Kalene Hill suite are enriched in copper . Three of them are Archean granitoi ds : L- 372 * , L-375 a n d L-380 . The last is highly enriched. This is very important; especially if the copper mineralization is hypogene. Ot her high Cu sampl es are: L-024 , L-357 , L-358 , L-369 , L-377 a n d L-378 . Only one of the high heat produci ng granito id s ( L-377 ) contai n s anomalo u s copper . Only two of the Cu-ric h rocks are gabbroi ds ( L-024 a n d L-372* ); seven are granitoids. Samples with high zinc include : L-024 , L-358 , L-362 , L-366 , L-369 , L-372* , L-377 a n d L-378 . Of thes e, only L-372* a n d L-024 are gabbroi ds ; the rest are granito id s . L-372* is the only Archean rock. Samples L-369 , L-372 * , L-377 , L-378 an d L-380 are all felsic intrusive rocks and contain abundant Cu and Zn (Table 4.1.4.3 ) . This might be signific an t for Cu and Zn mineralization in the region. Of the group of samples with high Cu and Zn, L-376 , L-377 an d L-379 a l s o contain high sodium. None of the samples studied contain anomalo us uranium or niobium . Cerium and lanthanu m are high in: L-364 , L-365 , L-366 , L-367 , L-375 , L-376 , L-378 a n d L-380 . Cobalt is enric hed only in L-024 . 4.1.4.2.4 Geochronology Zircon concen t r a t e s from two samples from the Kalene H ill area were dated by (Key et al., 2001) using U-Pb SHRIMP II methods. These are L-372* and L-373* (respectively 3DA100 and 3DA101 in Key?s original number i ng ) . L-372* is a metalumino us mesocrat ic sodic ferrifer ou s monz ogabb r o that intersec t s the foliated, peralu m i n ou s subleu c o c r a ti c sodic ferrife r o us granit e L-373* . The age of emplacemen t for L-373* is 2538?10 Ma. A metamorphic overpr i n t dated 714?66 Ma was identifi e d . L-372* produc ed an age of emplac e me nt of 2535?11 Ma. It had xenocry s t i c zircons with an age of 2543?5 Ma that correlate well with the age of emplac emen t for L-373* . Key et al., 2001 established that rocks from Group 1 were formed in the Archean (See Table A22.2 and event diagram A24 in the Appendix) . L-373* formed in a post-or og en i c environm e n t of emplacemen t. The environment of L-372* has not been identified. It could be a continental arc basalt, as indicated by the diagrams of Pearce & Cann, 1976. Rocks from Group 2 seem to have been emplac e d from 1913 to 1952 Ma, as indicated by the SHRIMP age of L-030* , a sample that correlates well with Group 2, and other simila r ages in the envir o ns . Geoc hr o n o log y of L-030* will be discussed under the section for the Kabompo Dome. A tentative order of intrus ion for the groups of rocks from the Kalene Hill may be establi s h e d : Group 1 was intruded by 2. 4 intruded 2. 3 probably also intrude d 2. 3 and 4 might be of simila r age and ther e is no evidence for relative age difference among them. 9 5 4.1.4.2.5 Environment of Emplacement As shown on Table 4.1.4.5, most of the Archean rocks formed in a contine n t a l epeirog e n ic uplift environ m en t , except for L-373 a n d L-374 that formed in a post orogenic environmen t. Proterozoic samples formed in anorogenic, mainly continental epeiroge n i c environme n t s , except for four; thes e are L- 023, L-025 , L-027 a n d L-363 , as shown on Table 4.1.4.5. L-027 m a y have formed in an island arc environ me n t , and the environ me n t of the other three samples is uncert a in . The new proc edu r e to compar e trac e and major oxide elemen t chemis tr y with a database of over 4000 well-lo c a t e d chemic al analys is of granitoid s using artificial intelligence may help to identify the true environment of emplacem ent of all the granitoid s in the Kalene Hill area. 4.1.4.2.6 Conclusions Four distinc t groups of rocks were identif i e d in the Kalene Hill area. One is Archean and three are Paleoproteroz o ic . Archean rocks from Group 1 are enriched in copper. Paleoproterozoic rocks from Group 2 are widely spr ead, simila r rocks are known in the Mwombe z h i and Solwezi domes, and pr obably also occur in the basement to the Copperbelt. Some of them contain high Th. Some contain high Cu values. There are severa l Paleop r o t e r oz o ic granit o i d s enriche d in copper and zinc. Minor subductional magmatism may have taken place during the Paleoproterozoic to form part of the rocks pres ent at Kalene Hill. 9 6 4.1.4.3 INTRODUCTION TO THE GEOL OGY OF THE DOMES REGION, NW ZAMBIA From west to east, the Domes region of northwes t ern Za mbia can be subdivide d into three main zones: th e Kabompo Dome, the Mw ombezhi Dome and the Solw ezi Dome (Fig M12) . Discussion of sampling and results will be presente d in that order. Lack of outcrop , and strong overpr i n t by younge r orogen i es mask Paleoproterozoic structur es and geology of the domes region in Zambia. Very little literature is available on the geology of that part of the country. Paleop ro t er oz o ic rocks are exposed in the basemen t domes ; these are covered by younger Mesop r o t e r oz o ic and Neopr o t er oz o ic supracr us t a l rocks. Neoproterozoic orogenies modified the domes deformi n g and thrusti n g their rocks into the arcuate trend that is know n today. Domes tend to run paralle l to the main structu r a l tr end of the Lufilia n Arc, as indicated on Fig 4.1.4.7. Fig 4.1.4.7 Generalized geological map of the domes region in Zambia. T he black rectangle encloses the main do mes. Note t he arcuate shape of the do mes, and their ext ension of approximately 50 0 km along the Lufilian Arc. Rock outcrops are only a very small portion of the do mes, most o f the land is covered by regolith. Extracted from P orada, 19 89. In northwestern Zambia , geology is largely obscured by thick soil cover , Karoo roc k s , calc rete and Kalaha r i sand. Outcrops of the domes are only s parse l y expose d along river and stream beds. All the domes are compose d of gneis ses, migmatites, amphibolites , metagranites and quartz -kyanite- m u s c o v i t e schists . The oldest rocks are cons ider e d to be biotite and hornblen de gneisse s derived from both sedimen t ar y and igneous protoli t hs . No detaile d subdiv i s i o n of the gneisse s has been attempt e d , and great portions of the domes appear on geolog ical maps as large, uniform units (Klinck, 1977; Master, 1996 and Mulela & Seifert, 1980 - 1998). Typical paragenesis of the gneisses are: a) biotit e + K-feld s pa r + quar tz + garnet + sulfid e s b) biotit e + epidote + sphene c) hornbl e nd e + plagioc l as e + quartz + sphene + scapol i t e d) biotit e + quartz + epidot e Migmatites are clos ely associated with the gneisses fr om whic h they were derived. The melanoso m e of the migmatites contains more biotite than the gneisse s , while the paleoso m es compris e fine-gr a i n ed gneiss and pegmatitic microcline granite. Massive and foliated granite s intrude the gneisses and are cons ide r ed to be partly responsible for migmatitization. Quartz+kyanite + m usc o v i t e ? e p i do t e ? K- f e l d s p a r is the dominan t mineral assembla g e in the schis ts, which are mainly found at the basement-cover contac t. Kyanite-bearing biotite schist occurs as lenses and bands within the gneiss es . Amphibo lites interbanded with the gneisses are a minor component of the basement domes ; their typical mineral assemblage is: hornblende+plagio- 9 7 c las e+ q ua r tz? b io tite ?e p ido te . Thes e roc ks are commo n ly converted to talc -chlorite schists along shear zones (Mas ter, 1996). Neopro t er oz oi c Katanga n metased i m enta r y rocks contai n economic minera l iz a t io n in the Domes region . The larges t mineral deposits are copper mineralization at Lumwana in the Mwombezhi Dome (Benham, Greig, & Vink, 1976; Master , 1996; Equinox Re sour c es , 2003; and Equino x Resour c e s , 2004). Main copper product i o n from the Domes Region historic a l l y came from the Kans anshi mine just north of the Solwezi Dome. This is a deposit enriche d in copper , gold, uranium and silver (B roughton, Hitzman, & Stephens, 2002; Hitzman, 2001; Master, 1996; O'Brien, 1958; Torrealday, 2000; Torr ealday, 2001; and Torrealday et al., 2000). Basement rocks contain minor dissemi n a t e d and vein copper minera li z a t i o n . The region has been explored for other minerals, including gold, ur anium (Jay, 1960 in Men eghe l , 1981a; Meneghe l , 1981b; Meneghe l , 1981c; Cosi et al., 1989; Cosi et al., 1992; and Master, 1996), ra re earths, cobalt, nickel, manganese, iron and diamonds. Deposits at Lumwana and Kansan sh i are curren tl y being developed into world-cl a s s copper mines. The follow i n g chapt e r s will discus s new geolo g ic a l findings from the Kabompo, Mwombezh i and Solwez i Domes. 4.1.4.4 Kabompo Dome 4.1.4.4.1 Introduction Rocks of the Kabompo Dome cons ist of a complex of migmatized gneiss, hornblendite and amphibolite. These rocks are overlain by migmatitized psamites and pelites. Katanga quartzites, and talc -muscovite and kyani t e - b e ar in g schis ts surrou n d the ro cks of higher metamorp h is m . The various gneisses, migmatites and amphibo l i t e s are describe d by Klinck, 1977. Four sample s were collecte d in the field. Table A7.1 lis ts their chemical analyses. Table 4.1.4.7 presents their basic geochemi s t r y and result s of studies to unders t a nd their environment of emplacement. Very few outcrops were found, and the greatest amount of information w ill be extracted from them. Geology, geochemis try and other aspects of the main rocks observed in the Kabompo Dome will be describ ed in the followin g pages. Table 4.1.4.7 Rock name, basic geoche mistry and environment of emplacement for samples from the Kabompo Dome, NW Zambia (Samples with an asterisk were dated. S ee acronym descrip t i on on section 2.4.3.) Sample Rock Name Debon & LeFort Maniar & Piccoli Whalen Pearce Mafic Rb/10HfTa Rb/30Hf/Ta Nb-Ta L-028 Quartzmonz onite Metaiv mesoNaMg N O3/4 OUTU L-029 Tonalite Peraiii mesoNaMg N L-030* Granit e Perai leucoKF e POG A S2/4 O2/4 VA- II INV L-047* quartz syenite Metav mesoNaFe CEUG A W3/4 OUTU 4.1.4.4.2 Description of Samples Collected in the Field 4.1.4.4.2.1 Samples L-028 and L-029 Sample L-028 w as identifi e d in the field as an amphibo l i t e . It is a black and white, metalu m i n ou s sodic magnes ic quartz mo nz o n i te , that plots near the border with the monzodior ite field. No in situ outcro ps were found; but 6- to 10-mete r diamete r boul de rs of the same material were seen along the river. Several samples of that rock were collected under a bridge loca ted on UTM coordina t es 35L 0282993/ 86 98 4 1 1 , 1843m, as show n on Figs M13 and M10. Based on the chemis tr y , this sample can be assign e d to an undefi n ed oroge n i c environment of emplacement (Table 4.1.4.7). It has high total Fe, Mg, Sr, Ni, Cu and Pr. L-029 was collec t ed from under a bridge on UTM 35L 0281721 / 8 6 9 93 9 2 . Very little rock outcrop s could be seen for kilome t e r s around . Large boulde r s of amphib o l i t e - f ac i es , foliate d schists or gneisse s were sampled on the river bed. They are not in situ , but are reasonably well located, ac cording to the geological map sheet. The chemistry of this black, andalus i t e , peralumin o us , mesocratic sodic magnesic tona lite only allows to state that it formed in an orogenic environment (Fig 4.1.4.7). The sample is enriched in alumina , Mg, Sr, Ni and Cu. No analysis for Pr was carried out. 9 8 4.1.4.4.2.2 Sample L-030* By far the best outcrop seen in many tens of kilomete r s was the box cut to access a bridge along the main paved road from Solwezi to Mwinilunga, on UTM coordinates 35L 0295813/8692365, 1405masl. L-030* was collect e d from a 35 m long outcrop on the southe r n side of the road, althou gh both sides are well exposed. Figs 4.1.4.8 to 4.1.4.10 illustrate ma in aspects of the outcrop . All three were draw n at 90? to the main rock foliation. Fig 4.1.4.8 General aspect of the outcrop where samples L-029 and L-030 were collected. Geological hammer for scale. A straigh t , 8 cm wide dike of felsic gneiss with quartz augen lies along the main foliat i o n . Medium- gr a i ne d quartz - f e ld s pa r and biotite flakes make the darker bands . Several generat i o ns of 2.5 cm-wide, irregul ar fels ic sills that intersect the main rock foliation are cut by small displa cement thrust faults. Late inverse faults , 5 mm wide, filled by mafic minerals and iron oxides cut all other structur es and break the main foliation. Most quartz in the thrust faults and gneiss e s tends to be brow n and smok ey. Rock foliati o n is at an angle to the gneissic light and dark banding. Note the angles of white banding, augen in both light gray mass and in lighte r bands (Fig 4.1.4.10). Some of the quartz-rich veins di spla y small refolds, as show n on Fig 4.1.4.9. Fig 4.1.4.9. Main aspects of the outcrop where sample L-030 was collected. M ore details are included in the t e x t . Brunton g eo l o gical compass for scale. 9 9 L-030* was dated by U-Pb SHRIMP II analysis on zircon s and is one of the few samples that has comple t e rare earth analysis (Fig 21, Appendix) . It is a foliat e d , peralu m in o us leuc ocra t i c potassic ferrifer o us granite and was formed at 1927.6? 7 . 1 Ma (See Tables 4.1.4.7 an d A7.1). Comple t e geochro no l og i c a l analysis from the sample is not available at the time of writing this document. Fig 4.1.4.10 Detail of the foliation and mineral banding of the rock that intersect at around 5-8 degrees. L-030* was collected as an oriented repres entative fragment (Fig 4.1.4.9). Its precis e location is indicated on the map of Fig M13. It is made by feldspar augen and light refold e d bands. This was the freshes t possib l e sample of the rock in the entire outcrop , but it still displays some weather i n g , and it does not carry apparen t magnetite. Main jointing in the outcrop is 095/31 ?S. Quar tz veins are oriented 107/59.5?S with slickens ides in ?nor ma l? faulti n g direct i o n (Figs 4. 1.4.9 and 4.1.4.8). General foliation on the opposi t e side of the road was 130/89? W . Another joint that carries a 6 mm quartz vein was oriente d 199/55? S . L-030* is slightly enric hed in uranium and thorium . It is a high-hea t produci ng granit oid, and at the time empl acement it had a 5.0 heat production value as indicated on Chapter 5. T h e chemic a l signatu r e of L-030* is very similar to that of L-364 , L-370 and L-020. That includes K, Rb, Ca, Sr, Ba and most of the other major oxides, minor elem en t s and rare earths . It can be establ is h ed with a good degree of certainty that Group 2 rocks from the Kalene Hill suite form ed in the same environme n t . They might have been produced during the same geological event. Thus, we can tentatively give Group 2 rocks an approxi m a t e age of 1928 Ma. That makes sens e, beca use Key et al., 2001 establis hed SHRIMP II U-Pb zircon ages for feldsp ar - ph y r i c granit o id s at 1934?6 Ma and 1940?2. 8 Ma in the Mwinilu n ga area, just east of the Kalene Hill area. This is also part of the Kabompo Dome. Detrita l zircon s from the environs of the Kalumbi l a deposit were dated by Steven & Arms trong, 2003 and produce d ages of 1924 to 1913 Ma and 1952 to 1939 Ma. These ages are all very near in time and could be the eviden ce of a major event of magmatism in the Kabompo Dome (See Table A22.3 and event diagram of Fig A24). L-031 was collec t ed from the same outcrop , in a more competen t fragment of float of fine-gr a in e d foliated gneiss that had very similar macrosc o p ic compos i t i o n. This sample has not been analysed . The envir onment of emplacement for this granite is so mewhat difficult to establis h, because the various schemes produce conflicting results. It has potassic alteration; for that reas on , the Maniar & Piccoli, 1989 tectonic discrimination proc es s state t hat it formed as a post-orogenic gr anitoid (Table 4.1.4.7). This is probably wrong, but other tectonic discrim i n a t i o n methodo l ogies don?t produce trustw orthy results either. The Whalen diagrams clearly show that it is an anorogen ic granito id . Pearce, Harris, & Tindle, 1984 discrim in at i o n proc edu r e s do not produce any clear results , while the proc ess pres ented by Harris, Pearce, & Tindle, 1986 indicate that the rock formed in a volcanic arc. If the anolog y of L-030* with the suite of Group 2 from the Kalene Hill area is extended , then L-030* probab ly formed in a continental epeirogenic uplift. Field descrip ti o n s of sample s L-032 to L-034 are included in Append ix A63. 1 0 0 4.1.4.4.2.3 Samples L-047* and L-048 Instructi o ns from Peter Mann of the AngloAme r ic a n explor ation office in Kitwe served as guide to find obscure outcrops wher e L-047* and L-048 were collected (Mann, P., personal communication, 2002). There is very little outcrop in the region; no outcrop s were seen al ong the entire route from the main paved road. Both sample s come from large boulde r s that lie semi-bur i e d on the ground, under cover of high grass and abundan t shrubs. L-047* comes from UTM coordina t e s 35L 0320870 / 8 6 60 39 3 . L-048 (Fig 4.1.4.13) was collected exac tly 50 m SW of the previous sample . The general locatio n of the samplin g sites is show n on the maps of Figs M13, 4.1.4.11 and 4.1.4.12. L-047* is a metalu m i n ou s mesocr a t i c sodic ferrif er o us quartz syenite; it repres en t s an intrusive event that cuts the ?basemen t ? granodior ite s in NW Zambia and Kat angan silicic la s t i c s and carbona t e s . Fig 4.1.4.1 3 show s general macroscopic featur es of the sample. Comple te chemic al analysis is presen ted on Table A7.1. This rock repres ents a large mapped area (See Fig M13). Studyi ng it is very relevant, becau se it might have some genetic association with the Kalumb ila Co-Ni- Cu deposit, which lies immediately to the south east (Steven & Armstrong, 2003). L-047* is highly enriched in almost all the rare earths; Y, Zr, Nb, Nd, Pr, Ce, La, Yb, Eu, Tb and Lu are all very high. In fact the sample has the highe st values of such element s in the collect i o n of rocks from NW Zambia. It also has a high Na content and very low Cu, Zn, Co, Ni or Th. The sample lies isolated in all of the geoche m ic a l diagra ms (Figs 4.1.4.1 to 4.1.4.6). It is a midalkaline rock and is not relate d to any of the other rocks in the NW Zambia suite. Fig 4.1.4.13 Slabs of L-047* and L-048. Note the abundant op en spaces in betw een the crystals. This red-altered rock is associated with small b odies of gabbroids and massive iron oxide as se en on Fig 4. 1.4 . 11. It probably is associated with iron oxide-copper-gold mineralization. Both scales in centimeters and millimeters. Both samples have abundan t miarolitic cavities, as seen on Fig 4.4.4.13. Quartz fills part of the voids between potassi u m feldspa r and nepheli ne . Maybe the origina l rock lacked quartz altogeth e r and that mineral came later after the more alkali ne minera ls in the rock were formed . This topic was not ev aluated in detail. Textures from granitoid s that are responsible for iron oxide-c o p p er - g o l d mineral iz a t i on in the Kafue Flats and around the Hook Granite batholith have many similar featur es to those of L-047* . The fact that a quartz syenite is so enric hed in some rare earths and minor elements is very signific ant. The follow ing rocks have chemic al signat u r es simila r to L-047* : L-195 , L-259 , L-402 , L-439 and L-713 . L-047* was provisionally dated for this project at approxi mately 730 Ma. Precis e U-Pb zircon SHRIMP II data is not available at the time of writing this document. Geolog ic a l events with similar ages in NW Zambia are listed on Table A22.3 and illustrated on the event diagram of Fig A24. R egional-scale metamorphic events were reported by Cosi et al., 1989; Cosi et al., 1992 and Key et al., 2001 (Events 2, 3 and 4 of Fig A24). Key et al., 2001 report fels ic volcan ism with a SHRIMP II U-Pb age of 735?5 Ma at Luamata, and a 765?5 Ma basalt effusion at Lwanu in the Mwinilunga area. Thes e events are very near in time and space to the emplac e me n t of L-047* . Unfortunately, the chemistr y of volcani c rocks dated by Key et al., 2001 is not availabl e for comparis on and interpre t a t io n . They probably are midalkal in e rocks. 1 0 1 1 0 2 1 0 3 Sample L-047* has been interpr e t ed as a continen t a l - e pe i r o g e nic uplift granitoid. It probably formed as a single ring complex. The various granitoi d bodies mapped may be faulted portions of a single body (Figs 4.1.4.11 and 4.1.4.12). The evalua ti o n of sample L-047* opens a new concep t for explor a t i on in the southe as te r n portio n of the Kabompo Dome. Rocks like L-047* were very explosive and produc e d hydrot h er m a l breccia t i o n . The intrus i v es inters e c t ed Katang an silici c la s t i c s , dark s hales and carbona t es . There is some minor epigene t i c copper mineral i z a t i on in the environs , gold mineralization, red-altered quar tz syenites with abundant miarolitic cavities and explosive brecciation, nearby ir on oxide bodies, abundan t small gabbroi c bodies , strong widespread sodic alteration , and red-rock alteration. A ll of those features are common in the environs of iron oxide-copper-gold systems (Chapter 8). In addition to that, there is a nearby sedimentar y-ho sted Co-Ni-Cu deposit. The south eastern portion of the Kabompo Dome is another locati o n where iron oxide- c o pp er - gold mineralization may be associated to sedimentar y-host ed copper mineralization in the Greater Lufilian Arc. 4.1.4.4.3 Conclusions Foliated , peralum i n o us , leuc oc r a t ic to subleuc oc r a t ic , fe rrife r o us granite s and alkali granite s were emplace d at least from 1952 to 1913 Ma in the Kabompo Dome. This is probabl y the evidenc e of a major anoroge n ic magmatic event that is presen t in the Kalene Hill, Kabompo Dome and Solwezi Dome. The granitoids were emplaced in a continental epeirogenic uplift environment. The south easter n portion of the Kabomp o Dome has a ll the charac t e r is t i c s of being prospective ground to explore for iron oxide-copper-gold miner alization. Red-altered quar tz syenites with abundant miarolitic cavities that were emplace d around 730 Ma in a continen t a l epei rog en i c uplift environ me n t are intima t e l y associa te d with small gabbroic bodies and massive iron oxide bodi es. They intersec t Katangan silicicla s t ic s , organic shales and carbona t e s . There might be a relation s h i p between iron oxide-co pp er gold systems and sedimentar y-hosted Co-Ni-Cu mineralizat ion in that part of the Kabompo Dome. 1 0 4 4.1.4.5 Mwombezhi Dome 4.1.4.5.1 Introduction According to Master, 1996 and Mulela & Seifert, 1980 - 1998, the basemen t of the Mwombe zh i Dome compr is es the follo w i ng units : a) A biotite-rich migmatitic complex, dominated by granites and biotite - h or nblende gneisses that are intruded by syenites and microgranite stocks and dikes. b) Muscovit e- p h l og o p i t e schists with epidote, biot ite, kyanite, quartz and feldspar porphyroblas ts produce d by shearing of the migmat itic comple x. This rock-type repr es en ts major shear zones in the basement. c) Scapolite-garne t metagabbros and hornb lend ites and amphibo l i t e s occur as lens es and bands within the other compone n ts of the dome. d) Katangan meta-sediments that uncon formab ly overlay the crystalline basement of the dome. Significant subhoriz on tal shearing of basement and Ka tang a n sedime n ts with later folding of the sheare d rocks, produced the comple x structur al setup of the Mwom bezhi Dome. All four rock units were folded into large east-wes t - t r en d i ng structur e s . Outcrops of the Mwombezhi Dome are uncommon. Neve rthe less, 15 granitoid sample s were collected from the Chitungulu sodalite syenite that lies just north of the dome, and three from the Shilend a area, south of the dome. Eleven samples of the syenite quarry and one from Shilenda were analysed. This chapter will review genera l aspect s of the Lumwana coppe r deposi t , the Sh ilend a mafic volc anic s , and the sodalit e syenite quarry. 4.1.4.5.2 Lumwana Copper Mineralization The Lumwana copper mineraliz a t i o n is probably the la rges t comple t e l y undevelo p e d resourc e of copper in Zambia today. General location of Lumwana is indicated on Fig M13. It occurs within refolde d folds and shear zones in the Mwombez h i Dome. The camp is made by se veral mineraliz ed areas, the most important of which are Malund we and Chimiw ung u . A short visit to the deposit, with assistanc e of geolog is ts from Equinox and Phelps Dodge is the basis for the follow in g accoun t . In principle, mineralization at the deposits is hosted in highly deformed metavolcanics. The age of these schists is not know n, but may be the extrusi v e equiva l e n t s of the granit o id sample d in L-030* . And have an age of circa 1930 Ma. The age of mineralization has not been well constrained. Fig 4.1.4.14 Cross section of the Malundwe Cu deposit at Lumwana, Zambia. Geol ogy here is greatly simplified. Note the width of mineralization and th e de pth at which the ore is kn ow n. Malundw e is planned to b e mined as an ope n pit; und erground o perations probably will be gin in the last stages of t he project. The footwall g neiss is considered to b e a meta-granitoid, and the hangingwall schists and g neisses are metavolcanics. Horizontal marks are every 200 m and vertical marks are every 1 00 m. Image from Equi no x Res ou rces, 2004. T h e mineraliz e d body is a 100 m wide sheet that occurs at an appr oxim a t e depth of 150 m in an area of 1400 m by 4000 m (Fig 4.1.4.14). The body sometimes thin s to around 50 m. Minera l iz a t i on at the Malund w e 1 0 5 d e p os i t is thought to be syn-meta mo r p hic . A shear zone at upper amphibol i t e facies took place at the same time as miner alization. Publicly available figures on reser ves and resou rc es from the Lumwa na distr i c t are listed on Table 4.1.4.8. Table 4.1.4.8 Resources and Reserves at the Lumwana District, Zambia ( From Equinox Res ources, 2003 ; and Equinox R es ources, 20 0 4) Lumwana Resource Tonnage Grade Deposit Class (Mt) Cu% Co (ppm ) Au (g/t) Measure d 47.0 1.1 4 1 3 7 0.05 Indica t e d 83.3 0. 8 0 1 6 0 0.01 Inferred 31.4 0.74 115 0.03 Malundw e Subtot a l 161.7 0. 8 9 1 4 4 0.03 Measure d 82.5 0.7 6 2 9 6 0.02 Indica t e d 56.7 0. 7 5 2 2 8 0.02 Inferred 600.4 0.64 48 0.01 Subtot a l 739.6 0. 6 6 8 9 0.01 Chimiw u ng o Total 901.2 0.70 99 0.01 Lumwana Ore Reserves Tonnage Grade Deposit Class (Mt) Cu% Co (ppm ) Au (g/t) Proved 42.6 1. 0 9 1 4 0 0.05 Probab l e 44.7 0. 7 9 1 1 6 0.01 Total Ore Reserv e s 87.3 0. 9 4 1 2 8 0.03 Inferred Resourc e 8.3 0.64 8 0 0.02 Malun dw e Total Miner a l Re sou r c e s 95.6 0. 9 1 1 2 4 0.03 Proved 80.1 0. 6 9 2 9 5 0.02 Probab l e 37.9 0. 6 8 2 0 2 0.02 Total Ore Reserv e s 118.0 0. 6 9 2 6 5 0.02 Inferred Resourc e 134.6 0.6 0 5 7 0.01 Chimiw u ng o Total Miner a l Re sou r c e s 252.6 0. 6 4 1 5 4 0.01 Proved 122.7 0. 8 3 2 4 1 0.03 Probab l e 82.6 0. 7 4 1 5 5 0.01 Total Ore Reserv e s 205.3 0. 7 9 2 0 7 0.02 Inferred Resourc e 142.9 0.6 1 5 8 0.01 Lumwana Combin e d Total Mineral Resources 348.3 0.72 146 0.02 Malundwe contain s abundan t copper, gold, cobalt and minor uranium mineral iz a t i o n . Co was conc entr a t ed in hinge zones during folding, but it source is not yet cl ear. Uranium was introdu c e d much later during shearin g , or along the shear zone (Bouda, St even, persona l communic a t io n , 2002). The mining operati o n will leach uranium from select portion s of the deposit . Gold is much lower grade at the Chimiw u n gu deposit than elsewhe r e at Lumwana . Fig 4. 4.4 . 1 4 shows a gener al i z e d cr oss section of Malundw e . Meta volcanic units at Malundwe underwent extreme shearing and metamorphism. Temperature and pressure of metamorphism are thought to be 650?C and 13kbar s; that corresp o nd s to upper amphibo l i t e facies. Very coar se kyanite porph y r ob l a s t s were rotate d by shear i n g of the rocks. Quar tz-f e l d s p a r partial melts in the rock are abundant. Some pegmatit i c veins that occur in t he deposit might indicat e a possible relatio ns h ip of mineralization with the migmatitizati o n proc ess . Ther e is also abundan t red garnet; copper is pres en t in the shearing shadow of the garnets . Ext ensive red-rock alteration is ubiquitous : pink is iron oxide, white is the gneiss. It is not quite clear when copper mineral iz a t io n took plac e. In June, 2002, the source of copper and the age of mineral iz a t i on were uncerta i n (Boud a, Steven, persona l communication, 2002). At the Chipata site, granit i c gneiss intrud es the Lu mwan a miner a l iz e d rocks (Bouda, Steven, personal communic a t io n , 2002). 1 0 6 4.1.4.5.3 Mafic Volcanics from Shilenda Mafic volcan ic s with very partic u l ar surfac e textur e s we re sampled around the site of Shilenda, just south of the Mwombez h i Dome, as show n on Figs M12 and M13. Samples L-311 a nd L-319 are green to black lati- andesites with a micro- pillow texture, joined by a white substanc e that erodes more readily than the surrounding rock, to form a very irregular surface (F igs 4.1.4. 1 5 ) . The white materia l is a sodium - r ic h carbonate that is readily disolvable in the surfac e environment. Fig 4.1.4.15 Photographs of hand samples a nd slabs from the Shilenda mafic volcanics . A show s the irregular surface that the rocks display on outcrop. B is a fresh cut with the hammer, and C and D are slabbed surfaces. Note that the w hite substance is less resistant to erosion and w eathers negatively. T he righ t side of C show s a perpendicular cross section of the surface, with d eep incision along th e so dium carbonate w hite material. C also show s concentric zonation and crystal size distribution o f the black lava particles. Coarse r crystals te n d to b e in th e middl e, w hile t he chilled margins have finer size. All scales are in millimeters. More details in the text. The separa te fragme n ts in the breccia displa y concen t r i c minera l zonati o n, and conc en t r i c crysta l size distribu t i o n . Coar ser grains tend to be in the midd le. Most of the fragments have a lensoid shape in cross section . That texture may be due to progress i v e cooli ng of the semi-mol t en lava and rapid quenchin g of the borde r s , or to some degas s i n g proc es s . The rock has many similarities with hyaloclastites. Chemical analysis of nearby rocks show gabbro ic compos i t i o ns . Klinck , 1977 describe d thes e rocks as autobrecc i a t e d lavas. Most of the autobreccias carry sulfid es includ ing pyrite and chalcopyrite that have primar y origin. The rocks have been altered to scapoli t e , hornblend e and epidote . Sample L-311 is a metalu m i n o us mesoc r a t ic sodic magnes ic lati- a n de s i t e . The vario us proc e du r es to evaluate environment of emplacement for mafic volcanic ro cks do not coincide in their interpre t a t i o n of the tectonic environment for the rock. The Ti-Zr-Y diagram of Pearce & Cann, 1973 indicate that it is a calc alkaline basalt. Using the proc edur e by Meschede, 1 986, the sample falls in the field of within-plate tholeiit e s and volcanic arc basalts. The prec ise age of the lavas is not known, but they are probab l y extrus i v e correl atives of the abundant Neo- Proteroz oic gabbroid bodies that intersec t Katangan meta sediments in the area. 1 0 7 4.1.4.5.4 Chitungulu Sodalite Syenite 4.1.4.5.4.1 Introduction Rocks of this sodali t e syenit e quarry are important because they intrude into Katang an metased i m e n ts and could produce a minimu m age for their deposi t i o n . The qua rry is located NW of Solwezi along the Chitung u l u river, northeas t of the Mukumbi Lubing a village, and is curren t l y mined for its striki n g cobalt - b l u e , speckle d dimens io n stone. The occurrence of foid-bear ing syenites is compos ed of at least five bodies with ellipsoidal perimeter, each of one to a few hundre d meters in diamet e r that make a ring complex cluster. Thes e are the only mapped such features , but there are probably many more alkaline intr usio ns of varying composition that intersec t Katangan sediments in the region . The bodies of syenite are cl osely related to many gabbroid intrusions of similar dimens i o ns . A few gold and copper occurr e nc es and abunda n t bodies of massiv e iron oxides have been mapped in the environ s . The Lumwan a deposi t s lie 18 km south of the sodali t e syeni tes. The quarry site was found by following large boulders of sodalite syenite up the river . There was no clea r outcrop on the surface . The largest body of syenite occurs near a right bend of the Chitungulu river and covers approximately 2.6 square kilome t e r s . The quarry was visite d becaus e it is one of the few well mapped intr us i on s into Katang a n rocks, and becaus e of its accessibility. This account w ill only describe the largest of the three syenite bodies. 4.1.4.5.4.2 Sampling A reconnaissance geological map of t he quarry with all the sampli n g si tes is present e d on Fig 4.1.4.1 6 . Accordin g to the mine geologis t , Mr. Remo Tognalet ta fr om GTM Stones Limited, it is the first geological map ever made of that deposit (Tognaletta, R., persona l commun ic a t io n , 2002). Eleven samples were taken from the most represen tative rock units at the quarry. Tw o more major oxide analysis of nepheline syenites from the same locality were compiled from the literatur e 2 . All samples and their chemistry are listed on Table 4.1.4.9. 4.1.4.5.4.3 Description of the rocks Syenites at the quarry are equigranular, medium- to c oarse- g r a i n ed , and ocassio n a l l y become porphyr i t i c with large feldspar crystals . A recently re-edited report of the Zambian Geological Survey states that the proper petrogr ap h ic al name for the sodalite syenite is aegirine ditr oite (Mulela & Seifert, 1980 - 1998). Petrography of the sodalit e syenite s was describ e d in some detail by Mulela & Seifert, 1980 - 1998, and is included in the Append i x . Colors of the rock vary great ly: from white to light blue, gray, pink, brown, red and even into light green, as discus sed below. The main product of the quarry is a light gray, bluish, massive, non-foliated, metalumino us subleucocratic, markedl y ferrife r o us sodalite syenite . The rock has abundan t blue specks of sodali t e that displa y s unifo r m texture and no preferential crystal orientat i o n (Fig 4.1.4.1 7 B, C and D). Samples L-037 , L-043 a n d L-044 are typical of the ?blue? rock. That type of rock is not ea sy to find fresh at the quarry, becau se most of the faces have been weathered along joints. The ?blue? rock contains a few white xenoliths made of plagioc lase, quartz and disper se magnetite. An unidentified hard, gray sulfide is also pr esen t in the sodalite syenite. All rock types at the deposit carry abundant magnetit e , as seen on Fig. 4.1.4.1 7 , and nepheli ne is a rock- form i n g miner al. Various facies of foid syenites intru de into each other and grade from one composi t i on to another, in a way not completely well established. T hey may obey to telescoping plugs of slightly varying composition. L-045 is a red, finer grained variety of the syenite. L-046 i s a fresh ?brown? , co arse-grained syenite. L-039 is a pink syenite that intrudes the blue and gray syenite bodies . All contacts are net, and none of the rocks is foliated. L-040 contains a 4-cm wide, massive vein of blue so dalit e; that is not commonl y found at the quarry. Although L-041 is a darker variety of syenite, its chemistry is very similar to the other rocks (Table 4.1.4.9) . 4.1.4.5.4.4 Weathering, Jointing and Problematic Structures for Mining Nepheline weathers readily on the surface environ m e nt , and produce s a white, etched rock with angula r vugs . Most of the rock at the quarry is deeply weathered along the main joints. Surface alteration of feldspathoids along the fractures extend s for more than fifty meters below the surface. ?Brown? and ?pink? varieties of 2 These sample s were labeled ZGSI and ZGSII, that stands for Zambian Geological Survey I and II. 1 0 8 1 0 9 syenite in the quarry are difficult to find fresh (Fig 4.1.4.17A and G). The soil pr oduced by weathering of the sodalite nephe line syenites contains a high propor tion of magnetite. Fig 4.1.4.17 Photographs of slabbed syenites fr om the Chitungulu sodalite syenite quarry, Zambia. A is sample L- 036; B, L- 03 7; C, L-04 4; D, L- 043; E, L- 03 9; F , L-046; G, L- 045. B, C and D are typical ?blu e ? sye nites. A and G are ?red ? syenites and E and F are ? brown ? sye nites. Note the rock text ure in E and F. A is more w eathered ( or hydrot hermally altered?) than the other rocks. B displa ys a white weathering rim towa rds the left, due to feldspat hoid kaolinization. All scales in millimeters. See more descriptions in text. SSW NNE SSE Fig 4.1.4.21 Intrusive relationships between the different facies of sodalite syenites observed at the quarry . T here is no clear order of intrusion, and maybe that can be explained by gradual facial changes of the syenites within a single intrusive ev ent. See more details in the text. 1 1 0 T h e red syenite at WPT 092 ( L-036 ) (See Figs 4.1.4.2 1 and 4.1.4.1 6 ) is in tr uded by irregula r bodies of light gray to white, finer-grained ?blue? sodalite syenite that weathers white. There is an 8m wide dike of sodalite syenite intersecting the red syenite. Contact s between the various units ar e straight. No xenoliths of the red syenite were found in the blue syenite. The outcrop of syenite at the quarry shows a massive , sparsely - j o i n t e d non-foli a t e d granitoi d . Main joint families are 044/89?W, 080/02?W, 060/64?S, and151/ 88?NE. These are unevenl y spaced , approximately every 5 meters. They ar e open and display weathering a nd white leaching (See Fig. 4.1.4.1 7B ) . The spacio us jointin g enables blocks of 2-6 meters on side to be cut for dimens i on stone exploit a t i o n . Black veins, a few centimeters wide are a problem for mi ning. They extend for at leas t 200m and are oriented 118/57? S . An importa n t shear zone crosses the quarry on its wester n si de with orienta t i o n 000/78? E . Hydrothe rmal alteration and frac turing occurs in the su rround i n g rock for at leas t 1 m, and 3m in some places. No blocks of good quality for dimensio n stone can be cut near the shear zone. 4.1.4.5.4.5 Geochemistry Thirteen chemical analysis of rocks from the quarry ar e listed on Table 4.1.4.9. Chemistr y of the samples plots on pluton ic rock diagra ms as illustr a t e d on Figs 4.1. 4.18 and 4.1.4.19. All samples analysed except for tw o are foid-be a r in g syenite s . Fig 4.2.4.2 0 illustr a t es the chem ic al variation of rocks at the quarry in a logarithmic major oxide diagram. Table 4.1.4.9 Chemical Analysis of the sodalite syenite quarry, Zambia (Complete elemental analysis on Table A7.4, Appendix) Sample SiO2 TiO2 Al2O3 Fe2O3 FeO MnO MgO C aO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni N o t c h 50.00 1.00 15. 5 0 6.00 0.15 2. 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 30 2.00 200 400 60 360 40 30 16 L-032 59.58 1.09 15. 5 2 7.08 0.00 0. 0 7 3 . 0 7 5 . 0 1 2 . 8 0 3 . 1 3 0 . 5 4 0 . 8 2 9 8 . 7 1 1 1 0 566 26 284 23 25 34 L- 0 3 4 60.10 0.04 23 . 0 1 3.98 0.00 0. 0 7 0 . 1 1 0 . 1 4 6 . 8 2 4 . 4 7 0 . 0 7 1 . 6 8 1 0 0 . 4 9 7 9 342 27 708 92 <6 12 L-036 73.57 1.10 15. 9 7 1.46 0.00 0.0 2 0 . 1 2 0 . 1 0 0 . 0 3 0 . 2 5 0 . 0 9 7.83 100.54 34 51 30 635 38 <6 26 L- 0 3 7 56.10 0.04 21 . 6 5 3.00 0.00 0. 1 2 0 . 0 4 1 . 2 0 1 0 . 2 2 5 . 5 1 0 . 0 5 2 . 5 3 1 0 0 . 4 6 9 2 465 33 792 101 <6 7 L- 0 3 8 56.45 0.12 21 . 0 7 3.77 0.00 0. 0 8 0 . 0 0 0 . 3 2 1 2 . 2 7 4 . 3 2 0 . 0 7 2.01 100.48 72 244 29 859 114 <6 7 L- 0 3 9 57.37 0.05 21 . 3 2 3.71 0.00 0. 2 0 0 . 0 8 0 . 7 5 9 . 6 8 4 . 6 3 0 . 0 6 2.64 100.49 87 355 37 808 120 <6 <6 L - 0 4 0 55.44 0.04 20. 9 8 5.81 0.00 0. 3 4 0 . 0 2 1 . 2 9 9 . 8 9 6 . 1 4 0 . 0 6 0 . 4 4 1 0 0 . 4 5 7 5 283 38 922 135 2 8 L-0 4 1 57.71 0.05 20 . 8 1 4.02 0.00 0. 0 7 0 . 0 0 0 . 6 0 8 . 8 9 5 . 4 1 0 . 0 2 2.85 100.45 85 283 33 950 134 <6 <6 L - 0 4 4 57.32 0.03 21 . 0 2 3.15 0.00 0. 1 4 0 . 0 0 0 . 6 5 1 2 . 0 4 4 . 2 8 0 . 0 5 1 . 7 0 1 0 0 . 3 8 1 0 9 616 107 1758 178 4 8 L-0 4 5 57.75 0.10 20. 9 4 6.96 0.00 0. 0 3 0 . 0 0 0 . 1 4 7 . 9 6 4 . 1 6 0 . 0 6 1 . 17 99.27 58 367 20 186 98 <6 11 L- 0 4 6 55.67 0.05 20 . 9 2 3.40 0.00 0. 1 9 0 . 0 9 1 . 0 7 8 . 5 1 5 . 2 7 0 . 0 6 5.21 100.44 82 311 30 670 82 <6 6 ZGSI 58.04 Tr 20.76 4.45 0.20 0. 0 9 0 . 9 5 9 . 2 2 4 . 8 1 Tr 1.99 100.51 ZGSII 56.31 Tr 19.89 4.28 0. 30 0. 1 6 0 . 2 6 0 . 7 4 8 . 3 3 5 . 7 5 n . d . 3 . 5 6 9 9 . 5 8 Sample Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Eu Gd Tb Dy Ho Er Tm Yb Lu Notch 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 100 4 30 5 20 3 9 36 8 2 L-032 17 58 19 151 78 703 <6 <15 16 8 54 83 109 37 96 1 1 1 L-034 8 18 17 74 87 705 <6 20 11 311 134 L-036 36 37 28 52 30 196 <6 36 <10 282 240 L-037 10 171 25 <12 117 423 9 17 <10 108 39 71 139 63 51 0 1 1 L-038 12 108 26 <12 65 318 8 32 <10 261 146 L-039 12 127 27 <12 68 349 9 30 <10 231 166 L-040 8 106 25 4 139 261 8 30 <10 278 186 L-041 6 98 27 <12 <12 347 11 22 <10 183 109 L-044 10 227 26 11 120 1441 10 31 <10 0 4 1 9 6 0 37 1.5 1.2 0.3 0.7 L-045 32 34 27 <12 45 764 7 18 <10 1.9 7.1 58 20 214 1 5 8 0 . 3 2. 4 9 . 7 2 1 4 1 . 2 4.7 0.8 4.5 0.8 2.1 0. 3 2 . 0 0. 3 L-046 115 168 24 <12 51 526 <6 29 <10 1 1 7 204 1 44 1 1 0 1 Table 4.1.4.10 lists the rock name, macroscopic field descrip t i o n and general geoche m i c a l paramet er s of the sample s, according to Debon & LeFort, 1983 and Debon & LeFor t, 1988. In general terms, rocks from the quarry displa y homo ge n eo us chemis t r y . They contain abunda n t alumina and soda, accompanied by high values of Zr, Nb, Zn, Ga, Ce and La. As shown by the TAS diagram of Fig 4.1.4.18 , most samples plot on the nepheli ne syenite portion . L-037 , L-038 , L-040 a n d L-044 are simila r to each other both chemically and macroscopically. They are all blue sodalit e nepheli ne syenite s . L-039 , L-045 , L-046 a nd L-041 are chemica l l y similar to each other, but di ffer slightly from the group of sodalite-rich syenites. The first three are varieties of pink syenite, while the fourth is a dark, finer-grained rock collected near the north-s o u t h- t r e ndin g shear zone, as indicat e d on the map of Fig 4.1.4.16. The only rocks with signific a n t copper enrichme n t are thos e of the pink variety, especial l y L-046 (Fig 4.1.4.17F). This last sample also has a high loss on ignition, but does not deviate significantly from the av erage syenite at the quarry. 5 5 6 0 6 5 7 0 7 5 SiO2% 0 1 2 3 4 5 6 7 8 9 1 0 1 1 1 2 1 3 1 4 1 5 1 6 1 7 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM Sodalite Syenite Quarry, Zambia; Lufilian G.P. (Based on Middlemost, 1994, 1997) S a m pl e s Pe tr o gr a ph ic fie ld s L-032 L-034 L-036 L-037 L-038 L-039 L-040 L-041 L-044 L-045 L-046 ZGSIZGSII Fig 4.1.4.18 Fig 4.1.4.18 - 5 0 0 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti) 5 0 0 1 0 0 0L-032 L-034 L-036 L-037 L-038 L-039 L-040 L-041 L-044 L-045 L-046 ZGSI ZGSII R1R2 PLUTONIC ROCK CLASSIFICATION Sodalite Nepheline Syenite, Zambia; Lufilian G.P. (After De la Roche et al, 1980) P e t r o g r a p h i c fie ld s S a m p l e s Fig 4.1.4.19 Fig 4.1.4.19 1 1 3 Table 4.1.4.10 Chemical character of sam ples from the Sodalite Syenite Quarry, Zambia ( s ee acronym description on s ection 2.4.3 . ) Sample Rock Name Aluminosity, color, Na/K, Fe/Mg Macroscopic field description L - 0 3 2 Gabb ro - d i o r i t e Metalu m i n o u s v me soc r a t i c Na low Fe mafic dike L-034 Syeni t e Peral u m i n o u s I subl e u c o c r a t i c Na high Fe Syeni t e L-036 Gran od i o r i t e Peralu m i n o u s I leuc oc r a t i c K high Fe ?red? s yeni t e L-040 Nephe l i n e s yeni t e Metal u m i n o u s v mesoc r a t i c Na high Fe ?blue ? s ye ni t e with sodal i t e vein L-045 Nephe l i n e s yeni t e Peral u m i n o u s ii mesoc r a t i c Na High Fe ?pink ? s yeni t e L-037 Nephe l i n e s yeni t e Metal u m i n o u s v subl eu c o c r a t i c Na high Fe ?blue ? s ye ni t e L-038 Nephe l i n e s yeni t e Metal u m i n o u s v subl eu c o c r a t i c Na high Fe ?blue ? s ye ni t e L-039 Nephe l i n e s yeni t e Metal u m i n o u s v subl e u c o c r a t i c Na high Fe ?pink ? s yeni t e L-041 Nephe l i n e s yeni t e Metal u m i n o u s v suble u c o c r a t i c Na high Fe Dark gra y fine-g r a i n e d s yenit e L-044 Nephe l i n e s yeni t e Metal u m i n o u s v subl eu c o c r a t i c Na high Fe ?blue ? s ye ni t e L-046 Nephe l i n e s yeni t e Metal u m i n o u s v subl euc o c r a t i c Na high Fe ?bro wn ? s ye nit e ZGSI Nephe l i n e s yeni t e Metal u m i n o u s iv suble u c o c r a t i c Na Mg ?blue ? s ye ni t e ZGSII Nephe l i n e s yeni t e Metal u m i n o u s iv suble u c o c r a t i c Na Mg ?blue ? s ye ni t e Four of the samples collected differ from the ma in chemistr y of nepheline syenite: these are L-032 , L-045 , L- 034 a n d L-036 . The first is a gabbro-diorite, the second a granodiorite. L-045 , L-034 an d L-036 h a v e more silica than normal for nepheline syenitic rocks; they may have been contami n ate d by Katanga n silicic la s tic s during intrus io n . L-045 a nd L-036 also are enriched in copper. The red granito i d porphyr y of L-036 differs significantly from the suite of rocks; it might be a different type of rock altogethe r (Fig 4.1.4.17A). It displa ys abnormally hi gh loss on igniti o n , is enric h ed in Ti, has the lowest alumina value of the suite, contain s normative quartz, higher Th and U values , and it probably was depleted in Na and K. The sample was collect e d from a small intr usi v e body that intersect e d the blue syenite and was itself intersected by a dike of sodalit e syenite (See the map of Fig 4.1.4.16). Few analys i s for rare earth s were carrie d out. Only one repr es ent a t i v e sample ( L-045 ) was analys e d for the comple t e suite of element s , and it displa y s a slight enri chm en t in the light rare earths. That seems to be the case in the rest of the rocks, based on the figures for Ce and La. A gabbro ic dike ( L-032 ) intrudes the syenites. It carries some unidentified black minerals and is enriched in V, Sr, Ni, Nd and Pr; it also carries abundant magnetit e. Although P 2 O 5 and Zr content s are high in the suite of rocks from the quarry, no outstanding values of U and Th were recorded , except in L-036 with 36 ppm Th. 4.1.4.5.4.6 Environment of Emplacement As illus trated on Table 4.1.4.11, all samples plot on the ?anorogenic ? portion of the Whalen diagrams , and most plot on the the ?within plate? environment of Pearce et al., 1984. The mafic dike of L-032 f o r me d in a within-plate environment. None of the samples produc ed coherent results in the proc edure devised by Maniar & Piccoli, 1989 to evaluate environment of emplaceme n t . Bodies of nephelin e syenite worldwid e are known to form in environ m e n t s of co ntinental crust extension. Syenites from the Chitungulu quarry probably formed as one in a series of anorog e n ic ring comple x e s . Table 4.1.4.11 Tectonic envir onment of emplacement for sodalite syenite quarry, Zambia ( S e e acronym descrip t i o n on section 2.4.3.) Sample Whalen Pearce Mafic Harris Rb/10HfTa Rb/30HfTa Nb-Ta L-032 A O3/4 Wpab OUTU L-034 A V1/2 L-036 A W L-037 A O-W 2-2 OUTU L-038 A W L-039 A W L-040 A W L-041 A W L-044 A O-W 2-2 OUTU L-045 A W3/4 WP WP INW L-046 A O2/3 OUTU 1 1 4 Fig 4.1.4.20 Major oxide logarithmic plot for samples from the Chitungulu sodalite syenite quarry. Note general similarity betweeen mo st of the sample s, e xcept for L-032 and L-036 . M ore discussion on t he geochemistry is included in the text. 4.1.4.5.4.7 Geochronololgy During the 1980?s, Italian geologists from the AGIP SPA Corporation establis hed t hat the nepheline syenites at the quarry cooled below 350?C at 41 3?5 Ma, based on K/Ar in biotite (Cos i et al., 1989; Cosi et al., 1992). (See Tables A22.2) . The same group dated zircons fr om the sodali t e syenit e quarry and produ c ed a U/Pb age of 458 to 427 Ma (Cos i et al., 1989; Cosi et al., 1992) . That age may still be reflecting orogenic events and not the original time of emplacement. A zircon concentrate from sample L-043 was sent to the ANU for U-Pb SHRIMP II dating and result s are not available at the time of editing this document. The new age will be correlat e d with the ot her two just described. Cores of zircons are expected to be older than previ ously thought, approximately around 750 to 780 Ma. It could provide a good time cons tra in to Katangan sedimen t ation in that portion of the Greater Lufilian Arc. 4.1.4.5.4.8 Conclusions The Chitung ul u sodalit e syenite s that occur north of the the Mwombe z h i Dome in NW Zambia formed as an anorogen i c , alkalin e ring comple x that intruded silicic l as tic Katangan meta-sed iments. Several facies of foid- be a r in g syenite s intersec t each other. The rock is quar ri ed for its strikin g cobalt - b l ue speckle d dimens i o n stone. The typical rock is a white, medium- to fine-gr a i ne d , metalu m i n ou s subleuc oc r a t ic sodic ferrif e r o us sodalite nephelin e syenite. Deep joints that enhance weathe r in g of the rock, some minor dikes and shear zones, sometimes render it useles s for extraction . A new SHRIMP II age is expected to plac e further cons trains on the time of deposition of the Katangan sequence. 0.01 0.1 1 10 100 L-036 L-032 L-034 I II L-040 L-037 L-038 L-044 L-041 L-046 L-039 L-045 III S iO 2 T iO 2 A l2O 3 Fe2O 3 MnO MgO C aO N a2O K 2O P 2O 5 1 1 5 4.1.4.6 Solwezi Dome 4.1.4.6.1 Introduction Four different rock types can be identified in the So lw ez i Dome, and relationships between them are not well exposed. According to Master, 1996, thes e are: a) Migmatit i c gneiss occurs mainly in the central part of the dome. They are composed by a garnetiferous biotite gneiss in whic h pegmatit i c leucosom e s ar e well develop e d paralle l to the gneissic foliatio n . b) A poorly-exposed leuc oc ratic two mica granite covers the northern part of the dome. Its main constituen ts are sodic plagioclase, perth itic microc line, quartz , biotite and muscovite. c) A fine-grained gneiss, which is compositionally simila r to the migmatitic gneiss, but is fine-grained, and has less well developed gneissic banding . d) Metabas i t e s occur as lozeng e - s ha p ed bodies within mega shear zones that inters ec t the other rock types. The lower units of the Solwez i Dome metased i m en t ary envelope are muscovite-hematite quartzites and schists , while the upper units are domi na n t l y marbles . Metase d i men t a r y rocks outcrop in conc en t r ic aureole s around the main body of the dome, as seen on the genera l iz ed geolog i c a l map of Fig M15. Isolat e d wedges of Katangan metasedi me n t s are mapped in the central part of the dome. 4.1.4.6.2 Sampling Outcrops of the granitoid s that make the basement of the Solwez i Dome were very diffic u lt to find in the field. Ten samples collect e d in and around the dome are list ed on Table 4.4.4.12 and shown on Fig M15. They include 3 samples from mafic intrusi ve rocks that in tersect Katangan metasediments in boreholes around the Kansanshi mine, 2 from outcrops of mafic intrus ives, and 2 from outcrop s of felsic granito i ds from the core of the dome itself. Rock name, basic geochemi s t r y and environ m en t of emplac e me n t of the sample s collect e d are listed in Table 4.1.4.13. Figs 4.1.4.1 to 4.1.4.6 are geochemic a l diagr ams of their properti es . As seen on Fig 4.1.4.1, most of the sample s are midalka l i n e . Table 4.1.4.12 Chemical Analysis of samples from the Solwezi Dome, Zambia (Complete elemental analysis on Table A7.2, Appendix) Sample SiO2 TiO2 Al2O3 FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total N o t c h 50.00 1.00 15.50 6 . 0 0 0 . 1 5 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2 . 0 0 L-063 46.39 0.84 12.95 3 . 1 0 0 . 0 9 5 . 9 5 9 . 7 1 6 . 9 7 0 . 1 5 0 . 1 2 1 4 . 1 2 100.39 L-064 47.31 0.82 12.99 3 . 2 3 0 . 1 0 5 . 7 6 9 . 3 8 6 . 8 5 0 . 0 5 0 . 1 2 1 3 . 8 7 100.48 L-065 39.63 0.57 9.98 4. 1 6 0 . 1 1 7 . 6 2 1 3 . 4 0 4 . 8 0 0 . 1 2 0 . 0 7 1 9 . 8 0 100.26 L-060a 45.83 4.36 11.86 1 7 . 8 4 0 . 2 6 6 . 2 4 9 . 4 9 2 . 2 9 1 . 1 2 0 . 4 3 0 . 3 8 100.11 L-060b 76.30 0.15 11.89 1. 79 0 . 0 4 0 . 1 4 0 . 5 3 3 . 6 5 5 . 7 4 0 . 0 4 0 . 2 8 100.55 L-060c 45.43 4.31 11.83 1 7 . 8 6 0 . 2 8 6 . 2 3 9 . 3 7 2 . 1 1 1 . 0 9 0 . 4 5 0 . 4 2 99.57 L-049 47.30 2.03 15.47 1 3 . 4 9 0 . 2 5 5 . 4 1 1 0 . 5 1 3 . 0 4 0 . 9 3 0 . 2 2 0 . 9 2 99.58 L-050 46.86 2.06 15.40 1 3 . 3 5 0 . 2 1 5 . 2 0 1 0 . 4 6 3 . 7 3 0 . 8 9 0 . 2 7 0 . 5 2 98.95 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Sm Nd Pr Ce La Hf Ta Eu Gd Yb Lu Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 50 50 15 175 95 10 120 4.0 30 7.5 1.6 L-063 4 51 19 192 7 <6 18 7 22 21 86 36 <20 <6 <15 23 25 16 L-064 4 51 19 175 7 <6 18 8 28 20 92 36 <20 <6 <15 24 16 <12 L-065 4 125 24 108 8 <6 20 8 29 12 102 45 <20 <6 <15 30 6 2 19 15 10 71 1.0 0.8 L-060a 149 64 19 128 10 31 39 20 105 396 38 477 5 4 7 0 4 2 7 9 1 1 3 61 4 1 0.6 2.7 2 . 7 0. 4 L-060b 154 64 23 141 13 <6 <6 14 25 22 <12 54 481 <6 <15 35 37 20 L-060c 24 330 38 165 27 37 39 29 101 387 33 118 L-049 13 346 30 109 17 34 46 143 119 19 296 85 127 <6 <15 31 23 <12 L-050 11 321 31 114 16 46 49 91 70 18 321 171 93 <6 <15 34 30 <12 4.1.4.6.3 Samples from the Solwezi Dome L-420 a nd L-421 come from foliate d granito i ds in the core of the Solwez i Dome (Fig M13) and were selecte d from the rock collection of the Zambian Geolog ical Survey in Lusaka. L-420 is a peraluminous subleucocratic sodic ferrife r ou s biotite granite . L-421 is a peralumi no u s mesocra ti c potassic ferrife r o us granite . It is enriche d in K, Rb, Cu, Ba, Th, Ce, La, P 2 O 5 and Ti. Both samples correlate quite well with the chemis try of Group 2 from the Kalene Hill area; both probably formed by t he same geologic a l process in the same environme n t . They might even have a similar age, but that has not been confirmed. L-420 always plots in the middle of the Group 2 cluste r , while L-421 d e v i a t es from the cluste r (See Figs 4.1.4.3 to 4.1.4.6 ) . L-420 h a s evide nc e of sodic alteration, while L-421 has eviden ce of potassic alteration. Their chemis try indicates a post-orogenic origin in the (Maniar & Piccoli, 1989) process. Neverthel e s s , if their associa t i o n wi th group 2 from the other domes is correct, they probably formed in a continental epeirogenic uplift environ ment. 1 1 6 N u m er ou s outcr o ps of gabbro and other basic rocks were observ ed , especia l l y to the east and northe as t of the Solwez i Dome. No physical relations h i ps with the hos t rocks were establi s he d due to poor outcrop . These gabbroi ds are not as defor me d as those in the Solwezi Dome, and are cons ide r e d to be mainly pod-shap e d bodies and not dikes. Table 4.1.4.13 Rock name, basic geochemistry and environment of emplacement for samples from the Solwezi Dome, NW Zambia (See acronym descript i o n on section 2.4.3.) Sample Rock Name Debon & LeFort Maniar & Piccoli Whalen Pearce Mafic Rb/10HfTa Rb/30Hf/Ta Nb-Ta Solwezi Dome L-049 Saturated olivine gabbro Metav mesoNaFe wpab L-050 Undersaturated olivine gabbro Metav mesoNaFe emor L-060a saturated olivine gabbro Metaiv mesoNaFe wpab L-060c satura t ed olivin e gabbro Metav leucoK F e wpt L-060b Granite Metaiv mesoNaFe A O L-420 Granite Peraii subleucoNaFe POG A L-421 Granite Peraiii mesoKFe POG A East of Solwezi Dome L-063 Essexite Metav mesoNaMg ? L-064 Essexite Metav mesoNaMg wpab L-065 Theralite Metav mesoNaMg arc OUTU Samples L-049 an d L-050 ar e gabbros from outcrops north of the Kansanshi depo sit. L-049 is a metalumi no us sodic ferrife r o us saturate d olivine gabbro, and L-050 is a metalu mino us sodic ferr ife r o us undersat u r a t e d olivine gabbro. The en vironmen t of emplac emen t of these rocks has been interpreted as within-plate alkali basalt and e-morb , respec tively. They are similar to L-060a , L-060c , and to a lesser degree, to L-024 . As is typical in that type of gabbroids , they contain high values for Co, Ni, Cu, Zn and V. L-060a to L-060c were collected from core in boreholes t hat interse c t intr us i v e rocks cutting mineral i z e d metased i m ents within and around the Kansans h i deposit (See Figure M13) . L-060a and L-060b were taken from boreho le s K-256 from a depth of 158.70m and 166.28m respec t i v e l y . L-060c c o me s from bore ho le K- 292 at a depth of 109.15m. A geologica l map from the ex plorat io n company that drilled at Kansan sh i (Fig 4.1.4.22 A) shows the locati on of the two boreholes. Cro ss sectio n s prepar e d by the same group to illustrate undergr o u nd geolog y around the borehol e s are show n on Figs 4.1.4.2 2 B and C. V e r y little else may be said about the saturate d olivine gabbros L-060a a n d L-060c (Fig 4.1.4.22 ) , because they are somewha t weathe r e d . They clearly intrude into Katangan rocks and produce contact metamorphic haloes. They contain anomalous Ti, P2O5, Th, Pb as well as Co, Ni, Cu, Zn and V. Variou s proc edures to evaluate the environment of emplac em e n t indica t e that the sample s formed in an anoroge n i c within- p la t e environment. N o in situ granitoids were identified in the environs of the Kansan s hi deposit . The only outcropp i n g rocks were the gabbroid s just described . L-060b is a fine- to medium- g r a in e d , metalum i no us mesocra t i c sodic ferrife r ou s biotite alkali granite with foliated texture and coar se plagioclase that makes augen. It is very similar to sample s of Group 2 from the Kalene Hill and Mwombe z h i Dome areas. If it forms part of that group, it displa ys slight hydrothe rmal alteration, as sh own on Figs 4.1.4.1 to 4.1.4.6. This rock could be a granite dike or a xenolit h transp o r t e d during intrus io n of the gabbro ic bodies into Katangan sediments. Relationships in the borehole were not clear in one way or another. The sample displays hydrothermal alteration related to potass ic enrich m en t , Ca and Fe deplet i o n and has high Sc content. The alteration observed would be reas ona b l e in any case. L-060b is a high heat producing granite, due to its high Th content. It formed in an un-defi n e d anoroge n ic environ m en t . This rock may repr es ent the basement to the Katangan rocks in the environs of the Kansanshi mine. 4.1.4.6.4 Geochronology A zircon concen trate of L-060a was dated by U-Pb SHRIMP II at approximately 750 Ma. Definitive geochro n o lo gi c a l data are not availab le at the time of editing this document. That age correlates well with SHRIMP II ages publis hed by Barron, Broughton, Armstrong & Hitzman, 2003 for a gabbro located immediately north of the Kansanshi mine. They report an age of 762?8.6 Ma. Another gabbro, from the schist and phyllite unit of the domes region da ted by Barron et al., 2003 produc ed a SHRIMP II age of 745?7.8 Ma, with metamorp h ic overgr ow t h s in zircon s whic h returned an age of 510?7.8 Ma. Similar age rocks occur throughout NW Zambia, as show n on Tables A22.3 and A22.2, and illustrated on the event diagram of Fig A24. 1 1 7 Fig 4.1.4.22 Geological map and cross sections to locate boreholes from the environs of the Kansanshi deposit, Solwezi, Zambia. Sample location is indicated on th e cross sections. Basic information obtained from Carruthers, H., personal communication, 2002. 1 1 8 4.1.4.6.5 Samples from East of Solwezi Three sample s of a pink, fine-gr a i ne d rock (Fig 4.1.4.2 3 ) were collect ed east of the Solw ezi Dome along the main road: L-063 , L-064 an d L-065 (Figs M12 and M15). Thes e were excepti ona l l y fresh and produce d a bell tinge when hammered . Field observat io n s indicate d they were a fine-gr a i ne d intrusi v e or well-ce m en t e d fine- grained volc an ic rock (Fig 4.1.1.23). Their uncommon chemis try (very high CaO, high Mg, Na, Ni, Sc, V, Pr, and extremely low Ba and Rb) was not easy to understand. The loss on ignition for the samples is high: respec tively, 14.12%, 13.87 %, 19.8%. Such high values may be related to abundant CO 2 related to a high conten t of calc ium and other carbona t es. Fig 4.1.4.23 Photographs of slabs from the samples that make L-063. These rocks are essexites, and were the freshest igneous rocks avail able in many kilometers. Other notes in text. Scales are in millimeters. L-063 and L-064 are essexites, and L-065 is a melteigit e . They all have metalumi n o us mesocrat i c sodic magnes ic charac t e r . L-063 a nd L-064 are alkaline rocks; L-065 is alkaline. The samples plot as foid gabbros and foidolite on the TAS diagram modified by Middlem o s t , 1994a. These uncommo n rocks probabl y formed in an anoroge n ic , rift-re la t e d environm e n t . 4.1.4.6.6 Conclusions The granitoi ds from the nucleus of the Solwez i Dome are similar to those of group 2 identifie d in Kalene Hill. The gabbroids that were studied in the envir ons of the Solwez i Dome were emplace d at circa 750 Ma in an anorogenic within-plate environmen t into Katangan sedim e n ts . Some of them produc ed large bodies that were able to transport xenoliths from the basement. Anoroge n ic alkali ne mafic intrus io ns (essex i t e s and meltei g i t e s ) were intr ud ed in rift-r e la t e d enviro nm e n ts east of Solwezi. 4.1.4.7 Conclusions on the Entire NW Zambia Region F o l i a t e d , peralum i n o us , leuc oc r a t ic to subleuc oc r a t ic , fe rrife r o us granite s and alkali granite s were emplace d at least from 1952 to 1913 Ma in Kalene Hill and the Kabompo, Mwombezh i and Solw ez i domes. This is probab l y the evidenc e of a major anorog e n ic magmati c event. The granitoi ds were emplac ed in a continenta l epeirog en i c uplift environ me n t . Some of the rocks contai n high Th. Some contain high Cu values. This was identified as Group 2 of Kalene Hill. Archean rocks from Kalene Hill are enriched in copper. 1 1 9 S e v e r a l Paleop r o t er oz o ic granit o id s were found to be enric h ed in copper and zinc. There is evidence of minor subductional magmatis m in Paleoproterozoic rocks of Kalene Hill. Katangan metased i me n t s were intruded in anorog en i c rift-related environments by alkaline and midalkaline rocks at the Chitungu l u sodalite syenite quarry and essexite s and me lteigites east of Solwezi. The south eas ter n portio n of the Kabomp o Dome is pros pective for IOCG mineralization. Red- altered quartz syenites with miaroli t ic cavitie s were emplace d circa 730 Ma in a continental epeirogenic uplift environment. They are intimately associated with small gabbroic bodies and massive iron oxide bodies. There might be a relatio ns h ip between IOCG systems and sedimen t a r y - h o s ted Co-Ni- Cu mineralization in that part of Zambia. Gabbroi ds that were studie d in the enviro n s of the Solwez i Dome were emplaced at circa 750 Ma in an anorogenic within-plate environmen t into Katangan sedim e n ts . Some of them produc ed large bodies that were able to transport xenoliths from the basement. 1 2 1 4.1.5 MAIN ZAMBIAN COPPERBELT 4.1.5.1 Introduction Sampling in the environ s of the Zambian Copperb e l t was carried out to establi s h the chemica l compos i t i o n of the basemen t granito i ds and to find intrusi v e rocks that cut the Katangan sediment a r y sequence . This chapter will cover the results of obser v a t i o ns and analys is for rocks from the Nchang a , Chambi s h i , Mufuli r a 1 , and Muliashi granitoids, rocks that host the Samba depos it an d some intrusive rocks that intersec t the mineralized sequence at the Nchanga mine. The projec t? s current database has 51 sample s analysed . T able A8 discrimin at e s the chemic al analyses into the differe n t areas. Coordin a t e s of all samples are listed on the Appendix A16. Their chemical analyses are pres ented on Table A8, and they are located on Figs M1, M16 and M17. Rocks from the region span a large range of lithol og i e s , mainly granitoid s, gabbroids and syenitoids (Figs 4.1.5.1 and 4.1.5.2) . In general terms, geochemis t r y for the suite of samples shows that 62% are subalka l i n e and the rest are midalka l in e . Forty percent of the total rocks are midalkal i n e , 52% are subalkal i ne and 8% are alkalin e . As show n on Table 4.1.5.1 , most of the sample s are granit es , alkali granites, granodior ites and quartz monzonites. Minor g abbroids and syenitoids constitute a sm all percentage of the rocks sampled. Table 4.1.5.1 Statistics of rock types, basement to the Copperbelt, Zambia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type Number % Granitoids Groups A l k a l i gran i t e 6 12.00 Q u a r t z m o n z o n i t e 5 10.00 S ye n i t e 2 4.00 M o n z o n i t e 1 2.00 37 . 8 4 Monzo d i o r i t e 2 4.00 M o n z o g a b b r o 3 6.00 Midalkaline Rocks A l k a l i gabbr o 1 2.00 40.00 Granite 15 30.00 G r a n o d i o r i t e 8 16.00 6 2 . 1 6 Diorit e 2 4.00 Subalkaline Rocks Gabb ro 1 2.00 52.00 Foid s yenit e 1 2.00 F o i d monzo- d i o r i t e 1 2 . 0 0 Alkaline Rocks F o i d gabbr o 2 4.00 8. 0 0 Total 50 100.00 1 0 0 . 0 0 100.00 1 The local term Mufulira has varied spelling in Englis h. Among these, ?Mufulila? and ?Mufulid a ? have also been used in the geolog ical literature. Mufulira was chosen in this document, for being the most widely used term. 4 0 4 5 5 0 5 5 6 0 6 5 7 0 7 5 8 0 SiO2% 3 4 5 6 7 8 9 1 0 1 1 1 2 1 3 1 4 1 5 1 6 1 7 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM Copperbelt Granitoids, Zambia; Lufilian G.P. (Based on Middlemost, 1994, 1997 ) Sa m ple s Pe t r o g r a p hi c fi e l ds L-07576 L-077 L-078 L-157 L-158 L-159 L-160 X-01X-02 X-03 X-04 X-05 L-155 X-42X-06 X-07 X-08 X-09 X-10 X-11 L-268 L-269 L-273 L-279 X-34 X-35 X-36 X-37 X-38 X-39 X-40 P-28 P-29 L-151 L-153 L-154 L-162 L-150 L-167L-167a L-168 L-170 L-172L-173 X-41 L-166 L-163 L-161 X-13 X-14 L - 1 6 7 an d L- 16 7 A Fig 4.1.5.1 0 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti) 5 0 0 1 0 0 0 1 5 0 0 R 2 = 6C a +2M g +A l L-07576 L-077 L-078 L-157 L-158 L-159 L-160 X-01 X-02 X-03 X-04 X-05 L-155 X-42 X-06 X-07 X-08 X-09 X-10 X-11 L-268 L-269 L-273 L-279 X-34 X-34A X-35X-36 X-37 X-38 X-39 X-40 P-28 P-29 L-151 L-153L-154 L-162 L-150 L-167L-167a L-168 L-170 L-172L-173 X-41 L-166 L-163 L-161 X-12 X-13 X-14 R1R2 PLUTONIC ROCK CLASSIFICATION Copperbelt Granitoids, Zambia; Lufilian G.P. (After De la Roche et al, 1980) P e t r o g r a p h i c fie ld s S a m p l e s Fig 4.1.5.2 Fig 4.1.5.2 0 50 100 -50 0 50 L -0 7 5L -0 7 6 L- 0 7 7 L - 07 8 L - 15 7 L - 1 58 L- 1 5 9 L - 1 60 X -0 1 X- 0 2 X- 03 X -0 5 L -1 5 5 X -4 2 X- 0 8 L -2 7 3 L- 2 7 9 X- 3 4 X -3 4 a X- 35 X-3 6 X- 3 7 X- 39 X- 4 0 P- 29 L - 15 1 L - 15 3 L -1 5 4 L -1 6 2 L- 1 6 8 L- 1 7 2 L - 1 73 X- 4 1 L - 16 6 Muliashi Porphyry trend Nchanga Granite cluster AB Diagram ( A ft e r Debo n & LeFo r t , 1994 ) Copperbelt Granitoids, Zambia; Lufilian Ar c Granitoid Project Fig 4.1.5.3 0 0.2 0.4 0.6 0.8 1 K/(Na + K) 0 50 100 150 200 250 300 350 400 450 500 B = F e + M L - 0 7 5L - 0 7 6 L - 0 7 7 L - 0 7 8 L - 1 5 7 L - 1 5 8 L - 1 5 9 L - 1 6 0 X - 0 1 X - 0 2 X - 0 3 X - 0 5 L - 1 5 5 X - 4 2 X - 0 6 X - 0 7 X - 0 8 X - 0 9 X - 1 0 X - 1 1 L - 2 6 8 L - 2 6 9 L - 2 7 3 L - 2 7 9 X - 3 4X - 3 4 a X - 3 5 X - 3 6 X - 3 7 X - 3 8 X - 3 9 X - 4 0 P - 2 8 P - 2 9 L - 1 5 1 L - 1 5 3 L - 1 5 4 L - 1 6 2 L - 1 5 0 L - 1 6 7 L - 1 6 8 L - 1 7 2 L - 1 7 3 X - 4 1 L - 1 6 6 L - 1 6 3 L - 1 6 1 X - 1 3 X - 1 4 KB Diagram (After Debon & LeFort, 1994) Co p p e r b e l t Gran i t o i d s , Zamb i a ; Greater Lufi lian Arc Gran it oid Pro jec t. S a m pl es Muliashi porphyry trend Nchanga Granite Nchanga mine Fig 4.1.5.4 Fig 4.1.5.4 0 2 0 0 4 0 0 6 0 0 . 1 0 . 2 0 . 3 0 . 4 0 . 5 0 . 6 0 . 7 0 . 8 B K 1 6b B K 19 a B K 1a B K 1b B K 1c B K 24 a B K 27 a L- 075 L- 076 L-0 77 L- 078 L- 157 L-1 58 L- 159 L- 160 X -01 X -0 2 X -0 3 X - 05 L- 155 X - 42 X - 06 X - 07 X - 08 X - 09 X - 10 X - 11 L- 268 L- 269 L- 273 L- 279 X -34X - 34a X - 35 X -3 6 X - 37 X - 38 X - 39 X -4 0 P -28 P -2 9 L -15 1 L- 153 L- 154 L- 162 L -15 0 L- 167 L -16 8 L -17 2 L- 173 X -41 L- 166 L- 163 L- 161 X -1 2 X - 13 X -1 4 Muliashi Porphyry trend Muliashi Porphyry trend Nchanga Granite cluster MgB Diagram ( A f t e r Debo n & LeFor t , 1994 ) Samples from the Copperbelt Zambia; Lufilian Arc Granitoid Project gabbroids Fig 4.1.5.5 1 2 7 4.1.5.2 Nchanga Granite 4.1.5.2.1 Introduction The Nchanga Granite is an isolated, roughly ellipsoidal body of pink to red and gray, medium- to coarse- gr a i ne d granite body that is exposed to the south of the Nchang a copper mine. That mine is the largest copper depos it in Africa, and a major mine by any standar d. A large portion of the Chingola town is built o n the Nchanga Granite. Its dimensio ns are roughly 9.5 x 15 kilometers (Figs M16 and 4.1.5.8). A comprehensive review of the Nchanga Granite, its geol og y, structur e and relation with mineraliz a t i on was publis h e d by Garlick , 1973. Armstro ng , Robb, Master , Kruger, & Mumba, 1999 dated the emplacement of the Nchanga Granite at 877?11Ma . In the past, some aut hors called the granitoid body ?Nchanga Red Granite?. This document prefers the name ?Nchanga Granite?. Among the new finding s are that the Nchanga Granite has all the charac te r i s t ic s of an anoro g en i c ring comple x, and that it might have contributed to the origin of copper in its envir ons . The Nchang a red granite , or part of it high heat producing granite that probably main tained a long-lived circulation of hydrothermal fluids. Sections 8.4.2.1 and 8.5 of this document discus s iron oxide-co p pe r - g o ld mineraliz a tio n that may be associ a t e d with the Nchang a Granit e . 4.1.5.2.2 Sampling Some new data can be interpr e t e d from the chemica l analyses compiled by Garlick, 1973, and from the evalua t i o n of sample s collec t e d and studie d for this projec t . Thirtee n samples have been analysed from th e Nchanga Granite. Nine were collected in the field; of these, three were analysed . Two reas onab l y well docume n t ed sample s with comple t e chemic a l analys i s from the center of the Nchanga Granite come from Pepper, 2000. Seven major oxide analys is, mainly from Gr ay?s quarry were extracted from Garlick, 1973. Part of them were previously disclosed in other public ations of the Northern Rhodesia Geological Survey. A sample from the deep borehole at Konkola that was put in for geotec hn ical studies of a new deep shaft correla t e s well with Nchang a Granit e rock s and was includ e d here (Table 4.1.5 . 5 ) . Fig 4.1.5.6 W-E geological cross section of underground exposure of the Nchanga Granite . Drawn along 970 level at Nchanga Mine. As show n, tw o different granitoids make the pluton . It formed a positive paleotopo graphy. Cop per mineralization exten d s six meters in to the granitoid at the site. It is partly hosted in fractures, and partly disseminated in metamorphosed pal eosol w h ere microcline lost its perthitic texture. The u nconformable character of Katangan sediments and of miner alization pinching on t o p o f t h e granitoid is also apparent. Vertical and horizontal scales are not the same, as indicated. Taken directly from Fleischer, Garlick & Haldane, 1976, p. 268. 1 2 8 4.1.5.2.3 Main Rock Types Samples analysed for the Nchanga Granite show a wide compositional variety. 73% of the granitoid s have subalkal i n e charac ter , while the rest are midalkal i n e (T able 4.1.5.2). Three quarters of the total samples are subalkal i n e rocks, the remainin g quarter is made by midalkaline rocks. Two thirds of all the samples are granit es se nsu s tricto . Table 4.1.5.2 Statistics of rock types, Nchanga Granite, Zambia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type number % Granitoids Groups A l k a l i gran i t e 1 8.33Midalkaline Rocks S ye n i t e 2 16.67 2 7 . 2 7 25.00 Granite 8 66.67Subalkaline Rocks D i o r i t e 1 8.33 72 . 7 3 75.00 Total 1 2 1 0 0 . 0 0 1 0 0 . 0 0 100.00 Table 4.1.5.3 Rock name, basic geochemistry and environment of emplacement for samples from the Nchanga Granite, Zambia (See acronym descrip t i on on section 2.4.3.) Sample Rock type Debon & LeFort Maniar & Picc Whalen Pearce Rb/10HfTa Rb/30HfTa Nb-Ta P - 2 8 Nephe l i n e s yeni t e Metal u m i n o u s iv suble u c o c r a t i c Na Fe ? VA- VA-II I INW-I N V P-29 Granit e Metalu m i n o u s iv subl e u c o c r a t i c Na-K F? VA- III INW-IN V L-151 alkal i grani t e Metal u m i n o u s iv leuc o c r a t i c K Fe RRG A W3/4 WP- III OUT U L-153 alkal i grani t e Peral u m i n o u s iii leuco c r a t i c Na-K Fe RRG A W L-154 alkal i grani t e Peral u m i n o u s ii leuc o c r a t i c K Fe ? A O-W 2-2 WP- WP-III OUT U L-162 Grani t e Peral u m i n o u s iii leuco c r a t i c Na-K Mg POG A X-34 Alkal i grani t e Metal u m i n o u s iv leuc o c r a t i c K Fe Pog-rr g X-35 Grani t e Peral u m i n o u s iii leuc o c r a t i c K Fe ? X-36 alkal i grani t e Peral u m i n o u s i leuco c r a t i c Na low Mg POG X-37 Grani t e Peral u m i n o u s iii leuc o c r a t i c K Fe ? X-38 Gran o d i o r i t e Metal u m i n o u s iv meso c ra t i c K Fe RRG X-39 Syeni t e Peral u m i n o u s i leuc o c r a t i c K low Mg ? X-40 Syeni t e Metal u m i n o u s iv leuc o c r a t i c K Fe ? 4.1.5.2.4 Samples P-28 and P-29 Accordin g to Pepper, 2000, P-28 was collected from one of many rounded inselberg outcrops near the side of the Kitwe- Ch in g o l a road. The outcrop is located roughly in the middle of the Nchanga Granite (Fig M16). It is a white to slightly pink, very coar se (>2cm crystals ), po rphyr i t i c , metalum i n o us subleu cocratic sodic ferriferous syenite. It has feldspar phenocrystals of up to 2-3 cm, no obvious mineral orientation and minor chlorite alterat i o n . It also contains clear subhedr a l to anhedra l quart z and chlor i t i z ed biot ite. Macroscopically, Pepper describ e d the rock as made of ?60% plagioc l as e , 30% quartz, 10% biotite, <5% amphiboles?. No petrogr ap h ic al work was done on it. Thin sectio ns and hand samples were not availa b l e for re-eva l u a t i o n . P-29 was collec t e d by Pepper , 2000 from large inselb e r g ou tcrops near the main road (Fig M16). Its external general appearan c e is similar to that of P-28 . It is a white to slightly pink, holocrystaline porphyritic , metalumino us subleu cocratic sodic to potassic ferrife r o us granite with minor chlorit e alterat io n of the biotite and no specific crys tal orientation. It contains porphyri t i c plagioc l as e phenocr yst a l s up to 3 cm. Macrosc op i - c a l l y , the rock is made of 55% plagioc la s e , 35% quartz, 10% biotite, <3% amphiboles. Under the micros cope, the rock is a porphyrit i c granite that cooled slow ly. Its bi otites are partially chloriti z e d , very small epidote crys- tals occur inside plagioc lase, and there is comple x intergrowth of different feldspar compos itions. A portion of 1 2 9 t h e slide studie d by Pepper contain e d abundant zircons. Microscopically th e rock is made of 40% quartz , 25% plagioc l as e , 15% perthite (micro), 10% microcline, <10% epidote, ~5% biot ite, <5% amphibole, <5% chlorite, <3-4% allanite , <2% muscovite, <2% sphene, <2% opaques (magnetite?) Based on the chemic al analysis of P-28 provided by Pepper, 2000, the rock is a nepheline syenite sens u De la Roche, Leterrier, Gandc laude, & Marchal, 1980. It plots as a syenite on the TAS diagram modified by Middlemos t , 1994. Accordin g to the IUGS softwar e to ev aluat e rock nomenc l a t ur e and calcula t e CIPW norms, P-28 is the plutonic equivale n t of a comenditi c trac hyte . That is ?a variety of peralkaline trachyte of TAS field T in which Al 2 O 3 >1 . 3 3 x total iron as (FeO + 4.4)? (LeMaitr e et al., 2002). It contains normativ e albite, orthoc las e and quartz; other minerals pres en t in order of abundance are: sodium metasilicate, diopside , acmite , hypersthene, ilmenite, hydr oxiapatite, and zircon. A strong albitiz a t i o n of the core of th e Nchang a Granit e could produc e the high Na 2 O value of P-28 . In any case, the pres ence of that amount of sodium in a rock is extrao rd in a r y . Samples P-28 and P-29 from Nchanga Granite are enric hed in all REE, Th and Cu. The chemistry of P-28 and P-29 has slightly lower silica, higher total iron oxide, Ca , Na, Ti and Mn than the rest of the rocks from the Nchanga Granite suite. P-29 falls into the Nchanga Granite general trends in the various geochem ic a l plots, while P-28 definitely has a contrasting chemistr y (Figs 4.1.5.1 to 4.1.5.5). It is interes ting to note that the MgB plot of Debon LeFor t (Fig 4.1.5.5) shows both P-28 and P-29 well within the general trend of the other Nchanga Granite rocks, although enric hment in to tal iron and magnes iu m were identi f i e d for P-28 . After comparin g the chemis tr y of sample s P-28 and P-29 us ing the isoc on diagram of Grant, 1986, both rocks actually have very similar basic chemistry. Major ch anges have taken plac e after hydrothe r m a l albitiza t i o n , especially with respect to the rare earths . The amount of Na 2 O doubled in P-28 ; it was also enric he d in total iron, P 2 O 5 , MnO, MgO, As, Pb, Ni, Rb, Zr, Zn, Y, Th, U, Pr, Sm, Dy, Gd, Eu, Sm, La, Ce and all the other rare earths. Ther e were depletio n s in CaO, Sr, Sc and Cu. K 2 O, Sc, Ba, Cr, Al 2 O 3 and SiO 2 remain e d relati ve l y cons tant. A relative change in the rock volume during alteration is not apparent, although albitization involves a net volume reduction. Several questions come to mind. What produced the severe alteration of P-28 ? Why was only that portion of the Nchanga Granite altered ? Why were the other samples not altered? L-162 does not seem to have been altered in the way that the other sample s were. Did t he alteration take plac e along the NW-SE fault that is show n on the map of Fig 4.1.5.8? Fig 4.1.5.9 Inselberg and whaleback of Nchanga Granite at the Chiwempala Hill . T his is probably the b e s t o u tcrop of th e p l u t o n . S e v eral samples were collect ed from there and from the lo w er outcrops that lie to the left of the main hill. The hill stands out due to silic ification along many intersecting shear zones. S e v eral other hills have been us e d as source for road and railroad ballast. 1 3 0 4.1.5.2.5 Samples from Chiwempala Hill One of the best outcrops of the Nchanga Granite is made by a granite inselbe r g at the Chiwemu p a la Hill, approximately 5 km south of t he Nchanga mine (Fig 4.1.5.8) . L-151 was collec te d from ther e. The rock is a metalumino us leuc oc ratic potassic ferriferous alkali granite, and was produced in a rift-rela t e d anorogen ic environm e n t . The granite massif has been subjec t to at least three distinct families of shearing in differen t directions along which quar tz veins formed. Almost every linea r meter has several quartz veins or small shear zones filled by quartz braiding. The inselberg is probably due to the dense quartz veining and silicific a t i on of the massif (Fig 4.1.5.9). Samples L-153 and L-154 come from an outcrop of lower el evatio n that lies a few hundred meters southe as t w ard from the previous l y describe d inselber g (Fig 4.1.5.8). Plagioclas e phenocry s t a ls in these outcrops are 4-5 cm in diamete r . Layers 1 to 5 meters thick of fine and coar ser - gr a i ne d porphyr i t i c rock are clearly discernible. L-153 is a slightly- fo l i a t e d , metalu mi n o us leucoc ra tic sodi c to potas s ic ferr i fer o us alkal i granite. L-154 is a peralum i n o us leuc oc r a t ic potass ic ferrif e r ou s alkali granite. The average plane of foliatio n is 130/79 ? N. This rock was produced in a rift -related anorogenic environment (Table 4.1.5.3.). L-151 and L-153 have large (up to 3 cm) angula r plagio c l as e porphyr o b l as t s with a pink nucleu s and white rim. Coar se (2-5 mm), anhedral blue quartz phenocrysts are anothe r character i s t i c feature of both samples. Fig 4.1.5.7 Geological cross sections through the Nchanga Granite . Location of the sections is indicated on Fig 4.1.5.8. Section AB, across the Nchanga mine area, shows t he main fault where the ? lamprophyre? was intruded. Katangan sediments over the Nchanga Granite we re not as severely fo l d ed as elsew h ere. Section CD s ho w s Gray?s Quarry and the C hiwempala Hill, th e l o cation of th e road, and the e x t ension of t h e fault. Note refolding of Katangan sediments on the borders of th e pluton , and that the limits of the pluton are drawn vertically. Section CD s how s s ev eral inselbergs of th e granitoid; one of them is ex ploited at Gray?s Quarry. Taken from Garlick, 1973. 1 3 1 Fig 4.1.5.8 Geological map of the Nchanga Granite . T h e n u mb ers around the p l uto n are stations measured every kilomet er for reference in the original des cription. No t e t h e l ocation of Gray?s Quarry around No . 1 3 , and the C hiwempala Hills around No . 3 7 . Parts of t h e Nchanga mine are found from Nos . 1 t o 8 . T h e ? lamprophyre? dike de scribed in the t e x t is emp laced along the fault that outcrops at the Nchanga mine in No. 6 . A s s ho w n , n u merous E- W trending fracture zones w ere identified on air photographs. There is a road that intersects the p l u t o n roughly N W - S E , and several obs ervations were made on ou tcrops along it. Main inselbergs are indicated by b lack irregular shapes. Cross sections AB and CD are included on Fig 4.1. 5 . 7 . F o liation of th e rocks that surround the Nchanga Granite is uniform in NW-SE direction: that corresponds approximately with the surface deformation of the . Figure taken from Garlick, 1973. 4.1.5.2.6 Gray?s Quarry Gray?s quarry is locate d on the NE part of the pluton, as show n on Figs M16 on the site of 2006. Samples X- 35 and X-36 that come from the typical red and grey granites at the quarry are very similar. At first glance, the only parameters that seem to vary b etween them ar e Ti and P. A closer look shows that both are peraluminous leucocratic potassic ferriferous granites. X-34 , an alkali granite, has roughly the same chemistr y as the previou s two sample s descri b ed . X-36 is a peraluminous leucoc ratic so dic low magnesic alkali granite aplite , and shows a minor enric h me n t in Na with deplet i o n s in K, Ca, Ti and Mn compar ed to the rest of the other rocks at the quarry. Garlic k , 1973 state s that the values of Na 2 O and K 2 O for sample X-34 were misplac ed by previo us author s . He exchanged the values to make them fit with the rest of the data. With the information that is now available, the original data presented by Mendel sohn, 1961 and earlier by other author s makes more sens e. It is shown on Table 4.1.5. 4 as X-34a . A higher value for soda is compatible wi th hydr othermally altered rocks that deviate from the average composi t i on . The change does not modify the TAS diagram (Fig 4.1.5.1), but transfor ms the sample from a granite into an alkali granite on the R1/R2 diagram (Fig 4.1.5.2). Other geochem ic a l diagrams show that X-34a deviate s from the main clus te r of the Nchanga Granite (Figs 4.1.5. 3 to 4.1.5.5). A compar ison of the rest of the samples colle cted in the Nchanga Granite point that the chemical analysis for X-34 is probably correct. Most of the samples cont ain K2O values around 5%. See Table 4.1.5.4. 1 3 2 Table 4.1.5.4 Exchange in values for Na and K in chemical analysis of sample X-34. Sample SiO2 TiO2 Al2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total X-34 7 6 . 7 5 0.09 11.78 0. 8 2 0 . 5 8 0 . 0 3 0 . 1 6 0 . 7 2 3 . 0 8 5 . 0 1 0.1 0.84 99.96 X-34a 7 6 . 7 5 0.09 11.78 0. 8 2 0 . 5 8 0 . 0 3 0 . 1 6 0 . 7 2 5 . 0 1 3 . 0 8 0.1 0.84 99.96 4.1.5.2.7 Various Dikes Dikes of varying composition occur on and around the Nchanga Granite. Some of them are syenitic and granodior i t i c ; others granitic . The last three sample s of Table 4.1.5.5 show completely different chemis try and are not related to the main Nchanga Granite body. They are not related to each other either. X-39 (Gray?s quarry pegmati t e microc l in e ) and X-40 (Nkana vein adular i a) are similar to each other in general composi t i o n . They plot as syenites on the R1/R 2 and TAS diagrams . X-39 is a peralu m i n ous leuc oc r a t i c potass ic magnes ic syenite, while X-40 is a metaluminous leucocratic potassic ferr if e r o us syenite . They are both enriched in potash and could be potassi c segr ega t i o n s of the general Nchanga Granite body. X-38 , described by Garlick as a biotit e - r ic h schlie r en rock from Gray? s quarr y , is a bizzar e mafic rock of the type called lamprop h y r e in the Copperbelt. It plots as a metaluminous mesocratic potass i c ferrif er o us granod io r i t e . These dikes seem to be related to the Nchanga Granite, as late intrus ions in the sys tem. L-168, L-170 , L-171 , L-172* and L-173 are other dikes that will be discussed in the next chapter. L-172* and L-173 ar e extreme l y similar in compos i t io n to rocks from the Nchanga Granite. But they have to be younger, because they intersec t Katangan sediment s . 4.1.5.2.8 Geochemistry Table 4.1.5.5 Chemical analysis of samples from the Nchanga Granite and others in the basement to the Zambian Copperbelt (complete elemental analys es are on Table A8.4, Appendix) No. SiO2 TiO2 Al2O 3 FeT MnO MgO CaO Na2O K2O P2O5 LOI Tota l Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th X-3 4 76. 75 0.0 9 11. 78 1.4 0 0 . 0 3 0.1 6 0.7 2 3.0 8 5 . 0 1 0 . 1 0 0 . 8 5 9 9 . 97 X-34 a 76. 75 0.0 9 11. 78 1.4 0 0 . 0 3 0.1 6 0.7 2 5.0 1 3 . 0 8 0 . 1 0 0 . 8 5 9 9 . 97 X-35 76. 84 0.0 8 10. 70 1.3 0 0 . 0 4 0.1 0 0.8 0 2.3 0 4 . 9 0 0 . 0 2 0 . 8 4 9 7 . 92 X-36 76. 90 0.0 1 12. 30 0.6 0 0 . 0 1 0.1 0 0.5 0 3.6 0 4 . 4 0 0 . 0 4 0 . 4 3 9 8 . 89 X-37 78. 20 0.0 4 10. 30 1.1 0 0 . 0 4 0.1 0 0.7 0 2.2 0 4 . 9 0 0 . 0 1 0 . 5 3 9 8 . 12 L-16 2 76. 11 0.1 9 12. 33 1.2 5 0 . 0 0 0.2 8 0.7 0 3.4 8 4 . 9 2 0 . 0 3 0 . 5 9 9 9 . 88 1 1 9 1 5 5 1 4 9 6 1 0 6 <6 7 22 13 17 1 5 7 9 3 <6 <15 L -1 5 1 77. 00 0.1 0 11. 82 1.6 7 0 . 0 3 0.1 7 0.1 1 3.4 7 5 . 5 4 0 . 0 2 0 . 5 1 1 0 0 .4 4 3 5 1 3 2 1 5 8 1 9 7 9 1 1 0 8 42 39 24 <12 4 2 4 4 1 1 1 6 5 L -1 5 3 77. 40 0.0 7 11. 91 1.6 5 0 . 0 3 0.1 2 0.2 7 3.5 1 4 . 8 9 0 . 0 1 0 . 5 1 1 0 0 .3 7 4 3 8 2 5 1 1 7 1 0 6 7 0 <6 8 58 33 24 <12 6 0 2 3 6 1 1 4 4 L -1 5 4 77. 07 0.0 7 12. 06 1.2 2 0 . 0 0 0.0 0 0.2 5 3.0 7 5 . 7 8 0 . 0 1 0 . 5 0 1 0 0 .0 5 4 7 8 2 7 6 8 1 2 2 5 8 7 <6 17 22 23 <12 <1 2 2 5 5 <6 44 P -2 8 68. 49 0.3 4 12. 40 3.4 3 0 . 1 2 0.2 6 1.0 6 8.7 4 5 . 3 2 0 . 1 1 0 . 1 3 1 0 0 .2 7 3 4 5 5 8 6 1 7 2 6 1 6 4 3 4 19 <3 97 24 <4 8 68 9 1 3 9 8 P -2 9 72. 84 0.3 1 13. 07 2.7 1 0 . 1 1 0.1 9 1.2 8 4.0 4 5 . 5 6 0 . 0 8 0 . 1 7 1 0 0 .1 9 2 7 8 7 9 8 9 1 8 3 4 6 3 8 3 6 58 22 <4 8 72 4 9 6 5 X-3 8 59. 80 1.1 0 10. 40 12. 6 0 . 3 0 0.6 0 4.3 0 1.7 0 2 . 9 0 0 . 0 8 1 . 0 6 9 4 . 84 X-3 9 66. 60 0.0 1 18. 00 0.2 0 0 . 0 2 0.0 3 0.2 0 2.4 0 1 1 . 90 0 . 0 1 1 . 1 3 1 0 0 .5 0 X-4 0 64. 80 0.0 1 16. 70 0.4 0 0 . 0 1 0.0 3 0.1 0 0.7 0 1 5 . 50 0 . 0 0 0 . 0 0 9 8 . 25 The suite of sample s from the Nchang a Granit e crosses the fields of alkalin e to non-alk a l i ne rocks. That happens especia l l y on the TAS diagram (Fig 4.1.5.1 ) . All samples are leuc oc r a t ic and only two (28 and 29) are subleu cocratic . All samples from the Nchanga Granite that were analysed fo r Th are strong l y enriche d in it; to a point that they are all high-he a t produc in g granit o i ds . Most of the sample s from the Nchang a Granite contain high values of K 2 O. They are all leucoc ra t i c in char ac t e r and tend to be ferric accordi ng to the MgB Debon LeFort diagram . L-151 , L-153 , L-154 , P-28 a n d P-29 a l l have very simila r chemic a l signat ur e. They contain high values for K 2 O, Sc, Ba, Cr, Al 2 O 3 , SiO 2 . Maybe all the samples from the Nchanga area carry that same chemical signat u r e . U Samples L-151 , L-153 and L-154 (more foliate d) display lower Ca values than the first four samples , but correla t e well with them in the various plots (Figs 4.1.5. 1 to 4.1.5.5 and logarithmic pl ots of Figs 4.1.5.10 and 4.1.5.11). As shown on the table above, L-162 has very simila r major oxide chemistr y to the rest of the samples from the Nchanga Granite. It falls neatly into the trends of the Nchanga Granite in the various plots (Figs 4.1.5.1 to 4.1.5.5). That body was intersected in the Konkola deep bo reho l e that is describe d later on in this chapter . It 1 3 3 could cons titute an apophysis of the Nchanga Granite body, or another isolate d anoroge n ic plutoni c body tha t formed in a similar envir onm e n t and intrude d in to the Muliashi Porphyry. Nevertheless, L-162 d o e s not show any of the minor eleme n t and rare ea rth enric h me n t that is eviden t in ot her sample s from the Nchang a Granit e (Table 4.1.5.5). L-162 correlate s very well with X-36 , the gray granite of Gray?s quarry . Maybe these two rocks are isolated repr es entatives of the original composition of th e Nchanga Granite that was turned pink by subs equent hydrothermal alteration. Plot MgB of Debon LeFort shows that L-162 suffered minor alteration. Maybe sample L-162 has the original, unaltered Nchanga Granite chemistr y. That hydrothe r m a l enrichme n t probably is not pres ent in apophyses of the Nchanga Gr anite. Samples from the Nchanga Granite plot as an elongat ed clus ter on the R1/R2 diagram, as a curved line on the TAS diagram, as a cluster on the BMg diagram, and as a trend on the KB diagram (Figs 4.1.5.1 to 4.1.5.5). Fig 4.1.5.10 Logarithmic scale plot of major oxid es to compare Nchanga Granite with Nigerian and Namibian granitoid ring complexes. A l l major oxides behave in roughly t he same way. Only M g , Mn and P 2 O 5 are higher in the Nchanga Granite. The first twelv e samples, u p t o K D 1 2 come from Nigerian granitoids; the last five (X-92 to X-96 ) come from Namibian gran itoids. X-34 t o L - 1 73 come from the Nchanga Granite. Same numbering scheme and order for Figs 4.1. 5 . 1 1 and 4.1.5. 1 2 . F or more deta ils, see Table 4.1.5.6. 1 3 4 Fig 4.1.5.11 Logarithmic scale plot of minor elemen ts and rare earths to compare Nchanga Granite with Nigerian and Namibian granitoid ring complexes. Note that the Nchanga Granite has higher Ba and Cu values . The ranges for Zr are equivalent. Fig 4.1.5.12 Logarithmic scale plot of minor elemen ts and rare earths to compare Nchanga Granite with Nigerian and Namibian granitoid ring complexes. N o t e t hat Sr and Rb are roughly e qual; Zn is lower; Nb and Ce are slightly lower. 1 3 5 4 .1.5.2.9 Anorogenic character of the Nchanga Granite Many separate observat i on s lead to conclude that the Nchanga Granite is an anorogen i c ring complex. The following section will presen t that evidence. First of all, the shape of the Nchanga Granite is charac teristic of slightly deform e d anorog en ic ring complex e s . The map of Fig 4.1.5.8 was carefull y prepared followi n g outcro ps along the outlin e of the Nchanga Granite. Figs 4.1.5.7 show geologic a l l y - c o n tr o l l e d cross section s through that map. Cross sections draw n by other authors also maintain the same general pattern for th e Nchanga Granite (Figs 4.1.5.13): cylindrical geometry with subver tical walls. The pluton acted as a ri gid buttres s against which the surroun d in g sedimen t s flow ed and folded, as indicated in Fig 4.1.5.7 and 4.1.5.13 . The oval shape displayed by the pluton is a feature commonl y obs erved worldw i d e in granitic anor ogen i c comple xes that have been subjec t to slight defor mation. Numer ou s examp l es of simila r bodies are found in Bonin, 1986; Nuelle, Day, Sidder, & Seeger, 1992; and Wooley, 2001. Chemistry of biotite granites from the Nigerian anor ogen ic ring complex es and from some of the Namibia n Mesoz o ic grani ti c ring compl e xe s shows signi fic a n t sim ilar i t i es with samples from the Nchanga Granite (Table 4.1.5.7, Fig 4.1.5.10). High values for Rb, Y, Nb, Th , Pb, Ce and La are all present in analysis from the Nchanga Granite. Equivalent figures occur in sample s from Spitskopp e and Erongo Namibian granitoi d ring anorogen i c complexes . Samples from the Nchanga Granite contain more Ba and Cu (Fig 4.1.5.1 0 A ) . Zn, Nb and Ce are slight l y lower in the Nchanga Granit e (Fig 4. 1.5.10B). All other values for ranges of the elemen ts public l y availab l e are similar . This is another obse rvation that supports the hy pothesis that the Nchanga Granite is an anorogen i c ring complex . L-162 does not have the chemica l signat ure of the rest of the samples from the Nchanga Granite. It does not contain high Rb, Y, Nb, Th, Pb, Ce or La, although the major oxide composition is akin to that of the rest of the sample s from the suite . L-162 might be an apophyse s of the main Nchanga Granite that was subjec t to depletion in some elements. If this hypothesis is true, then the original rock contained low Sr and Ba, while most of the rest of the metals and minor elements were depleted by later proc esses. Table 4.1.5.6 Comparison of chemical data from anorogenic ring complexes and the Nchanga Granite ( C o mp l e t e trace element analysis on Table A8.4 ) Sam ple SiO 2 T iO 2 Al2O 3 F e2O 3 FeO FeO t MnO MgO CaO Na2O K2O P2O 5 LO I T otal Rb Sr Y Zr Nb Cu Zn V Ba T h Pb Ce La Hf Nigerian granitoid ring complexes AMN 24 72.6 0 0.29 14.0 7 0.90 1.73 2.63 0.07 0.43 1.01 3.36 5.74 0.07 0.47 100. 74 185 100 63 246 57 61 9 362 27 22 144 59 6 RN75 75.9 0 0.11 12.8 5 0.33 1.05 1.38 0.05 0.02 0.24 3.91 4.31 0.01 0.88 99.6 6 979 15 696 399 214 120 376 0 109 111 56 296 234 28 PAN 112 73.9 0 0.15 14.8 8 0.43 0.80 1.23 0.02 0.67 0.43 3.98 5.17 0.02 0.61 101. 06 192 28 117 234 88 0 80 25 22 195 189 7 J O N147 73.2 0 0.18 14.1 8 0.67 1.19 1.86 0.02 0.08 0.73 3.45 5.32 0.03 0.98 100. 03 296 38 227 330 118 126 0 264 41 38 251 218 8 B34 76.0 0 0.10 11.7 4 0.37 0.89 1.26 0.02 0.09 0.83 3.78 5.77 0.04 0.24 99.8 7 574 4 115 141 158 60 12 39 40 74 114 64 5 MD33 3 75.4 0 0.10 13.3 3 0.01 0.96 0.97 0.02 0.04 0.34 4.26 4.53 0.01 0.20 99.2 0 620 0 139 129 78 9 68 0 0 66 70 79 28 9 NG 208 75.7 0 0.20 13.1 8 1.48 0.01 1.49 0.03 0.09 0.44 3.41 5.10 0.01 0.66 100. 31 318 29 75 186 80 70 2 151 63 57 156 83 7 T 15A 74.3 0 0.08 11.7 4 0.33 0.89 1.22 0.02 0.01 0.26 3.88 4.59 0.01 0.64 96.7 5 502 1 86 166 132 7 61 3 0 69 37 153 166 7 DR11 76.7 0 0.14 13.3 6 0.00 1.16 1.16 0.03 0.05 0.33 4.41 3.58 0.02 0.34 100. 12 966 0 87 81 119 103 4 0 61 47 149 88 9 DW 1 78.0 3 0.06 12.1 4 0.33 0.89 1.22 0.01 0.09 0.52 4.59 3.56 0.01 0.42 100. 65 389 22 356 207 205 77 0 71 42 16 275 169 10 F G 5 77.4 4 0.08 11.9 9 0.37 0.87 1.24 0.02 0.07 0.49 3.89 4.45 0.01 0.34 100. 02 347 3 189 161 148 42 0 43 39 27 117 64 8 KD12 76.5 0 0.10 12.8 3 0.35 0.84 1.19 0.02 0.07 0.46 4.17 4.39 0.01 0.34 100. 08 283 4 144 147 96 48 0 4 36 41 62 27 6 Nchanga Granite X - 34 76.7 5 0.09 11.7 8 0.82 0.58 1.40 0.03 0.16 0.72 3.08 5.01 0.10 0.84 99.9 6 X - 34a 76.7 5 0.09 11.7 8 0.82 0.58 1.40 0.03 0.16 0.72 5.01 3.08 0.10 0.84 99.9 6 X - 35 76.8 4 0.08 10.7 1.3 1.30 0.04 0.10 0.80 2.30 4.90 0.02 0.69 97.7 7 X - 36 76.9 0.01 12.3 0.6 0.60 0.01 0.10 0.50 3.60 4.40 0.04 0.35 98.8 1 X - 37 78.2 0.04 10.3 1.1 1.10 0.04 0.10 0.70 2.20 4.90 0.00 5 0.44 98.0 25 P- 28 68.4 9 0.34 12.4 0 3.43 3.43 0.12 0.26 1.06 8.74 5.32 0.11 0.13 100. 27 345 58 617 261 64 <3 97 <4 689 98.0 61 600 383 11 P- 29 72.8 4 0.31 13.0 7 2.71 2.71 0.11 0.19 1.28 4.04 5.56 0.08 0.17 100. 19 278 79 89 183 46 6 58 <4 724 65.0 53 204 101 6 L- 151 77.0 0 0.10 11.8 2 1.67 1.67 0.03 0.17 0.11 3.47 5.54 0.02 0.51 100. 44 351 32 158 197 91 42 39 <12 441 65.0 167 49 7 L-153 77.4 0 0.07 11.9 1 1.65 1.65 0.03 0.12 0.27 3.51 4.89 0.01 0.51 100. 37 438 25 117 106 70 58 33 <12 236 44.0 87 38 L- 154 77.0 7 0.07 12.0 6 1.22 1.22 0.00 0.00 0.25 3.07 5.78 0.01 0.50 100. 05 478 27 68 122 58 17 22 <12 255 44.0 90 4 4 L-162 76.1 1 0.19 12.3 3 1.25 1.25 0.00 0.28 0.70 3.48 4.92 0.03 0.59 99.8 8 119 155 14 96 10 7 22 17 793 <15 82 37 L- 172 74.4 2 0.06 13.0 7 1.32 1.32 0.04 0.21 0.14 1.85 7.48 0.06 0.71 99.3 6 316 32 49 113 85 242 23 <12 668 48.5 27 79 50 5 L- 173 74.6 9 0.09 12.5 5 1.37 1.37 0.03 0.28 0.14 1.87 7.51 0.05 0.78 99.3 6 314 29 78 172 128 232 20 <12 598 58.0 85 49 Spitzkoppe Complexes, Namibia X - 92 76.9 9 0.1 11.7 3 2.06 2.06 0.02 0.08 0.74 3.03 5.23 0.02 0.52 473 14 157 196 141 3 44 2 75 148 84 X - 93 76.0 4 0.04 12.8 3 1.57 1.57 0.02 0.04 0.62 3.89 4.93 0.01 0.46 604 2 208 112 88 3 58 6 9 63 26 X - 94 75.6 7 0.04 12.9 4 1.71 1.71 0.02 0.05 0.65 4.05 4.84 0.02 0.45 620 1 214 128 83 4 45 2 2 54 21 X - 95 69.7 5 0.51 12.5 5 5.77 5.77 0.08 0.11 2.30 2.55 6.29 0.09 1.38 243 81 68 474 24 - - - 1051 162 77 Erongo Complex, Namibia X - 96 76.2 6 0.07 13.3 1.43 1.43 0.03 0.06 0.43 3.08 5.07 0.26 - 637 25 155 60 26 2 38 76 The following diagrams illustrate the small range of variation for the ma jor oxides, minor elements and some rare earths . When plotte d on a logarit hmi c scale, val ues for major oxides and minor elemen t s are compar ab l e . These rocks, as seen, have striki n g simila r i t i e s in their chemic a l charac t e r . 1 3 6 There might have been some reactivation of magmatis m in the Nchanga Granite at the Nchanga mine after the emplacement of the Katangan sedim ents , and after copper- c ob a l t mineral iz a t i o n . The dikes L-168, L-170, L-172, and L-173 seem to be chemic al l y related to th e Nchanga Granite as show n on Table A.8. L-172 and L- 173 have similar minor element chemis t r y to the Nchanga Granite chemistr y , except that they contain high values of chrome and copper , lower Na 2 O and higher K 2 O. Sr and Rb are in the same ranges. Zn is lower, and Nb and Ce are slightly lower. After taking a closer look at the Nchanga Granite, the following ques tions come to mind: 1) Are ther e many more Nchanga- l i k e plutons under Katang a n rocks in the Zambia n Copper be l t ? 2) Could the anorog en i c ring comple x of the Nchang a Granit e may be in some way respon s i b le for copper mineralization at the Nchanga mine? 3) Could an iron oxide- c o pp e r - g o ld minera l deposi t ha ve formed on the upper portion of the Nchanga Granite before eros ion ? 4) Could the copper in at least part of the Za mbian Copperbelt have been produced by the event of emplac eme n t of the Nchanga Granite and later eroded an d re-mobilized to favorable stratigraphic-redox tr ap s in the Katangan sediments ? Figure A26 shows an event diagram of the radiome t r ic ages availab l e from the Nchanga mine area. 4.1.5.2.10 Conclusions 1. The Nchang a Granit e has all the char ac t er is t i c s of an anorogenic granite ring complex. It probably formed as a granit e plug in an anoroge n ic ring comple x clus te r 2 that is not well exposed, and lies in the basemen t of the Zambian Copperbelt. 2. Chemistry of the Nchanga Granite crosses t he fields of midalkal i n e to subalkal i n e rocks. 3. The pluton behaves as a coherent cluster in all geochemical diag rams . 4. The pluton , or parts of it, are high heat produci n g granites that probabl y maintai n e d a long-liv e d circulati o n of hydrothermal fluids. 5. The Nchanga Granite might have contributed to the origin of copper in its environs . 2 The term anorogenic ring comple x clus ter will be introduc e d in chapter 7. 1 3 7 4.1.5.3 Nchanga Mine Area 4.1.5.3.1 Introduction Several dikes that evidently intersec t the mineralized Katanga n sedimen t ar y sequenc e in the environ s of the Nchanga mine were sampled in borehol e s at the Nc hanga mine core warehou s e . The borehol es , samples collec t e d and depths are listed on Table 4.1.5.7. Results of t he chemical analysis are listed on Table 4.1.5.9. Interpretation of the major oxide chemistr y and detaile d geochemical parameters are listed on Table 4.1.5.8. The rocks sample d were not fres h, but weathe r e d and alte red. In any case, the best rocks were chos en for zircon pickin g. Table 4.1.5.7 Borehole samples collected in the environs of the Nchanga open pit mine, Zambia. ( u n derlined sample n u mb ers indicate chemical analysis) Sample Borehole depth (m) Field description R1R2 nomenclature Shrimp II age (Ma) L-167a N O P - 6 8 1 52.70 Weathe r e d granit o i d Essexi t e L-168 N O P - 6 8 1 33.00 Weath e r e d grani t o i d alkal i grani t e L-169* N O P - 6 8 1 105.00 Weathe r e d granit o i d alkali granit e 765?3 emplac e m e n t age; 1860?1 0 inhe ri t e d zircon L-170 N O P - 6 8 1 43.55 Weather e d granit o i d Granite L-171 N O P - 8 3 6 302.9 0 Basal polym i c t i c sedim e n t a r y brec c i a n.a. L-172 N O P - 5 8 9 76.41 Grani t o i d dike alkal i grani t e L-173 N O P - 5 8 9 74.28 Grani t o i d dike alkal i grani t e L-172c* N O P - 5 8 9 compo s i t e compo s i t e of L-1 72 and L-173 alkal i grani t e 765?3* 3 empla c e m e n t age Table 4.1.5.8 Rock name and main geochemical parameters of samples from the Nchanga Mine ( S e e acrony m descrip t i o n on sectio n 2.4.3. ) Sample Rock type Debon & LeFort geochemical characteristics L - 1 5 0 Syeno - d i o r i t e dike Peral u m i n o u s iii mesoc r a t i c K high Fe L-167 a Syeno - d i o r i t e dike Peral u m i n o u s ii mesoc r a t i c K high Fe+Mg L-168 * Alkal i grani t e Peral u m i n o u s I leuco c r a t i c K Fe L-170 Grani t e Peral u m i n o u s I mesocr a t i c K Mg L-172 * Alkal i grani t e Peral u m i n o u s I leuco c r a t i c K Fe L-173 Alkal i grani t e Peral u m i n o u s I leuco c r a t i c K Mg Table 4.1.5.9 Chemical analysi s from the Nchanga Mine environs Sample SiO2 TiO2 Al2O3 Fe2O3 MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Notch 50.00 1. 0 0 15.50 6. 00 0.1 5 0 2 . 0 0 5 . 0 0 4 . 9 0 5 . 50 0.30 2.00 200 400 60 360 40 L-150 51.05 2 . 9 1 15.47 10.19 0 . 0 0 1 0 . 0 9 0 . 6 8 1 . 6 9 6 . 1 2 0 . 3 6 1 . 1 6 9 9 . 7 2 361 24 45 150 28 L-167 47.14 0 . 7 8 19.71 6.10 0. 0 8 1 2 . 9 8 0 . 0 0 0 . 0 0 8 . 7 0 0 . 0 8 4 . 0 0 9 9 . 5 7 255 64 101 781 147 L-168 79.68 0.15 10.06 0. 72 0. 0 2 0 . 1 0 0 . 0 2 0 . 1 9 7.61 0.08 0.59 99.22 132 125 19 258 11 L-170 70.45 0.8 6 15.35 3.22 0. 0 3 1 . 5 0 0 . 0 1 0 . 0 2 5 . 0 2 0 . 1 3 3.05 99.64 110 46 42 320 79 L-172 74.42 0.06 13.07 1. 32 0. 0 4 0 . 2 1 0 . 1 4 1 . 8 5 7 . 4 8 0 . 0 6 0 . 7 1 9 9 . 3 6 316 32 49 113 85 L-173 74.69 0.09 12.55 1. 37 0. 0 3 0 . 2 8 0 . 1 4 1 . 8 7 7 . 5 1 0 . 0 5 0 . 7 8 9 9 . 3 6 314 29 78 172 128 Sample Co Ni Cu Zn Ga V Cr Ba U Th Sc Sm Nd Pr Ce La Ta Eu Gd Yb Lu Notch 30 16 25 85 26 100 100 1300 20 37 20 50 50 15 175 95 120 4 30 7.5 1.6 L-150 851 191 623 66 24 424 94 349 6 <15 29 13 13 55 18 7 221 0.263 1.250 L-167 266 57 1896 65 28 95 74 615 12 37 12 43 13 L-168 32 <6 261 10 <9 16 59 1190 <6 <15 <10 10 61 1 0.175 0.48 L-170 131 14 1954 25 29 92 335 766 10 <15 11 6 26 30 44 21 46 0.188 1.963 1.413 0.888 L-173 11 6 232 20 22 <12 453 598 7 58 <10 85 49 Samp le Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb S m Nd P r Ce La Cs Hf Ta Eu Gd Tb Dy Ho Er Tm Yb L u No t c h 30 16 25 85 26 100 100 1300 2 0 3 7 2 0 2 0 5 0 5 0 1 5 1 7 5 9 5 3 1 0 1 2 0 4 3 0 5 20 3 9 36 8 2 L -1 7 2 9 8 242 23 21 <12 618 668 5 4 8 <1 0 27 9 4 1 1 1 7 9 5 0 1 5 3 0 7 1 10 2 7 1 7 1 As seen on Table 4.1.5.9 , most of the samples hav e high potassiu m values, and all of them contain anomalo us copper . That could have been brought recent ly, as impregnations in microfractur es due to migration of copper-saturated fluids. Cobalt va lues may have been increased in a similar way. 3 Radiom e t r ic age data marked with an asteris k has not been completely determined. These should be cons idered preliminar y data obtained by the U-Pb SHRIMP system on zircons . Most of this work was done at the ANU in Canberra. 1 3 8 L - 1 70 , L-172 and L-173 contain high chromiu m . L-172 and L-173 have almost identic a l values for all element s . Their macrosc o p ic feature s were also similar . L-167 and L-170 have high values for losses on ignitio n . Three samples contai n enough thoriu m to make them high heat producin g granite s : L-167, L-173 and L-172 . 4.1.5.3.2 Comparison of Gabbroid Rocks L-167a and L-150 are both syeno- d i or it e s and they seem to be similar to alkaline mafic rocks L-161 a n d L- 163 f r o m the Konkola deep boreho l e descri be d unde r the Muliash i Porphyr y section (4.1.5. 4) . Both groups of mafic rocks were emplac ed in ext ensi on a l environ m e n ts . Thus both the Muliashi Porphyry around Konkol a and the Katang a n rocks in the enviro n s of the Nchanga mine were intrude d by rocks of similar compostion. Maybe the chemical similarities of these rocks are mere coinci de nce and they were emplac ed at different times. Maybe they are all from t he same event of mafic dikes. That is not complete l y well understood yet, and only L-150 was observed in the field. If t he rocks happe n ed to have been empla c ed during the same event, then ther e would be several coincide nc es between the Nchanga and Konk ola areas: the mafic rocks and the Nchanga - l ik e granite s . All four sample s (L-150, L-161, L-163, L-167a) have high alumina values L-150, L-161 and L-163 hive high Co, Ni, V, Ti and contain Na and Ca. L-167a has high Y, Zr, Nb, Ca, Cu, Th, K. No Ca or Na. L-150, L-161 and L-167a have high K L-150 has high Cu L-161 and L-163 have low Cu L-150, L-161 high Rb/Sr L-163 low Rb/Sr high Mn, low K 4.1.5.3.3 Nchanga Lamprophyre Dike One of the main structures of the Nchanga open pit is the so-call ed ?lampro p h y r e dike?. It outcrop s on the southe r n wall of the pit, and has been reas ona b l y well documen t e d in the literat ur e (Figs 4.1.5.6, 4.1.5.13, 4.1.5.7, 4.1.5.8). According to the mine geolosits, it normally contains 3-7% Cu, higher grade than most of the orebody. A well-loca t e d sample of the dike was colle cted, its coor dinates are listed in the Appendix. Fig 4.1.5.13 WSW-ENE Schematic geological cr oss section throgh the Nchanga Granite along the Nchanga mine, Zambia . N o t e t h e f o l ds o f Katangan sediments o v er the Nchanga pluton, the normal faults, and the irregular paleotopography of the granitoid surface. Sedimentary beds were strongly folded around the pluton. The ?lamprophyre? dike is illustrated to t he right of the image. Taken from Garlick, 1973. L-150 is an extremely fres h, highly micaceou s, 5-15 m wide, peralum in o us potassi c ferrifer o us syenodio r i t e dike with very slight foliation. It does not show alte ration like the surrounding rocks. As observed on the pit face, it was intruded into highly sheared rocks with abundant hydrother m a l ism , along a pre-exi s t i n g shear zone. The Katangan sediment s that over lie the Nchanga Granite display major drag folds towards the shear zone. This was seen on outcrop and is show n on the vari o us maps and cross secti o ns (Figs 4.1.5.6, 4.1.5.13, 4.1.5.7, 4.1.5.8). Abundant thin hy drothe r m a l quar tz veins cut the near by mineral i z e d Katanga n host rocks, but the gabbro is not altered or cut by any signifi c an t quartz veins. The contact of L-150 with the Nchanga Granite is chilled; it has quartz recrysta llization and a halo of contact alteration. T he dike does not seem to have been subject to shearin g or hydr oth e r ma l alterat i o n , nor seems to have been subject to major fluid flow. The mafic dike is full of secondary Cu miner als that impregna t e both matrix and surfac es . 1 3 9 4.1.5.3.4 Samples with Special Character L-168 , L-172 and L-173 are a complet e l y indepen de n t group of ro cks; different from the Muliashi Porphyry and the Nchanga Granite. They follow a leuc oc ratic trend on t he KB diagram , and it is not related to neither of the trends of the Nchanga Granite or the Mu liashi Porphyry. It simply runs parallel. The L-168 , L-172 , L-173 t r e n d on the MgB diagram seems to run along the cr itical or common Mg-Fe line of Debon & LeFort. 4.1.5.3.5 Geochronology Two intr us i v e rocks that interse c t Katanga n sedim ents under the Nchanga open pit were dated by the SHRIMP II method at approximately 765 Ma. Thes e are L-169 and L-172c . Detail s of the sampli n g sites and sample numbers are listed on Table 4.1.5.7 . An inherit e d zircon in L-169 gave and age of 1860?10 M a . L-169 is very similar to sample L-168 . In principle, the SHRIMP ages of L-172c a n d L-169 are within error of each other. They define an intrus ive event, or at least one of the last intrus ive events in the environs of the Nchanga copper mine. The new ages are very significant, because they pr ovide the oldest age of depositi o n for the Katanga sediment a r y sequence at Nchanga. That is a significa n t brac ket for the deposit i o n and mineral iz a t i on . If funds become available, the lamproph yre of L-150 should be dated. It could provide another age constra i n for copper mineral iz a t i on at Nchanga . Below is a list of the new radiometric SHRIMP zirc on U-Pb ages obtained in the northern portion of the Copperbelt. These all plotted in the ev ent diagram of Figs A29 and A27. Table 4.1.5.10 New SHRIMP U-Pb ages from the Copperbelt area, Zambia Number Field description of sample Age (Ma) L - 1 7 2 c Alkal i grani t e dike in a boreho l e 765?3* 4 L - 1 6 9 Alkali granit e dike in a boreho l e 765?3* L - 1 6 9 Dike in a boreho l e , inheri t e d zircon 1860?1 0 L - 0 7 5 Rapak i v i grani t e from the Mulia s h i Porph yr y 1865? 5 . 4 L - 1 6 0 Undefo r m e d light gra y granit o i d fr om the Mulias h i Porph yr y in the Konkol a deep bor eho l e 1866?5 . 4 L - 1 5 8 Folia t e d pink gra ni t o i d from the Mulia s h i Porphy r y in the Konkol a de ep boreho l e 1874?1 4 4.1.5.3.6 Conclusions M a f i c rocks studie d in the Nchang a mine area were emplace d in anoroge n ic extensio n a l envir on me n t s . Alkali granit e dikes studied do not seem to be direct l y related to the Nchanga Granite . They formed in an extensional, anorogenic environment. New radiometr i c ages of the felsic , midalk a l in e dikes (~765 Ma) provide an oldest age of deposit i on for the Katanga sedimentary sequence at Nchanga. That also provides a significa n t brac ket age for mineraliz a tio n . 4 Radiom e t r ic age data marked with an asteris k has not been completely determined. These should be cons idered preliminar y data obtained by the U-Pb SHRIMP system on zircons . Most of this work was done at the ANU in Canberra. 1 4 0 4.1.5.4 Muliashi Porphyry 4.1.5.4.1 Introduction Muliashi Porphyry is the name given to some of the co arse- gr a in e d to porphy r i t i c granitoid s that make the basement to the Katanga sedimentar y rocks throughout mo st of the Copperbe l t area. In some public a t io n s this body is refered to as the ?gray granite?. The rock is often a pink granite, due to minor natural variations in chemic al composition and overprint ed potassic alteration. Sometimes the granites vary into gneisses; and they often have sub-sphe r ic a l 1.5 to 6 cm diameter felds par porphyroblas ts that grew over a previous foliated texture with abundant biotite. Major oxide chemic al analys is of these rocks were provid e d by Mendels o hn , 1961 and are listed on Tables 4.1.5.24 and 4.1.5.11. This body of granites is widely spread in the base ment to the Copperbelt. Similar gray and gray-pink granito id s are observe d as basemen t around Konkola (o ld Bancroft area), Chambishi, Mufulira, Nkana and around the Roan Antelope mine. Chemis try from the vari ous sites indica t e s a large similar i t y betwee n them. This sub-chapter will review the main observations and findings from geochemic al studies and geochronology in those rocks. Table 4.1.5.11 Chemical analysis of sampl es from the Muliashi Porphyry, Basement to the Copperbelt, Zambia Sample SiO2 TiO2 Al2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Tot al Rb Sr Y Zr Nb Co Ni Cu Notch 50.00 1.00 15. 5 0 6.00 0.15 2. 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 30 2.00 200 400 60 360 40 30 16 25 L- 0 7 5 65.53 0.91 13.9 1 5.81 0.00 0.07 1. 4 6 2 . 5 9 3 . 4 3 5 . 1 0 0 . 2 3 1 . 1 4 100.18 162 217 33 50 17 0 0 0 L-076 65.53 0.91 13.9 1 5.81 0.00 0.07 1. 4 6 2 . 5 9 3 . 4 3 5 . 1 0 0 . 2 3 1.14 100.18 182 212 48 361 26 22 16 105 L-077 66.70 0.79 14.45 4. 66 0.00 0.06 1. 3 6 2 . 6 6 3 . 7 8 5 . 0 6 0 . 2 1 0 . 7 7 1 0 0 . 50 174 216 39 290 22 14 11 28 L-078 67.56 0.89 13.59 5. 37 0.00 0.07 1. 2 7 3 . 0 8 3 . 9 3 3 . 7 8 0 . 2 3 0 . 8 1 1 0 0 . 58 143 235 47 343 25 19 13 31 L- 1 5 7 75.81 0.19 12.4 8 1.25 0.00 0.00 1. 1 6 0 . 1 8 0 . 1 9 6 . 9 5 0 . 0 3 1 . 3 9 9 9 . 6 3 225 12 12 107 17 26 8 7 L-15 8 73.58 0.20 12.8 5 1.36 0.00 0.00 1. 4 6 0 . 9 3 0 . 3 3 7 . 1 1 0 . 0 4 2 . 0 0 9 9 . 8 7 233 19 13 109 16 32 7 <6 L-159 68.02 0.64 14.2 3 2.82 0.00 0.00 1. 7 4 1 . 4 2 0 . 9 5 6 . 8 0 0 . 1 6 2 . 1 0 9 8 . 8 7 303 47 34 209 28 38 7 <6 L-160 67.96 0.55 14.7 8 2.29 0.00 0.00 1. 4 7 1 . 6 7 2 . 4 6 5 . 6 9 0 . 1 6 2 . 1 0 9 9 . 1 4 264 40 49 223 32 39 9 <6 X-01 73.81 0.08 12. 2 9 0. 37 1.52 0.04 0.7 0 2 . 2 4 4 . 2 1 4 . 8 3 0 . 0 4 0 . 6 6 1 0 0 . 7 9 X - 02 72.56 0.23 14. 2 8 0.94 0.68 0.02 0. 8 3 0 . 7 6 2 . 8 8 6 . 1 2 0 . 0 5 1 . 9 6 1 0 1 . 3 1 X - 03 70.95 0.42 15. 0 7 1.13 1.29 0.03 1. 3 2 0 . 8 3 4 . 2 3 3 . 0 3 0 . 1 1 2 . 6 0 1 0 1 . 0 1 X - 04 75.20 0.33 10. 1 0 1.55 1.69 0.04 2. 8 1 2 . 0 8 2 . 0 2 2 . 1 3 0 . 3 4 2 . 3 6 1 0 0 . 6 5 X - 05 65.27 0.84 15. 1 8 3.20 1. 94 0.08 1. 0 1 2 . 9 0 3 . 0 0 4 . 7 0 0 . 3 1 1 . 3 9 9 9 . 8 2 Sample Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta Eu Gd Tb Dy Ho Er Tm Yb Lu Notch 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 4 30 5 20 3 9 35.5 7.5 1.6 L-075 0 16 0 0 1339 <6 16 <10 21 9 5 3 1 3 1 6 0 6 1 2 1 1 1. 9 7 . 8 1. 1 6.7 1.3 3.5 0.5 3. 2 0 . 5 L-076 35 17 82 56 1344 <6 17 10 137 61 L-077 46 18 59 41 1391 <6 14 <10 11 35 86 1 1 9 4 1 75 1.1 1.2 1.1 L-078 48 17 74 51 964 <6 18 10 131 61 L-157 14 14 20 15 618 <6 18 <10 43 17 L-158 13 14 20 14 628 6 26 <10 108 26 6 3 7 6 3 1 2 8 0.5 0.6 L-159 19 17 57 18 919 11 24 10 118 60 L-160 18 16 47 16 805 <6 15 13 118 42 1 0 2 1 5 6 4 9 28 1.1 2.8 1.0 4.1.5.4.2 Sampling and composition of samples Four sample s were collec t e d from an outcrop along the Muliashi river. Five analysis were compiled from the literatu r e . Addition a l samples from the Konkola deep boreho l e , the Chambis hi area and the Samba copper deposit serve to complete the suite. Thes e will be discus sed independently in later chapters. Table 4.1.5.13 indicates that 62.5% of the samples ava ilable from the Muliashi Porphyry are subalkaline while the rest are midalkaline rocks. Most of the samples are granites and granodi or i t e s . This includes rocks from the Samba deposit. Table 4.1.5.13 Statistics of rock types, Muliashi Porphyry, Zambia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type Number % Granitoids Groups A l k a l i gran i t e 2 12.50Midalkaline Rocks Q u a r t z m o n z o n i t e 4 25.00 3 7 . 5 0 37.50 Granite 5 31.25Subalkaline Rocks Gran odiorite 5 31.25 6 2 . 5 0 62.50 Total 1 6 1 0 0 . 0 0 1 0 0 . 0 0 100.00 1 4 1 Table 4.1.5.12 Chemical characteristics and environment of emplacement for Muliashi Porphyry samples, Zambia (See acronym descrip t i o n on section 2.4.3.) Sample Rock type Debon & LeFort Maniar & Picc Whalen Pearce Rb/10HfTa Rb/30HfTa Nb-Ta L - 0 7 5 * Quart z m o n z o n i t e Metal u m i n o u s iv mesoc r a t i c Na-K Fe ? N S2/4 O2/4 VA II INV L-076 Quart z m o n z o n i t e Metal u m i n o u s iv me socr a t i c Na-K Fe ? A O-W1- 1 L-077 Quart z m o n z o n i t e Metal u m i n o u s iv me socra t i c Na-K Fe ? A O3/4 OUT U L- 0 7 8 Gran o d i o r i t e Metal u m i n o u s iv mesocr a t i c Na Fe ? A O-W1- 1 L-157 Grani t e Peral u m i n o u s i suble u c o c r a t i c K Fe ? A L-158* Granit e Peralu m i n o u s ii mesocr a t i c K low Fe Mg N O2/3 WP- II OUT U L- 1 5 9 Gran od - g ra n i t e Peralu m i n o u s i mesocr a t i c K Mg ? A O-W1- 1 L-160* Grani t e Peral u m i n o u s ii mesoc r a t i c K Mg ? A O3/4 OUT U L- 1 6 1 Syeno - d i o r i t e dike Peral u m i n o u s ii mesoc r a t i c K high Fe Mg ? A O-W1- 1 Wpab- wp t L-163 Syeno - g a b b r o dike Peral u m i n o u s i mesoc r a t i c K high Fe ? N Emor X-01 Grani t e Metal u m i n o u s iv subl e u c o c r a t i c Na Mg iag-c a g X-02 Grani t e Peral u m i n o u s ii suble u c o c r a t i c K Mg iag- c a g , c c g X-03 Grani t e Peral u m i n o u s ii mesoc r a t i c Na Mg Ccg X-04 Alter e d grano d i o r i t e Peral u m i n o u s ii mesoc r a t i c Na Mg ? X-05 Gran o d i o r i t e Metal u m i n o u s iv mesoc r a t i c K Fe RRG The suite from the Muliashi Porphyry crosses the fiel ds of alkalin e to non-alk a l in e rocks. That happens especially on the TAS diagram 4.1.5.4.3 Description of samples A well exposed outcrop of the Muliashi Porphyry was studi ed near the Muliashi river. Fig 4.1.5.14 illustrate s main relationships of intrus ive rocks at the site. Co ordinates of the samples collected are pres ented in the Appendi x A16. Figs 4.1.5.1 3 are slabbed su rfaces of the sample s. Large samp les were collected at this site and analysed in detail. The results are listed on Table 4. 1.5.1 4 . The rocks are metalu m i n ou s mesocr a t i c sodic to potassic ferriferous biotite quartzmonzon ites. Alt hough the samples were collect e d from the fres he s t possible rocks, geochem ist r y show s that they have been subjec t to weathe ring . There is blue, opalesc e n t quartz and biotit e in the slight l y -foliated matrix. Many very fine-gr ained, white to light gray aplite dikes cut the rock. Mafic, preferentially-oriented, spindle shape xenoliths with reaction rims and lesser development of plagioc lase orbicles occur throughout. There are many pink potass ic feldsp ar porph y r ob l a s ts that enclos e mafic minera ls and seem to grow over the previously-foliated matrix. Mafic minerals remain as witness of previous texture. L-075 comes from the fres hes t rock poss ib le . Plagioc las e orbicl es are concen t r ic a l l y zoned: the outer rim is white, then light green- gr a y , later pink, and in the core, white or gray. Outer rims weathe r more readil y. Colora t i on re flec ts the varying composition of the feldspar. Such spheres are more resist an t to weather i n g and produc e a grape-like surface text ur e made by sphere s of differ e n t sizes (Figs 4.1.5.1 4 and 4.1.5.1 5 ) . All sample s are anorog e n ic granit o id s . 4.1.5.4.4 Geochronology Zircons from sample L-075 were dated by SHRIMP II U/Pb methods to obtain an age of 1864.9 ? 5.4 Ma. 4.1.5.4.5 Discussion on the Muliashi Porphyry and its Correlatives Several of the rocks from the Muliashi Porphyry contai n signifi c an t copper, even when they are distant from the coppper mines. That might be due to an origina l hypogene high copper content , to contamin a t i on by groundwater, or to a combination of both. Most of the samples are mesocratic. 1 4 2 Fig 4.1.5.14 Main features of the Muliashi Por phyry as observed on outcrops. Photographs of the same. 1 4 3 Fig 4.1.5.13 Photographs of slabs from the Muliashi Porphyry, basement to the Copperbelt, Zambia. Samples L- 07 5 and L- 076. N o t e t h e overgrowth of s pherical potasium feldspar por phyroblasts. There was a previous me dium-grained igneous t e x t ure that was overprin ted by the macrocrysts. Most of the matrix is made of biotite. See description in tex t. Scales in centimeters and inches. The Muliashi Porphyry plots as a distinct trend on the R1R2, TAS, AB, QP, KB, MgB and QB diagrams. On the TAS diagr am, the Muliashi Porphyry trend extend s well into the field of monzonites ( X-07 ) along the limit between granite and granodi o r i t e , as illustr a t ed (Fig 4.1.5.1 and 4.1.5.2). Some samples like X-04 (Nkana) and X-09 (Chambishi) seem to be regionally altered versio ns of the Muliashi Porphyry. Samples from the Mufuli r a granite ( X-41 and L-166 ) follow the general trend of the Muliashi Porphyry . Three samples X-38 , L- 273 and L-279 ) seem to be a spec ial variatio n of the Mulia shi Porphyry. Maybe they were produced by a particular type of magma mixing or enrichmen t in biotite by country-rock assymilation. L-268 and L-269 from the Samba copper prospect seem to lie along the Muliashi Porphyry trend on the AB diagram of Debon & LeFort. L-273 and L-279 lie on that trend on the MgB diagram. L-268 , L-273 and L-279 (and L-269 ?) lie on the Muliashi Porphyry line on the KB diagr am. The QP diagram does not show any reas ona b l e correla t i o n between the two grou ps of samples . On the QB diagram , L-273 , L-279 , L-268 an d L- 269 seem to run along the same general trend as the Muliash i Porphyr y . On the R1R2 diagram , L-268 lies just in the middle of the Muliashi trend. L-279 and L-273 , as well as L-269 are off the main trend. The TAS diagram show s no direct correla t i o n with the Muliash i tr end, unless we connect it with the Chambis h i samples ( L-155 and Chambis h i Gray). In that case, there is a long, winding trend of samples that connect s the Muliash i to the Chambishi and then to the Samba samples. On the MgB diagram, the Samba trend continues along the trend of the Muliashi Porphyry. In conclusion , there are clear trends that continu e the Muliash i line on the MgB diagram, the KB diagram, the AB diagram, partially on the R1R2 diagram and not at all on the QP diagram. Samples from the Samba deposit pl ot on the main Muliashi Porphyry trend. Mafic rocks that intersect the basement to the Copper bel t were emplace d after the Katangan sedimen t s were cons o l id a t e d , and in some cases after the copper - c o ba l t mi neraliz ati o n took place. The chemis tr y of dikes that intersect the Katangan rocks varies widely from midalkaline felsic to gabbroid. Although the various methods to evalua te environment of emplac emen t for Muliashi Porphyry granitoids did not produc e coheren t result s , the majori t y of those sample s have an anorog e n ic origin , accord i n g to the method of Whalen et al, 1987 (Table 4.1. 5.12). There is no eviden ce that in dicate s the pluton ic and volcan ic rocks in the suite formed in a magmatic arc, as Master et al, 2003 indicate. The information available does not support a subductional origin for the Muliashi Por phyr y . Furthe r work will be carried out to define the environment of emplacement of these rocks using artificial intelligence an d a large geochemic al database, as indicate d on section 2.4.1.7. 1 4 4 4.1.5.5 Deep Borehole, Konkola Mine T h e deep operatio ns of the Konk ola deposit certainl y ar e one of the larges t un-developed copper resour ces of Zambia. Konk ola is located on Fig 4.1.5.16, on the eas tern limb of the Konkola dome. The deposit is shared with the Democra t i c Republi c of Congo and the Congoles e portion is called Musoshi , as show n on Fig 4.1.5.16. Feas ibility studies for the project indicate that major capital investment is required and the Zambian governme n t is not prepared to go ahead on it without private capital. Severa l multinational corpor ations have evaluated the projec t. ZCCM, the Zambian entity that managed most of that natio n ?s co pper deposits for the la st twenty years, drilled a deep boreho l e to study geolog i c a l and geotec hn i c a l f eatures of the rocks in order to plan and build a new deep shaft to exploi t copper resourc es around the so-c alled Konk ola Deep area. Significant portion s of that boreho l e were exposed by ZCCM geolog i s ts for loggin g and samplin g . The borehol e log, as describ ed by ZCCM geolog i s t s , is synthe s iz e d on Table 4.1.5.16 and Fig 4.1.5.17. L-157 to L-163 were colle c ted from the deep borehole . Table 4.1.5.1 5 shows main data from t he sample s , includi n g depth of collect i o n , tempor a r y unit names for interpre t a t i on and SHRIMP ages. Chemical analysis from samples are listed on Table 4.1.5.14 . Samples collec t e d are descri be d below. Table 4.1.5.14 Chemical An alysis of samples from the deep borehole, Konkola mine, Zambia (Complete elemental analysis on Table A8.2, Appendix) Sample SiO2 TiO2 Al2O3 FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total N o t c h 50.00 1.00 15.50 6 . 0 0 0 . 1 5 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2 . 0 0 L-157 75.81 0.19 12.48 1. 25 0 . 0 0 1 . 1 6 0 . 1 8 0 . 1 9 6 . 9 5 0 . 0 3 1 . 3 9 99.63 L-158 73.58 0.20 12.85 1. 36 0 . 0 0 1 . 4 6 0 . 9 3 0 . 3 3 7 . 1 1 0 . 0 4 2 . 0 0 99.87 L-159 68.02 0.64 14.23 2. 82 0 . 0 0 1 . 7 4 1 . 4 2 0 . 9 5 6 . 8 0 0 . 1 6 2 . 1 0 98.87 L-160 67.96 0.55 14.78 2. 29 0 . 0 0 1 . 4 7 1 . 6 7 2 . 4 6 5 . 6 9 0 . 1 6 2 . 1 0 99.14 L-162 76.11 0.19 12.33 1. 25 0 . 0 0 0 . 2 8 0 . 7 0 3 . 4 8 4 . 9 2 0 . 0 3 0 . 5 9 99.88 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Sm Nd Pr Ce La Hf Ta Eu Gd Yb Lu Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 50 50 15 175 95 10 120 4.0 30 7.5 1.6 L-157 225 12 12 107 17 26 8 7 14 14 20 15 618 <6 18 <10 43 17 L-158 233 19 13 109 16 32 7 <6 13 14 20 14 628 6 26 <10 108 26 63 76 31 2 8 0.5 0.6 L-159 303 47 34 209 28 38 7 <6 19 17 57 18 919 11 24 10 118 60 L-160 264 40 49 223 32 39 9 <6 18 16 47 16 805 <6 15 13 118 42 102 156 49 28 1.1 2.8 1.0 L-162 119 155 14 96 10 6 <6 7 22 13 17 15 793 <6 <15 82 37 Table 4.1.5.15 Data from borehole samples, Konkola Deep borehole, Zambia Sample Age (Ma) Depth (m) Field description Lithology Notes Unit for interpretation L-157 44.10 M e d i u m gra y gra nit o i d Gr a n i t e Simila r to L-158, intrud e s Unit A C L-158 1874?1 4 45.86 M e d i u m gra y gra nit o i d Gr a n i t e Simila r to L-157 C L-159 123.02 P i n k coars e - g r a i n e d folia t e d grani t o i d Granite - g r a n o d i o r i t e Abund a n t bioti t e , stron g folia t i o n A L-160 1866?5 . 4 127.44 P i n k coarse - g r a i n e d folia t e d grani t o i d Granit e Strong foliat i o n . Overpr i n t e d by la rge, rou nd K feldsp a r porph y r o b l a s t s and abun da n t biotit e . Simila r to L-075, L-076 and L-15 5 (Mulia s h i Porph yr y). A L-161 776.62 F o l i a t e d fine-gr a i n e d gabbroi d Syeno d i o r i t e Folia t e d , fine- g r a i n e d mass with la rge white plagi o c l a s e augen . Some with rot at i o n ; serpe n t i n i z e d . D L-162 889.50 L i g h t gra y coars e - g r a i n e d gr ani t o i d Coarse-g ranied granite Coarse - g r a i n e d , unfoli a t e d , with minor biotit e , mafic s are mainl y amph y b o l e . B L-163 812.08 G a b b r o i d Syeno- g a b b r o Ver y fine -g r a i n e d , foliat e d , serpen t i n i z e d gabbroi d . E 1 4 5 1 4 6 Table 4.1.5.16 Simplified log of exp loratory Konkola Deep Borehole, Zambia From To Lithology Thickness Unit Samples 0 . 0 0 40.30 Conglo m e r a t e an d congl o m e r a t i c sands t o n e . 40.30 40.30 65.70 Gre y coarse - g r a i n e d quartz po rph yr y in a biotite gr ound m a s s . 25.40 C L-157 , L-158 6 5 . 7 0 80.70 Dark gra y foliat e d quartz feldsp a r granit i c porph y r y . 15.00 80.70 112.20 Light gra y to pink quartz porp h yr y wi th pink calci t e veinl e t s and strai n i n g in the felds p a r s . 31.50 112.20 205.7 0 Pink to gra y po rp h yr o b l a s t i c augen gneis s of pink felds p a r 5 cm in diame t e r . 93.50 205.70 320.8 0 Pink to gra y qu ar t z felds p a r folia t e d gneis s . 115.1 0 A L-159 , L-160 3 2 0 . 8 0 506.60 Dark gra y po rph y r i t i c , foliat e d quart z felds p a r micac e o u s gneis s . 185.8 0 506.60 584.50 Pink to gra y biotit e porpho r o b l a s t i c gneis s in dark bioti t e groun d m a s s . 77.90 584.50 667.70 Dark gra y po rph y r o b l a s t i c bi oti t e - f e l s p a r - q u a r t z gn eis s . 83.20 667.70 785.60 Black to dark gray por ph y r o b l a s t i c bioti t e schis t . 117.9 0 D L-161 785.6 0 815.3 5 Black bioti t e - r i c h schis t . 29.75 E L-163 815.35 820.35 Pink to dark gra y porph y r y t i c foliat e d feldsp a r - q u a r t z - b i o t i t e gneiss 5.00 820.35 900.00 Gra y to pink coar se - g r a i n e d grani t e with potas s i u m felds p a r 79.65 B L-162 Fig 4.1.5.17 Stratigraphic column of exploratory Konkola Deep Borehole, Zambia L-157 and L-158 were collec t e d from a gray porphy r it i c granit e s en s u s tricto , at the depths shown on Table 4.1.5.1 5 and make Unit C. Both are enriche d in K, Rb and Co. Maybe that was due to alterati o n by fluids related to near by Cu-Co mineraliz ation. L-162 sampled a light gray to white granite and makes Unit B. This sample is not enric h ed in K, Rb and Co. It has remarkably similar major oxide chemistry to the ro cks sample d at the inselbe r g of the Nchanga Granite. L-159 and L-160 come from a pink, coar se-g r a in ed porph yri t i c gneissos e granite, with abundant quartz veining, frac turing and foliation; they make Unit A. Anomalous K 2 O, Rb, Co, Sm and Pr are the same as in samp le s L-158 , L-159 and L-160 . 90 0 800 700 600 500 400 300 200 100 0 D ep th in m et er s G r a y to pi nk coar s e - g r a i n e d gran i t e w ith potas s i u m fe ld s p a r P i n k to da rk gray porp h yr y t i c fo lia t e d fe lds p a r - q u a r t z - b i o t i t e gn e iss B l a c k bio t ite - r i ch sc h is t. B l a c k t o da rk gray po r p h y r o b l a st i c bio ti t e s ch is t . D a rk gr a y po rph y r o b l a s t i c bio ti t e - f e l s p a r - q u a r t z gn eis s . P i n k to gr ay bioti te por ph y r o b l a st i c gn ei ss in da rk biot ite gro u nd m a s s. D a rk gr a y po rphy r i t i c, fo li at ed qu ar tz fel ds p ar mic a c eo u s gne is s. P i n k to gr ay quart z feld s p a r fo liat ed gn eis s . P i n k to gr ay porph y r o b l a s t i c auge n gn eis s of pin k fe lds pa r 5 cm in dia m ete r . L i g h t gra y to pink qua rt z po rph y r y wi th pink ca lc i te ve in let s an d strai ni n g in the fe ld s p ar s . D a rk gr a y fol ia ted qua r tz fel ds pa r gr a nit i c po rp hy r y . G r e y co a rs e- g r a i n e d qua rt z po rp h y r y in a bio t ite gr ou n dm a s s . C o n g l o m e r a t e an d co n gl o m e r a t i c sa nds t o n e . L-162 L-161 L-163 L-159 L-160 L-157 L-158 B E B A C 1 4 7 L-161 is a syenodior i t e porphyry that make s Unit D. Its major oxide compos ition is remarkably similar to that of L-150 from the mafic dike at the Nchanga mine. They both probably had a simila r origin and could be from the same geological event. L-161 seems to have formed in an extens i ve anoroge n ic within- p l a t e environ me n t and probably L-150 did too. L-163 is a peralum i n o us potass ic ferrif e r o us syeno- g a b br o dike and makes Un it E. Most samples from that rock type were extremely foliated into a schistos e, talcou s rock, probably serpen tinized. Cobalt, chrome, vanadiu m and nickel content s are high, as would be ex pected of a mafic rock. It was probably emplaced in an extensiv e anorogen ic within -p l a t e environm e n t . Units A and C are chemically distinct. Unit A contains high Ca, Al, Ce, Ba and Sr, while C has low Ca, Al, Ce, Sr and Ba. Copper is surpris in g l y low in units B and C. They we re assemb le d before the copper enric hme n t proc ess took place, and were kept away from it. This amalgamation of both units has very little evidence of quartz veining and defor mation. In principle, relationships observed in the core show ed that there were three generat i o ns of granito i d s . One was more foliated than the other, and a series of ma fic intrus ives were sign ific antly more deformed and sheared to conform schistos e texture of mylonit e s . The followin g structur a l relationships were observed at the hole: C intrudes A. B intrudes A and C. D and E intrude B, A and C. A tentative geological history is listed on Table 4.1.5.17 . Table 4.1.5.17 Geological history interpre ted from the Konkola deep borehole, Zambia Order Event 1 Pink granitoid of Unit A was intruded. 2 Pink granitoid of Unit A was def ormed and its porphyroblas ts grew. 3 Pink granitoid was intr uded by medium gray granitoid (Unit C). 4 1 0 0 0 milllion years later, a white, coarse -grained Nchanga Granite-like pluton (Unit B) intruded into the pink (A) and gray (C) granitoids. 5 G a b br o ic dikes (Units D and E) intruded the older rocks. 6 Deformation of the entire suite took pl ace; mafic dikes were serpen t i n i z ed and sheared , granit o i d rocks suffer e d less deform a t i on . Conclusions G e oc h e m ic a l and geochro n o l og i c a l data from the Konkola deep boreho l e helped to deduce the geologi c a l history in the environs of Konkola . Ther e might be an anoroge n ic granit o i d intrus i on similar to the Nchanga Granite in the area. It might happen that correlation of L-162 with rocks from the Nchanga Granite is wrong. L-162 s h ou l d be dated and further evaluated. The possibility of other Nchanga Granite-lik e bodies in the basement to the Copperbelt is very relevant and should be investigated . 1 4 8 4.1.5.6 Chambishi Granite 4.1.5.6.1 Introduction The Chambis h i copper mine is located near Kitw e, Za mbia, as shown on Figs M17 and 4.1.5.18. It is the norther n mo s t copper minera l iz a t i o n of a series of deposi t s in the Chambis h i - N k a na basin. Katanga n silic ic las tics and carbonates unc onfor mably overlie bas ement granitoids . Gabbroids that intrude the Katangan metasediments are an important lithology in the basin. A single sample ( L-155) was coll ec te d from the grani te that outcrops as basement on the Chambishi open pit (Fig 4.1.5.18). Seven chemical analysis of various rocks from the environs of the mine were also compiled for this projec t, labeled with the prefix X, and are listed on Table 4.1.5.18 . Table 4.1.5.18 Chemical analysis of samples from the Chambishi copper mine environs, Zambia (complete elemental analys is on Table A8.2, Appendix) Sample Origin a l # SiO2 TiO2 Al2O3 Fe 2 O 3 Fe O MnO MgO CaO Na2O K 2O P2O5 LOI Total Na+K Not c h 50.00 1.00 15.50 6. 0 0 0 . 1 5 0 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0.30 2.00 L-15 5 L-155 72.00 0.28 12.99 2.5 7 0 . 0 0 0 . 0 0 1 . 5 1 0 . 9 5 1 . 0 3 6 . 0 3 0.09 1.71 99. 1 7 7 . 0 6 X - 4 2 Chambi s h i Gra y 68.64 0.3 13.95 1 . 1 4 1 . 2 5 0 . 0 6 2 . 2 9 2 . 2 5 2 . 1 3 4 . 0 4 0.11 3.54 99. 7 6 . 1 7 X - 0 6 Chamb i s h i amphi b o l i t e 51 46.85 15.87 3.3 3 7 . 4 0 0 . 1 1 8 . 6 1 7 . 2 9 3 . 6 5 2 . 5 0 0.15 3.06 98. 8 2 6 . 1 5 X - 0 7 Chamb i s h i trans i t i o n amph i b o l i t i c granoph yr e 52 58.63 13.08 6. 0 7 6 . 6 8 0 . 1 5 1 . 8 7 4 . 7 0 5 . 5 0 0 . 6 6 0.32 1.66 99. 3 2 6 . 1 6 X - 0 8 Chamb i s h i granoph yr e 53 67.94 12.08 7. 2 3 1 . 0 1 0 . 0 4 0 . 6 0 1 . 6 5 6 . 7 0 0 . 2 0 0.07 1.70 99. 2 2 6 . 9 0 X - 0 9 Chamb i s h i granoph yr e 54 59.26 16.65 1.2 6 0 . 4 3 0 . 0 6 2 . 0 4 4 . 5 9 9 . 8 0 0 . 2 0 0.65 4.48 99. 4 2 1 0 . 0 0 X - 1 0 Chamb i s h i amphi b o l i t e 55 47.87 14.53 4.5 0 9 . 0 5 0 . 1 5 6 . 1 3 6 . 1 2 2 . 9 5 1 . 5 5 0.37 7.22 100 . 4 4 4 . 5 0 X - 1 1 Chamb i s h i amphi b o l i t e 56 48.19 14.53 4.1 3 7 . 1 8 0 . 1 2 6 . 6 6 9 . 0 0 4 . 2 5 1 . 4 0 0.17 3.60 99. 2 3 5 . 6 5 Sa m p l e Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Sm Nd Pr Ce La Ta Eu Yb Lu Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 50 50 15 175 95 120 4 7.5 1.6 L-155 219 62 20 99 13.0 61 12 <6 26 15 44 21 848 <6 <15 <10 1 0 9 . 6 2 5 . 3 4 5 6 . 8 1 69 23 36.41 0.5 0.2 0.713 4.1.5.6.2 Geochemistry Although eight samples might not be repres en tative, T able 4.1.5. 1 9 shows statis t i c s of their alkalini t y discrimin a t i o n. 80% of the granitoid s from the Chambish i mine area fall within the subalka l i ne field, the rest in the midalkaline field. 62.5% of the samples available fr om the Chambis h i granite are subalka l i n e , the rest are midalkaline. Table 4.1.5.19 Statistics of rock types, Chambishi granite, Zambia The fifth column (granitoids) is the sum of underlined rock types. alkal i gran i t e 1 12.50 2 0 . 0 0 monzog a b b r o 1 12.50 Midalkaline Rocks a l k a l i gabbr o 1 12.5 0 37.50 granite 1 12.50 g r a n o d i o r i t e 3 37.50 8 0 . 0 0 Subalkaline Rocks gabbro 1 12.50 62.50 Total 8 100.00 1 0 0 . 0 0 100.00 L-155 was collect e d on GPS station 0613444 / 86 0 05 64 , from the granite basement in the Chambishi open pit as shown on Fig 4.1.5.18 . Katangan sedi ment ar y rocks lie unconfor m ab l y on top of it and are exposed at the pit as well as underground. It is a fresh, foliated, peral u m i n ou s mesoc r a t i c potas s i c ferriferous biotite granite with high high K, Co, Sm and Pr. Garlick , 1973 states that X-42 is a repres en tative sample of the Chambishi Gray granite. The rock is effectively a peraluminous mesocratic potassic ferriferous granodior ite. Both L-155 and X-42 fall within the general trends of t he Muliashi Porphyry granitoids. L-155 has very similar chemis try to L-158 from the Muliashi Porphyry. They plot together on all the geochemic a l diagrams . X-42 1 4 9 1 5 0 s h ows a slight deviati o n from the main trend on the R1 /R2 diagram, due to hydrothermal alteration. This is also evident on its high losses on ignition . Table 4.1.5.20 Chemical character and environm ent of emplacement for samples in the Chambishi mine environs, Zambia (See acronym description on section 2.4.3.) Sample Rock type Debon & LeFort Maniar & Piccoli Whalen Pearce Nb-Ta L - 1 5 5 Granit e peralu m i n o u s ii mesocr a t i c K Fe ? N O3/4 OUT U X-42 Gran o d i o r i t e peral u m i n o u s ii mesoc r a t i c K Fe ? X-06 Syeno g a b b r o metal u m i n o u s iv mesoc r a t i c Na Fe ? X-07 Quart z m o n z o n i t e metal u m i n o u s iv mesocr a t i c Na Fe Rrg-ce u g X-08 Grani t e metal u m i n o u s iv mesoc r a t i c Na Fe Rrg-c e u g X-09 Nephe l i n e s yeni t e VI mesoc r a t i c Na Mg ? X-10 Gabb r o metal u m i n o u s iv mesoc r a t i c Na Fe ? X-11 Syeno g a b b r o metal u m i n o u s iv mesoc r a t i c Na Fe ? 4.1.5.6.3 Chambishi Gabbroid Rocks Mwambas h i gabbros are a major outcro p p i ng rock type in the environs of the Chambishi mine, as well as around Nkana North and Chibul u m a mines. This can be s een on Fig 4.1.5.18. Several samples of these rocks were reported by Mendelsohn, 1961. T he sample s are listed on Table 4.1.5.18 . X-6 , X-10 , X-11 a n d X-13 are repr es entative of the gabbroid rocks. Below is a literal transcription 5 from a report on the Chambishi gabbroids and related ?granoph yres?. It is very important, becau se it may be eviden ce of iron oxide- c o pp e r - g o l d mineral iz a t i o n in the environs of the Chambish i deposit. That mineraliz a t i on seems to be associat e d to the gabbroid s . ?At 200 to 400 feet above the base of the dolomite a thick, somewha t irregu l a r sill interr u p t s the sedimentar y section. The dark, greenish-grey to al mos t black , coar se l y crysta l l i n e rock consis ts of amphibo l e enclos ing light-co lo r e d patches of scapolit e pseudomo r ph s after plagioc l as e feldspar . Rarely a sub-ophitic texture is apparent. Most of t he rock can be called amphibo l i t e . Ther e are a few pegmat i t i c zones of coar ser scapol i te and amphi bole. Zones of chloritic rock and amphibole, commonly with narrow dolomite veins and a spar se mineraliz ation of pyrite, a little pyrrhotite, and chalcop y r i t e , repr es e n t shear zones. See Appendi x 1, Nos. 51-56.? 6 ?The deepest drill hole on the propert y passed through 400 feet of gabbro in the top of this sill, then through about 170 feet of granophyr e , then through 25 f eet of magnetite-rich ro ck, 110 feet of gabbro, 50 feet of dolomite, and finally 25 feet of gabbro . These thick ne s s es are meas u r e d perpend i c u la r to the contac ts, which generally show 1 foot or more of fine-gr ained chilled margin.? Fig 4.1.5.19 Stratigraphy of drillhole into Chambishi gabbros and granophyres . The dimensions have been modified to the metric syst em. Top is to the left. Based on description by Garlick, W.G. in Mendelsohn, 1961, page 287. 5 Underlining was added here to stress important information. 6 Mendels o hn ?s sampl es 51 to 56 have been re-numbe red in this document with numbers X-06 to X-11, as show n on Table 4.1.5.24. 1 5 1 ? T h e surfac e distri bu t i o n of the meta-g ab b r o through Chambishi and adjacent grants indicates that it is intruded apparen t l y as a sill into the Upper R oan dolomit e . Four drill holes have been collare d in gabbro and passed through the contac t into underlyi ng dolomite. In the eastern part of Chambishi the meta-ga b br o cuts across the bedding of the Upper Roan dolomit e and reac hes the base of the Mwas hia. Detailed pitting in 1930 at a basal contac t of the gabbro indicated that it was intruded essentia l l y parallel to the bedding of the Upper Roan dolomite , even where the latter is folded. This observat i o n and the almost comple te scapolit i z a t i o n and amphibo l i ti z a t i o n of the gabbro with evidenc e of many shear zones indica t es that it was probab l y intrude d either before or during the folding . This tentati v e conc lus i o n is based on ob servat i o n s in decomp os e d formation in pits and from a few drillho le s .? From report by Garlick , W.G. in Mendelsohn, 1961, page 287. The stratig r ap h y of the borehole describ e d is show n in meters on Fig 4.1.5.19 . The granophy r e describe d in the text was sample d as X-07 , X-08 an d X-09 (Table 4.1.5. 1 8 ) . Based on their chemis tr y , we know that they respec tively are a quar tzmonzonite, a granite and a nepheline syenite. These rocks intrude the Katang an metasedi m ents as sills, along with the gabbroids . The gabbroi ds , in turn are sample s X-06 , X-10 and X-11 . From their major oxide chemic al analysis , we know that they are metalu m i no us sodic syenog a b br os and a gabbro. Accordin g to Garlick , at the base of the granoph y r e sequen c e lies 7.5 meters of ?magnetite rock?. The descrip tion is not spec ific, to be sure if that m eans a body of massive magnetite, but it probably does. This implies that the gabbroi d s , granophy r e s and ?magnet i t e-rock? were intimately related. All three probably formed in the same series of events, during a shor t time span. In addition, the gabbroids and granophyres show evidence of hydrothe rmal altera tion. Table 4.1.5.18 indicates that th eir losses on ignition are high, the granoph yr es contain anomalo us sodium, and two of t hem, anomalou s iron. This may be evidence of hydrothermal albitization and hematitization. The presence of massive iron oxides , midalkaline intr usio ns, hydrothermal alteration and nearby related copper mineralization, are all indications of a potentia l iron oxide- copper-gold envir onment in the environs of Chambishi. 4.1.5.6.4 Geochronology Rainaud et al (2004) dated a sample of what she call s ?Chamb i s h i Granit e? from boreho l e NN75, drille d in the Chambishi South-East prospect, 13 km NE of drill hole BN53. The sample was collected near the bottom of the hole, ?14 meters below the nonconf o r m ab l e cont act between the basal Roan Group sediment s of the Katanga Supergr o up , and an underly i n g granite ? . She describe s the sample as a medium to coar se- g r a in ed , weakly foliated biotite granite. Her age of emplacement for the granite, based on 207 Pb/ 20 6 Pb is of 1983?5 Ma. 4.1.5.6.5 Environment of Emplacement Although the environm e n t of emplac e me n t for samples L-155 and X-42 is not clear, they behave as a clus ter with the Muliashi Porphyry rocks on most of the geoc hemical diagrams, and formed roughly at the same time. An undefined anorogenic environment seems to fit best for the Chambishi granite, just as for the Muliashi Porphyry. X-07 and X-08 are given a rift-rela t e d or continen t a l epeir ogenic uplift environment of emplacemen t by the method of Maniar & Piccoli. The rest of the gabbro ids and granophy r es have a midalkali n e affinity and probably formed in an anorogen ic environ m e n t as rift grani t o id s or contine n t a l epeirog e n ic uplift granit o i d s . 4.1.5.6.6 Conclusion There are some similar ities betw ee n the suite s of ro cks from Chambishi and Muliashi. Both have equivalent granitoid s of comparab l e age, they both also c ontain midalkal i n e intermed ia t e to mafic rocks. A large volume of gabbroi d rocks intrude d the Katanga n metased i m e n t s in the environs of Chambis h i . Those rocks were acccomp a n ie d by the emplace me n t of grano phyres, an iron oxide body and charac t e r is t i c sodic and hematite alteration s. That might be eviden ce fo r iron-c opp e r - g o ld minera l iz a t i o n at or around the Chambish i deposit. This concep t has to be further evaluate d . 1 5 2 4.1.5.7 Mufulira Granite 4.1.5.7.1 Introduction The Mufulir a deposit is one of Zambia?s major histor i c a l copper producer s . It is lo cated near the border with the D.R.C on go . The distr i c t conta i n ed sedime n t ar y - h os t e d copper minera l i z a t i o n that lead to the undergrou nd operation of the Mufulira mine. According to Fleische r, Garlick & Haldane, 1976, it contained around fifteen millio n tonnes of recover a b le copper , and once was the world? s deepes t copper mine. It had an average grade of 3.47% Cu. Several samples of the Mufulira granite were collecte d from a large outcrop along a main road, near the Mufulira Zambian Army firing range, as illustrated on Figs M17 and 4.1.5. 21. Sample coordinates are presen- ted in Appendix A16. One sample from that site was analysed and its chemistry is pres ented on Table A8.6. Fig 4.1.5.20 Underground cross section of the Mufulira West orebody in relation to the basement highs. The granite paleo-hill has a fissur e that is filled by ch alcopyrite-rich arkose . Note zonation of mineralization: pyrite is abundant as the mineralized laye rs get near the paleo-hill. Chalcopyrite, chalcopyrite- bornite and the n b ornite occur as the distance progressive ly increases from the granite paleo hill. Vertical and horizontal scales are very different, as illustrated. Taken from Fleischer, Garlick & Haldane, 1976, p. 320. 4.1.5.7.2 Sample description and geochemistry L-166 is a medium-g r a i n ed , pink metalu m i n o us mesocra t i c sodic ferriferous granite with no visible xenoliths. It is intersected by minor aplitic thin white veinlets spac ed every 15 cm t hat are more resistant to weathering. This sample has low cobalt values. Samples L-160 , X-01 and X-02 are very similar to L-166 ; they plot together on most diagrams . Many of the trace element va lues are compar able. Total iron, K, Rb, Sr, Sm, Nd, Pr, Cu, Zn, Cr and Ba are almost equivale n t in the four samples. This suite contains no Cu, some Co, and low Ba. The rock probab l y formed as a post-or o ge n ic granit o i d in an anoroge n ic envir o n em e n t . Table 4.1.5.21 Chemical analysis of samples from the basement to the Mufulira copper mine, Zambia Sampl e SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K 2O P2O5 LOI Total Na+K Notch 50.00 1.00 15.50 6.00 0.1 5 0 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2.00 X-41 64.2 1.05 14.8 2.89 2.6 8 0 . 0 5 1 . 6 8 3 . 1 1 3 . 7 4 . 6 5 0 . 3 1 0.97 100 8.35 L-1 6 6 70.84 0.39 13.91 2.93 0.0 0 0 . 0 0 0 . 6 1 1 . 9 7 4 . 1 3 4 . 5 4 0 . 1 3 0.44 99.89 8.67 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Sm Nd Pr Ce La Hf Ta Eu Yb Lu Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 50 50 15 175 95 10 120 4 7.5 2 X - 41 1500 1600 L-166 209 89 31 89 18 6 <6 22 18 15 <12 17 741 <6 15.0 <10 109 34.36 63.5 105 35 3.063 3. 313 0.713 0.863 1 1 5 3 Fig 4.1.5.21 Geological map of the Mufulira mine environs, Zambia. Note location of the border with D.R.Congo, indicated as a dash-dot line. Taken fr om Fleischer, Garlick & Haldane, 1976, p. 304. A Major oxide chemic a l analysis from the Mufulir a ?t onali t e? was publishe d by Garlick , 1973. The rock of sample X-41 is actually a quartz monz onite with high TiO 2 and P 2 O 5 . It is the only sample with those char ac t e r is t i c s in the basemen t to the Copperb e l t . Samples L-075 , L-076 a n d L-077 have simil a r compos i t io n , and they plot roughly in the same location on most di agra ms . This suite contai ns high Cu and Ba and low Co, Rb and K. The high values of copper for X-41 must obey to some type of hypogene copper enrichment, and that is very signific ant. Rainaud, et al, 2003 describe two distinc t granito i d phas es in the environs of the Mufulir a mine. They are prec isely the two rock types just described. 1. ? T h e wester n Mufuli r a Grey Granod i orite, which is the most abund ant, is uniformily grey and is charac terized by xenoliths of Lufubu schists. This is a typical biotite-granodiorite (also called tonalite by Darnley, 1960), comprising epidote, plagioc lase, quartz, biotite (someti m es altered to chlorit e ) , scarce muscovite, magnetite, ilmenite and sphene.? (X- 41 is a represen tative sample of that rock.) 2. ? T h e pink granit e compris es microc l i n e , quartz , sc arce plagioc lase, and abundant muscovite (but no biotite or epidote) together with magnetite, rutile and hematite as accesory minerals . This granite lacks xenoliths of Lufubu schists.? (L-166 is repr es en tative of that phase.) 4.1.5.7.3 Geochronology Rainaud, et al 2003 dated the pink granite at 1993 ?7.1 Ma. They state that ?The ages of the Mufulira Lufub u schists (1968 Ma) and the Mufulir a Pink Granite , togethe r with the fact that the Mufulira Grey Granodiorite contains xenoliths of Lufubu schists, indicate that t he pink and grey granites are not two phases of the same granite, but are two separate intrusion s emplac ed at differen t times.? ?The older intrusion is the Mufulira Pink Granite dat ed at 1994 Ma. This was follow e d by extrus i on of the Lufubu volcan ic s in the Mufulira region at 1968 Ma, an event that was followed by the intrus ions of the Mufulir a Grey Granodi or i t e , which, followi n g model 1 of Cahen et al., 1970c, may be ca. 1945 Ma in age.? This makes sens e. Similar features are observed in the Mulia shi Porphyry, where the same two types of granitoids were sampled . 4.1.5.7.4 Discussion If X-41 and L-166 are repr es entative of the Mufulira area, then that area has precis e l y the same petrogr ap h ic al and physic al features of the Muliash i Por phyry: two different rock type s. Both rock types plot together with the Muliashi Porphyry samples on all geoc hem ic a l diagrams as show n (F igs 4.1.5.1 to 4.1.5.5). 1 5 4 A cross sectio n of the Mufuli r a deposi t was publis hed by Fleischer , Garlick & Haldane, 1976. The basement portion of that section has been modified with the rec entl y underst o o d structur a l re lation ships of the basement as show n on Fig 4.1.5.2 2 . The bornite , chalcop y r i t e and pyrite mineral iz a t i o n in veins of the basemen t has not been satisfactorily explained. It might be related to the emplacement of the gray granite, as indicated. This should be look ed into in greater detail. Fig 4.1.5.22 Cross section of th e basement of the Mufulira mine area . It includes all the observations and new g eochronology . C o pp er-bearing quartz veins were exposed on the surface at the time of deposition of the Katangan sediments. Thos e seem to be related to the emplacement of the gray granite. Modified from the g e n eralized stratigraphic column of M u f u lira, by Fleischer, Garlick & Haldane, 1976 . 1 5 5 4.1.5.8 Samba Deposit 4.1.5.8.1 Introduction The so-call ed Samba ?Cu-Por p h y r y? , hosted in the base ment to the Katangan sedimentary sequence to the south west of the main Copperbelt was also evaluated during the Greater Lufilian Arc granito id projec t. The following pages will illustrate t he results of that evaluation. On 1978, Wakefi e l d publish e d a paper about a Paleop r o t er oz o ic deforme d porphy r y -type copper deposit in the baseme nt of the Zambia n Copper be l t (Wakef i e ld , 1978) . That paper has caus ed a lot of confus i o n . The Samba depos it has reserve s of over 50 Mt of 0. 5% Cu, and is the larges t concentr a t i o n of copper minerali z a t i o n in the pre- Ka ta n g an base ment of the Copperbelt. According to Master, ?The deposit, situated at 27?50?E, 12?43?S, consis ts of disseminated pyrite, ch alcopyrite and bornite in deformed pre-Katangan granodior itic and quartzmonzonitic por phyri t i c intrus iv e rocks, with associate d quartz -s er i c i t e and biotite- q u a r tz - s er i c i te schists . ? (Maste r , 1996, p. 8). Fig 4.1.5.2 3 shows a general iz e d geologi c a l map of the deposit, and Figs 4.1.5.24 and 4.1.5.25 are two contro l l e d cross sectio ns to illust r a te general geometry of the deposit. Fig 4.1.5.23 Generalized geological map of the Samba copper deposit in the basement to the Copperbelt, Zambia . N o te t h e l ocation of cross sections of Figs 4.1.5.24 and 4.1.5.25. From Wakefield, 1978. 4.1.5.8.2 Sampling and Geochemistry A repr es en t a ti v e suite of 18 samples from the deposi t was collec t ed from boreho l e s CT-115 , CT-116 , CT-124 and CT-13 0 at the Kalulus h i cores h ed (samp le s L-268 to L-284 ) . Boreho l es CT-115 are show n on Figs 4.1.5. 2 4 . Four samples were anal ysed for this research project: L-268 , L-269 , L-273 a n d L-279 . Their location , field descrip t i o n and rock name are include d on Table 4.1.5.22 . Chemistr y of the samples is listed on Table A8.3, and is plotted on Figs 4.1.5.1 to 4.1.5. 5. The rocks analysed were ho sting mineraliz ation, and were the most likely sample s to hav e been porphyrytic volcanic rocks. The samples are rhyolitic and rhyodacitic, fine- to m edium- g r a i n ed , volcan ic l ast i c rocks (Table 4.1.5. 2 2 ) . L- 268 a n d L-269 were subjec t to intense hydrothermal alteration . They produce high losses on ignition due to abundan t hydr ous minerals. They were subject to sili cification and got a significant input of chrome . L-268 is highly enric he d in copper. Samples L-268 and L-170 are striki ngly simila r on the TAS and R1 R2 diagrams (Figs 4.1.5. 1 and 4.1.5.2 ) . Maybe both rocks were subject to simila r proc es ses. They have high Cr, Cu, Al, their loss on ignition is 3 to 3.6, and they contain low Th and Zn. Nevetheles s, their Nb and Cu values are different. 1 5 6 Fig 4.1.5.24 Eastern borehole-controlled geologi cal cross section, Samba copper deposit, Zambia . It is marked as the s ection line from Fig 7 on Fig 4.1.5.23 . Taken from Wakefield, 1978. Fig 4.1.5.25 Western borehole-controlled geologi cal cross section, Samba copper deposit, Zambia . It is marked as section line of Fig 8 on Fi g 4.1.5.23. Taken from Wakefield, 1978. 1 5 7 Table 4.1.5.22 Main details of analysed samples from the Samba copper deposit, basement to the Copperbelt, Zambia Sample Number Borehole Depth (feet) Field Description Rock Name L - 2 6 9 CT-11 5 241.1 Fract u r e d schis t o s e rocks that conta i n disse m i n a t e d chalc o p y r i t e and pyrit e . Pera l u m i n o u s subl e u c o c r a t i c pota s s i c ferri fero us rh yol i t e L-273 CT-11 5 257.0 Bioti t e schis t with sulfi d e ve in l e t s . Pera l u m i n o u s meso c r a t i c sodi c magn e s i c rh yo da c i t e L-279 CT-11 6 195.2 Schist s after igneou s rock (?) Metal u m i n o u s mesoc r a t i c sodic ferri f e r o u s rh yo da c i t e L-268 CT-12 4 315.5 Schist with stockwo rk and hemati t e / g o e t h i t e oxidat i o n of pyrit e Peral u m i n o u s mesoc r a t i c potas s i c ferri f e r o u s rh yol i t e Samba samples plot along the general trend of the Muliash i Porphyr y rocks in most of the Debon & LeFort diagrams (Figs 5.1.5.1 to 5.1.5.5). De viation from the main trend in some of the diagrams is probably due to hydrothermal alteration associated to the mineraliz ing proc es ses. Rainaud, Master, Arms trong, & Robb, 2003 commen t that schis ts from the Samba deposit are part of the Lufubu Schist Group of rocks. This had been previous ly hinted by Master , 1996, when he stated the likeli ho od of Samba rocks being ?of Paleopro t er o z o ic age?, and ?related to other Paleopro t er oz o ic granitoid s in the Kafue Anticline and surround i n g areas (e/g. Mufulira , Mokambo, Luina and Roan Antelope granites ) .? 4.1.5.8.3 Geochronology Rainaud et al., 2003 dated schists from the same borehol es and produced a U-Pb SHRIMP age in zircons of 1964?12Ma (Table A22.7) . That is the age of the volcanic pr otolith for the schists. The relevance of that age to mineralization, and the type and origin of the Samba copper concentration are not well understood. Several questi o ns remain : Do the zircons have eviden c e of a strong metamo r p h ic ev ent? Is that process reflec t e d in their shape and ages ? Rainau d was not able to solve these questions (Rainaud, C., personal communication, 2003). 4.1.5.8.4 Discussion Observati o n of core from the original boreholes dri lled to explore the Samba property did not detect any intrusive porphyritic rocks; only what seemed to be me tamor ph os e d fine- to medium- g r a i n ed volcanic rocks. Few aspects of typical porphy ry copper mineralization were eviden t. No significant brecciat ion or stockworking was seen. Hydrot h er m a l altera t i o n patter n s and minera ls were not those of a porphyr y copper deposi t . Mineralization of coarse bornite and chalcop y r i t e in veins and dissemi na t e d fashion was observed in core; but many of the patter ns common in copper porphy r y sy stems know n from the Central Andes and the North American Cordillera were missing. The author looked at the core at approximately the same time as Richar d Sillit o e did. And, after discus s in g the issue together in Kitwe, both agreed that the minera lization does not seem to be due to porphyry copper proc es s e s or bears resembl a n c e with thos e mineral iz e d systems (Sillitoe, R., per sonal communication, 2002). One of the main problems to cons ide r the Samba ?por p h y r y? a true porphyr y copper depos i t is the strong deforma t i o n of its host rocks. They a ll are schistos e and lack true plutonic charac t e r . If mineral iz ed volcanic rocks were the protolith of the schist s, induration of parts of the rock by silicification, potassic and phyllic alterat i o n would be expecte d ; that would prec lud e schisto se deformation. No evidence of epidote, nor phyllic, argillic or potassic alteration was seen. A possible origin of copper mineralization at the Samba prospec t could be a high sulfida t i o n copper dissemina t i o n in volcanic ash. This probably took plac e in an anoroge n ic environ m e n t like that of the Muliashi Porph y r y- L u fu b u Schis t group of rocks. Ash was subjec t to defor mat io n and metamorp h is m that reconc e n tr a t ed iron and copper sulfides , to become what is now the Samba pros pec t . Samba ?porph y r y ? is a misnome r and should be changed definit e l y for ?Samba copper deposit ? to avoid further confusi o n . 1 5 8 4.1.5.9 Conclusions on Granitoids in the Copperbelt General Conclusions 1 . The Nchanga Granit e has all the charact e r i s t i c s of an anorogen i c granite ring complex. Chemistr y of its rocks cross the fields of midalkaline to subalkaline ro c k s . The pluton behaves as a cohere nt cluste r in all geochemic al diagrams. The pluton, or parts of it, is made of high heat produ cin g granites that probabl y maintained a long-lived circulation of hydrothermal fluids. The Nchanga Granite might have contributed to the origin of copper in its environs . 2 . Mafic rocks and midalka l i ne grani ti c dikes were studied in the Nchanga mine area. Both were emplace d in anorogen i c extensi o na l environ m en t s . The granitic dikes were dated at ~765 Ma. They provid e an oldest age of deposit i o n for the Katanga sedimen t a r y sequen ce at Nchanga, and might provide a significan t brac ket age for mineral iz a tio n . 3. Mafic rocks that intersect the basement to the Copper b e l t were emplac e d after the Katanga n sedime n t s were cons ol ida t e d , and in some cases, after the coppe r-cobalt mine ralization took place. The chemistry of dikes that intersect the Katangan rocks varies widely from midalkaline felsic to gabbroid. 4. The Muliash i Porphyr y plots as a distin c t trend on all geochemic al diagrams evaluated. A few of the sample s studied display variati o ns by hydroth er m a l alterat i o n or metamo r p h is m . Samples from the Chambish i and Mufulira environs , as well as from the Samba copper deposit, plot on the Muliashi Porphyry trend. 5. Geoc hem ic a l and geochron o l o g ic a l data from the K onkola deep borehol e helped to deduce part of the geolog ical history in the environs of that mine. Ther e might be an anorogen i c granitoi d intrusio n similar to the Nchanga Granite in the area. 6. A large portion of the rocks in the base me n t to the Copper be l t are enrich ed in K 2 O, Rb and Pr. Select groups of samples are enriched in Nb and Cu. Tectonic Environment of Emplacement 7. The proc edu r e of (Maniar & Piccoli, 1989) cannot identify environment of emplacement for 70% of the granit o id s in the basemen t to the Copper b e l t . Few samples produc e meaning f u l result s , as indica t ed on Table 4.1.5.25 . This is probably due to particular modi fications of the rocks at regional scale that make them unrecognizeable by the Maniar & Piccoli proc edures . 8. Intense sodic alteration and hematitization were observed in the basement to the Copper belt. Maybe other unident i f i e d process es of regional metamorphism have occurred, that modify the basic chemis try of rocks. One altera t i o n proces s could be a net enrichm e n t in potassiu m that is evident in the abundant biotite and alkali feldspar overgr ow th. 9. The regiona l metamor p h ic proces s mention ed in the previou s conc lu s i on seems to have taken place before the emplacemen t of the Nchanga Granite, becaus e the method of Maniar & Piccoli, 1989 produc ed results for several samples from the Nchanga Granite and young intrusives that cut Katangan sediments at Chambis h i. Results of the methods to evaluat e gr anitoid environment of emplacement were not clear for rocks older than the Nchanga Granite . 10. Although the various methods to evaluate environmen t of emplacement for Muliashi Porphyry granitoids did not produc e coherent results, the majority of those samples have an anoroge n i c origin , accord in g to the method of Whalen et al, 1987 (Table 4.1.5.12). T here is no evidence that i ndic a t e s the pluton ic and volcan ic rocks in the suite formed in a magmati c ar c, as Master et al, 2003 indicate. The information available does not support a subductional origin for th e Muliashi Porphyry. Furthe r work will be carried out to define the environment of emplac emen t of thes e rocks using artifi c ia l intell i g e nc e and a large geochem ic a l databas e , as indicat e d on section 2.4.1.7 . Mineralization 11. A large volume of gabbroid rocks intruded the Katangan metasediments in the envir ons of Chambishi. Those rocks were acccompanied by the emplacem ent of granophyres, an iron oxide body and char ac te r is t i c sodic and hematite alterati o n s . That mi ght be evidence for iron-cop pe r - g o ld mineraliz a t io n at or around the Chambis h i deposit . The conc ep t has to be studied further . 1 5 9 12. Rocks from the Mulias h i Porphyr y contain signi ficant copper that might have a hypogene origin . 13. Mineralization of the Samba coppe r deposit does not seem to be due to porphyr y copper proc es s e s or bears resembla n c e with thos e mineraliz ed systems. Lithologic Correlation 14. Rocks with ?identical? chemistry may form from the sa me protolith, in similar environments that are ver y separated in time. This occurs with samples from th e suites of Muliashi Por phyry and Mufulira. They both have pink and gray granitoi d s with simila r compos it i on s , but the ages of the rocks are complete ly different. Stratigraphic Relations 15. The stratigr ap h i c model that Robb, Master and Rainaud have been using for the basement to the Zambian Copper be l t during the past few years can be sli ghtly modified with the new information from this resear ch project. Fig 4.1.5.26 illustrates most of the relevant intrusive and stratigraphic relations. It show s the new radiometric ages obtained for this project. Fig 4.1.5.26 Main stratigraphic relationships be tween rock units in the main Copperbelt area, Zambia . Figure modified after model of the Economic Geology Research Institute [Robb, L., personal communication, 2003] . 1 6 0 Table 4.1.5.23 Regional correlation of dated Pale oproterozoic granitoids in the Greater Lufilian Arc Event Kalene Hill, Zm Grootfontein, Nm Kamanjab, Nm Mufulira, Zm Konkola, Zm Muliashi, Zm NW Zambia Fe/Mg 9 L-158 gra y gt 1874;14 8 1872;14 L-944 granite 1856;24 L-993 L - 1 6 0 pink gt 1866;5. 4 L - 0 7 5 186 5;5.4 X-1, X-2 quart z m o n z o n i t e granite 1864 6 1945 L-1045 quart z m o n z o n i t e L-868 quart z m o n z o n i t e 1937;14 L-945 L - 8 5 5 granite 1939;19 X-41 gra y quart z m o n z o n i t e ~1945 L-030 granite 1927 ferri fero us 5 L-864 granod i o r i t e S a m b a 1964; 1 2 magne s i c 4 L-969 s yenite 1976;42 L-155 Cham b i s h i granite 1983; 5 3 L-1043 granite 1997;39 L-166 pink granite 1993; 7. 1 1994 2 L-968 granite 1 6 1 Table 4.1.5.24 Original data, additional samples fr om the literature on Copperbelt granitoids, Zambia Samples from Garlick, 1973 # Samp le SiO 2 TiO 2 A l2 O 3 Fe2 O 3 Fe O MnO MgO Ca O Na 2O K2O P2O5 CO2 S H2O+ H2O- Cu F BaO Tota l X-3 4 Nch a n ga Red Gra n ite 76. 75 0 . 0 9 1 1 . 78 0 . 8 2 0 . 5 8 0 . 0 3 0 . 1 6 0 . 7 2 3.0 8 5.0 1 0 . 1 0 0 . 0 5 0 . 0 1 0 . 7 9 n il tr. nil 99. 97 X-3 5 Gra y' s Qua rry Red 76. 84 0 . 0 8 1 0 . 70 1 . 3 0 1 . 3 0 0 . 0 4 0 . 1 0 0 . 8 0 2.3 0 4.9 0 0 . 0 2 0 . 0 5 0 . 1 5 0 . 4 5 0 . 1 9 0 . 0 1 9 7 . 93 X-3 6 Gra y' s Qua rry Aplit e 76. 90 0 . 0 1 1 2 . 30 0 . 6 0 0 . 6 0 0 . 0 1 0 . 1 0 0 . 5 0 3.6 0 4.4 0 0 . 0 4 0 . 0 7 0 . 0 8 0 . 2 5 0 . 0 3 0 . 0 1 9 8 . 90 X-3 7 Gra y' s Qua rry Gre y 78. 20 0 . 0 4 1 0 . 30 1 . 1 0 1 . 1 0 0 . 0 4 0 . 1 0 0 . 7 0 2.2 0 4.9 0 0 . 0 1 0 . 0 3 0 . 0 9 0 . 3 2 0 . 0 9 0 . 0 1 9 8 . 13 X-3 8 Gra y' s Qua rry Sch lie re n 59. 80 1 . 1 0 1 0 . 40 1 2 . 6 0 . 3 0 0 . 3 0 0 . 6 0 4 . 3 0 1.7 0 2.9 0 0 . 0 8 0 . 0 3 0 . 0 7 0 . 9 2 0 . 0 4 0 . 0 1 9 4 . 85 X-3 9 Gra y' s Qua rry pegm a t it e mic ro c lin e 66. 60 0 . 0 1 1 8 . 00 0 . 2 0 0 . 2 0 0 . 0 2 0 . 0 3 0 . 2 0 2.4 0 11. 90 0 . 0 1 0 . 0 9 0 . 1 8 0 . 7 1 0 . 1 5 0 . 0 1 1 0 0 .5 1 X-4 0 Nka n a vein adu la ria 64. 80 0 . 0 1 1 6 . 70 0 . 4 0 0 . 4 0 0 . 0 1 0 . 0 3 0 . 1 0 0.7 0 15. 50 t r. 0.4 9 9 8 . 74 X-4 2 Cha mb is h i Gre y 68. 64 0 . 3 0 1 3 . 95 1 . 1 4 1 . 2 5 0 . 0 6 2 . 2 9 2 . 2 5 2.1 3 4.0 4 0 . 1 1 1 . 7 7 t r. 1.6 8 0 . 0 9 0 . 0 3 9 9 . 73 X-4 1 Muf u lira Tona lit e 64. 19 1 . 0 5 1 4 . 80 2 . 8 9 2 . 6 8 0 . 0 5 1 . 6 8 3 . 1 1 3.7 0 4.6 5 0 . 3 1 0 . 0 8 0 . 1 8 0 . 8 5 0 . 0 4 0 . 1 5 0 . 1 6 1 0 0 .5 7 Samples from Mendelsohn, 1961 # Samp le SiO 2 TiO 2 A l2 O 3 Fe2 O 3 Fe O MnO MgO Ca O Na2 O K2O P2O 5 CO2 S H2O+ H2O- H2OT Cu F BaO Cl ZrO2 e qu iv Fe S 2 t o t a l X-0 1 Roa n Ant e lo p e Gra y Gra n it e 1 73. 81 0 . 0 8 1 2 . 29 0 . 3 7 1 . 5 2 0 . 0 4 0 . 7 0 2 . 2 4 4 . 2 1 4.8 3 0.0 4 0 . 3 3 1 0 0 .5 X-4 2 Cha mb is h i Gra y Gra n ite 2 68. 64 0 . 3 0 1 3 . 95 1 . 1 4 1 . 2 5 0 . 0 6 2 . 2 9 2 . 2 5 2 . 1 3 4.0 4 0.1 1 1 . 7 7 t r 1.6 8 0 . 0 9 0 . 0 3 9 9 . 73 X-0 2 Moka mb o adam e llite 3 72.56 0 .2 3 1 4 . 28 0 . 9 4 0 . 6 8 0 . 0 2 0 . 8 3 0 . 7 6 2 . 8 8 6.1 2 0.0 5 0 . 9 3 0 . 0 5 0 . 0 6 0 1 0 0 .4 X-0 3 Mwe k e ra gra y gra n it e 4 70. 95 0 . 4 2 1 5 . 07 1 . 1 3 1 . 2 9 0 . 0 3 1 . 3 2 0 . 8 3 4 . 2 3 3.0 3 0.1 1 t r tr 1.2 1 0 . 0 9 0 . 0 5 9 9 . 76 X-0 4 Ndo la gra y gra n it e 5 75. 20 0 . 3 3 1 0 . 10 1 . 5 5 1 . 6 9 0 . 0 4 2 . 8 1 2 . 0 8 2 . 0 2 2.1 3 0.3 4 0 . 0 7 0 . 0 2 0 . 9 1 0 . 2 0 0 . 0 8 0 . 0 5 n il 99. 62 X-4 1 Muf u lira ton a lit e 7 64. 19 1 . 0 5 1 4 . 80 2 . 8 7 2 . 6 8 0 . 0 5 1 . 6 8 3 . 1 1 3 . 7 0 4.6 5 0.3 1 0 . 0 8 0 . 1 8 0 . 8 5 0 . 0 4 0 . 1 5 0 . 1 6 0 . 2 1 0 0 .4 X-0 5 Ban c rof t Mulia s h i Porph yr y 8 65. 27 0 . 8 4 1 5 . 18 3 . 2 0 1 . 9 4 0 . 0 8 1 . 0 1 2 . 9 0 3 . 0 0 4.7 0 0.3 1 0 . 0 5 t r 1.3 2 0 . 0 2 n il tr 99. 82 X-3 4 a Nc h a n ga red gra n it e 9 76. 75 0 . 0 9 1 1 . 78 0 . 8 2 0 . 5 8 0 . 0 3 0 . 1 6 0 . 7 2 5 . 0 1 3.0 8 0.1 0 0 . 0 5 0 . 0 1 0 . 7 9 n il tr. nil tr 99. 97 X-1 2 Chirin go li pho s p ha t ic sch is t 48 30. 05 0 . 3 7 8 . 6 0 3 9 . 65 4 . 4 8 0 . 0 5 0 . 2 7 6 . 8 2 5.78 n il 4 nil 0.3 5 1 0 0 .5 X-1 3 Luf ub u rive r norit e SW of Chibu lu ma 49 49. 41 2 . 6 7 1 2 . 71 2 . 1 8 1 0 . 07 0 . 1 4 6 . 9 3 1 0 . 46 2 . 4 6 0.8 0 0.4 6 0 . 0 6 t r 0.8 5 0 . 1 2 0 . 0 3 0 . 4 0 . 1 9 9 . 65 X-1 4 Luf wa n ya m a valle y sca p o lit ize d gab b ro 50 46. 76 3 . 3 0 1 0 . 31 5 . 8 1 9 . 1 0 0 . 1 4 7 . 2 5 1 0 . 24 4 . 2 6 0.8 6 0.3 8 n il 0.2 2 1 . 0 4 0 . 1 7 n il 1.4 0 . 3 1 0 0 .9 X-0 6 Cha mb is h i am ph ib o lit e 51 46. 85 1 5 . 87 3 . 3 3 7 . 4 0 0 . 1 1 8 . 6 1 7 . 2 9 3 . 6 5 2.5 0 0.1 5 1 . 4 3 0 . 1 0 0 . 2 9 7 . 46 X-0 7 Cha mb is h i tran s it io n am p h yb o lit ic gra n op h yre 52 58. 63 1 3 . 08 6 . 0 7 6 . 6 8 0 . 1 5 1 . 8 7 4 . 7 0 5 . 5 0 0.6 6 0.3 2 0 . 7 5 0 . 0 8 0 . 8 9 9 . 32 X-0 8 Cha mb is h i gra n o ph yre 53 67. 94 1 2 . 08 7 . 2 3 1 . 0 1 0 . 0 4 0 . 6 0 1 . 6 5 6 . 7 0 0.2 0 0.0 7 0 . 8 8 0 . 2 4 0 . 1 7 0 . 1 9 8 . 86 X-0 9 Cha mb is h i gra n o ph yre 54 59. 26 1 6 . 65 1 . 2 6 0 . 4 3 0 . 0 6 2 . 0 4 4 . 5 9 9 . 8 0 0.2 0 0.6 5 2 . 4 6 0 . 6 9 0 . 3 2 0 . 2 9 8 . 56 X-1 0 Cha mb is h i am ph ib o lit e 55 47. 87 1 4 . 53 4 . 5 0 9 . 0 5 0 . 1 5 6 . 1 3 6 . 1 2 2 . 9 5 1.5 5 0.3 7 3 . 3 5 0 . 2 6 0 . 2 9 7 . 03 X-1 1 Cha mb is h i am ph ib o lit e 56 48. 19 1 4 . 53 4 . 1 3 7 . 1 8 0 . 1 2 6 . 6 6 9 . 0 0 4 . 2 5 1.4 0 0.1 7 1 . 7 3 0 . 0 7 0 . 3 9 7 . 71 1 6 2 1 6 3 4.2 NAMIBIAN DOMAINS 4.2.1 KAMANJAB BATHOLITH, NAMIBIA 4.2.1.1 Introduction The Kamanjab Batholith is one of the most significan t geologic a l features on norther n Namibia . Surpris i ng l y , very little was know n about its geology until 2003. Only generalized maps and a few isolated reports were available; little or no comprehe ns ive literature on this large unit of igneous rocks could be found. Age cons tra in t s were not very tight. The mineral potenti a l of the region was consid ere d to be signifi c a n t . For these reas ons, the batholith cons titutes one of the main foci for sampling in this project. The Kamanjab Batholith may be reached by a 300 km paved road from Windhoek, capital of Namibia. It lies roughly south-west of the Etosha Natural National Pa rk. A few farms in the region have airstrip s for small aircraft. Most of the secondary road s are unpaved, but are in general good shape. The area has electrical power lines supplied by the main Namibian grid. A few farm homes te a ds are connect ed with the main Namibia n telephon e grid, and some farmers have microw a v e and radio communi c a t i o ns . The neares t well- e q u i pp e d hospit a l is in Otwija r o n go . The neares t gas stations are located in Outjo and Khor ixas , approximately 100 km from the main batholith. Some farm s sell diesel fuel and gasoline in small quantit i es at a surcharge. Rainfall is very low in the semi-desert climate of th e Kamanjab region. All the drainage system is ephemer al; no rivers or creeks are perenn i a l . Ther e is a rapid decreas e in rainfa l l toward s the wester n portio n of the Kamanjab Batholith, where the Et endeka Plateau and the Namib desert begin. As discuss ed by Frets, 1969, ?the year can be divided into a dry winter period with moderat e temper a t u r e and a hot summer period with occasiona l rainfall . The proper rainy season occurs fr om November/Dec ember to April. Years with a normal rainfall alaternate, however , with droug ht years.? Each farm has several water wells that constitute the main sour ce of water. Most of the pumping is done usin g small wind-dr i v e n pumps and engine s . A few private , small dams gather water during the rainy seas ons . V egetation is scarce, short and thor ny. A portion of the land, especial l y towards the northeas t ern part of the batholith, is cover ed by extensi v e game farms and bad quality pastures for cattle. Small numbers of various ty pes of antelopes, zebra, wildebeast, giraffe, desert elephan t and rhinoc er os are seen occasio na l l y . Desert lizar ds , small mammals and snak es are common l y found in the rocky outcrop s and inselbe r gs . Main econom ic activities of the region are game viewin g and extensiv e goat and sheep rais ing. A great portion of the land is barren; no industr i a l crops are grown; most foods are brought from outside. The Kamanjab Batholith has been given several names in the literatur e. Some of these are: Franzfontein Granite, Fransfontein Granite Suite, Huab Gneiss, Ka manja b Graniti c Comple x and Kamanjab Inlier. The term Kamanjab Batholith is proposed here to name the plutoni c body and its associ a te d volcan i c l as t i c materi a l . The best map available of the entire batholith was a 1:200,00 0 compila t i o n by Ajagbe, 2001, based on the 1:1?000, 00 0 scale geologic a l map of Namibia. Some po rtions of the batholith were available at 1:100,000 scale (Frets , 1969; Porada, 1974; and Anonym o us , 1997). Geolog ic a l sheet 20 14 Fransfontein that covers the southe r n part of the Kamanj a b Bathol i t h was availab le at 1:250, 0 00 scale in prelimin a r y form at the Geologic a l Survey of Namibia. Geological reports on the area we re publis hed by Cliffo rd, Rook e, & Allsopp, 1962b; Clifford, Nicolaysen, & Burger, 1962a; Siedner, 1968; C lifford, Rooke, & Allsopp, 1969; Frets, 1969; Guj, 1970; Porada , 1974; Burger & Coetze, 1975; Burger, Cli fford, & Miller, 1976; Tegtmeyer & Kroner, 1985; Steven, 2000; Steven, 2001a; Steven, 2001b; and Steven & Armstr ong, 2002. Various types of mineral iz a t i o n have been identif ie d throughout the Kamanjab Batholith. The liter ature available indicates significant copp er, gold and fluorite occurren c es and mines. A review of mineral resour c es of the Kamanjab Batholith region was compiled by Ajagbe , 2001. Namibia n copper minera l iz a t i on was reviewed by Schneider & S eeger, 1992 and gold mineraliz ation was reviewed by Burnett, 1999; both reports includ e some inform a t i on about deposi ts and pros pec t s in the batholith. Several compan y reports have been issued during the past few years on the merits of th e iron oxide-cop p e r - go l d Tevrede property , located in the northwestern portion of the batholith (Anonymous, 2003; Boulde r Mining, 2002; Boulder Mining, 2002-2004; Boulder Mining , 2003a; Boulder Mining, 2003b; Boul der Mining, 2004a; and Boulder Mining, 2004b). Reconn a is s an c e field sampl i n g was done along the main public roads that transect the batholith. Very few volcan ic rocks were sample d . 170 sample s were collec t e d in the field; 97 of those were analyse d . Ninetee n additi o na l chemic a l analys es of sample s were compil e d from the literat u r e , for a total databas e of 116 sample s . Table 4.2.1.1 lists their chemica l analysis . All samples collected in the Kamanjab Batholith are 1 6 4 l o c a t ed on the series of maps of Figs M27 to M39. A guide to find waypoints and samples is presented on Table 4.2.1.18. Maps have been consecutively numbered wi th the prefix ?K-?. For example, L-958 is located on the southea s t er n corner of map sheet K-18. That is codified as K-18 SE. Sample L-942 is located on the western central portion of the same map. It has been c odified as K-18 WC. For easy reference, a key map for all the larger scale maps has been include d (Fig M27) . Table 4.2.1.3 lists general char act er is t i c s of all samples collected in the Kamanjab Batholith. The followin g pages will describe main findings in the Kamanjab Batholit h . 4.2.1.2 Geochemistry The Kamanjab Batholith is made by a series of three ma jor rock types with five or six subord i n a t e types that make dikes and smaller pluton ic bodies . At first sight it seems to have a rather homogen e ou s chemist r y , becaus e almost 60% of the rocks cluste r around the quartz m onz o n i t e- a lk a l i granit e litholog i e s on the TAS diagram (Figs 4.2.1.1 and 4.2.1.2). Ne vert h e l es s , after carefu l inspec t i o n , sever a l clear disti n c t i o ns betwe e n rock types are apparent. 73% of the granitoids from the Kamanjab Batholith fall with in the midalkaline field, while 27% of them fall in the subalkaline field (Table 4.2.1.2). 69% of all rocks sample d are in the midalk a l in e field, 27% are subalk a l in e and 5% are alkaline . By far the most abundan t rocks in the batholith are quartzmonzonites; more that a third of all samples collecte d come from that group. The dom inan ce of midalkaline rocks stresses the fact that the batholith formed in an anorogenic environment. Table No. 4.2.1.1 CHEMICAL ANALYSIS OF SAMPLES IN THE KAMANJAB INLIER, NAMIBIA; GREATER LUFILIAN AR C PAGE 1/2 Sample SiO2 TiO2 Al2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Notch 50.00 1.0 15.5 6.00 0.15 2.00 5.00 4.90 5.5 0.3 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 4 30 5 20 3 9 35.5 7.5 1.6 L-832 73.67 0.32 12.24 1.83 0.00 0.04 0.14 0.46 4.39 5.23 0.11 0.63 99.06 154 297 38 307 15.0 8 10 19 70 17 46 <12 1468 <6 19.0 <10 121 58 9.62 L-834 59.92 0.47 16.55 4.88 0.00 0.05 0.10 1.72 0.29 14.1 0.12 1.28 99.44 283 70 49 274 20.0 7 <6 14 19 9 26 <12 1842 7.0 25.0 <10 12.06 41.53 111.4 192 54 2.88 77 .3 0.70 2.45 1.28 14.4 L-835 65.67 0.65 15.35 3.98 0.00 0.08 0.87 2.29 4.41 4.48 0.19 1.44 99.41 135 203 38 342 15.0 <6 <6 7 68 17 40 <12 1318 <6 15.0 10 127 60 8.89 L-836 67.42 0.74 14.82 4.07 0.00 0.10 0.86 2.21 4.08 4.77 0.20 0.79 100.06 159 266 40 343 17.0 6 <6 19 69 0 45 <12 1272 0.0 0.0 0 0 0 8.85 L-838 67.61 0.61 14.50 3.84 0.00 0.09 0.82 2.37 3.62 4.48 0.18 0.50 98.62 208 69 22 93 15.6 <6 8 10 30 15 12 <12 552 4.0 21.2 <10 130 55 8.10 L-839 76.62 0.29 11.26 1.41 0.00 0.04 0.23 0.35 3.05 5.28 0.07 0.47 99.07 218 67 27 163 17.0 <6 9 19 35 13 12 <12 565 <6 16.0 <10 102 44 8.33 L-840 70.88 0.42 13.61 2.64 0.00 0.07 0.48 1.29 3.97 4.93 0.13 0.75 99.17 176 247 37 237 15.0 <6 8 20 47 16 20 <12 1054 <6 18.0 <10 127 62 8.90 L-842 65.32 0.68 14.27 4.45 0.00 0.10 1.13 2.64 4.17 3.50 0.19 2.76 99.21 141 316 38 361 16.0 10 11 37 83 16 49 13 1668 <6 16.0 12 11.19 33.40 82.63 135 41 1.48 62 .9 1.013 1.64 1.08 7.67 L-843 75.42 0.33 12.58 1.52 0.00 0.03 0.25 0.31 3.01 4.39 0.10 1.13 99.07 163 61 41 199 20.0 <6 <6 6 25 14 16 177 907 <6 21.0 <10 113.0 35.20 74.00 126 32 3.95 10. 0 0.65 2.04 0.88 7.40 L-844 68.18 0.63 14.42 3.75 0.00 0.08 0.82 2.22 3.87 4.35 0.20 1.02 99.54 137 259 39 345 16.0 6 7 20 62 17 42 <12 1378 6.0 16.0 <10 129 63 8.22 L-846 67.61 0.60 14.35 3.72 0.00 0.08 0.89 1.97 4.09 4.59 0.18 0.78 98.86 134 246 44 306 16.0 6 10 18 56 15 39 <12 1240 <6 19.0 <10 11.76 41.76 86.50 133 45 50.4 1 .00 1.913 1.09 8.68 L-849 73.54 0.33 12.99 1.74 0.00 0.02 0.20 0.14 3.78 5.57 0.04 0.55 98.90 189 43 24 243 27.0 <6 7 <6 22 18 17 217 451 <6 16.0 <10 107.3 30.33 47.85 152 20 1.013 33 .7 0.26 0.24 0.38 9.35 L-855 76.63 0.15 11.87 1.14 0.00 0.02 0.05 0.25 4.70 4.06 0.02 0.25 99.14 88 39 10 71 10.0 <6 10 9 11 15 <12 <12 328 <6 <15 <10 39 16 8.76 L-857 73.33 0.32 13.00 1.84 0.00 0.04 0.43 1.21 4.01 4.21 0.11 1.00 99.50 155 211 17 141 14.0 <6 9 26 28 15 22 <12 1081 <6 <15 <10 80 38 8.22 L-863 64.77 0.71 14.71 5.42 0.00 0.08 1.57 3.06 3.37 3.86 0.24 1.14 98.93 155 288 33 228 19.0 14 15 23 72 18 100 122 1004 <6 17.0 11 89 44 7.23 L-864 66.28 0.74 14.57 5.01 0.00 0.09 1.56 2.96 3.05 4.14 0.33 1.62 100.35 97 249 23 39 11.9 10 16 28 58 16 91 273 1039 3.1 13.4 10 17.4 6.19 37.8 9.86 78 45 0.83 1 .38 0.8 1.27 5.35 0.73 4.38 0.86 2.38 0.34 2.22 0.32 7.19 L-864 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0 0 0 0 0.0 0 0 0 0 <9 <6 <15 <10 23 <12 0.00 L-865 66.29 0.76 14.63 4.88 0.00 0.08 1.51 2.53 3.09 4.38 0.27 1.26 99.68 179 240 34 241 19.0 10 20 21 68 17 84 226 1100 <6 16.0 10 129 67 7.47 L-868 66.57 0.77 14.29 4.73 0.00 0.10 1.11 2.09 3.56 4.38 0.29 1.15 99.04 112 186 32 22 15.3 10 13 14 . 19 68 114 1100 <6 <15 10 14.6 8.72 52.03 13.28 154 79 1.07 0 .84 0.6 1.83 7.21 0.99 6.12 1.18 3.36 0.47 3.09 0.45 7.94 L-874 96.83 0.09 0.64 0.69 0.00 0.01 0.00 0.02 0.02 0.31 0.03 0.08 98.72 11 8 5 29 4.0 <6 13 8 6 17 <12 538 30 6.0 17.0 11 144 73 0.33 L-874a 67.47 0.89 13.68 4.67 0.00 0.10 1.05 1.71 3.48 4.99 0.27 1.09 99.40 155 181 57 348 24.0 12 14 19 69 63 17 1380 8.47 L-875 66.20 0.78 14.38 5.11 0.00 0.12 1.18 2.90 3.74 4.25 0.30 1.32 100.28 138 222 46 329 23.0 7 13 14 68 18 71 181 1294 <6 <15 10 12.16 42.90 111.4 157 54 76.6 1. 59 1.96 1.23 7.99 L-877 66.24 0.93 13.94 5.04 0.00 0.09 1.14 2.08 3.48 4.74 0.41 1.24 99.33 140 224 54 377 23.0 9 16 22 75 19 62 17 1371 <6 17.0 10 169 87 8.22 L-878 67.83 0.67 13.61 4.34 0.00 0.09 0.95 1.67 3.73 4.58 0.23 1.08 98.78 152 176 57 329 19.0 9 12 34 71 19 46 16 1143 <6 17.0 <10 12.29 39.36 92.38 150 41 56.1 1. 150 2.56 1.213 8.31 L-895 55.24 0.90 18.42 6.32 0.00 0.11 3.12 4.54 4.23 4.61 0.50 1.93 99.92 164 840 22 172 7.0 18 43 164 69 18 134 91 1382 <6 <15 14 8.250 23.24 53.84 74 22 98.6 0.3 3 0.36 0.91 8.84 L-898 69.20 0.58 12.94 5.11 0.00 0.08 0.60 1.62 4.21 5.14 0.15 0.09 99.72 112 193 33 215 15.0 <6 7 17 46 27 189 1049 9.35 L-899 71.98 0.41 12.65 2.41 0.00 0.06 0.72 1.79 4.23 3.72 0.11 0.69 98.77 112 193 33 210 18.0 <6 7 17 46 17 26 182 1049 <6 16.0 <10 119 56 7.95 L-900 67.40 0.67 14.52 4.30 0.00 0.08 1.12 2.21 4.83 4.01 0.21 0.90 100.25 101 244 40 361 16.0 8 8 17 43 17 48 <12 1239 <6 16.0 11 127 61 8.84 L-902 77.60 0.17 12.00 0.96 0.00 0.02 0.08 0.11 4.16 4.81 0.10 0.34 100.35 160 35 18 95 22.0 <6 7 33 15 15 13 <12 131 <6 25.0 <10 85 39 8.97 L-903 79.24 0.19 10.48 1.02 0.00 0.02 0.12 0.14 2.98 4.99 0.04 0.32 99.54 262 21 23 103 16.0 <6 8 10 15 13 <12 <12 132 <6 25.0 <10 80 38 7.97 L-904 76.77 0.24 11.40 1.61 0.00 0.05 0.16 0.10 3.59 4.81 0.05 0.45 99.23 242 44 30 149 18.0 <6 8 15 37 15 <12 14 233 <6 21.0 <10 107.0 29.65 49.94 99 23 7.2 0.28 1 .30 0.90 8.40 L-905 77.13 0.29 11.44 1.46 0.00 0.03 0.23 0.54 5.65 1.54 0.06 0.51 98.88 75 80 40 160 19.0 <6 9 17 23 13 13 <12 672 <6 22.0 <10 116 55 7.19 L-906 76.57 0.27 12.23 1.45 0.00 0.03 0.07 0.32 3.00 5.97 0.03 0.42 100.36 254 43 51 164 21.0 <6 7 37 14 13 <12 269 219 <6 19.0 <10 122 62 8.97 L-907 71.26 0.43 13.59 2.43 0.00 0.06 0.51 1.34 3.85 5.07 0.11 0.52 99.17 175 181 41 248 16.0 <6 8 11 44 15 24 <12 1136 <6 16.0 <10 135 69 8.92 L-908 66.78 0.41 16.95 1.82 0.00 0.08 0.28 0.22 9.57 2.63 0.03 0.34 99.11 96 28 10 66 15.5 <6 8 12 53 26 <12 <12 125 <6 15.0 <10 9.7 2.50 17.12 5.04 82 40 1.49 2.03 1.1 0.29 1.92 0.28 1.78 0.37 1.19 0.20 1.64 0.29 12.2 L-909 71.39 0.41 13.73 1.94 0.00 0.07 0.35 0.72 4.37 4.96 0.08 0.91 98.93 153 134 46 285 18.0 <6 8 25 56 17 15 <12 1346 <6 18.0 <10 163 82 9.33 L-910 70.84 0.59 13.17 3.28 0.00 0.04 0.51 0.53 4.21 4.24 0.20 1.11 98.72 129 126 44 360 17.0 <6 8 12 47 16 26 <12 1115 <6 <15 <10 152 76 8.45 L-911 72.60 0.37 14.49 2.24 0.00 0.03 0.81 0.22 0.16 5.19 0.11 2.40 98.62 170 16 45 344 27.0 <6 10 33 48 19 17 139 398 <6 19.0 <10 145 75 5.35 L-912 73.33 0.37 13.50 1.75 0.00 0.02 0.70 0.22 2.05 5.30 0.08 1.55 98.87 139 29 38 273 20.0 <6 7 9 34 17 15 <12 787 <6 16.0 <10 148 47 7.35 L-917 71.65 0.73 12.99 3.87 0.00 0.08 1.25 0.71 3.95 4.48 0.20 0.63 100.54 113 116 16 39 15.2 6 12 17 50 15 46 15 967 <6 <15 <10 13.4 5.26 30.24 7.86 85 42 1.40 1.3 6 0.9 1.04 4.56 0.63 3.72 0.68 1.87 0.27 1.86 0.27 8.43 L-919 87.60 0.31 4.60 3.09 0.00 0.03 0.08 0.09 0.12 2.09 0.04 0.79 98.84 79 9 11 99 8.0 6 15 13 14 <9 27 32 297 <6 <15 <10 55 26 2.21 L-920 36.93 0.23 6.77 1.19 0.00 0.03 0.22 0.29 2.90 2.72 0.06 49.0 100.35 124 81 20 208 15.0 <6 <6 16 29 14 17 134 1088 <6 <15 <10 113.1 35.71 61.91 99 29 18.9 0.6 6 0.20 0.70 5.62 L-922 68.49 0.77 14.39 4.18 0.00 0.07 0.89 1.69 3.76 4.88 0.23 0.98 100.33 143 206 56 426 27.0 8 9 15 58 18 56 244 1598 <6 16.0 10 22.13 52.85 122.3 159 56 61.6 1. 73 4.29 2.49 1.13 8.64 L-923 70.32 0.62 13.18 3.95 0.00 0.06 0.59 0.92 4.03 4.67 0.17 1.02 99.53 162 156 56 425 21.0 6 12 11 55 18 37 <12 1168 <6 21.0 <10 159 89 8.70 L-924 71.99 0.63 12.33 2.83 0.00 0.05 0.57 1.46 3.58 3.97 0.13 1.69 99.23 82 63 46 359 22.0 8 9 14 26 15 38 <12 1811 <6 19.0 <10 158 79 7.55 L-938 70.06 0.58 13.36 3.13 0.00 0.05 0.58 1.70 4.16 4.11 0.19 0.90 98.82 76 244 38 294 19.0 6 7 11 44 16 40 266 1785 <6 <15 <10 23.8 117.0 49.23 83.50 96 37 1.37 3 .22 38.5 1.43 3.22 0.53 3.70 0.77 2.40 0.39 1.213 0.89 8.27 L-939 68.27 0.56 15.25 3.83 0.00 0.08 0.63 1.89 3.55 5.28 0.14 0.74 100.22 132 422 22 166 11.0 15 16 29 68 16 89 23 1059 <6 <15 11 8.325 30.34 57.99 77 28 77.5 0.5 8 0.93 8.83 L-940 62.87 0.57 14.38 5.03 0.00 0.09 1.98 6.05 4.02 3.40 0.20 0.69 99.28 133 422 23 173 12.0 14 13 22 64 18 94 17 1043 <6 <15 11 9.050 25.39 64.13 90 31 79.8 0.43 0.64 0.98 7.42 L-943 74.31 0.15 13.23 1.77 0.00 0.04 0.03 0.75 3.70 5.72 0.11 0.29 100.10 137 123 4 65 7.2 <6 9 19 17 14 13 15 350 <6 28.0 <10 18.5 0.91 6.77 2.16 42 20 2.27 3.29 0 .5 0.15 0.72 0.10 0.64 0.14 0.46 0.09 0.83 0.17 9.42 L-945 67.85 0.52 15.01 3.25 0.00 0.07 0.55 1.40 4.19 5.08 0.11 0.92 98.95 169 235 45 386 18.0 9 8 20 64 18 2 13 1409 <6 19.0 <10 12.43 41.88 115.1 178 53 61.2 0.85 1.66 2.46 1.13 9.27 L-946 67.96 0.48 14.78 2.89 0.00 0.06 0.59 1.58 4.39 5.01 0.12 0.73 98.59 165 232 38 250 19.0 6 8 8 45 16 30 185 1451 <6 <15 <10 175 88 9.40 L-948 70.39 0.65 13.17 3.48 0.00 0.11 0.62 1.58 4.48 4.47 0.13 0.41 99.49 160 174 63 368 21.0 7 8 10 73 17 22 <12 1424 <6 15.0 <10 175 92 8.95 L-951 66.61 0.52 15.75 3.69 0.00 0.02 0.04 0.50 11.34 0.33 0.12 0.19 99.11 4 30 50 261 24.0 <6 10 6 9 16 39 137 <20 <6 22.0 <10 10.83 28.36 109.6 166 14 48.5 0.71 3 .14 1.89 1.09 11.67 L-952 67.68 0.59 15.55 4.09 0.00 0.02 0.15 0.73 10.86 0.35 0.15 0.22 100.39 6 38 36 308 23.0 <6 9 6 10 16 31 173 52 <6 <15 <10 38 27 11.21 L-955 67.86 0.41 16.46 3.50 0.00 0.05 0.11 0.33 10.16 0.19 0.23 0.82 100.12 4 37 40 340 17.0 <6 13 333 142 21 36 <12 30 <6 <15 16 13.25 62.33 671.3 965 405 42.8 0. 40 1.79 1.03 10.4 L-956 61.48 2.00 9.60 15.05 0.00 0.04 0.23 2.72 7.38 0.01 0.92 0.23 99.66 5 36 63 321 14.0 9 11 7 17 17 91 <12 51 <6 <15 24 41.30 97.50 116 63 297 3.05 2.13 7.39 L-957 75.71 0.31 11.71 1.52 0.00 0.04 0.21 1.09 2.90 4.90 0.05 0.66 99.10 126 135 32 207 20.0 <6 7 <6 36 14 <12 228 571 <6 26.0 <10 112.1 34.19 59.59 156 79 3.20 7 .2 0.28 0.34 0.68 7.80 L-958 47.73 1.22 15.13 13.06 0.00 0.23 7.23 8.03 3.57 0.36 0.22 2.21 98.99 5 188 34 105 5.0 63 122 59 119 19 296 107 297 <6 <15 37 15 <12 3.93 L-963 88.82 0.21 4.22 2.07 0.00 0.03 0.19 0.14 1.00 1.77 0.06 0.66 99.17 63 17 18 133 8.0 8 11 20 15 <9 25 12 308 <6 <15 <10 64 31 2.77 L-965 67.45 0.59 13.65 6.24 0.00 0.03 0.32 0.69 4.10 5.73 0.19 0.42 99.41 156 43 88 358 29.0 <6 11 8 24 17 33 12 741 7.00 30.0 <10 125 56 9.83 Table No. 4.2.1.1 CHEMICAL ANALYSIS OF SAMPLES IN THE KAMANJAB INLIER, NAMIBIA; GREATER LUFILIAN ARC (Cont. ) PAGE 2/2 Sample SiO2 TiO2 Al2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Notch 50.00 1.0 15.5 6.00 0.15 2.00 5.00 4.90 5.5 0.3 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 4 30 5 20 3 9 35.5 7.5 1.6 L-966 68.15 0.60 12.90 6.30 0.00 0.02 0.16 0.43 4.46 5.68 0.19 0.27 99.16 144 39 74 108 17.1 <6 9 6 19 16 42 193 708 5.82 27.2 <10 17.8 6.29 34.8 9.84 103 45 0.41 3 .12 1.2 0.89 7.00 1.36 10.3 2.34 7.51 1.13 7.93 1.21 10.14 L-967 70.72 0.48 12.92 3.64 0.00 0.07 0.46 1.11 3.78 5.05 0.12 0.63 98.98 269 119 83 395 22.0 8 9 13 60 17 31 <12 883 8.00 36.0 <10 259 130 8.83 L-967a 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0 0 0 0 0.0 0 0 0 0 15 0 0 0 <6 20.0 <10 153 119 0.00 L-968 72.13 0.34 13.69 2.21 0.00 0.03 0.17 0.89 3.99 4.79 0.05 0.51 98.80 136 145 37 225 15.0 7 9 20 86 15 16 <12 1370 <6 23.0 <10 110.0 16.73 28.51 110 11 2.86 26 .2 0.49 0.76 8.78 L-969 59.46 0.49 19.16 4.28 0.00 0.05 0.68 0.38 0.55 14.31 0.08 0.84 100.28 393 66 59 293 24.0 6 <6 47 53 22 61 <12 2451 6.00 29.0 <10 10.51 36.03 92.38 159 37 7. 20 60.2 0.66 3.05 1.29 14.9 L-971 64.34 0.54 17.73 1.51 0.00 0.09 0.14 0.68 4.58 8.51 0.11 0.69 98.92 148 66 47 358 22.0 <6 9 10 14 13 34 <12 2236 <6 <15 <10 137 81 13.1 L-973 71.06 0.42 12.34 2.89 0.00 0.04 0.12 1.90 0.51 9.97 0.09 0.97 100.31 266 42 47 249 19.0 6 <6 141 70 9 28 12 1800 <6 18.0 <10 9.588 33.88 96.50 128 42 5.85 36 .5 0.50 3.23 1.138 10.5 L-975 72.48 0.35 13.19 2.05 0.00 0.06 0.27 0.82 3.81 5.40 0.10 0.56 99.09 164 149 34 215 16.0 7 9 45 47 14 19 <12 1327 <6 21.0 <10 137 68 9.21 L-976 72.48 0.37 13.10 1.84 0.00 0.04 0.29 0.71 4.00 5.29 0.06 0.50 98.68 195 113 55 203 21.0 <6 10 8 29 18 209 1114 115.8 48.35 91.75 71 3.23 13.4 1.03 2.21 2.9 3 1.08 9.29 L-977 74.68 0.27 11.99 1.72 0.00 0.04 0.24 0.55 3.86 5.21 0.04 0.45 99.05 121 81 27 197 13.0 <6 8 <6 39 15 12 <12 766 <6 16.0 <10 110 57 9.07 L-978 76.43 0.22 11.10 2.76 0.00 0.10 0.04 0.28 4.16 5.19 0.05 0.18 100.51 139 58 15 133 16.9 <6 10 37 73 20 14 20 264 3.59 19.1 <10 21.3 2.08 13.4 4.14 50 25 0.75 5.11 1.0 0.29 1.79 0.29 2.06 0.48 1.79 0.33 2.76 0.49 9.35 L-979 66.06 0.48 15.03 3.97 0.00 0.09 1.33 3.18 4.23 3.67 0.14 0.79 98.97 108 435 35 143 15.0 10 10 76 88 16 68 242 1077 <6 <15 11 92 44 7.90 L-980 67.03 0.53 15.05 4.32 0.00 0.09 1.37 3.20 4.47 3.48 0.18 0.77 100.49 115 424 32 157 17.0 10 15 28 62 17 72 200 1140 <6 <15 <10 104 52 7.95 L-982 66.31 0.56 15.11 3.80 0.00 0.09 1.18 3.09 4.72 3.57 0.19 0.80 99.42 99 495 25 176 12.0 11 10 11 56 17 54 <12 1245 <6 <15 <10 8.588 26.96 66.38 74 30 53.8 0.3 6 0.55 0.83 8.29 L-983 72.59 0.29 13.57 1.83 0.00 0.04 0.07 0.90 4.08 4.95 0.04 0.51 98.87 197 156 28 181 17.0 <6 6 7 32 15 13 <12 963 <6 19.0 <10 90 39 9.03 L-985 72.90 0.46 12.76 2.61 0.00 0.05 0.29 1.39 3.72 4.25 0.06 0.63 99.12 123 219 5 51 6.1 <6 7 9 46 14 25 173 1580 1.49 17.1 <10 25.6 3.41 33.2 9.78 103 61 2.13 1. 48 0.2 1.09 2.00 0.20 0.97 0.17 0.46 0.07 0.54 0.10 7.97 L-987a 45.74 2.33 16.73 14.31 0.00 0.17 4.10 10.53 2.62 1.59 0.46 1.99 100.57 22 598 11 18 1.9 41 8 75 109 17 429 <12 397 <6 <15 36 7.7 2.50 10.86 2.08 <12 <12 0.2 9 0.51 0.0 1.03 2.95 0.39 2.37 0.46 1.20 0.15 0.92 0.13 4.21 L-987b 40.92 2.62 19.28 13.71 0.00 0.19 4.13 12.81 2.45 0.79 1.19 2.06 100.15 35 646 19 31 4.0 28 <6 37 72 17 307 <12 284 <6 <15 32 7.100 29.40 16 5 284 1.34 3.24 L-990 53.79 0.31 13.92 7.16 0.00 0.15 8.22 7.59 5.52 0.32 0.10 2.29 99.37 10 267 12 84 10.0 38 178 73 69 13 75 584 187 <6 <15 20 39 22 5.84 L-991 48.45 0.96 11.97 11.52 0.00 0.19 11.57 9.20 3.07 0.46 0.12 1.70 99.21 7 217 20 53 9.0 64 251 83 93 12 255 870 188 <6 <15 35 19 12 3.53 L-992 50.94 0.49 19.38 7.11 0.00 0.15 5.16 9.79 3.16 1.87 0.09 2.25 100.39 67 659 10 28 3.4 27 53 35 53 16 144 100 460 0.24 0.9 26 4.4 1.92 9.78 2.25 19 9 0.49 0.75 0.13 0.79 2.03 0.30 1.93 0.39 1.11 0.16 1.04 0.15 5.03 L-993 71.34 0.39 13.57 2.03 0.00 0.05 0.39 1.42 3.97 5.33 0.07 0.81 99.37 115 224 27 75 11.5 <6 6 8 34 15 24 160 1595 <6 17.0 <10 22.5 7.25 47.18 12.68 139 69 0.45 2.38 0.59 1.21 5.76 0.82 5.12 1.00 2.86 0.42 2.84 0.41 9.30 L-994 70.70 0.40 13.83 2.09 0.00 0.05 0.43 1.46 3.95 5.07 0.09 0.73 98.80 110 226 37 208 19.0 6 7 10 33 15 32 195 1763 <6 <15 <10 142 70 9.02 L-995 39.21 3.69 11.13 22.15 0.00 0.26 7.20 10.83 1.60 0.53 1.13 1.13 98.86 14 449 21 27 4.0 59 <6 54 128 19 491 <12 457 <6 <15 45 <12 <12 2.13 L-996 69.95 0.44 14.71 2.86 0.00 0.06 0.50 1.75 4.30 4.78 0.11 0.95 100.41 121 274 24 78 13.9 6 9 67 71 16 30 <12 1498 2.82 14.9 <10 23.0 6.17 39.6 10.8 113 49 0.6 9 2.30 0.83 1.22 4.96 0.74 4.69 0.93 2.78 0.42 2.93 0.42 9.08 L-997 69.62 0.34 15.29 1.59 0.00 0.04 0.27 0.51 5.88 5.33 0.05 0.73 99.65 135 65 57 241 22.0 8 9 8 24 16 19 <12 542 <6 33.0 <10 111.4 28.71 57.06 156 21 4.19 11.06 2.45 0.95 11.21 L-998 64.78 0.73 15.67 4.59 0.00 0.11 1.41 2.78 4.52 4.03 0.24 1.33 100.19 103 300 34 347 15.0 6 9 29 96 18 53 13 2134 <6 <15 10 10.00 32.01 78.50 106 38 63.0 0.94 1.04 1.03 8.55 L-999 67.68 0.49 14.73 3.02 0.00 0.07 0.74 1.83 4.31 4.65 0.13 1.19 98.84 140 252 37 288 20.0 <6 9 10 58 17 33 205 1537 <6 16.0 <10 9.700 36.04 91.88 144 44 1.53 3 9.2 0.83 1.49 0.89 8.96 L-1000 67.91 0.47 15.37 2.32 0.00 0.06 0.52 1.06 4.28 5.11 0.10 1.68 98.88 192 112 37 251 18.0 <6 10 62 58 17 35 <12 1206 <6 20.0 <10 11.55 90.10 152.3 134 80 82. 0 3.48 2.58 1.20 9.39 L-1002 77.59 0.26 11.61 1.64 0.00 0.05 0.10 0.32 3.59 4.97 0.03 0.33 100.49 180 40 25 134 22.0 <6 8 6 14 14 10 <12 180 <6 28.0 <10 104.0 18.61 52.50 87 26 3.35 5.4 1.60 0.93 8.56 L-1003 68.00 0.50 15.07 2.73 0.00 0.05 0.58 1.60 4.64 5.26 0.12 0.69 99.24 145 242 40 289 16.0 <6 8 12 47 17 32 <12 1796 <6 15.0 <10 8.450 28.94 79.13 133 26 2.58 31.7 0.78 1.71 0.95 9.90 L-1005 71.20 0.48 12.46 3.35 0.00 0.06 0.56 1.47 3.93 4.47 0.18 0.76 98.92 171 218 46 298 18.0 7 9 15 50 17 26 16 1194 <6 18.0 <10 132 64 8.40 L-1007 64.26 0.56 15.15 5.20 0.00 0.10 1.92 3.56 4.03 3.92 0.20 0.55 99.45 169 234 45 318 16.0 7 10 22 61 17 38 <12 1413 <6 22.0 <10 160 78 7.95 L-1009 66.67 0.69 15.06 4.31 0.00 0.09 1.05 2.81 4.12 4.42 0.26 0.88 100.36 129 347 38 354 15.0 7 7 18 71 17 53 <12 1757 <6 16.0 10 115 55 8.54 L-1010 63.36 0.80 15.40 5.08 0.00 0.11 1.26 3.27 4.15 4.24 0.34 1.17 99.18 138 385 37 372 15.0 9 10 21 74 18 53 <12 1944 <6 <15 12 110 55 8.39 L-1011 66.33 0.64 14.74 3.94 0.00 0.09 0.94 2.72 4.53 4.43 0.19 0.82 99.37 152 302 38 308 20.0 7 9 21 73 17 50 126 1322 <6 17.0 10 129 66 8.96 L-1012 64.77 0.68 15.28 4.30 0.00 0.20 0.95 3.01 5.41 3.94 0.20 0.97 99.71 132 337 42 332 22.0 8 10 9 331 17 53 105 1550 <6 17.0 <10 139 74 9.35 L-1013 67.41 0.61 14.33 4.04 0.00 0.08 0.94 2.09 4.00 4.72 0.21 0.95 99.38 171 240 39 331 16.0 6 10 26 67 17 47 <12 1290 <6 19.0 <10 108.4 40.58 79.25 131 35 48.2 0.64 1.74 0.98 8.72 C-1 74.03 0.27 12.73 1.15 1.51 0.05 0.31 0.48 3.67 5.09 0.05 0.71 100.05 100 50 70 500 30.0 <10 <10 n.d 25 <3 10 1200 25.0 95 <100 <3 <3 <3 0 <3 8.76 C-2 69.71 0.68 14.17 1.69 1.57 0.04 0.84 0.82 4.10 5.30 0.27 0.67 99.86 70 110 45 550 30.0 25 35 25 2100 8.0 90 35 9.40 C-3 68.63 0.67 15.43 1.74 1.03 0.10 0.51 1.99 4.50 4.42 0.18 0.50 99.70 90 350 140 700 40.0 25 35 11 2500 25.0 130 30 8.92 C-4 73.63 0.33 14.16 1.13 0.24 0.02 0.00 0.50 3.14 6.35 0.07 0.44 100.01 200 80 20 380 20.0 20 9 13 1200 40.0 95 11 9.49 C-5 75.35 0.27 13.18 1.08 0.22 0.02 0.00 0.62 3.15 5.50 0.05 0.36 99.80 110 100 35 280 10.0 20 5 15 1400 30.0 65 12 8.65 C-6 66.09 0.69 14.60 3.06 1.72 0.08 1.81 2.54 3.25 4.71 0.28 1.11 99.94 150 480 25 280 <10 20 85 18 1900 14.0 75 25 7.96 C-7 69.29 0.47 14.55 1.81 1.48 0.06 1.19 2.83 3.33 4.40 0.17 0.46 100.04 230 650 25 320 10.0 19 70 35 1700 16.0 70 13 7.73 C-8 73.88 0.33 13.85 0.87 0.24 0.03 0.18 0.26 4.05 5.93 0.09 0.39 100.10 130 40 55 450 15.0 20 7 11 400 20.0 65 4 9.98 C-9 73.30 0.32 13.20 2.93 0.48 0.01 0.00 0.24 3.46 5.67 0.07 0.34 100.02 130 50 80 650 30.0 30 <3 14 1200 12.0 85 9 9.13 C-10 68.63 0.49 15.01 1.62 1.44 0.07 1.22 2.74 4.41 3.60 0.20 0.57 100.00 65 720 25 230 <10 20 55 30 1900 18.0 70 20 8.01 C-11 78.84 0.29 10.79 0.95 0.27 0.03 0.09 0.60 2.94 5.20 0.06 0.22 100.28 120 65 55 180 18.0 15 5 25 560 20.0 100 <3 8.14 C-13 ( w 75.89 0.41 12.46 1.07 0.13 n.d. 0.05 0.25 3.60 5.71 0.04 0.50 100.11 100 40 65 650 40.0 <10 <10 n.d. 25 <3 10 1000 30.0 90 <100 <3 <3 <3 0 <3 9.31 C-14 48.69 1.26 13.27 4.86 8.71 0.18 6.15 10.49 2.41 1.05 0.22 0.50 97.79 3.46 Felsic volcanics, Namibia Notch 50.00 1.0 15.5 6.00 0.15 2.00 5.00 4.90 5.5 0.3 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 4 30 5 20 3 9 35.5 7.5 1.6 Li Be Ge Mo Na+K Notch 50.00 1.0 15.5 6.00 0.15 2.00 5.00 4.90 5.5 0.3 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 4 30 5 20 3 9 35.5 7.5 1.6 X-16 75.93 0.26 12.08 2.96 0.32 0.01 0.36 0.48 7.93 0.13 0.07 0.42 100.95 8.06 X-17 72.07 0.33 13.36 3.76 0.25 0.02 1.33 1.01 7.95 0.30 0.04 0.49 100.91 8.25 X-18 69.24 12.00 0.55 3.83 5.36 0.00 90.98 9.19 X-19 72.02 0.32 13.78 2.24 1.02 0.02 0.20 0.39 4.07 5.18 0.03 0.65 99.92 9.25 X-20 76.01 0.23 12.05 0.80 0.91 0.03 0.20 1.02 3.09 5.02 0.01 1.14 100.51 8.11 3 5 4 0 4 5 5 0 5 5 6 0 6 5 7 0 7 5 8 0 8 5 9 0 9 5 1 0 0 SiO2% 0 1 2 3 4 5 6 7 8 9 1 0 1 1 1 2 1 3 1 4 1 5 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM Kamanjab Batholith, Namibia; Lufilian G.P. (Based on Middlemost, 1994, 1997) S am p l e s P et r o g r a p h i c fie l ds L-832 L-834 L-835 L-836 L-838 L-839 L-840 L-842 L-843 L-844 L-846 L-849 L-857 L-863 L-864 L-865 L-868 L-874 L-874a L-875 L-877 L-878 L-895 L-898 L-899 900 L-902 L-903 L-904 L-905 L-906L-907 L-908 L-909 L-910 L-911 L-912 L-917 L-919 L-920 L-922 L-923 L-924 L-938 L-939 L-940 L-943 L-945 L-946 L-948 L-951 L-952 L-955 L-956 L-957 L-958 L-963 L-965 L-966 L-967 L-968 L-969 L-971 L-973 L-975 L-976 L-977 L-978 L-979 L-980 L-982 L-983 L-985 L-987a L-987b L-990 L-991 L-992 L-993 L-994 L-995 L-996 L-997 L-998 L-999 L-1000 L-1002 L-1003 L-1005 L-1007 L-1009 L-1010 L-1011 L-1012 L-1013 C-1 C-2 C-3 C-4 C-5 C-6 C-7 C-8 C-9 C-10 C-11 C-13 (weath 1) C-14 Fig 4.2.1.1 Fig 4.2.1.1 6 0 6 5 7 0 7 5 8 0 SiO2% 7 8 9 1 0 1 1 1 2 1 3 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM Kamanjab Batholith, Namibia; Lufilian G.P. (Based on Middlemost, 1994, 1997 ) Samples Pet rographic fields L-832 L-835 L-83 6 L-83 8 L-83 9 L-840 L-842 L-84 3 L-84 4 L-84 6 L-84 9 L-857 L-863 L-86 4 L-865 L-86 8 L-874a L-875 L-87 7 L-87 8 L-89 8 L-89 9 L-900 L-902 L-903 L-904 L-905 L-906 L-907 L-908 L-909 L-910 L-912 L-917 L-922 L-923 L-924 L-93 8 L-93 9 L-940 L-94 3 L-945 L-94 6 L-948 L-951 L-952 L-955 L-956 L-957 L-965 L-96 6 L-96 7 L-96 8 L-971 L-97 3 L-975 L-976 L-97 7 L-97 8 L-97 9 L-980 L-982 L-98 3 L-985 L-993 L-99 4 L-99 6 L-99 7 L-99 8 L-99 9 L-1000 L-1002 L-1003 L-1005 L-1007 L-1009 L-1010 L-1011 L-1012 L-1013 C-1 C-2 C-3 C-4 C-5 C-6 C-7 C-8 C-9 C-10 C-11 C-13 (weath 1) Fig 4.2.1.2 Fig 4.2.1.2 - 5 0 0 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti) 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 R 2 = 6C a +2M g +A l L-832 L-834 L-835 L-836 L-838 L-839 L-840 L-842 L-843 L-844 L-846 L-849 L-857 L-863 L-864 L-865 L-868 L-874 L-874a L-875 L-877 L-878 L-895 L-898 L-899 L-900 L-902 L-903 L-904 L-905 L-906 L-907 L-908 L-909 L-910 L-911 L-912 L-917 L-919 L-920 L-922 L-923 L-924 L-938 L-939 L-940 L-943 L-945 L-946 L-948 L-951 L-952 L-955 L-956 L-957 L-958 L-963 L-965 L-966 L-967 L-968 L-969 L-971 L-973 L-975 L-976 L-977 L-978 L-979L-980 L-982 L-983 L-985 L-987a L-987b L-990 L-991 L-992 L-993 L-994 L-995 -996 L-997 L-998 L-999 L-1000 L-1002 L-1003 L-1005 L-1007 L-1009 L-1010 L-1011 L-1012 L-1013 C-1 C-2 C-3 C-4 C-5 C-6 C-7 C-8 C-9 C-10 C-11C-13 (weath 1) C-14 R1R2 PLUTONIC ROCK CLASSIFICATION Kamanjab Batholith, Namibia; Lufilian G.P. (After De la Roche et al, 1980) P e t r o g r a p h i c fi e l d s S a m p l e s Fig 4.2.1.3 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 Ti) 5 0 0 L-832 L-835 L-836 L-838 L-839 L-840 L-842 L-843 L-844 L-846 L-849 L-857 L-863 L-864 L-865 L-868 L-874a L-875 L-877 L-878 L-898 L-899 L-900 L-902 L-903 L-904 L-905 L-906 L-907 L-909 L-910 L-912 L-917 L-922 L-923 L-924 L-938 L-939 L-943 L-945 L-946 L-948 L-957L-965 L-966 L-967 L-968 L-973 L-975 L-976 L-977 L-978 L-979 L-980 L-982 L-983 L-985 L-993 L-994 L-996 L-998 L-999 L-1000 L-1002 L-1003 L-1005 L-1007 L-1009 L-1010 L-1011 2 L-1013 C-1 C-2 C-3 C-4 C-5 C-6 C-7 C-8 C-9 C-10 C-11 C-13 (weath 1) R1R2 PLUTONIC ROCK CLASSIFICATION Kamanjab Batholith, Namibia; Lufilian G.P. (After De la Roche et al, 1980) P e t r o g r a p h i c fields Sampl e s Fig 4.2.1.4 Fig 4.2.1.4 1 7 1 1 7 2 1 7 3 Table 4.2.1.2 Statistics of rock ty pes, Kamanjab Batholith, Namibia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type Number % Granitoids Groups A l k a l i gran i t e 26 24.07 Q u a r t z m o n z o n i t e 38 35.19 S ye n i t e 3 2.78 M o n z o n i t e 2 1.85 73 . 4 0 Monzo d i o r i t e 1 0.93 M o n z o g a b b r o 1 0.93 Midalkaline Rocks A l k a l i gabbr o 3 2.78 68.52 Granite 22 20.37 G r a n o d i o r i t e 3 2.78 26 . 6 0 Quartz o l i t e 3 2.78 Subalkaline Rocks Garb o 1 0.93 26.85 Foid s yenit e 2 1.85 Fo i d o l i t e 2 1.85 Alkaline Rocks P e r i d o t gabbr o 1 0.93 4.63 Total 1 0 8 9 9 . 0 7 1 0 0 . 0 0 100.00 In general terms, geochemistry of the Kamanjab Batholit h shows the follow i n g trends (Fig 4.2.1. 5 ) : There is a negative correlation of silica with titanium dioxide, al umina, total iron oxide, manganes e oxide, magnesia , lime, soda and P 2 O 5 ; a positive correla tion was observed between silica and potas h. The correlation trends are very narrow and rather simple, as illustrated. There is a general uniformity in the chemical variation of the rocks . Mos t of the samples clus ter from 63 to 78% silic a . The diagrams of Si vs total iron, Si vs Al and modified TAS show two very distinct gr oups of granitoids (See Fig 4.2.1.5). Samples in each of t he two separate groups from the two diagrams are the same. After various studies , it became clear that the two groups have clear geochem i c a l and physica l distinc t i o n s . This will be discussed again in greater detail on section 4.2.1.6. Char ac t e r is t i c barium (and La?) enrichm e n t is wide spread throughout the batholith. Samples L-987 to L-992 all show enrichment in Mn, Mg, Ca, Cu and Sc. That suite seems to have formed in a non-anorogenic environment related to crustal contamination. Some groups of samples have high Pr values. 4.2.1.3 Main Rock Suites At least two contrasting rock types were identified in most of the regions visited through ou t the Kamanja b Batholi t h . These contras t in g rocks out crop togeth er in close spatia l associ a t i on . Each suite of samples was collec ted to obtain the repres entative roc k ty pes from a given, relatively small area. Table 4.2.1. 4 review s main aspects of each of the suites. In this case, rock names are based on the modified TAS diagram, and they have been plotted on Figs F1 to F16 in the Appendix. The suites are well spread across the Kamanjab Batholit h , as show n on Fig 4.1.2. 6. Six suites are described below for greater clar ity; more detailed descrip t i o ns of the rock suites are in clude d in Appendi x A64. Rock subgrou p s that make the suites are normally different from those of other suites . No two suites were identical. Althoug h severa l rock types may be repres e n t ed in a su ite, that does not mean the entire universe of rock types is present . There are many conditi o n s that bias sampli n g . For these reason s , the number of rock types in each of the suites of Table 4.2.1.4 should be cons idered to be an absolute minimum of the true conditions. Macros copically visible sulfides were found to be pres ent in a few of the suites. Copper primary sulfides and secondary minerals were also detected in select locations. This will be furt her described in section 4.2.1.10. 4.2.1.3.1 Examples of Rock Suites Suite B (Fig F2) has at leas t six disti nc t rock types : L-843 a n d L-839 make two differen t groups of granites ; L- 840 is an alkali granite; L-1011 an d L-1012 , L-838 an d L-842, a nd L-1010 make three contras t i ng groups of quartz monzon ites. Suite E (Fig F5) is made by three distin ct rock types: L-908 in the syenite field; L-904 , L-905 , L-906, L-911 a n d L-912 in at least three parts of the granite field, L-907 , L-909 an d L-910 in the alkali granite field. 1 7 4 Fig 4.2.1.5 Correlation diagrams between silica and the major oxides for samples from the Kamanjab Batholith, Namibia. All values are in percentage. Suite G (Fig F7) has L-940 in the monz on ite - qu ar tz mo nz on ite limit; L-939 , L-945 , L-946 a n d L-948 in the quartz monzon ite-alkali granite field, and L-943* in the alk ali granite. L-939 is a medium-grained granite. L-940 is one the very abundant mafic xenoliths contained by L-939 . L-945 is a foliated, coarse-grain ed granitoid that acts as hos t to all the other rocks in the suite . L-943* is one of many dikes that intersect L-945 , L-939 a nd L- 948 . All the chemis t r ie s are roughly similar , but on clos er examination, they can be discrim i n a t e d . The two main rock types have a non-ano r o g e n ic sign ature. Figs 4.2.1.19 are typical text ures of the four types of rocks. Note that all of them show the ?fuz zy? texture, especially Fig 4.2.1.19C. L-943* that was dated is shown too. In Suite H (Fig F8), L-958 is an alkali grabbro ; L-956 is a monzonite; L-957 is a granite, L-951 a nd L-952 span the syenite and quartzmonzonite fields; and L-955 is a quartzmonz on ite. The environs of this suite contain abundan t mineral iz e d hydr othe r m a l breccias hoste d in quar tzi t es and mainly confor me d by quartzi te s . Samples of the breccia s contain sulfides . None of the samples has been assayed to date. Figs 4.2.1.20 are typical textures of three of the suite ?s main rock types . 1 7 5 1 7 6 Table 4.2.1.4 Kamanjab Batholith rock suites that are made by two or more rock types ( U n d e r l i n e d suite s are miner a l i z e d . Dat ed sampl e s are marke d with an aster i s k . Photog r a p h e d sa mple s are in italic s . Bold sample s we re not anal ys e d . ) Sample number Samples Analysed Rock Types (sensu TAS) (#, quality, types) Environment of emplacement Map Notes Rock Groups TAS diagram A 4 L-832, L-834, L-835 3 Ver y good. Quart z m o n z o n i t e , alkal i grani t e , neph e l i n e s yeni t e Anorog e n i c K-17 CE 1, 8, 10 B 1 0 L-838, L -839 , L-8 40, L-842, L-843, L-1 010, L-1011, L -1012 6 Good Granite and Quartz m o n z o n i t e Non-A n o ro g e n i c (L-838 ) K-16 C 3, 5, 6, 8, 9, 10 , 14 C 9 L-863, L-864, L-8 65, L-868*, L -8 7 4 , L- 874-, L-875, L-867A, L-871, L-873 4 Ver y good. 2 quart z m o n z o n i t e s , granodi o r i t e an d altered granite Non Anoro g e n i c , subdu c t i o n ? (L- 864, L-86 8) K-14 SW Con t a i n s Au and Fe miner a l i z a t i o n , near major N-S fault 8, 11, P, Q D 6 L-898, L-899, L -9 0 0 , L-902, L-903 3 Good. Qua rtz m o n z o n i t e , granit e Anoro g e n i c Rift- re l a t e d K-16 WC Dis s e m i n a t e d Cu miner a l i z a t i o n 5, 10, 12 E 1 0 L-904 , L-905, L-9 06, L-907 , L-908, L-9 09, L-910, L-911, L-9 12 6 Ver y good. Sye nit e , grani t e , alkal i grani t e Anoro g e n i c K-16 WC 2, 9, 10, 12, 13, 14 F 4 L-919 , L-920, L -9 2 2 3 Ver y good. Quartz m o n z o n i t e , gabbro and altere d grani t e Anorog e n i c K-15 NW 3, 5, Q G 9 L - 9 3 9 , L -9 4 0 , L -9 4 3 * , L-945 , L-946, L -9 4 8 4: 2 quartz m o n z o n i t e , 2 alkal i gran i t e Non Anoro g e n i c (L-940 ) K-18 WC 5, 7, 9, 10 H 1 0 L-951, L-952, L -9 5 5 , L-956, L-957, L -9 5 8 , L-954 4 Ver y good. Gra nite , gabbr o , mo nzo n i t e Non-A n o ro g e n i c (L-958 ?) K-18 SC Dis s e m i n a t e d Cu miner a l i z a t i o n 3, 7, 10, G I 7 L-963 , L-965, L-9 66, L-967, L -9 6 7a 4 Good. Qua rtz m o n z o n i t e , alkal i n e grani t e , alter e d grani t o i d , monzo ni t e Anorog e n i c K-19 WC 5, 9, P, Q J 6 L - 9 6 8 , L -9 6 9 * , L - 9 7 1 , L-973 , L-975, L-9 76 4 Ver y good. Ne phe l i n e sye ni t e , s yen i t e , alka l i granite Anoro g e n i c K-19 SW Dis s e m i n a t e d Cu miner a l i z a t i o n 1, 2, 4, 9 K 6 L-977a, L -978 , L- 979, L-980, L -982 3 Ver y good. Quart z m o n o z o n i t e , alkal i granite Non-A n o ro g e n i c , Subduc t i o n (L-97 9, L-980, L-982) K-21 NW One of th e rock type s was not anal ys e d . 8, 10 L 4 L-983 , L-985, L-984, L-986 3 Not clear . Gran i t e , alkal i granite K-20 CW One of th e rock type s was not anal ys e d . 9 M 13 L-987, L -9 8 7a, L - 990, L-991 , L-992, L-9 93* , L-994, L -995, L -9 9 6 , L-997 , L-998 6 ver y go od. Alkal i grani t e , quart z m o n z o n i t e , vario u s gabbr o i d s , qua rt z syeni t e Non-A n o ro g e n i c , Subduc t i o n (L-99 1) K - 2 0 CW Dis s e m i n a t e d Cu miner a l i z a t i o n . Seems to have a large fract i o n a t i o n seque n c e . 3, 6, 9, G N 6 L-998, L-999, L -1 0 0 0 , L-1001, L -1 0 0 2 , L - 1 0 0 3 2 good, qua rt z m o n z o n i t e , granite Anoro g e n i c K-24 C Disse m i n a t e d Cu miner a l i z a t i o n around a major E- W fract u r e zone. 5, 10 O 1 L-855* (Se e sampl e plotte d on the TAS diagra m for Suite A) 3 granit e Anoro g e n i c K-14 WC Hos t to IOC G miner a l i z a t i o n at Tevred e , NW Kaman j a b , Nami b i a 5, 8, 10 P 5 C-2, C-3, C -4, C-5, C- 6 3 Simpl e . Quart z m o n z o n i t e , alkal i granite Anorog e n i c K-24 5, 8, 10 Q 11 C-1, C-2, C -3, C-4, C- 5, C-6, C-7, C-8, C-9, C-10, C-12 4 Simpl e . Quart z m o n z o n i t e , alkal i granite Non-A n o ro g e n i c , ma ybe subdu c t i o n a l . (C- 10) K-24 Zirco n s from suite date d coll e c t i v e l y by Cliffo r d , 1969. 5, 8, 10, 15 1 7 7 Suite J (Fig F10) is made by at least four distinct rock types. L-969 is a nepheline syenite; L-971 is a syenit e ; L-973 is a granite of group D; and L-968 , L-975 a nd L-976 are granit es of group K. The copper anomaly shown by the granitoids is marked by signifi c an t potassic enric hmen t (Table 4.2.1.1 ) . That alterat i o n was what originally called attention to the sample s. Note the hi gh Rb to Sr ratios in the suite of rocks. L-971 has miarolitic cavities. Also note the fuzzy texture in L-968 and L-969. As show n on the location map, this suite occurs along a major E-W trending fault zone (Fig 4.2.1.6). Suite K is composed of three contrast i ng rock types. Fig F11 shows two of them, a quartz m on z on i t e ( L-979 , L-980 and L-982 ) , and an alkali granite ( L-977 a nd L-978 ). Suite M (Fig F13) is specia l , becaus e it has a wide range of rock types that make at least six contrastin g group s of rocks . L-993 , L-994 a n d L-996 are alkali granites; L-997 a n d L-998 are two distinc t types of quartz monzon ites; L-990 is a monz od ior ite ; L-992 is a monz og a bbr o ; L-987a and L-991 are alkal i gabbr os ; L- 987b is a foid gabbro; and L-995 is a peridot gabbro. Significant di sseminated copper mineralization is associated to the suite. Varied type s of minera l i z a t i o n occur along the fractur e zone, includ i n g iron oxide- c o pper gold sys tems . L-993 is a dioritic rock with xenoliths. L-995 contains high Ti, Fe, Ca and Cu. L-997 intrudes L-998. L-996 also contain s high Cu. L-997 has abundant miarolit i c cavities . Table 4.2.1.4 shows that most of t he differ e n t suites have granit es or alkali granit e s in common . Whenev e r intrusive relationships were observed, these rocks we re the oldest, make the local basement, and were intruded by quartzmo nz on ite s , syenites , other granitoid s and/or gabbroid s (See also Table 4.2.1.1 7 ) . In the proc es s , the older granite s were someti m e s heavil y al tered. The samples that plot as quartz olites are intensely silicified grani tes from that group. L-874 from Suite C is an example of that type of rock with silic a alteration. Fig 4.2.1.2 1 shows a few of these ro cks. Although the images are in sharp focus, the crystalline texture of the granito id s is not distinc t . That is a common featur e obs erved in the majority of rocks throughout the Kamanjab Batholith. Most of the mineral constituen ts have been ?solde red ? together by hydrother m a l or metamorph i c proc es se s . Fig 4.2.1.21 Photos of rocks with ?fuzzy? texture, Kamanjab Batholith. A, L-923; B, L-853; C, L-100 6a; D, 100 7b (quartmon zo nite). T hese samples sh ow gradational contac ts betw een crystals and coarse blue q uartz ph enocrystals. Both features s ee m to have formed by incipient migmatit ization. More details in the text. Scale in millimet ers. 1 7 8 Fig 4.2.1.19 Photos of samples from Kamanjab Suite G . A, L-939a; B, L-940; C, L- 943 b; D, L-945 ; and E, L-948. Fig 4.2.1.20 Photos of samples from Kamanjab Batholith Suite J . A, L-968; B, L-97 1; C, L-973. 1 7 9 4.2.1.4 Sample Grouping The samples from the Kamanja b Batholi th were geochem i c a l l y subdiv i d e d using logari t hmi c major oxide plots into five main rock groups and a few unc las s i f i ed sample s, as indicated on Table 4.2.1.12. The main gr ou ps are: 1) Quartz m o nz on i t e s , 2) Alkali granite s , 3) Grani tes, 4) Syenites, and 5) Gabbroid rocks. Chemic al analyses of the samples sorted by grou ps are listed on Tables 4.2.1.5 to 4.2.1.10, and they have been plotted as major oxide logarit h m ic diagrams on Figs 4.2.1.7 to 4.2.1.1 2 . Trace elements and some rare earths were plotted on Figs 4.2.1.13 to 4.2.1.18. Geoc hemic al char ac t er is t i c s of the variou s groups are descri be d below. 4.2.1.4.1 The Group of Quartzmonzonites is made of samples that are mainly quartz m on z on i t e s s e nsu the R1/R2 diagram of De la Roche, 1982. More than 95% of the samples that make the group are metalu mino us and mesocrati c . The majority is sodic and all are ferrifer o u s. A typical rock of that group is a metalumino us iv mesocrat i c sodic ferrifer o us quartzmo n z o n i t e . Gran odi or i t es and granite s are also include d with quartz mon z on i t e s . Surprisi n g l y , the group has the la rges t numbe r of non-anor o g e n ic sample s, as show n by the proc edu r e of Whalen et al, 1987 (Tabl e 4.2.1.1 2) . Three of the sample s ( L-979 , L-980 an d L-982 ) plot as granit o id s of island arc or contine n t a l arc environ m ent in the diagram s of Maniar & Piccoli, 1985. Sample s from the Group of Quartzmonz onites are preety hom ogen eo us , as show n on the close matc h of the logarit hmi c major oxide diagrams (Fig 4.2.1.7 ) , and on the R1R2 and TAS diagrams (Figs 4.2.1. 2 and 4.2.1.4). In comparison with the rest of the granitoids in the Kamanjab Batholith, they contain relatively high values of total iron, MgO, P 2 O 5 , MnO (around 0.1%), and TiO 2 ; SiO2 and K 2 O values are low. The variation in CaO is minima l, and values for K 2 O, Na 2 O and total iron are all very similar to each other (Fig 4.2.1.7). Barium is normal l y high, and most of the sample s analys e d contain anomal o us Pr. The genera l order of abundanc e for the major oxides below Fe, Na and K is: Ca, Mg, Ti, P, Mn. Trac e elemen t logarit h m ic plots also show similar chemis t r y among the group of quartz m o nz on i t e s . Most elements except for chrome have elemental values that oscilla te in less than an order of magnitu d e . The general order of abundanc e for trac e elements is the follo wing: Ba, Sr, Zr, Rb, Zn, V, Y, Cu, Ga, Th, Nb, Sc, Ni, Co, U. Samples from the quartzmo n z o n i t e group produc e a dens e clus ter in most of the geoc he mical variation diagrams. They cons titute a discrete and probably related family of rocks. 1 8 0 Table 4.2.1.5 Chemical Analysis of the Gr oup of Quartzmonzonites, Kamanjab Batholith Sample SiO2 TiO2 Al2O3 FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu C-10 68.63 0.49 15.01 3.06 0.07 1.22 2.7 4 4 . 4 1 3 . 6 0 0 . 2 0 0 . 5 7 1 0 0 . 0 0 6 5 720 25 230 <10 C-6 66.09 0.69 14.60 4. 78 0.08 1.81 2. 5 4 3 . 2 5 4 . 7 1 0 . 2 8 1 . 1 1 9 9 . 9 4 1 5 0 480 25 280 <10 C-7 69.29 0.47 14.55 3. 29 0.06 1.19 2. 8 3 3 . 3 3 4 . 4 0 0 . 1 7 0 . 4 6 1 0 0 . 0 4 230 650 25 320 10 L-1007 64.26 0.56 15.15 5.20 0.10 1.92 3. 5 6 4 . 0 3 3 . 9 2 0 . 2 0 0 . 5 5 9 9 . 45 169 234 45 318 16 7 10 22 L-1009 66.67 0.69 15.06 4.31 0.09 1.05 2. 8 1 4 . 1 2 4 . 4 2 0 . 2 6 0 . 8 8 100.36 129 347 38 354 15 7 7 18 L-1010 63.36 0.80 15.40 5.08 0.11 1. 26 3. 2 7 4 . 1 5 4 . 2 4 0.34 1.17 99.18 138 385 37 372 15 9 10 21 L-1011 66.33 0.64 14.74 3.94 0. 09 0.94 2. 7 2 4 . 5 3 4 . 4 3 0 . 1 9 0.82 99.37 152 302 38 308 20 7 9 21 L-1012 64.77 0.68 15.28 4.30 0.20 0.95 3. 0 1 5 . 4 1 3 . 9 4 0 . 2 0 0 . 9 7 9 9 . 71 132 337 42 332 22 8 10 9 L-1013 67.41 0.61 14.33 4.04 0. 08 0.94 2. 0 9 4 . 0 0 4 . 7 2 0 . 2 1 0.95 99.38 171 240 39 331 16 6 10 26 L-832 73.67 0.32 12.24 1. 83 0.04 0.14 0. 4 6 4 . 3 9 5.23 0.11 0.63 99.06 154 297 38 307 15 8 10 19 L-835 65.67 0.65 15.35 3.98 0.08 0.87 2. 2 9 4 . 4 1 4 . 4 8 0 . 1 9 1 . 4 4 9 9 . 4 1 135 203 38 342 15 <6 <6 7 L-836 67.42 0.74 14.82 4. 07 0.10 0.86 2. 2 1 4 . 0 8 4.77 0.20 0.79 100.06 159 266 40 343 17 6 <6 19 L-838 67.61 0.61 14.50 3. 84 0.09 0.82 2. 3 7 3 . 6 2 4 . 4 8 0 . 1 8 0 . 5 0 9 8 . 6 2 208 69 22 93 16 <6 8 10 L-8 4 2 65.32 0.68 14.27 4.45 0. 10 1.13 2. 6 4 4 . 1 7 3 . 5 0 0 . 1 9 2.76 99.21 141 316 38 361 16 10 11 37 L- 8 4 4 68.18 0.63 14.42 3.75 0. 08 0.82 2. 2 2 3 . 8 7 4 . 3 5 0 . 2 0 1.02 99.54 137 259 39 345 16 6 7 20 L-846 67.61 0.60 14.35 3. 72 0.08 0.89 1. 9 7 4 . 0 9 4.59 0.18 0.78 98.86 134 246 44 306 16 6 10 18 L-863 64.77 0.71 14.71 5. 42 0.08 1.57 3. 0 6 3 . 3 7 3.86 0.24 1.14 98.93 155 288 33 228 19 14 15 23 L- 8 6 4 66.28 0.74 14.57 5.01 0.09 1.56 2. 9 6 3 . 0 5 4 . 1 4 0.33 1.62 100.35 97 249 23 39 12 10 16 28 L- 8 6 5 66.29 0.76 14.63 4.88 0. 08 1.51 2. 5 3 3 . 0 9 4 . 3 8 0 . 2 7 1.26 99.68 179 240 34 241 19 10 20 21 L-868 66.57 0.77 14.29 4. 73 0.10 1.11 2. 0 9 3 . 5 6 4.38 0.29 1.15 99.04 112 186 32 22 15 10 13 14 L- 8 7 5 66.20 0.78 14.38 5.11 0.12 1.18 2. 9 0 3 . 7 4 4 . 2 5 0.30 1.32 100.28 138 222 46 329 23 7 13 14 L-8 7 7 66.24 0.93 13.94 5.04 0.09 1.14 2. 0 8 3 . 4 8 4 . 7 4 0.41 1.24 99.33 140 224 54 377 23 9 16 22 L-8 7 8 67.83 0.67 13.61 4.34 0. 09 0.95 1. 6 7 3 . 7 3 4 . 5 8 0 . 2 3 1.08 98.78 152 176 57 329 19 9 12 34 L-9 0 0 67.40 0.67 14.52 4.30 0.08 1.12 2. 2 1 4 . 8 3 4 . 0 1 0.21 0.90 100.25 101 244 40 361 16 8 8 17 L-940 62.87 0.57 14. 38 5.03 0.09 1.98 6. 0 5 4 . 0 2 3 . 4 0 0 . 2 0 0 . 6 9 9 9 . 2 8 1 3 3 422 23 173 12 14 13 22 L-979 66.06 0.48 15.03 3.97 0.09 1.33 3.1 8 4 . 2 3 3 . 6 7 0 . 1 4 0 . 7 9 9 8 . 9 7 1 0 8 435 35 143 15 10 10 76 L-980 67.03 0.53 15.05 4.32 0.09 1.37 3.2 0 4 . 4 7 3 . 4 8 0 . 1 8 0 . 7 7 1 0 0 . 4 9 1 1 5 424 32 157 17 10 15 28 L-982 66.31 0.56 15.11 3.80 0.09 1.18 3.0 9 4 . 7 2 3 . 5 7 0 . 1 9 0 . 8 0 9 9 . 4 2 9 9 495 25 176 12 11 10 11 L-998 64.78 0.73 15.67 4.59 0.11 1.41 2. 7 8 4 . 5 2 4 . 0 3 0 . 2 4 1 . 3 3 100.19 103 300 34 347 15 6 9 29 Sample Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta Eu Gd Tb Dy Ho Er Tm Yb Lu C-10 20 55 30 1900 18 70 C-6 20 85 18 1900 14 75 C-7 19 70 35 1700 16 70 L-1007 61 17 38 <12 1413 <6 22 <10 160 78 L-1009 71 17 53 <12 1757 <6 16 10 115 55 L-1010 74 18 53 <12 1944 <6 <15 12 110 55 L-1011 73 17 50 126 1322 <6 17 10 129 66 L-1012 331 17 53 105 1550 <6 17 <10 139 74 L-1013 67 17 47 <12 1290 <6 19 <10 108 41 7 9 131 35 48 0.6 1.7 1.0 L-832 70 17 46 <12 1468 <6 19 <10 121 58 L-835 68 17 40 <12 1318 <6 15 10 127 60 L-836 69 0 45 <12 1272 0 0 0 0 0 L-838 30 15 12 <12 552 4 21 <10 130 55 L-842 83 16 49 13 1668 <6 16 12 11 33 83 135 41 1.5 63 1. 0 1.6 1.1 L-844 62 17 42 <12 1378 6 16 <10 129 63 L-846 56 15 39 <12 1240 <6 19 <10 12 42 87 133 45 50 1.0 1.9 1.1 L-863 72 18 100 122 1004 <6 17 11 89 44 L-864 58 16 91 273 1039 3 13 10 17 6 38 10 78 45 0. 8 1 . 4 1 1 . 3 5 . 3 0.7 4.4 0.9 2.4 0.3 2. 2 0 . 3 L-865 68 17 84 226 1100 <6 16 10 129 67 L-868 . 19 68 114 1100 <6 <15 10 15 9 5 2 1 3 1 5 4 7 9 1 . 1 0. 8 1 1. 8 7 . 2 1. 0 6.1 1.2 3.4 0.5 3. 1 0 . 4 L-875 68 18 71 181 1294 <6 <15 10 12 43 111 1 5 7 5 4 77 1.6 2.0 1.2 L-877 75 19 62 17 1371 <6 17 10 169 87 L-878 71 19 46 16 1143 <6 17 <10 12 39 92 150 41 56 1.2 2.6 1.2 L-900 43 17 48 <12 1239 <6 16 11 127 61 L-940 64 18 94 17 1043 <6 <15 11 9 25 64 90 31 80 0.4 0.6 1.0 L-979 88 16 68 242 1077 <6 <15 11 92 44 L-980 62 17 72 200 1140 <6 <15 <10 104 52 L-982 56 17 54 <12 1245 <6 <15 <10 9 27 66 74 30 54 0.4 0.6 0.8 L-998 96 18 53 13 2134 <6 <15 10 10 32 79 106 38 63 0.9 1.0 1.0 1 8 1 4.2.1.4.2 The Group of Alkali Granites is less well cons tra in e d . It mainly has leucocr a t i c to subleuc oc r a t i c ferriferous granitoids. It is composed by alkali granites and granites of varying charac ter, as shown on Table 4.2.1.6 and Fig 4.2.1.8. The name of the group was derived from the majorit y of the samples . One of the main featur es of these rocks is that pot ash is more abundan t than soda, and s oda is more abundant than total iron; all three are clearly separate d from each other on the logarit hmi c major oxide plot. MnO and P 2 O 5 values tend to be low, and silica high. The general order of abundance for major oxides is: K, Na, Fe, Ca, Ti, Mg, P, Mn. Trac e element correl a t i o n is not very clos e , altho ug h most eleme n ts have a small range of variat i o n , as show n on Fig 4.2.1.14 . Table 4.2.1.6 Chemical Analysis of the Group of Alkali Granites, Kamanjab Batholith Sample SiO2 TiO2 Al2O3 FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu C-11 78.84 0.29 10.79 1.22 0. 03 0.09 0.6 0 2 . 9 4 5 . 2 0 0 . 06 0.22 100.28 120 65 55 180 18 C-13 (w 75.89 0.41 12.46 1. 20 n.d. 0.05 0 . 2 5 3 . 6 0 5 . 7 1 0 . 0 4 0 . 5 0 1 0 0 . 1 1 1 0 0 4 0 65 650 40 <10 <10 n. d. C-4 73.63 0.33 14.16 1. 37 0.02 0.00 0. 5 0 3 . 1 4 6 . 3 5 0 . 0 7 0 . 4 4 1 0 0 . 0 1 200 80 20 380 20 C-5 75.35 0.27 13.18 1. 30 0.02 0.00 0. 6 2 3 . 1 5 5.50 0.05 0.36 99.80 110 100 35 280 10 C-8 73.88 0.33 13.85 1. 11 0.03 0.18 0. 2 6 4 . 0 5 5 . 9 3 0 . 0 9 0 . 3 9 1 0 0 . 1 0 1 3 0 4 0 55 450 15 C-9 73.30 0.32 13.20 3. 41 0.01 0.00 0. 2 4 3 . 4 6 5 . 6 7 0 . 0 7 0 . 3 4 1 0 0 . 0 2 1 3 0 5 0 80 650 30 L-1002 77.59 0.26 11.61 1. 64 0.05 0.10 0. 3 2 3 . 5 9 4.97 0.03 0.33 100.49 180 40 25 134 22 <6 8 6 L-839 76.62 0.29 11.26 1. 41 0.04 0.23 0. 3 5 3 . 0 5 5 . 2 8 0 . 0 7 0 . 4 7 9 9 . 0 7 218 67 27 163 17 <6 9 19 L-843 75.42 0.33 12.58 1. 52 0.03 0.25 0. 3 1 3 . 0 1 4.39 0.10 1.13 99.07 163 61 41 199 20 <6 <6 6 L-849 73.54 0.33 12.99 1. 74 0.02 0.20 0. 1 4 3 . 7 8 5.57 0.04 0.55 98.90 189 43 24 243 27 <6 7 <6 L-855 76.63 0.15 11.87 1. 14 0.02 0.05 0. 2 5 4 . 7 0 4.06 0.02 0.25 99.14 88 39 10 71 10 <6 10 9 L-902 77.60 0.17 12.00 0. 96 0.02 0.08 0. 1 1 4 . 1 6 4.81 0.10 0.34 100.35 160 35 18 95 22 <6 7 33 L-903 79.24 0.19 10.48 1. 02 0.02 0.12 0. 1 4 2 . 9 8 4 . 9 9 0 . 0 4 0 . 3 2 9 9 . 5 4 262 21 23 103 16 <6 8 10 L-904 76.77 0.24 11.40 1. 61 0.05 0.16 0. 1 0 3 . 5 9 4 . 8 1 0 . 0 5 0 . 4 5 9 9 . 2 3 242 44 30 149 18 <6 8 15 L-905 77.13 0.29 11.44 1.46 0.03 0.23 0. 5 4 5 . 6 5 1 . 5 4 0 . 0 6 0 . 5 1 9 8 . 8 8 75 80 40 160 19 <6 9 17 L-906 76.57 0.27 12.23 1. 45 0.03 0.07 0. 3 2 3 . 0 0 5 . 9 7 0 . 0 3 0 . 4 2 1 0 0 . 3 6 254 43 51 164 21 <6 7 37 L-909 71.39 0.41 13.73 1. 94 0.07 0.35 0. 7 2 4 . 3 7 4.96 0.08 0.91 98.93 153 134 46 285 18 <6 8 25 L-912 73.33 0.37 13.50 1. 75 0.02 0.70 0. 2 2 2 . 0 5 5.30 0.08 1.55 98.87 139 29 38 273 20 <6 7 9 L-917 71.65 0.73 12.99 3. 87 0.08 1.25 0. 7 1 3 . 9 5 4.48 0.20 0.63 100.54 113 116 16 39 15 6 12 17 L-943 74.31 0.15 13.23 1. 77 0.04 0.03 0. 7 5 3 . 7 0 5.72 0.11 0.29 100.10 137 123 4 65 7 <6 9 19 L-957 75.71 0.31 11.71 1. 52 0.04 0.21 1. 0 9 2 . 9 0 4.90 0.05 0.66 99.10 126 135 32 207 20 <6 7 <6 L-968 72.13 0.34 13.69 2.21 0. 03 0.17 0. 8 9 3 . 9 9 4 . 7 9 0 . 0 5 0.51 98.80 136 145 37 225 15 7 9 20 L-973 71.06 0.42 12.34 2. 89 0.04 0.12 1. 9 0 0 . 5 1 9 . 9 7 0 . 0 9 0 . 9 7 1 0 0 . 3 1 266 42 47 249 19 6 <6 141 L-975 72.48 0.35 13.19 2.05 0. 06 0.27 0. 8 2 3 . 8 1 5 . 4 0 0 . 1 0 0.56 99.09 164 149 34 215 16 7 9 45 L-976 72.48 0.37 13.10 1. 84 0.04 0.29 0. 7 1 4 . 0 0 5.29 0.06 0.50 98.68 195 113 55 203 21 <6 10 8 L-977 74.68 0.27 11.99 1. 72 0.04 0.24 0. 5 5 3 . 8 6 5.21 0.04 0.45 99.05 121 81 27 197 13 <6 8 <6 L-978 76.43 0.22 11.10 2. 76 0.10 0.04 0. 2 8 4 . 1 6 5.19 0.05 0.18 100.51 139 58 15 133 17 <6 10 37 L-983 72.59 0.29 13.57 1. 83 0.04 0.07 0. 9 0 4 . 0 8 4.95 0.04 0.51 98.87 197 156 28 181 17 <6 6 7 L-985 72.90 0.46 12.76 2. 61 0.05 0.29 1. 3 9 3 . 7 2 4.25 0.06 0.63 99.12 123 219 5 51 6 <6 7 9 L-997 69.62 0.34 15.29 1.59 0.04 0.27 0. 5 1 5 . 8 8 5 . 3 3 0 . 0 5 0 . 7 3 9 9 . 65 135 65 57 241 22 8 9 8 X -18 69.24 12.00 0.00 0.55 3. 8 3 5 . 3 6 0 . 0 0 9 0 . 9 8 X-19 72.02 0.32 13.78 3.26 0.02 0.20 0. 3 9 4 . 0 7 5 . 1 8 0 . 0 3 0 . 6 5 9 9 . 9 2 X-20 76.01 0.23 12.05 1.71 0.03 0.20 1. 0 2 3 . 0 9 5 . 0 2 0 . 0 1 1 . 1 4 1 0 0 . 5 1 Sample Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta Eu Gd Tb Dy Ho Er Tm Yb Lu C-11 15 5 25 560 20 100 C-13 (w 25 <3 10 1000 30 90 <100 C-4 20 9 13 1200 40 95 C-5 20 5 15 1400 30 65 C-8 20 7 11 400 20 65 C-9 30 <3 14 1200 12 85 L-1002 14 14 10 <12 180 <6 28 <10 104 19 5 3 87 26 3.4 5 1.6 0.9 L-839 35 13 12 <12 565 <6 16 <10 102 44 L-843 25 14 16 177 907 <6 21 <10 113 35 7 4 126 32 4.0 10 0. 7 2.0 0.9 L-849 22 18 17 217 451 <6 16 <10 107 30 4 8 152 20 1.0 34 0. 3 0.2 0.4 L-855 11 15 <12 <12 328 <6 <15 <10 39 16 L-902 15 15 13 <12 131 <6 25 <10 85 39 L-903 15 13 <12 <12 132 <6 25 <10 80 38 L-904 37 15 <12 14 233 <6 21 <10 107 30 5 0 99 23 7 0.3 1.3 0.9 L-905 23 13 13 <12 672 <6 22 <10 116 55 L-906 14 13 <12 269 219 <6 19 <10 122 62 L-909 56 17 15 <12 1346 <6 18 <10 163 82 L-912 34 17 15 <12 787 <6 16 <10 148 47 L-917 50 15 46 15 967 <6 <15 <10 13 5 30 8 85 42 1.4 1 . 4 1 1 . 0 4. 6 0.6 3.7 0.7 1.9 0.3 1. 9 0 . 3 L-943 17 14 13 15 350 <6 28 <10 19 1 7 2 42 20 2.3 3 . 3 1 0. 1 0 . 7 0.1 0.6 0.1 0.5 0.1 0. 8 0 . 2 L-957 36 14 <12 228 571 <6 26 <10 112 34 6 0 156 79 3.2 7 0.3 0.3 0.7 L-968 86 15 16 <12 1370 <6 23 <10 110 17 29 110 11 3 26 0.5 0.8 L-973 70 9 28 12 1800 <6 18 <10 10 34 97 128 42 6 37 0.5 3.2 1.1 L-975 47 14 19 <12 1327 <6 21 <10 137 68 L-976 29 18 209 1114 116 48 9 2 71 3.2 13 1. 0 2 . 2 2.9 1. 1 L-977 39 15 12 <12 766 <6 16 <10 110 57 L-978 73 20 14 20 264 4 19 <10 21 2 13 4 5 0 2 5 0 . 8 5. 1 1 0. 3 1 . 8 0. 3 2.1 0.5 1.8 0.3 2. 8 0 . 5 L-983 32 15 13 <12 963 <6 19 <10 90 39 L-985 46 14 25 173 1580 1 17 <10 26 3 33 10 1 0 3 6 1 2 . 1 1. 5 0 1. 1 2 . 0 0.2 1.0 0.2 0.5 0.1 0. 5 0 . 1 L-997 24 16 19 <12 542 <6 33 <10 111 29 5 7 156 21 4.2 11 2.5 1.0 1 8 2 4.2.1.4.3 The Group of Granites is very homogeneous. It is almost exclus ively made of granites s ens u s tricto . Ranges of variation for most of the major oxides are small as show n on Table 4.2.1.7 and Fig 4.2.1.9. In general terms, the order of abundance of the oxides is: K 2 O, Na 2 O, FeOt, CaO, MgO, TiO 2 , P 2 O 5 and MnO. P 2 O 5 is normall y higher than 1 and MnO is lower than 1. In gener al, total iron values are higher than for the group of alkali granites, MgO and TiO 2 values are much higher, and lime has a small range of variati o n. Ba and Pr values tend to be high. Trace element values ar e quite uniform for the group of granites, except for chrome, as shown on Fig 4.2.1.15. Table 4.2.1.7 Chemical Analysis of th e Group of Granites, Kamanjab Batholith Sample SiO2 TiO2 Al2O3 FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu C-2 69.71 0.68 14.17 3.26 0.04 0.84 0. 8 2 4 . 1 0 5 . 3 0 0 . 2 7 0 . 6 7 9 9 . 8 6 7 0 1 1 0 45 550 30 C-3 68.63 0.67 15.43 2.77 0.10 0.51 1.9 9 4 . 5 0 4 . 4 2 0 . 1 8 0 . 5 0 9 9 . 7 0 9 0 3 5 0 140 700 40 L-1000 67.91 0.47 15.37 2.32 0.06 0.52 1. 0 6 4 . 2 8 5 . 1 1 0 . 1 0 1 . 6 8 98.88 192 112 37 251 18 <6 10 62 L-1003 68.00 0.50 15.07 2.73 0.05 0.58 1. 6 0 4 . 6 4 5 . 2 6 0 . 1 2 0 . 6 9 9 9 . 24 145 242 40 289 16 <6 8 12 L-1005 71.20 0.48 12.46 3.35 0. 06 0.56 1. 4 7 3 . 9 3 4 . 4 7 0 . 1 8 0.76 98.92 171 218 46 298 18 7 9 15 L-840 70.88 0.42 13.61 2. 64 0.07 0.48 1. 2 9 3 . 9 7 4.93 0.13 0.75 99.17 176 247 37 237 15 <6 8 20 L-8 5 7 73.33 0.32 13.00 1.84 0. 04 0.43 1. 2 1 4 . 0 1 4 . 2 1 0 . 1 1 1.00 99.50 155 211 17 141 14 <6 9 26 L-898 69.20 0.58 12.94 5. 11 0.08 0.60 1. 6 2 4 . 2 1 5.14 0.15 0.09 99.72 112 193 33 215 15 <6 7 17 L-907 71.26 0.43 13.59 2. 43 0.06 0.51 1. 3 4 3 . 8 5 5.07 0.11 0.52 99.17 175 181 41 248 16 <6 8 11 L-9 1 0 70.84 0.59 13.17 3.28 0.04 0.51 0. 5 3 4 . 2 1 4 . 2 4 0.20 1.11 98.72 129 126 44 360 17 <6 8 12 L-9 2 2 68.49 0.77 14.39 4.18 0.07 0.89 1. 6 9 3 . 7 6 4 . 8 8 0.23 0.98 100.33 143 206 56 426 27 8 9 15 L-92 3 70.32 0.62 13.18 3.95 0.06 0.59 0. 9 2 4 . 0 3 4 . 6 7 0.17 1.02 99.53 162 156 56 425 21 6 12 11 L-9 2 4 71.99 0.63 12.33 2.83 0. 05 0.57 1. 4 6 3 . 5 8 3 . 9 7 0 . 1 3 1.69 99.23 82 63 46 359 22 8 9 14 L-93 8 70.06 0.58 13.36 3.13 0. 05 0.58 1. 7 0 4 . 1 6 4 . 1 1 0 . 1 9 0.90 98.82 76 244 38 294 19 6 7 11 L-939 68.27 0.56 15.25 3.83 0.08 0.63 1.8 9 3 . 5 5 5 . 2 8 0 . 1 4 0 . 7 4 1 0 0 . 2 2 1 3 2 422 22 166 11 15 16 29 L-945 67.85 0.52 15.01 3.25 0.07 0.55 1. 4 0 4 . 1 9 5 . 0 8 0 . 1 1 0.92 98.95 169 235 45 386 18 9 8 20 L-94 6 67.96 0.48 14.78 2.89 0. 06 0.59 1. 5 8 4 . 3 9 5 . 0 1 0 . 1 2 0.73 98.59 165 232 38 250 19 6 8 8 L-948 70.39 0.65 13.17 3.48 0.11 0.62 1. 5 8 4 . 4 8 4 . 4 7 0 . 1 3 0 . 4 1 9 9 . 4 9 1 6 0 1 7 4 63 368 21 7 8 10 L-967 70.72 0.48 12.92 3. 64 0.07 0.46 1. 1 1 3 . 7 8 5 . 0 5 0 . 1 2 0 . 6 3 9 8 . 9 8 269 119 83 395 22 8 9 13 L-99 3 71.34 0.39 13.57 2.03 0. 05 0.39 1. 4 2 3 . 9 7 5 . 3 3 0 . 0 7 0.81 99.37 115 224 27 75 11 <6 6 8 L-99 4 70.70 0.40 13.83 2.09 0. 05 0.43 1. 4 6 3 . 9 5 5 . 0 7 0 . 0 9 0.73 98.80 110 226 37 208 19 6 7 10 L-999 67.68 0.49 14.73 3. 02 0.07 0.74 1. 8 3 4 . 3 1 4.65 0.13 1.19 98.84 140 252 37 288 20 <6 9 10 Sample Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta Eu Gd Tb Dy Ho Er Tm Yb Lu C-2 25 35 25 2100 8 90 C-3 25 35 11 2500 25 130 L-1000 58 17 35 <12 1206 <6 20 <10 12 90 152 1 3 4 8 0 82 3.5 2.6 1.2 L-1003 47 17 32 <12 1796 <6 15 <10 8 29 79 133 26 2.6 32 0. 8 1.7 1.0 L-1005 50 17 26 16 1194 <6 18 <10 132 64 L-840 47 16 20 <12 1054 <6 18 <10 127 62 L-857 28 15 22 <12 1081 <6 <15 <10 80 38 L-898 46 27 189 1049 L-907 44 15 24 <12 1136 <6 16 <10 135 69 L-910 47 16 26 <12 1115 <6 <15 <10 152 76 L-922 58 18 56 244 1598 <6 16 10 22 53 122 1 5 9 5 6 62 1.7 4. 3 2.5 1.1 L-923 55 18 37 <12 1168 <6 21 <10 159 89 L-924 26 15 38 <12 1811 <6 19 <10 158 79 L-938 44 16 40 266 1785 <6 <15 <10 24 117 49 8 4 96 37 1.4 3.2 3 8 1 . 4 3. 2 0. 5 3.7 0.8 2.4 0.4 1. 2 0 . 9 L-939 68 16 89 23 1059 <6 <15 11 8 30 58 77 28 78 0.6 0.9 L-945 64 18 2 13 1409 <6 19 <10 12 42 115 1 7 8 5 3 61 0.9 1. 7 2.5 1.1 L-946 45 16 30 185 1451 <6 <15 <10 175 88 L-948 73 17 22 <12 1424 <6 15 <10 175 92 L-967 60 17 31 <12 883 8 36 <10 259 130 L-993 34 15 24 160 1595 <6 17 <10 23 7 47 13 1 3 9 6 9 0 . 5 2. 4 1 1. 2 5 . 8 0.8 5.1 1.0 2.9 0.4 2. 8 0 . 4 L-994 33 15 32 195 1763 <6 <15 <10 142 70 L-999 58 17 33 205 1537 <6 16 <10 10 36 92 144 44 1.5 39 0. 8 1.5 0.9 1 8 3 4.2.1.4.4 The Group of Syenites is far from homoge ne o us . Nephel i n e syenit e s , syenite s and quar tz syenit es have been joined togeth er . In broad terms, these rocks have low K and Mg, and high Na. The general order of abundance of the major oxides , is Na, Fe , Ca, Ti, K. Table 4.2.1.8 lists the chemical analysis of member s of this group. Their major oxides are plo tted on Fig 4.2.1.10 and their trac e element s are plotted on Fig 4.2.1.16 . Table 4.2.1.8 Chemical Analysis of th e Group of Syenites, Kamanjab Batholith Sample SiO2 TiO2 Al2O3 FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu X-16 75.93 0.26 12.08 3.28 0.01 0.36 0. 4 8 7 . 9 3 0 . 1 3 0 . 0 7 0 . 4 2 1 0 0 . 9 5 X-17 72.07 0.33 13.36 4.01 0.02 1.33 1. 0 1 7 . 9 5 0 . 3 0 0 . 0 4 0 . 4 9 1 0 0 . 9 1 L-955 67.86 0.41 16.46 3.50 0.05 0.11 0. 3 3 1 0 . 1 6 0 . 1 9 0 . 2 3 0 . 8 2 1 0 0 . 12 4 37 40 340 17 <6 13 333 L-951 66.61 0.52 15.75 3.69 0.02 0.04 0. 5 0 1 1 . 3 4 0 . 3 3 0 . 1 2 0 . 1 9 9 9 . 11 4 30 50 261 24 <6 10 6 L-952 67.68 0.59 15.55 4.09 0.02 0.15 0. 7 3 1 0 . 8 6 0 . 3 5 0 . 1 5 0 . 2 2 1 0 0 . 39 6 38 36 308 23 <6 9 6 L-908 66.78 0.41 16.95 1.82 0.08 0.28 0. 2 2 9 . 5 7 2 . 6 3 0 . 0 3 0 . 3 4 9 9 . 11 96 28 10 66 16 <6 8 12 L-920 36.93 0.23 6.77 1.19 0.03 0.22 0. 2 9 2 . 9 0 2 . 7 2 0 . 0 6 49.01 100.35 124 81 20 208 15 <6 <6 16 L-971 64.34 0.54 17.73 1.51 0.09 0.14 0. 6 8 4 . 5 8 8.51 0.11 0.69 98.92 148 66 47 358 22 <6 9 10 L-969 59.46 0.49 19.16 4.28 0.05 0.68 0. 3 8 0 . 5 5 1 4 . 3 1 0 . 0 8 0 . 8 4 1 0 0 . 2 8 393 66 59 293 24 6 <6 47 L-834 59.92 0.47 16.55 4.88 0.05 0.10 1. 7 2 0 . 2 9 1 4 . 0 6 0 . 1 2 1 . 2 8 9 9 . 4 4 283 70 49 274 20 7 <6 14 L-956 61.48 2.00 9.60 15.05 0.04 0.23 2. 7 2 7 . 3 8 0 . 0 1 0 . 9 2 0 . 2 3 9 9 . 6 6 5 3 6 63 321 14 9 11 7 L-997 69.62 0.34 15.29 1.59 0.04 0.27 0. 5 1 5 . 8 8 5 . 3 3 0 . 0 5 0 . 7 3 9 9 . 65 135 65 57 241 22 8 9 8 L-965 67.45 0.59 13.65 6.24 0.03 0.32 0. 6 9 4 . 1 0 5 . 7 3 0 . 1 9 0 . 4 2 9 9 . 4 1 1 5 6 4 3 88 358 29 <6 11 8 L-9 6 6 68.15 0.60 12.90 6.30 0.02 0.16 0. 4 3 4 . 4 6 5 . 6 8 0 . 1 9 0 . 2 7 9 9 . 1 6 1 4 4 3 9 74 108 17 <6 9 6 L-863 64.77 0.71 14.71 5. 42 0.08 1.57 3. 0 6 3 . 3 7 3.86 0.24 1.14 98.93 155 288 33 228 19 14 15 23 Sample Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta Eu Gd Tb Dy Ho Er Tm Yb Lu L-834 19 9 26 <12 1842 7 25 <10 12 42 111 1 9 2 5 4 2.9 77 0. 7 2.5 1. 3 L-863 72 18 100 122 1004 <6 17 11 89 44 L-908 53 26 <12 <12 125 <6 15 <10 10 2 17 5 82 40 1.5 2.0 1 0 . 3 1. 9 0.3 1.8 0. 4 1.2 0.2 1. 6 0 . 3 L-920 29 14 17 134 1088 <6 <15 <10 113 36 6 2 99 29 19 0.7 0.2 0.7 L-951 9 16 39 137 <20 <6 22 <10 11 28 110 1 6 6 1 4 49 0.7 3. 1 1.9 1.1 L-952 10 16 31 173 52 <6 <15 <10 38 27 L-955 142 21 36 <12 30 <6 <15 16 13 62 671 965 4 0 5 43 0.4 1.8 1.0 L-956 17 17 91 <12 51 <6 <15 24 41 98 116 63 297 3.1 2. 1 L-965 24 17 33 12 741 7 30 <10 125 56 L-966 19 16 42 193 708 6 27 <10 18 6 35 10 103 45 0.4 3.1 1 0. 9 7 . 0 1.4 10 2.3 7.5 1.1 7 . 9 1. 2 L-969 53 22 61 <12 2451 6 29 <10 11 36 92 159 37 7.2 60 0. 7 3.1 1.3 L-971 14 13 34 <12 2236 <6 <15 <10 137 81 L-997 24 16 19 <12 542 <6 33 <10 111 29 57 156 21 4 11 2.5 1.0 4.2.1.4.5 All Gabbroid Rocks have been grouped togethe r for conveni en c e . This group of samples has the lowest values for silica, at times total iron exceeds alum ina, and lime is normally around 10%. Special charac - teristics for the group include: high Mg, Mn and P. None of the major oxides is belo w 0.1 percent. The order of the oxide abundan c e varies widely as shown on Fig 4.2.1.1 1 and on T able 4.2.1.9. Surprisin g l y , trace elements are very uniform, except for chrome and niobium, as illustrated on Fig 4.2.1.17. Table 4.2.1.9 Chemical Analysis of th e Group of Gabbroids, Kamanjab Batholith Sample SiO2 TiO2 Al2O3 FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu C-14 48.69 1.26 13.27 13.57 0.18 6.15 10 . 4 9 2 . 4 1 1 . 0 5 0 . 2 2 0 . 5 0 9 7 . 7 9 L-895 55.24 0.90 18.42 6.32 0.11 3.12 4. 5 4 4 . 2 3 4 . 6 1 0 . 5 0 1 . 9 3 9 9 . 9 2 1 6 4 840 22 172 7 18 43 164 L-958 47.73 1.22 15.13 13.06 0.23 7.23 8. 0 3 3 . 5 7 0 . 3 6 0 . 2 2 2.21 98.99 5 188 34 105 5 63 122 59 L-987a 45.74 2.33 16.73 14.31 0.17 4.10 10 . 5 3 2 . 6 2 1 . 5 9 0 . 4 6 1 . 9 9 1 0 0 . 5 7 2 2 598 11 18 2 41 8 75 L-987b 40.92 2.62 19.28 13.71 0.19 4.13 12 . 8 1 2 . 4 5 0 . 7 9 1 . 1 9 2 . 0 6 1 0 0 . 1 5 3 5 646 19 31 4 28 <6 37 L-990 53.79 0.31 13.92 7.16 0.15 8.22 7. 5 9 5 . 5 2 0 . 3 2 0 . 1 0 2.29 99.37 10 267 12 84 10 38 178 73 L-991 48.45 0.96 11.97 11.52 0.19 11.57 9 . 2 0 3 . 0 7 0 . 4 6 0 . 1 2 1 . 70 99.21 7 217 20 53 9 64 251 83 L-992 50.94 0.49 19.38 7.11 0.15 5.16 9. 7 9 3 . 1 6 1 . 8 7 0 . 0 9 2 . 2 5 1 0 0 . 3 9 6 7 659 10 28 3 27 53 35 L-995 39.21 3.69 11.13 22.15 0.26 7.20 10 . 8 3 1 . 6 0 0 . 5 3 1 . 1 3 1 . 1 3 9 8 . 8 6 1 4 449 21 27 4 59 <6 54 Sample Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta Eu Gd Tb Dy Ho Er Tm Yb Lu L-895 69 18 134 91 1382 <6 <15 14 8 23 54 74 22 99 0.3 0.4 0.9 L-958 119 19 296 107 297 <6 <15 37 15 <12 L-987a 109 17 429 <12 397 <6 <15 36 8 3 1 1 2 <1 2 < 1 2 0. 3 0 . 5 0 1 . 0 2. 9 0.4 2.4 0.5 1.2 0.2 0. 9 0 . 1 L-987b 72 17 307 <12 284 <6 <15 32 7 29 16 5 284 1.3 L-990 69 13 75 584 187 <6 <15 20 39 22 L-991 93 12 255 870 188 <6 <15 35 19 12 L-992 53 16 144 100 460 0 1 26 4 2 1 0 2 19 9 0 . 5 0. 7 0 0. 8 2 . 0 0. 3 1.9 0.4 1.1 0.2 1. 0 0 . 2 L-995 128 19 491 <12 457 <6 <15 45 <12 <12 1 8 4 A few rocks could not be classi f i ed into the above gr oups, and they were left as undefined. Some of them have been subject to hydrothe r m a l alterati o n . Table 4.2.1.10 Chemical Analysis of the Gr oup of unclassified samples, Kamanjab Batholith Sample SiO2 TiO2 Al2O3 FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu C-1 74.03 0.27 12.73 2.66 0.05 0.31 0. 4 8 3 . 6 7 5 . 0 9 0 . 0 5 0 . 7 1 1 0 0 . 0 5 1 0 0 5 0 70 500 30 <10 <10 n. d L-874 96.83 0.09 0.64 0. 69 0.01 0.00 0. 0 2 0 . 0 2 0.31 0.03 0.08 98.72 11 8 5 29 4 <6 13 8 L-874a 67.47 0.89 13.68 4. 67 0.10 1.05 1. 7 1 3 . 4 8 4.99 0.27 1.09 99.40 155 181 57 348 24 12 14 19 L-899 71.98 0.41 12.65 2. 41 0.06 0.72 1. 7 9 4 . 2 3 3.72 0.11 0.69 98.77 112 193 33 210 18 <6 7 17 L-911 72.60 0.37 14.49 2.24 0. 03 0.81 0. 2 2 0 . 1 6 5 . 1 9 0 . 1 1 2.40 98.62 170 16 45 344 27 <6 10 33 L-919 87.60 0.31 4.60 3. 09 0.03 0.08 0. 0 9 0 . 1 2 2 . 0 9 0 . 0 4 0 . 7 9 9 8 . 8 4 7 9 9 11 99 8 6 15 13 L-963 88.82 0.21 4.22 2. 07 0.03 0.19 0. 1 4 1 . 0 0 1.77 0.06 0.66 99.17 63 17 18 133 8 8 11 20 L-99 6 69.95 0.44 14.71 2.86 0. 06 0.50 1. 7 5 4 . 3 0 4 . 7 8 0 . 1 1 0.95 100.41 121 274 24 78 14 6 9 67 Sample Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta Eu Gd Tb Dy Ho Er Tm Yb Lu C-1 25 <3 10 1200 25 95 <100 L-874 6 17 <12 538 30 6 17 11 144 73 L-874a 69 63 17 1380 L-899 46 17 26 182 1049 <6 16 <10 119 56 L-911 48 19 17 139 398 <6 19 <10 145 75 L-919 14 <9 27 32 297 <6 <15 <10 55 26 L-963 15 <9 25 12 308 <6 <15 <10 64 31 L-996 71 16 30 <12 1498 3 15 <10 23 6 40 11 1 1 3 4 9 0 . 7 2. 3 1 1. 2 5 . 0 0.7 4.7 0.9 2.8 0.4 2. 9 0 . 4 Three of the five main rock groups can be easily disting u i s h e d on the TAS and R1R2 diagrams . Thes e are the group of gabbroids, that of syenites and the unc lassified sample s. Alkali granite s, granites and quartz m on z on i t e s clus ter clos ely in both diagrams and ar e difficult to separate. The diagrams of Si vs total iron, and Si vs Al can be used to separat e quartzm o n z o n i t es from granites and alkali granites (See Fig 4.2.1.5). Clos e inspec tion of the TAS diagram can also achiev e that discri mi na t i o n (Fig 4.2.1.2) . Discrimi n a t i on between the alkali granite and granite gr oups was only possible using the logar i t hmi c major oxide diagram s . 4.2.1.5 Volcanic Rocks Volcan ic and volca n i c la s t ic rocks that have almost the same compositions as their plutonic counterparts, coexis t in the Kamanjab Batholith. This is due to t he intermediate level of eros ion in the plutonic/volcanic systems. Volcanic rocks correlate well with their plutoni c equival en t s . For example , X-16 and X-17 analysed by Frets, 1969, are the volc anic equival e n t of nepheli n e syenite s . Trac hyt i c rock L-834 is very similar to its pluto n ic counte r p ar t L-969 . Rhyolitic rock L-836 has very simila r chemis tr y to its granitic counte r p ar t L-1013 ; their major oxide and trace element chemistr y is almo st identic al. Something equivalent takes place between L-842 and L-1011 . L-842 is a rhyolit e with vacuoles and black matrix that carries significant copper; L-1011 is a quartzmo nz o n i t e . X-18 , X-19 an d X-20 correla t e well with the group of alkali granites . Table 4.2.1.1 1 pres ents example s of this feature , and their chemic a l similarity can be viewed on Figs 4.2.1.7 to .2.1.11. Table 4.2.1.11 Comparison of volcanic and plutonic rock types in the Kamanjab Batholith (See Figs 4.2.1.7 to 4.2.1.11) Volcanic Rocks Plutonic Rocks Sample Rock type Sample Rock type X - 1 6 , X-17 Alkal i rhyol i t e , rh yol i t e No preci s e match Nephe l i n e s yeni t e L-834 Trach yt e L-969 Nepheli n e s yenit e L-836 Rh yolite L-1013 Granite L-909 Alkal i rhyol i t e L-976 Alkal i grani t e L-842 Rh yol i t e with bla ck matri x L-101 1 quart z m o n z o n i t e L-977 , X- 18 Alkal i rhyol i t e L-839 , L-976 Alkal i grani t e L-1003 Quartz latite L-946, L-948 Granite X-18 Alkal i rhyol i t e L-977 Alkal i grani t e X-20 Rh yolit e L-957 Granite 1 9 8 Table 4.2.1.12 Groups of samples from the Ka manjab Batholith based on chemical similarity ( s ee acronym descrip t i on on section 2.4.3.) Group of Quartzmonzonites S a m p l e Rock Name Debon & Le Fort Mania r & Picco li Whal e n P i e r c e Mafic Rb/10 H f Ta Rb/30HfTa Nb-Ta L-832 alkal i grani t e metav leuco Na Fe POG A L-835 quart z m o n z o n i t e metai v meso Na Fe A L-836 granit e metaiv meso Na Fe A? L-838 granit e metaiv meso Na Fe N L-842 granit e metaiv meso Na Fe A O3/4 WP WP OUT U L-844 granit e metaiv meso Na Fe A L-846 granit e metaiv meso Na Fe A O2/3 OUT U L-863 granit e metaiv meso Na Fe A L-864 granod i o r i t e metaiv meso Na- K Fe N S2/4 O2/4 VA- II INV L-865 grano d i o r i t e perai i i meso Na-K A L-868 granit e metaiv meso Na Fe N S2/4 O2/4 VA- II INV L-875 granodi o r i t e metaiv meso Na Fe A? O3/4 OUT U L-877 granit e metaiv meso Na- K Fe RRG A O-W1- 1 L-878 granit e metaiv meso Na Fe A O3/4 OUT U L-900 quart z m o n z o n i t e metai v meso Na Fe A L-940 gabbro -d i o r i t e metav meso Na Fe N O3/4 OUT U L-979 quart z m o n z o n i t e metai v meso Na Fe IAG-CA G N L-980 quart z m o n z o n i t e metai v meso Na Fe IAG-CA G N L-982 quart z m o n z o n i t e metai v meso Na Fe IAG-CA G N OUT U L-998 quartz m o n z o n i t e metaiv meso Na Fe A O3/4 OUT U L-100 7 quart z m o n z o n i t e metai v meso Na Fe A L-1009 quart z m o n z o n i t e metai v meso Na Fe A L-1010 quart z m o n z o n i t e metai v meso Na Fe A L-1011 quart z m o n z o n i t e metav meso Na Fe A O-W1- 1 L-1012 Quart z m o n z o n i t e metav meso Na Fe A O-W1- 1 L-1013 Granite metaiv meso Na Fe A O3/4 OUT U C-6 Gran odi o r i t e metaiv meso Na- K Fe C-7 Gran od i o r i t e metaiv meso Na- K Mg C-10 Gran od i o r i t e metaiv meso Na Mg IAG-CA G Group of Alkali Granites S a m p l e Rock Name Debon & Le Fort Mania r & Picco li Whal e n P i e r c e Mafic Rb/10 H f Ta Rb/30HfTa Nb-Ta L-839 alkal i grani t e metai v leuco K Fe A L-843 alkal i grani t e perai leuco Na-K A O-W 2-2 WP- WP OUT U L-849 alkal i grani t e perai i i leuco Na-K Fe RRG -CE U G A O3/4 WP WP OUT U L-855 granit e metav leuco Na Fe RRG- C E U G A L-902 alkal i grani t e metai v leuco Na Fe RRG- C E U G A L-903 alkal i grani t e metai v leuco K Fe A L-904 alkal i grani t e perai i i leuco Na-K Fe RRG- C E U G A OUTU L-905 alkal i grani t e metai v leuco Na Fe POG N? O-W 1- 1 L-906 alkal i grani t e perai i i leuco K Fe POG A O-W 1- 1 L-909 alkal i grani t e metai v leuco Na Fe POG A O-W 1- 1 OUT U L-912 granit e perai subleu K Mg A O-W1- 1 L-917 granit e peraii i meso Na Fe A S2/4 O2/4 VA- II INV L-943 grani t e metai v leuco K Fe CEUG-R R G A S2/4 O2/4 VA- VA INV L-957 grani t e metai v leuco K Fe POG A O3/4 WP- WP OUT U L-968 granit e peraii i leuco Na Fe CEUG-R R G A O3/4 WP WP OUT U L-973 grani t e metav suble u K Fe A O3/4 WP WP OUT U L-975 granit e metaiv leuco Na-K Fe POG A L-976 alkal i grani t e metai v leuco Na-K Fe POG A O-W 2-2 WP- WP OUT U L-977 alkal i grani t e metav leuco Na- K Fe POG A L-978 alkal i grani t e metav leuco Na- K Fe RRG A S2/4 O2/4 VA- VA INV L-983 granit e metaiv leuco Na Fe CEUG- R R G A L-985 Granit e metaiv subleu Na Fe POG N S2/3 VA- VA OUT D-I NV L - 9 9 7 Quartz s yenit e metav leuco Na Fe CEUG A O-W 2-2 WP- WP OUTU L-100 2 Alkal i grani t e metai v leuco Na-K Fe RRG A VA- III OUTU C-4 Alkal i grani t e perai i leuco K Fe C-5 Granit e peraii leuco K Fe C-8 Alkal i grani t e perai i i leuco Na-K Fe POG C-9 Alkal i grani t e perai i suble u K Fe RRG C-11 Alkal i grani t e metav leuco K Fe C-13 Alkal i grani t e metai v leuco K Fe RRG X-18 Alkal i grani t e metav i leuco Na-K X-19 Alka l i gran i t e pera i i i subl e u Na-K Fe CEUG X-20 Grani t e metai v leuco K Fe POG 1 9 9 Group of Granites S a m p l e Rock Name Debon & Le Fort Mania r & Picco li Whal e n P i e r c e Mafic Rb/10 H f Ta Rb/30HfTa Nb-Ta L-840 Granit e metaiv subleu Na Fe POG A L-857 Alkal i grani t e metai v leuco Na Mg POG N L-898 Granit e metaiv meso Na Fe RRG- C E U G A L-907 Granit e metaiv subleu Na-K Fe POG A L-910 Alkal i grani t e perai i i meso Na Fe RRG- C E U G A O-W1 - 1 L-922 Granite metaiv meso Na- K Fe A O3/4 OUT U L-923 granit e metaiv meso Na Fe RRG- C E U G A O-W1 - 1 L-924 granit e metaiv meso Na Fe A O-W1- 1 L-938 granit e metaiv meso Na Fe A O3/4 WP WP OUT U L-939 grani t e perai i i meso Na-K Fe CEUG-RR G N? O3/4 OUT U L-945 granit e peraii i meso Na Fe CEUG A O3/4 OUT U L-946 granit e metaiv meso Na Fe A O-W1- 1 L-948 granit e metav meso Na Fe A O-W1- 1 L-967 granit e metaiv meso Na- K Fe RRG- C E U G A O-W1 - 1 L-993 granit e metaiv subleu Na-K Fe POG N? S2/4 O2/4 VA- VA INV L-994 granit e metaiv subleu Na-K Fe POG A O-W 1- 1 L-999 granit e metaiv meso Na Fe A O3/4 WP- WP OUT U L-100 0 grani t e perai i i suble u Na Fe A O3/4 OUTU L-100 3 quart z m o n z o n i t e metai v suble u Na Fe POG A O3/4 WP WP OUT U L-1005 granit e metaiv meso Na Fe RRG A O-W1- 1 C-2 grani t e perai i i meso Na-K Fe RRG C-3 granit e metaiv meso Na Fe Group of Syenites S a m p l e Rock Name Debon & Le Fort Mania r & Picco li Whal e n P i e r c e Mafic Rb/10 H f Ta Rb/30HfTa Nb-Ta L-920 sye ni t e metav leuco Na Fe CEUG A O3/4 wp ab OUT U L-969 nephe l i n e s yeni t e perai i meso K Fe CEUG A O3/4 WP WP OUT U L-951 nephe l i n e s yeni t e metav suble u Na Fe OP A V2/4 OUTU L-971 nephe l i n e s yeni t e metai v leuco K Fe CEUG A O-W1- 1 L-952 nephe l i n e s yeni t e metav meso Na Fe OP A V1/2 L-834 sye ni t e metav meso K Fe CEUG A O3/4 WP WP OUT U L-956 sye ni t e metav meso Na Fe OP A OUT U L-908 sye ni t e metav leuco Na Fe CEUG A S2/4 O2/4 VA- III INV L-955 nephe l i n e s yeni t e metai v suble u Na Fe OP A V3/4 OUTU L-965 quartz s yenit e metaiv meso Na- K Fe CEUG A W L-966 quartz s yenit e metaiv meso Na- K Fe CEUG- R R G A VA- III INV L-997 quart z s yeni t e metav leuco Na Fe CEUG A O-W 2-2 WP- WP OUTU Group of Gabbroids S a m p l e Rock Name Debon & Le Fort Mania r & Picco li Whal e n P i e r c e Mafic Rb/10 H f Ta Rb/30HfTa Nb-Ta L-895 sye no - d i o ri t e metai v meso Na Mg N? O3/4 wpt+v a b -c a b OUT U L-958 und-s a t oliv gabbr o metai v meso Na Fe NZn? V arc L-987a alkal i grani t e metav meso Na Fe NZn? emor VA- VA OUTD L-987b theral i t e metav meso Na Fe N V2/3 morb-i a t - c a b OUT U L-990 monzo- g a b b r o metav meso Na Mg N wp ab L-991 und-s a t oliv gabbr o metai v meso Na Fe N V arc L-992 und-s a t oliv gabbr o metai v meso Na Mg IAG-CA G N S2/4 O2/4 emor VA- VA INV L-995 alkal i gabbr o metai v meso Na Fe RRG A V morb- w p t C-14 ov sat oliv gabbr o metav meso Na Fe Group of samples that are not classified S a m p l e Rock Name Debon & Le Fort Mania r & Picco li Whal e n P i e r c e Mafic Rb/10 H f Ta Rb/30HfTa Nb-Ta L-874 out of plot high Si perai i i leuco K Fe RRG A V L-874a granit e metaiv meso Na- K Fe O-W1- 1 L-899 grani t e metav suble u Na Mg A L-911 granit e qua rtz o l i t e perai subleu K Mg A O-W1- 1 L-919 out of plot high Si peraii subleu K Fe RRG L-963 out of plot high Si perai i i leuco K Fe RRG L-996 granit e Metaiv subleu Na Fe N? S2/4 O2/4 VA- III INV C-1 alka l i gran i t e Perai i i subl e u Na-K Fe POG X-16 alkal i grani t e Metav suble u Na Fe RRG X-17 granit e Metaiv meso Na Fe 2 0 0 4.2.1.6 Environment of Emplacement As stated on section 2.4 of this documen t , the met hods to define granitoi d environ m en t of emplac eme nt based on geochemical data do not work well for Paleoprot erozoic rocks. Nevertheles s , the tests showed that several samples from the Kamanjab Batholi t h have a non-anor og en i c char ac t e r . A few sample s seem to have been emplace d in a subducti o na l environ m e n t . Table 4.2. 1.13, extracted from Tabl es 4.2.1.1 2 and 4.2.1.4 , shows details of the suites that contai n such roc ks, and Fig 4.2.1. 6 shows their locatio n . The spatia l distribu tion of the suites is large; they practically cove r all the batho lith. This probably reflec ts a period of time when mantle rocks mixed with crus tal rocks , producing a particular type of magmatism and vulcanism. This was not necessarily subduc tion magmatism. Not all roc ks emplac ed during that time have the mixed chemic a l signature. The areal extent of pluton s with mixed-chemistry does not seem to be very large; that probably is due to the fact that crus t and mantle mixing ocurred only during shor t periods of time in isolate d places. The volume of rock formed was not as large as that of typical anorogenic magmatism. Table 4.2.1.13 Kamanjab rock suites with samples of non-anorogenic or subductional character. ( N on - a n or o ge n i c sample s have a #. Bold sample s show subductional environ ment of emplacement. Dated sample s marked with an asteris k . Underl i n e d suites are minera l iz e d . ) Samples Analysed Rock Types (sensu TAS) (#, quality, types) Environment of emplacement Map Notes B L - 8 3 8 # , L-839, L- 840, L-84 2, L-843, L-1010, L- 1011, L- 1012 2 Simple . Granit e # and Quartz m o n z o n i t e Non-Ano ro g e n i c (L-838 ) K-16 C C L-863, L-864# , L-865, L- 868#* , L-874, L-874-, L- 875 3 Ver y good. Qu artz m o n z o n i t e , granodiorite# and altered granite# Non Anoro g e n i c , subduc t i o n ? (L-8 64 , L- 868) K-14 SW Contai n s Au and Fe miner a l i z a t i o n , near major N-S fault G L - 9 3 9 , L-940, L-9 43*, L-945, L-946, L -948 4: 2 quartz m o n z o n i t e , 2 alkali granit e Non Anoro g e n i c (L-940 ) K-18 WC H L-951, L -952, L -955, L-956, L-957, L-958# 4 Ver y good. Gra nite , gabbro# , monzo n i t e Non-An o ro g e n i c (L-958 ? ) K-18 SC Dissem i n a t e d Cu miner a l i z a t i o n K L - 9 7 7 a , L-978, L-979#, L- 980#, L-982# 2 Ver y good. Quartzmonzonite# , alka l i gran i t e Non-A n o ro g e n i c , Subduc t i o n (L-97 9, L- 980, L-98 2) K-21 NW M L-987# , L-98 7a, L-990, L- 991# , L-992 , L-993#* , L-994, L-995, L -996, L -997, L-998 6 ver y go od. Alkal i grani t e , quart z m o n z o n i t e , vario u s gabbroids# , granite#, quartz s ye ni t e Non-A n o ro g e n i c , Subduc t i o n (L-98 7 ? , L- 987A, L-990 , L-9 91, L- 992, L-99 3?) K-20 CW Disse m i n a t e d Cu miner a l i z a t i o n . Seem s to have a large fract i o n a t i o n seque n c e . Q C-1, C -2, C -3, C-4, C-5, C -6, C-7, C-8, C -9, C-10 , C-12 2 (or 3) Simple . Quartz m o n z o n i t e , alkal i grani t e , granodiorite Non-An o ro g e n i c , ma ybe subdu c t i o n a l . (C- 10 ) K-24 Zirco n s from suite date d coll e c t i v e l y by Cliffo r d , 1969. If the number of samples analysed repres en ts the entir e ba tholith, then 15% of the rocks in the batholith have a non-ano ro ge n i c origin , and 8% indicate mixed origin . This observation has to take into account that 7 out of 9 gabbroi d rocks turned out to be non-ano r og e n ic , and the proc edu r e of Whalen et al, 1987 was not designe d for mafic rocks . The environm e n t of emplace me n t for all sample s of t he Greater Lufilian Arc is currentl y being review ed using geostatistical artificial intelligence clus ter techniqu e s . Prelimi n ar y results shown on Table 4.2.1.1 2 may be due to crus tal contamination and not to true subduction proc es ses. 4.2.1.7 Evidence of Magma Mixing-Magma Mingling T h e r e are many indicati on s of magma mixing in the Kamanjab Batholith. These include rapakivi and antirapa k i v i texture s , abundan t mafic inclus i on s and hybr id inclusions, diffuse nature of crys tal contac ts, ovoida l alkali feldspa r pseudo p he n oc r ys t s in so me rocks, and spongy cellul ar plagio c la s e . T h e presenc e of two or more contras t i n g rock types implies that there were many pulses of magma with differen t composit i on s that were emplaced in a small area. Suites that display evidence of five or six contrasting rock types must have had a lot of mixing and interaction of the magmas . One of the important aspects of magma mixing and mingling is that thes e pr oc es s e s destab i l iz e the ionic balan c e of incomin g magma and may act as precipi t a t i on agent for various new mineral s and metal-b e a r in g sulfide s . 2 0 1 4.2.1.8 Granitoids sampled by Tom Clifford Clifford and his co-workers carried out pioneering work on the chemist r y and geochr o no l o g y of the Kamanja b Batholith (Clifford et al., 1962a; Clifford et al., 1962b; and Clifford et al., 1969). Table 4.2.1.14 shows chemic al analy s is of the sampl es he collec t e d . This was the only publicly available geochemic al information on the batholith before 1992. Preliminar y plots of their chemistr y indicate d a lar ge heterogeinity. Ten of Cliffo rd?s sample s were studied as Suite Q (Fig F16). C-1 , C-4 , C-5 , C-8 an d C-9 make a clus ter that spans from alkal i granite to granite; C-2 a n d C-3 , and C-6 make two clusters of quar tzmonzonites; while C-7 a n d C-10 make a clus ter in the triple point of quartz monzon ite, granodior ite and granite . Clifford et al., 1962a identified that mafic rocks ( C-14 ) interse c t ed the granito id s and were fossiliz ed by the Otavi sedimentary rocks. They al so identified some red granitoids 1 ( C-13 ) that, according to them were subject to sub-aereal ?weatherin g? before deposition of the Otavi silic ic lastic and carb onate sequ ences. Cliff o r d and his researc h group evalu at e d the rest of the granitoids as a single entity. Nevertheless, these rocks of varying compos ition formed at different times, as discussed in the following sections. Table 4.2.1.14 Chemical Analysis, Samp les analysed by Clif ford et al., 1969; Kamanjab Batholith, Namibia ( C omp l e t e analysi s is on Tables 4.2.1.1 and A9) Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LO I T otal Rb Sr Y Zr Nb Ga V Cr Ba Pb La T a Li Be C-1 74.0 3 0.27 12.7 3 1.15 1.51 0.05 0.31 0.48 3.67 5.09 0.05 0.71 100. 05 100 50 70 500 30 25 <3 10 1200 25.0 95 <10 0 <3 <3 C-2 69.7 1 0.68 14.1 7 1.69 1.57 0.04 0.84 0.82 4.10 5.30 0.27 0.67 99.8 6 70 110 45 550 30 25 35 25 2100 8.0 90 35 C- 3 68.6 3 0.67 15.4 3 1.74 1.03 0.10 0.51 1.99 4.50 4.42 0.18 0.50 99.7 0 90 350 ## 700 40 25 35 11 2500 25.0 130 30 C- 4 73.6 3 0.33 14.1 6 1.13 0.24 0.02 0.00 0.50 3.14 6.35 0.07 0.44 100. 01 200 80 20 380 20 20 9 13 1200 40.0 95 11 C- 5 75.3 5 0.27 13.1 8 1.08 0.22 0.02 0.00 0.62 3.15 5.50 0.05 0.36 99.8 0 110 100 35 280 10 20 5 15 1400 30.0 65 12 C- 6 66.0 9 0.69 14.6 0 3.06 1.72 0.08 1.81 2.54 3.25 4.71 0.28 1.11 99.9 4 150 480 25 280 <10 20 85 18 1900 14.0 75 25 C- 7 69.2 9 0.47 14.5 5 1.81 1.48 0.06 1.19 2.83 3.33 4.40 0.17 0.46 100. 04 230 650 25 320 10 19 70 35 1700 16.0 70 13 C- 8 73.8 8 0.33 13.8 5 0.87 0.24 0.03 0.18 0.26 4.05 5.93 0.09 0.39 100. 10 130 40 55 450 15 20 7 11 400 20.0 65 4 C- 9 73.3 0 0.32 13.2 0 2.93 0.48 0.01 0.00 0.24 3.46 5.67 0.07 0.34 100. 02 130 50 80 650 30 30 <3 14 1200 12.0 85 9 C- 10 68.6 3 0.49 15.0 1 1.62 1.44 0.07 1.22 2.74 4.41 3.60 0.20 0.57 100. 00 65 720 25 230 <10 20 55 30 1900 18.0 70 20 C- 11 78.8 4 0.29 10.7 9 0.95 0.27 0.03 0.09 0.60 2.94 5.20 0.06 0.22 100. 28 120 65 55 180 18 15 5 25 560 20.0 100 <3 C-13 75.8 9 0.41 12.4 6 1.07 0.13 n.d. 0.05 0.25 3.60 5.71 0.04 0.50 100. 11 100 40 65 650 40 25 <3 10 1000 30.0 90 <10 0 <3 <3 C-14 48.6 9 1.26 13.2 7 4.86 8.71 0.18 6.15 10.4 9 2.41 1.05 0.22 0.50 97.7 9 The granito i ds sampled and analys e d by Cliffor d et al., 1969 have been include d in the databas e of the Greater Lufilian Arc granito id projec t. Such samples were located as best as possible , with the help of the author, using 1:50,00 0 scale topogra ph i c a l maps that were not availab l e at the time of origina l samplin g (Cliffo r d , T., persona l communi c a t i o n , 2003). The samples have been numbered with the same digits and a ?C? prefix for identification. The chemistry of the samples helped to assign them to various rock groups of the Kamanjab Batholit h . C-6 , C-7 a n d C-10 were assigne d to the group of alkali granites ; C-4 , C-5 , C-8 , C-9 a nd C-11 to the group of granites; C-14 is listed with the gabbroi ds ; while C-2 an d C-3 were assigne d to the group of quartz monzon ites. C-1 has some similar i t i e s with the group of alkali granites . 4.2.1.9 Geochronology New radio m etr i c ages for sample s from the Kaman j ab Batholith were produced during this project, and are listed on Table 4.2.1.1 5 . Rocks from several suites sp read out across the batholit h were selected , to obtain the greates t repr es entativity, and date some of the main minera l i z in g events . Table A22.17 pres en ts all trustworthy geochronolog ical data from the Kamanjab area, and Table A22.15 lists only the ages that come from the main portion of the batholith. Geoc hronolog y proved to be definitive for the interpretation of the Kamanjab Batholith, its history and metallogenic events. The ?younger? granitoids from some suites were tested on purpos e, to see if ther e was a signific a n t magmati c event overprin ted on the Paleoproterozoic granitoids . Ages of 750 Ma were expected, but none were found. The ?old? intrusions of the suites still remain to be tested. Rocks older than 2000 Ma are expected to occur. Xenocr y s t ic ages of ~2600 Ma and ~2500 Ma were found in L-855 a n d L-969 (Table 4.2.1.15 ). That might be the age of the granite basement of the Kamanjab Batholit h. Until recently, such ages were unthinkable for the batholith. Zircons from several of the perceived-to-be old samples , were picked and are ready for dating. The order of priorit y for the rest of the samples to date is: L-968 , L-864 , L-985 , L-1045 a n d L-945 , as indicat e d on 1 The reddened rocks identified by Clifford may be he matite - a l t e r e d granitoi ds produced by hydrother m a l alteration. 2 0 2 Table 4.2.1.15 . The chemistry of the other ?old? granitoids listed on that table (i.e. L-864 a n d L-945 ) is comple tely different. See the Tables 4.2.1.12 and 4.2.1.16. Events 13 and 14 from Table A22.15, correlate reasonably well with each other . They repr es ent an important moment of magmatism. Samples L-1043 a n d L-1045 correla t e well with rocks fr om the Kamanjab Batholith both geochemically and geochronologically. In fact, L-1043 a nd L-855 have simila r chemis t r y , age of emplac e me n t and xenocr ys t i c zircon ages. Table 4.2.1.15 Granitoid samples from th e Kamanjab Batholith that were dated. ( Z i r c o n conc en tr a t e s from all sample s were dated for this project by laser ablation ICPMS at the Memorial University of Newfoundland, Canada, except for C-1. Precis e locatio n s of the rest of the dated samples from the batholi t h could not be obtained . ) Name of site Suite Sample Description Age (Ma) Error (Ma) Priority K a m d e s c h a farm C L-868 Quartz m o n z o n i t e . Youn g intru s i v e . Relat e d to sulfi d a t i o n and ma ybe to IOC G miner a l i z a t i o n 1937 14 Dated Kamdes c h a farm C L-864 Gran od i o r i t e . Old granit o i d . Hosts L-868 and is the local basem e n t . 2 Tevrede fa rm P L-855 Granit e . Sam ple collec t e d at the Tevred e pro per t y. Could be one of the intru s i v e s assoc i a t e d with IOC G miner a l i z a t i o n . 1937 19 Dated Tevred e fa rm P L-855 Inheri t e d zircon s ~2500 Dated N of Kamanja b town Q L-985 Granite . Aver age compo s i t i o n of the granit o i d s fro m the Kama n j a b Bath o l i t h . Easi l y acce s s i b l e . 3 Miner a l i z e d area 2 J L-969 Foid s yeni t e . Assoc i a t e d to dissem i n a t e d coppe r miner a l i z a t i o n in the Kaman j a b Ba tho l i t h . Has stron g potas s i c altera t i o n . 1976 42 Dated Miner a l i z e d area 2 J L-968 Grani t e . Hosts L- 969 and sho ws minor miner a l i z a t i o n . 1 Minera l i z e d area 3 M L-993 Grani t e . Assoc i a t e d to coppe r disse m i n a t i o n in the Kaman j a b Batho l i t h . Has potas s i c alter a t i o n . 1866 13 Dated Intru s i v e along E-W fault L-1013 Quartz m o n z o n i t e . Could be one of the you ng intru s i v e s . Empla c e d along a main E-W fract ur e . 1878 15 Dated End of road W of Kaman j a b Batho l i t h G L-943 Granit e . Is on e of man y young gra nio i t d dikes that inters e c t L-945, L -939 an d L-948. 1877 39 Dated End of road W of Kaman j a b Batho l i t h G L-945 Quartzm o n z o n i t e . Old, foliate d , coarse - g r a i n e d gra nit o i d that acts as host to all other rocks in the suite . 5 Franzfo n t e i n granit e , Franzf o n t e i n Q C-1 Alkali grani t e . Studi e d and anal ys e d by Cliffo r d et al, 1962; Cliffo r d et al, 196 9; and Burg er et al, 1976. Locate d in the southe r n po rtio n of the Kamanj a b Bathol i t h 1730 30 Dated Otavi Mount a i n s , basem e n t L-1043 Granit e . The you nge s t granit o i d in the region . Int ru d e s into L- 1045. 1939 64 Dated Otavi Mount a i n s , basem e n t L-1043 Inheri t e d zircon s 2544 78 Dated Otavi Mount a i n s , basem e n t L-1045 Quartz m o n z o n i t e . Old granit o i d in the region . Pa rt of the Groot f o n t e i n Inlie r . Ver y littl e is known about the ba sem e n t in this part of Nami bi a . 4 At least two ages for copper minerali z ation exist at the Kamanjab Batholith: the mineraliz ing granitoid of Suite J is dated at 1976 ? 42Ma and that of suite M, at 1866 ? 13Ma. These are separated by 110 Ma. The copper event from copper mineral i z a t i o n of su ite J may be correla te d with the 1987 ? 4 Ma age for Khoabendu s granitoid s of Hoffman & Kroner publis hed by Se th et al., 1998 (Table A22.15, and Fig A39). The age of the Cu-minera l i z a t i on event of suite M, dated at 1866 ? 13 M a is within error of the quartz- e ye rhyolite dated at 1862 ? 6Ma by Steven & Armstr ong, 2002 at the Ge lbingen farm, in the NE portion of the Kamanjab Batholith. The age of mineraliz ation at the Gelbinge n farm could be the same, althoug h the subvolc an i c rhyolit i c intrus ive that seems to be pr oducing mineralization at Gelbingen has not been dated. The age of the mineral i z ing intrus i o n at Suite J is also very near to the time of emplac eme n t for L-1013 . This might be very relevant, sinc e L-1013 was emplac ed along a major E-W fracture (Fig 4.2.1.6) . The granito i d that hosts copper mineral i z a t i o n of the suite J has an unknow n age. Sample L-968 should be dated with the highest priority. Of all the sample s co llected, it has potential to become the oldest known granitoid of the Kamanjab Batholith. 2 0 3 The anorogen i c magmatism of L-864 mu s t be dated. That rock may be repr es enti n g an event of subduc ti o na l - r e l a t e d magmati s m and should be studied . The sample doe s not seem to correlate with any of the other ones on the geochem i c a l databa s e . It could be younger or older than L-969 ; but defin itely older than ~1957Ma. Inherit e d zircons from the Kamanjab region indicat e ages of circa 2500 Ma and 2125 Ma for the baseme n t to the batholith. It is possible that some of the undated rocks from the bat holith are that old. All ages from the Kamanjab region have been put together on the event diagram of Fig A37 (Table A22.17 ). It shows a continuum of emplacemen t events from 1980 to 1560 Ma. A closer look helps to identify three discret e shorte r events: 1991 to 1923, ~1900 to 1776, and 1755 to 1632 Ma. These lasted 68, 124 and 123 Ma, respec tively. The last of the three lapses occurs main ly in the Khorixas Inlier. Information available is not enough to define if the first and second events are sepa rat e or form the same series of magmati s m . There is no record of magmati c events from 800 to 740 Ma in the main Kamanjab Batholith. Events Nos. 4 to 15 on Fig A37 are all from the Khorixas Inlier and environ s . That indicates that geolog ical history of the main Kamanjab Batholith and the Khorixas Inlier was different after circa 1600 Ma (Fig A40). Table 4.2.1.16 shows a hypothetical correl a t i o n of rocks based on rock types and new geochr o no l o g ic a l data for the Kamanjab Batholith . The age of L-945 is probably ~1937Ma and it seems to correla t e with L-868 , L- 855 and L-1045 . Table 4.2.1.16 Hypothetical correlation of the dated samples, Kamanjab Batholith and Grootfontein inlier, Namibia. (Base data from Table 4.2.1.15. Lithological co rrela t i o n based on the same chemic a l groups, as indicated on Tables 4.2.1.12 and 4.2.1.5 to 4.2.1.7). Suite/Unit C J G M P Q Region K a m a n j a b Kaman j a b Kaman j a b Kaman j a b K a m a n a j a b Kamanj a b Grootf o n t e i n Alkali Granite C-1 a l k a l i granit e , 1739;30 Alkali Granite L-944 youn g granite 1856; 24 Ma L-993 * granite 1866;13 Cu L-1043 you ng granit e ~1887; 3 9 Ma Quartzmonzonite L-868 * young quart z m o n z o n i t e 1937;1 4 Ma IOC G L-945 old quart z m o n z o n i t e L-855 g r a n i t e 1939;19 L-1045 Old quart z m o n z o n i t e ~1900? Granodiorite L-864 old granodi o r i t e Alkali Rocks L-969* young foid syen i t e 1976;42 Granites L-968 old granite 2600Ma? ~2500 Ma The event diagram for the Kamanjab Batholit h (Fig A39) looks very much like that of the anoroge n ic graniti c comple x cluste rs. Chapter 7 defines th e main characte r i s t ic s of anoroge n ic ring complex clus ter s , in terms of time distribution of intrus ions and length of magmatic events. Section 7.2.7 show s si milarities of the Kamanjab Batholith with other ring complex clus ters in the Greater Lufilian Arc. Z i r c o n concen t r a t e s from several samples were dated by Clifford et al., 1969 and Burger et al, 1976 (Nos. 3, 4, 7 and 11 on Table A22.15 and Fig A39) . If the hypotheses presen ted above 2 are true, then Burger et al, 1976 grouped rocks of three differ en t ages and compos i t i o ns to yield zircons for U-Pb dating. It is commonly underst oo d today that the methods used for dating of large amoun t s of zirco n s in a single batch are no t prec ise. As shown on the event diagr ams of Figs A39 and A37, ages 3 and 4 of Cliffor d et al., 1969 are too young by more than a hundr ed and twenty million years. 2 This refers to the hypotheses of 1) extens ive quart zmonzonite extrusion in the Kamanjab Batholith around 1937 Ma, 2) alkaline granites being intruded at around 185 6 Ma, and 3) granites being the basement of such intrus ions . 2 0 4 Table 4.2.1.17 Tentative correlation of the various rock units in the Suites from the Kamanjab Batholith. Namibia ( A s t er i s k s mark mineraliz ed suites and minerali z i ng granitoid s . # indicat e s sample s with non-an or og e n ic enviro n me n t of emplac e m ent. Ag= alk ali granite, Alk=alka l in e , Gb=gabbr o , Gd=grano d ior i t e , Gt =granite , Qm=quartzmonzonite. This table is an enlarge ment of Table 4.2.1.16.) The term ?non-ano rogenic? is used here to describe environments of granitoid emplac ement that do not fit the anoroge n i c paramate r s in discrim in a t i o n methodo l o g ie s commonly used today. The origin of such rocks is not clear at the time of writing. Nevertheles s, such rocks probably did not form in subductional environ ments. Events A B C* D* E F G* H* I J* K L M* N* O* P Q Gelbingen * Grootfontein A n o r o g e n i c magm a t i s m Ag C-1 1739; 30 Anoro g e n i c magm a t i s m 1862 ? 6 Ma L-849 Alk Gt* Anoro g e n i c magm a t i s m Gt* Alk Gt Alk Gt L- 934 1856;2 4 * Ag Ag Ag Ag Ag L-993 1866;1 3 * Ag Gt L-1 043 ~1887; 3 9 Non- a n o r o g e n i c magm a t i s m 2 Qm A m , Gt L-838# Am L- 868# Qm Qm Qm L-945 Qm Qm subduc- tion L-979#, L-980#, L- 982# Qm Qm Gt L-855 1939; 19 Qm Qm L-1045 ~1900 Non- a n o r o g e n i c magm a t i s m 1 Gd L- 864# Gt, L-939, L-949, gb, L-940# Gb L-958# Gabb roi d s , L-991# Gd C-10# Anoro g e n i c magm a t i s m Syenit e L-969* 1876;42 Anoro g e n i c magm a t i s m Gt Gt Gt Gt Gt Gt L-968 Gt Gt Gt ~2600 Gt ~2500 ~2600 2 0 5 2 0 6 4.2.1.10 Some Copper-Mineralized Systems in the Kamanjab Batholith Suites D, H, J, M and N contain varied disseminated copper mineralization (See Table 4.2.1.4). Such suites have macrosc o p ic simila r i ty with thos e of typical porphyry copper deposits, but a closer look shows that the granito id rocks are midalka l i n e and alkalin e . In additio n to that, hydroth er m a l alterat i o ns observed were not those associa t e d with typica l porphy r y copper minerali z a t i o n . Suites C and O seem to contai n iron oxide- co pp e r - go l d minerali z a t i o n . The Gelbinge n farm also ha s IOCG mineralization, but only a very small outcrop of subvolc a n ic porphy r i t ic intrus i v es was found. Some of these minera l iz ed areas were sought for, becaus e they occur along major east-w e s t- t r en d in g faults that s how abundan t mineral iza t i o n all along. The locatio n s were easy to sample, for being along main public roads and displa y i n g clear evidenc e of hydrothe r m a l alteration and mineralization. Reasons for emplacement of the mineralized suites that do not occur along mapped major frac tur e s are not well underst oo d . Suites D, J, N and O are entirely related to anorogen i c magmatis m , while C, H and M may have had a part ial subductional component (Table 4.2.1.4) . None of the mineral i z e d sites was describe d in detail. Field notes of the sites are included in the Appendix . Maybe the presence of differing magmas was the trigger for mineralization to occur. Mixing of magmas and/or mingling of contrasting litho logi es could have produc ed the prec ipitation of some sulfides . Porphy r i t ic intr us i v e rocks of the su ites H, J and M had abundan t chalc op y r i te and pyrite dissemination. Such features may be diagnostic of significant hydrothermal mineralization in the environs . The three suites contain contras t i ng rock types that occur in clos e association (Table 4.2.1.4) . The copper mineralization of Suite M (samples L-987 to L-996 ) may have been produced by the interaction of the contras t i ng gabbro i ds and granit o i ds . Both groups of rocks carry anomal o us copper in the form of visibl e chalcop y r i t e ; as may be expect e d , mafic rocks have high er values . Total iron cont ent in the mafic rocks is high, probably due to sulfide mineral iz at i o n . Mafic rock s also show high losses on igniti o n , and anomalo u s values of Mn, Ca, Mg, V, Cr and Ni. Thus, gabbroic ro cks could be a source of me tals for suite M. Another interes t i n g feature is that felsic rocks carry somew ha t high K values, don?t carry as much Cu and are enriche d in chromium. The entire suite has low Rb to Sr ratios. L-1000 , a sample from Suite N, contains anomalo us Cu and is located along the main frac ture that bisects the Kamanjab massif from east to west. Many copper occu rr e nc es and associ a t ed iron oxide bodies are know n to occur along that east- w es t- t r e nd i n g fractu r e zone (Fig 4.2.1. 6 ) . Common aspects of the mineralized suites from Tables 4.2.1.4 and 4.2.1.1 9 have been grouped in Table 4.2.1.20. Many useful deductions fo r exploration of mineral deposits in the Kamanjab Batholith can be made from Table 4.2.1.19. Mineralization tends to occur eit her along major fault systems or along the margi ns of anorogen i c plutons. The majority of the sulfide dissemin a t i o ns observed in the batholi t h occur near or along major fault systems. Nepheline syenites with dissemi nated sulfides were emplac ed along major fault systems. The type of intrus ive rocks pres en t in a suite seems to play a role in mineralization. Apart from the observa t i o ns alread y present e d on multipl e types of rocks that make Suites A to Q, some rock types show particu l ar involve m e n t in the minerali z i n g proc ess es . Quartzmonzonites are directly involved in four mineralized suites. Nepheline syenites carry disseminated sulfides in four suites. These two rock types, and their volcanic counterpart, seem to be the most impo rtan t mineraliz ing agents in the Kamanjab Batholith. A few of the mineralized suites share common features . Suites U, V and W are all IOCG-lik e, and occ ur near redox contr as t s on the margin s of anorogen i c plutons. Suites I and X contain disseminated sulfides associated to fault zones and hosted by quartz ites. In general, quartzite-hos ted mineralization is located near or along major fault systems , and displays signifi c an t brecciation, quartz veining and gossanous vugs. 2 0 7 Table 4.2.1.19 Rock suites that show mineralization or hydrothermal alteration in the Kamanjab Batholith, Namibia Sorted by Rock Suite Letter ( D a t e d sampl e s are marke d with an aster i s k . Photo g r a p h e d sam pl e s are in itali c s . Bold sampl e s we re not anal ys e d . Ke y: abund . = a b u n d a n t , diss= d i s s e m i na t i o n , gtd=g r a n i t o i d , hydr o t h . = h y d r o t h e r m a l , mag = m a g n e t i t e , mnzn= m i n e r a l i z a t i o n , qz=qu a r t z , rk=ro c k , sulf s = s ul f i d e s , w/=wi t h ) Sample Number Samples Analysed Rock Types (sensu TAS) (evidence of mineralization) Map Mineralization Type Notes C 9 L-863, L-864, L-8 65, L- 868* , L-874 , L-8 74-, L-8 75, L-867A, L-871, L-873 Q u a r t z m o n z o n i t e s , granod i o r i t e and alte re d gran i t e . Sili ci f ic a t i o n in some samp l e s . K-14 SW IOC G Contai n s Au and Fe miner a l i z a t i o n , near major N-S fault epido t e , qz, angul a r vugs, sulf s D 6 L-898, L-899, L -9 00, L-902, L-903 Quart z m o n z o n i t e , grani t e , volca n i c s . Some quart z veins and minor chlo ri t i z a t i o n . K-16 WC Not kno wn . Disse m i n a t e d Cu miner a l i z a - t i o n . No macro s c o p i c evide n c e . Near Cu prospe c t . . F 4 L-919 , L-920, L -9 2 2 Quartzm o n z o n i t e , gabbro and alte re d grani t e , volca n i c s and quart z i t e s . K-15 NW Not kno wn . Minor evide n c e Qz vein w/ specu l a r i t e cube, wide qz vein s H 1 0 L-951, L-952, L -9 55, L-956, L-957, L -9 5 8 , L-954 Granite , gabbro , monzon i t e , nephe l i n e s yeni t e with disse m i n a t e d sulf i d e s K-18 SC Nephe l i n e sye ni t e with Cu diss . Disse m i n a t e d Cu miner a l i z a t i o n , angul a r vugs. I 7 L-963 , L-965, L-9 66, L-967, L-967a s e v e ra l non- ana l ys e d Quart z i t e s , qua rt z m o n z o n i t e , alkal i n e grani t e , alter e d grani t o i d , monzo n i t e . Abund a n t miner a l i z e d brecc i a s . K-19 WC Unide n t i f i e d hydr o t h e r m a l miner a l i z a t i o n Abund . Brecc i a t i o n , sulfi d a t i o n in quartz i t e s . May be relate d to NW-SE regio n a l fault zone. J 6 L - 9 6 8 , L -9 6 9 * , L - 9 7 1 , L - 9 7 3 , L-97 5, L-97 6 Nephe l i n e s yeni t e , s yeni t e + grani t e with diss Cu, alkal i grani t e . Abun d a n t hydr o t h . alter a t i o n and sulfi d a t i o n . K-19 SW Nephe l i n e sye ni t e + other rks w/ Cu diss . Diss. Cu miner a l i z a t i o n , hydr o t h . alter a t i o n inclu d i n g K. Along E-W regio n a l fault zone. M 13 L-987, L -9 8 7a, L - 990, L - 9 9 1 , L-992, L-993*, L-994, L-995, L -9 9 6 , L -9 9 7 , L-998 Alkal i grani t e , quart z m o n z o n i t e , vario u s gabbr o i d s , quart z s yeni t e . Most conta i n disse m i n a t e d sulfi de s and sho w hydrot h e r m a l altera t i o n . K-20 CW Gabb ro i d s and grani t o i d s with diss e m i n a t e d copper . Disse m i n a t e d Cu mnzn. Large fract i o n a t i o n seque n c e . Ma y be relate d to bra nch of E-W regio n a l fault zone. N 6 L-998, L-999, L -1 0 0 0 , L - 1 0 0 1 , L-1 002 , L - 1 0 0 3 , L - 1 0 0 4 Quartzm o n z o n i t e , granit e Vugs in schis t os e rks; miaro l i t e s . Large amo un t of minera l i z a t i o n , quartz veinin g , quartz pods (? ) K-25 C Unide n t i f i e d hydr o t h e r m a l miner a l i z a t i o n Disse m i n a t e d Cu minera l i z a t i o n around a major E-W fract u r e zon e. O 1 L-855* (Se e sampl e plott e d on the TAS diag r am for Suite A) Granite K-14 WC IOC G Host to IOC G mi nera l i z a t i o n at Tevred e , NW Ka manj a b , Namib i a R 1 L-836 F o l i a t e d porph y r i t i c metalu m i n o u s mesocr a t i c sodic ferrif e r o u s rh yoli t e K-17 NC Just alter a t i o n , type unkno w n . With epido t e veinl e t s . Near border of pluton. S L-846 Grani t o i d s with quart z veini n g and abund a n t qu art z float in the envir o n s . Part of the qu art z has vugs. K-16 NC Unide n t i f i e d hydr o t h e r m a l miner a l i z a t i o n Vugs in quart z veins and quartz float. T 3 L-852, L-853 , L-854 M e d i u m - g r a i n e d granit o i d with qu artz and epido t e vein s . K-14 SC Unide n t i f i e d hydr o t h e r m a l miner a l i z a t i o n qz vein s w/ sulf s + poss i b l e hydr oth mnzn. On borde r of pluton . U 2 L-858 , L-859 M a g - r i c h , 2-3 cm wide veins cut fine- g r a i n e d gtd. Qua rtz pods. K-14 SW IOC G? Qz with large an gula r vugs. Outsi d e of a plut on , hoste d in meta- s e d i m e n t s . V 3 L-914, L-915, L-916 R e d o x cont r a s t in contac t aphib o l i t e / q u a r t z i t e has diss sulf s . Some coars e ma gne t i t e . K-15 C Possi b l e IOCG or other large diss e m i n a t i o n in rock cont a c t . Wide quar t z vein s with goss a n s and sulf i d e s . Ver y large gossa n o u s vugs. Near border of pluton. W 1 3 L-925 to L-937 N o chem i c a l anal ys i s Redox cont r a s t with black shale s . Abund a n t ?vugg y silic a t e s ? . Ver y abund a n t mine r a l i z a t i o n . K-15 WC IOC G or other unide n t i f i e d . Qz float w/ mag + sulfs , gossa n o u s vugs. Borde r of plutons , redo x contras t . X 2 L-959, L -9 6 0 No chemi c a l anal ys i s Quart z i t e s with di sse m i n a t e d sulfi d e s , dense fractu r e networ k s and abund a n t qu art z veinl e t s , grani t o i d s K-18 SE K-19 Unide n t i f i e d hydr o t h e r m a l miner a l i z a t i o n Dense l y-f ra c t u r e d , gossa n o u s gtd. Ma y be relat e d to NW-SE regio n a l fault zone. The pres ence of miar olitic cavities in various granitoid s is another feature that appears in five suites ; it seems to be key in processes that lead to disseminati on of sulfides but not to IOCG mineraliz ation. Various types of gossanous vugs and quartz veining occur in a lot of the suites. Quartz pods tend to occur in the environs of IOCG-type mineraliz ation. In general terms, the presence of granitoids (granodior i t e s , nephel in e syenit es and other granit o i d s ) produce s mineralization in multiple environments, along majo r faults and on the margin s of plutoni c bodies. 2 0 8 Table 4.2.1.20 Compilation of data from various mineralized rock suites in the Kamanjab Batholith, Namibia Name\Rock Suite C D F H I J M N O R S T U V W X Y G Gelbingen I OC G X X X X X X Disse m i n a t e d sulf i d e s X X X X X X X X X X X Near or along major fault s yste m s X X X X X X X X X On ma rgi n of an oro g e n i c pluto n s X X X X X X X Quart z m o n z o n i t e assoc i a t i o n X X X X Other grani t o i d assoc i a t i o n X X X X X X X X Nephe l i n e s yeni t e assoc i a t i o n X X X X Quartz i t e - h o s t e d X X X Mafi c rock asso cia t i o n X Redox cont r a s t or contr a s t i n g litho l o g y assoc i a t i o n X X X ? Brecc i a t i o n X X X Quart z vein i n g X X X X X X X X X X X X Magne t i t e assoc i a t i o n X X X X X Gossa n o u s vugs X X X X X X X X X X X X Miaro l i t i c cavi t i e s X X X X X Epidot e X X X Potas s i c alte r a t i on X X X Black shal e assoc i a t i o n X Mafic rocks were not sample d or describe d in as great detail as the granitoid s. They are under-represented . For that reason, deductions on the rele vance of mafic rocks to mineraliz ation derived from Tables 4.2.1.19 and 4.2.1.20 may be wrong. Most of the suites that show mineralization or hydr ot he rmal alteration are not well understood at the time of writing this report. 4.2.1.11 Discussion The presen t study of the Kamanjab Batholith was only of a reconna is s a nc e nature. Althoug h the numbe r of sample s is large, variation in rock types is too great fo r it to be representative. No detail work was carried out in any of the locations visited. The quality of outcr ops and their interconectivity did not allow for man y structu r a l relatio n s h ip s between rock types to be establi s h e d . Nevert he l es s , based on some of the radio m e t r ic ages and on gener al observations, a table that correlates the various granit o i d units in all rock suites has been devis ed. It makes geolog ical sens e at the location s visited. Table 4.2.1. 17 is based on lithol o g ic and geochemi c a l dat a, as well as on the partia l geochr on o l og i c a l information available. In the few cases wher e radiom e tr i c ages are availa b l e, quartzmonzonites seem to be a discrete event of intrusio n in an anoroge ni c environ m en t . Many of the su ites of Table 4.2.1.4 contain that rock unit. Quartz monzon ites seem to have produced mineralization. A widespre ad charac t er i s t i c of the Kamanjab Batholi t h is that most sites have suites of two or more contrast i ng rock types. No two suites are identica l , and t here is a large variety of rock types that make them. Ten geoc hem i c a l transec t s were drawn in differ e n t direct ions across the Kamanjab Batholith, but results were not meaning ful. Even though all of the repr es e n t a t i ve types of rock from ea ch site were sample d , in most areas the litho l o g y changed very often and no correla t i o n s could be establ i s h ed . The reason for that great rock variability may be that the batholit h is made of multiple granitic ring co mple x intrusions, ea ch with slightly varying chemistry. Radiometric, ma gn e to m e t r ic and gravi m e t r ic images from the Kamanjab Batholith were not available at adequate resolu tion to detect circul ar structures , but they are to be expected. 2 0 9 T h e r e is no direct proof of the pres e nc e of ring comp lexes at the Kamanjab Batholith. Nevertheless, several sources of evidence point to the batholith as a cluster of ring comple xe s . Among other s, thes e are: 1) the lack of continui t y in the rock types along traverses, 2) the pres ence of mult iple rocks types in at least fifteen discret e sites, 3) General anoroge n ic charac t e r of most of the rocks, 4) three quarters of the rocks in the suite are midalka l in e , 4) the size and shape of the batholith, as well as its event diagra m has simila r i t i e s with other ring comple x clus ters, as indicated on section 7.3. Rocks from the Kamanja b batholi t h and the Khor ixa s inlier seem to have had a similar geolog i c a l histor y up to 1600 Ma. After that, both massifs under we nt significantly different geolog ical events. They seem to have had a common geologic a l history once more for the past 550 Ma. A common feature observed throughout the Kamanjab Batholith is the ?out-of-fo cus? texture. More than 70% of the sample s from the masif display gradati on a l cont ac t s between crys ta ls . The contac t s betwee n grains may have been softened by incipien t metamorphism or hydrotherma l alteration. The original net crys tal bounda r ie s have been recrys t a l l i z e d and rocks lost their pr is tine intrusiv e textur es . The texture is generall y associ a t e d with coarse blue quartz phenoc r y s t a ls with gradational margins. These featur es may be an indication of incipient migmatitizati on that was experienced by the entire batholit h . Furthe r work on this issue is needed. 4.2.1.12 Gelbingen Farm, Outlier of Kamanjab Batholith, Namibia This farm is located to the northeast of the Kamanjab Batholith, as shown on Fig 4. 2.1.6. A single, very small outcrop of subvolcanic coarse-grained, porphyritic intrusion with rhyolite composition was observed at the farm. The intrusion seems to be associated with gold, iron and sulfide mineraliz ation hosted by brittle quartz it e s . Hydrother m a l brecciat i o n , massive iron oxide bodies and many gossans after various sulfides were sampled and described. Their interpretation will not be part of this document. L-985 is a porphy r i t ic subvol c an i c intrus ive that occurs in the Gelbingen Farm. The rhyolitic rock contains well zoned plagioc l as e phenocr y s t a l s and no quartz is visibl e to the bare eye (Fig 8.45). Petrogra p h ic analysis of L-985 shows strong hydrothermal alteration. Most of the plagio c la s es are altere d to clays and serici t e . This type of rock is cons ide r ed to have generat e d iron oxi de- c o pp er - gold minera l iz a tio n at the Gelbin g en farm. It was emplac ed in an anorog e n ic envir o nme n t at aroun d 1862 ? 6Ma, by corres pondence with rhyolitic volcanic rocks dated by Steven, 2002 at the farm. Several description s of mineraliz ation and types of breccias from the Gelbing e n Farm are include d in section 8.4.3.1 . 2 1 0 2 1 1 4.2.2 KHORIXAS INLIER 4.2.2.1 Introduction The Khorixas Inlier is an isolated, fault-bounded body of rock s that is located to the west of the Khor ixas town in Damarala nd , Namibia, as show n on Fig M20. Clim ate is very dry and vegetat i o n is mainly grasses and shor t thorny bush. The inlier is mainly composed of granito id rocks and was sampled during the Greater Lufilian Arc grantiod projec t. Descript i on of the Khor ix a s Inlier will be broken in two parts : one on the Oas Farm and the other on the Lofdal farm. Observations and sampli n g of the Mesopo t ami e farm was also includ e d under the Khorixa s Inlier headin g , althou gh it does not form part of the inlier strictly speaking, but makes anothe r fault-bo u nd entity. The Khor ixas Inlier is heavily inclined toward midalka line and alkaline rocks. 71% of the granitoids from that domain fall within the midalkaline field while 29% of t hem fall in the subalkaline field (Table 4.2.2.1) . All midalkaline rocks make 60.5% of the samples. 26% are sulbal k a l i n e and 14% are alka line rocks. Carbonat i t e s in this area play an importan t role. They have been k ept apart from the other ro cks in the evaluation of alkalinity, and make 17% of the samples studied . Table 4.2.2.1 Statistics of rock types, Khorixas Inlier, Namibia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type number % Granitoids Groups a l k a l i grani t e 10 23.26 Q u a r t z m o n z o n i t e 1 2.33 S ye n i t e 9 20.93 M o n z o n i t e 2 4.65 Mo n z o g a b b r o 1 2.33 Midalkaline Rocks a l k a l i gabbr o 3 6.98 70 . 9 7 60.47 Granite 8 18.60 Gr a n o d i o r i t e 1 2.33 ga b b r o -d i o r i t e 1 2.33 Subalkaline Rocks Gabb ro 1 2.33 29 . 0 3 25.58 foid monzo s ye n i t e 4 9 . 3 0 f o i d gabbro 1 2.33 Alkaline Rocks p e r i d o t gabb ro 1 2.33 13.95 Total 4 3 9 7 . 6 7 1 0 0 . 0 0 100.00 C a r b o n a t i t e 9 Total 5 2 Table 4.2.2.2 lists all samples collect ed in the Mesopot a m i e , Oas and Lofdal farms, along with their main geochem ic a l paramet e r s and studies for environ me n t of emplac ement. Samples from the Summas Mountains were included there too, for compar i s io n purpos es , and will be discus se d independ en t l y in the followin g chapte r . A regiona l model on the nature of granit o i d s and their metallogenic significan ce at Mesopo tamie, Lofdal and Oas farms in Namibi a was put togeth er during the Great er Lufilian Arc granito i d project. Fig 8.6 show s the location of the study area. Most of the mineralization at thos e sites is contro l le d by major E-W trendin g fault systems. In fact, most of the mineraliz a t i o n observ ed in or around the Kamanjab Batholith seems to be contro l l e d by subpar a l l e l region a l E-W-tr e nd i n g major fractur es . The term E-W struct u r es is used here somewha t loosel y . Most of the struct ures that fall under that denomination are actually N68?E; they follow the general trend of the Lufilian Arc. Rifting and later collisio n fronts had roughly the same relative orientation. 2 1 2 Table 4.2.2.2 Comparison of samples from the Khorixas Inlier and nearby Summas Mountains, Namibia (Samples with asterisk were dated. Se e acronym descript i on on section 2.4.3.) Mesopotamie Farm, Namibia S a m p l e Rock Name Debon & Le For t Mania r & Picco l i Whalen P e a r c e Mafic Rb/10H f Ta Rb/30H f Ta Nb - T a L-759* Granit e peralu m i leuco KFe A L-772 alkal i grani t e metal u m v leuco KFe A L-773 Grani t e peral u m i leuco NaFe A W L-783 Grani t e peral u m ii meso Na-KF e A O-W1- 1 WP WP OUT U L-784 Granit e metalu m iv meso Na-KFe RRG-CE U G A O3/4 Oas Farm, Namibia S a m p l e Rock Name Debon & Le For t Mania r & Picco l i Whalen P e a r c e Mafic Rb/10H f Ta Rb/30H f Ta Nb - T a L-668 * Syeni t e metal u m iv meso NaFe RRG A O-W 2-2 wp ab WP- WP INW L-669 Syeni t e metal u m iv meso NaFe CEUG A W WP- WP INW L-670 nephe l i n e s yeni t e metal u m iv meso NaFe RRG A O-W 2-2 ? OUT U-NE A L - 6 7 5 Syenit e peralu m i subleu c o NaFe CEUG A W3/4 wp ab OUT U L-676 Syenit e metalu m iv meso NaFe RRG-CE U G A W wp ab L-691 Monzo n i t e metal u m iv meso NaFe RRG-C E U G A W wpt L-693 * alkal i grani t e metal u m iv meso NaFe RRG A W3/4 WP- WP INW L-694 nephe l i n e s yeni t e metal u m v meso NaFe RRG A W wp ab L-695 nephel i n e s yenit e metalu m iv meso NaFe RRG-CE U G A O-W 1-1 wp ab L-697 Syenit e metalu m v meso NaFe RRG-CE U G A W3/4 wp ab WP- WP OUT U-NE A L - 6 9 8 alkal i grani t e metal u m v meso NaFe RRG-C E U G A O-W 2-2 OUT U L-699 Syeni t e metal u m iv meso NaFe CEUG A W L-708 Pyro xen i t e metalum v meso NaFe IAG-CA G A W? wp ab L-712 alkal i grani t e peral u m iii leuco NaFe POG A V L-713 quart z s yeni t e metal u m v leuco NaFe A O-W 2-2 WP W OUT U L-714 Grani t e metal u m v leuco NaMg OP A V L-714a alkal i grani t e peral u m ii leuco NaFe A V L-715 Granite metalum iv meso Na-KFe RRG-CEU G A O3/4 OUT U L-716 * Grani t e metal u m iv subleuc o NaFe CEUG- R R G A S2/4O2 / 4 VA- VA INV L-101 9 alkal i grani t e metal u m v suble u c o NaFe RRG A V2/4 WP- WP INW L-102 0 Grani t e metal u m v meso NaFe A W Lofdal Farm, Namibia S a m p l e Rock Name Debon & Le For t Mania r & Picco l i Whalen P e a r c e Mafic Rb/10H f Ta Rb/30H f Ta Nb - T a L-722 Carbon a t i t e metalu m vi meso KFe A OUT U L-728 * Grani t e metal u m vi subleuc o NaFe OP A ? WP- WP INW L-729 Granit e metalu m iv subleuc o Na-KFe P O G A O-W 1-1 L-740 nephel i n e s yenit e peralu m ii meso NaFe CEUG A O3/4 ? OUT U L-741 nephel i n e s yenit e metalu m iv meso KFe CEUG A O-W 2-2 wp ab OUT U L-742 granit e metalu m iv meso NaMg A O2/3 OUT U L-754 diorit e metalu m iv meso KFe RRG N arc L-1021 Granit e metalu m iv subleuc o NaFe RRG A W L-1022 nephe l i n e s yeni t e peral u m iii meso Na-KF e A O2/3 ? OUTU L-1023 sat. olivin e gabbro metalu m v meso NaFe IAG+CA G ?NZn V emor L-1024 a Carbo n a t i t e metal u m vi meso KMg A L-1024 c Carbo n a t i t e metal u m vi meso KMg A L-1025 under s a t . oliv. gab. metal u m v meso NaFe A arc WP WP OUT D-I NV L-102 7 nephel i n e s yenit e metalu m v meso KFe A W-O 2-2 ? OUT U L-1032 Unders a t . oliv. gab. me t a l u m iv meso NaFe N V2/4 emor WP WP OUT U Summas Mountains, Namibia (Volcanic Rocks) Sample Rock Name Debon & Le For t Mania r & Picco l i Whalen P e a r c e Mafic Rb/10H f Ta Rb/30H f Ta Nb - T a L-789 Syenit e metalu m iv meso NaFe RRG-CE U G A O-W 2-2 OUT U L-791 Alkal i rhyol i t e peral u m ii leuco KFe RRG-C E U G A W3/4 WP- WP INW L-791 a Alkal i rhyol i t e peral u m iii meso Na-KF e W 2 1 3 4.2.2.2 OAS FARM, NAMIBIA 4.2.2.2.1 Introduction The Oas farm is located in the eastern portion of the Khor ixas Inlier that lies south of the Kamanjab batholith , in Damaral a nd , norther n Namibia . The farm may be reac hed along dirt roads from the town of Khor ixa s . General locatio n is show n on Fig M20. The suite of chemical analyses from the Oas farm is made by a total of 29 samples. They may be subdivided geograph ically into 19 from the N-S transect, 2 from mi nera l iz ed quartz i t e s , 2 that come from outcro ps along the route of access, and 6 more samples with major ox ide chemistr y that were compiled from a report by (Frets, 1969). The Sample datab as e is listed on T able 4.2.2.3. Petrographically they may be grouped into three sets : granitoids that make the host rocks (or ?bas ement?), some syenitic rocks, and a few gabbroic rocks . Table 4.2.2.3 Chemical Analysis of Samples from the Oas Farm, Namibia (complete elemental analys is on Table A12, Appendix) Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 MnO MgO CaO Na2O K2O P2O 5 LO I Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h Sc Pb Sm Nd Pr Ce La Hf T a Eu Notc h 50.0 0 1.00 15.5 0 6.00 0.15 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 10 120 4 L- 668 62.6 1 0.89 17.3 2 4.83 0.14 0.72 1.80 6.42 4.79 0.36 0.59 121 474 69 710 193 7 7 6 127 26 14 139 2037 7 22 <10 14 101 182 235 110 4 23 1 L-669 64.3 4 0.61 16.7 6 4.66 0.12 0.36 1.46 6.43 4.80 0.23 0.74 115 350 73 378 204 <6 9 7 146 28 <12 124 1647 9 31 <10 22 18 102 28 267 137 8 12 4 L- 670 57.0 1 1.45 15.1 4 11.0 8 0.21 1.42 2.33 6.69 3.35 0.53 1.32 173 1219 73 1843 458 <6 9 9 85 42 <12 18 767 17 46 <10 3 27 72 219 42 74 0 L-675 60.7 1 0.10 21.9 9 3.59 0.09 0.13 0.94 4.92 6.41 0.03 1.61 125 384 123 1520 345 7 9 23 167 30 20 17 1321 10 78 11 140 592 844 440 238 3 L-676 59.3 5 0.87 18.1 3 5.92 0.17 1.24 2.05 5.20 5.55 0.24 1.84 226 634 58 553 139 7 7 11 177 26 19 31 1591 <6 19 <10 180 85 L- 691 50.2 4 3.31 12.9 5 14.1 5 0.21 4.13 6.53 2.95 2.82 0.55 1.51 151 589 52 368 62 39 32 190 166 19 357 66 617 <6 <15 33 110 61 L- 693 * 71.3 7 0.48 11.6 5 6.47 0.14 0.19 0.77 4.62 4.46 0.09 0.31 86 98 31 132 105 6 7 14 128 33 <12 60 241 2 9 <10 5 13 114 35 357 216 3 5 1 L- 694 59.1 8 1.09 17.0 7 5.91 0.17 1.01 2.48 6.84 4.89 0.36 0.54 106 633 39 333 93 7 <6 10 107 23 27 <12 1995 <6 <15 <10 166 87 L- 695 46.2 9 3.29 13.3 4 13.5 4 0.48 3.19 4.92 4.10 3.51 0.68 6.78 197 399 53 329 54 27 22 89 120 19 353 28 639 <6 <15 26 64 30 L- 697 59.9 4 0.86 16.9 0 5.28 0.17 0.99 2.06 6.58 4.59 0.32 1.54 169 491 151 1363 432 8 9 5 129 26 <12 117 1444 15 51 <10 127 480 582 291 2 108 5 L-698 71.6 8 0.46 11.4 0 5.84 0.10 0.10 0.85 4.91 4.10 0.10 0.40 77 45 50 329 124 <6 7 7 104 35 <12 207 157 <6 <15 <10 16 67 228 372 143 92 0 L-699 63.4 1 0.28 17.2 8 5.27 0.20 0.34 0.93 7.40 4.73 0.12 0.56 98 114 75 1246 307 <6 10 7 147 34 <12 126 458 15 50 <10 470 310 L- 708 47.1 5 0.47 8.72 11.2 7 0.53 13.1 2 14.2 1.46 1.77 0.04 1.79 86 578 146 469 126 16 26 13 279 17 68 14 2096 <6 <15 23 258 97 L- 712 79.1 1 0.04 12.0 4 0.83 0.04 0.11 0.40 5.47 1.95 0.01 0.54 33 159 12 17 7 <6 10 8 35 18 <12 47 662 <6 <15 <10 107 13 41 7 2 0 L-713 71.3 2 0.16 14.3 6 2.37 0.05 0.08 0.32 5.76 5.66 0.02 0.41 117 94 30 277 71 <6 8 9 53 25 19 49 909 <6 <15 <10 121 80 295 436 188 1 25 1 L-714a 77.5 5 0.05 13.1 9 0.73 0.03 0.17 0.85 6.33 0.76 0.02 0.67 16 338 9 250 9 <6 9 8 40 23 <12 50 538 <6 16 <10 106 3 83 3 0 L-714b 74.4 7 0.12 14.6 3 0.94 0.04 0.12 0.59 8.15 0.94 0.05 0.41 16 152 25 237 50 <6 8 <6 17 0 12 160 606 0 0 0 0 0 L- 715 72.1 3 0.48 13.0 2 3.49 0.09 0.48 1.12 3.88 4.88 0.12 0.50 118 147 58 348 25 8 11 12 67 18 28 47 1230 <6 19 <10 76 39 88 154 44 39 1 L-716 * 73.8 8 0.30 12.5 4 2.79 0.04 0.41 0.98 4.49 3.98 0.04 0.68 69 164 38 332 16 8 11 12 51 16 19 57 1389 7 24 <10 9 7 42 11 134 66 7 1 1 L- 1016 77.3 3 0.10 1.04 2.18 0.47 2.02 6.71 0.50 0.09 0.13 8.00 6 124 8 15 4 <6 <6 56 14 <9 <12 351 33 <6 <15 12 24 <12 L-1016 a 79.3 8 0.10 0.80 2.49 0.45 1.96 5.74 0.55 0.13 0.04 7.50 5 140 6 37 4 <6 7 28 27 <9 13 15 57 <6 <15 10 23 <12 L-1019 72.2 3 0.41 13.1 7 3.00 0.11 0.24 0.79 6.18 3.79 0.08 0.41 50 101 31 290 47 <6 10 9 62 17 <12 253 1351 2 17 <10 29 8 47 12 110 60 7 2 2 L- 1020 70.8 2 0.58 12.6 8 4.01 0.10 0.76 1.57 5.17 3.14 0.09 0.31 70 173 52 445 22 <6 8 64 85 17 19 <12 1364 <6 19 <10 180 95 Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI X-21 60.7 8 0.87 16.9 7 1.13 4.10 0.16 0.99 1.94 5.65 5.27 0.22 1.78 X - 22 64.4 2 1.12 14.6 9 4.34 1.80 0.07 1.37 1.17 3.71 5.64 0.25 1.78 X - 23 63.8 1 0.59 14.2 1 3.67 1.10 0.15 1.48 2.27 4.37 6.00 0.09 3.13 X - 24 51.2 9 0.40 19.0 6 5.95 1.05 0.42 0.82 4.79 6.75 5.19 0.30 3.38 X - 25 47.4 9 2.22 14.4 7 3.74 8.09 0.05 6.73 11.5 7 1.24 0.77 0.30 2.80 X - 26 48.8 2 1.03 12.2 1 3.62 6.54 0.15 13.6 8 9.63 1.77 1.10 0.59 1.16 4.2.2.2.2 4-km Long N-S Transect Across Oas Syenite Very little is written about the geolog y of the Oas Syenite, its chemis try, environment of emplac ement, mineral i z a t i o n and associa t e d hydrothe rmal alteration. The main referenc es on the geology of this part of Namibia are Frets, 1969; Hoffman n , Hawkin gs , Isac hs en, & Bowring, 1996; and Miller & Burger, 1983. Reports by Schneider & Seeger, 19 99 and Burnett, 1999 describe some co pper and gold occurrences in the Khorixas Inlier. A 4 km long N-S geolog ic a l transec t was carried out along a road, across the Oas Syenite, ro produce a reconnai s s anc e geologic a l map (Fig 4.2.2.1 ) . The r oad where the transe c t was done may be reac hed from Khorix as as indica t e d below: A gravel road leads s outhw es t from Khor ixas, as show n on 1:50,000 scale topographic sheet 2014BD. The Bella Vista farm intersec tion is crossed westward. After passing on to map sheet 2014BC, in the Bloemhoef 484 farm, there is a NNW gravel road. That road should be followed northwar d up to the farmhou s e of the Oas 486 farm. From there, a rough mounta i n road contin u es north. That is the site of the N-S transect. A reconnaissance geological map of exposures along t he road was produc ed (Fig 4.2.2.1) . Nine midalkaline ring comple x e s that make a clus te r were identi f i e d al ong the transect. Field notes on the transect, slightly 2 1 4 edited with result s from geoche m i c a l and geochr o no l ogical data, are included in Appendix A66. The location of all geological and sampling stations is also incl uded in the Appendi c e s A18 and A19. Most station s are show n on the maps of Fig 4.2.2.1. These syenit i c bodies were emplac e d along with ex plos i v e brecci a t i o n events . Massive magneti t e and hematit e were observe d in many sites; iron oxide hydrother m a l alterati o n (?red -r o ck? and ?brow n- ro ck ? types), quartz pods, widespr e ad sulfid a t i o n , and abunda n t gossans were sample d and mapped in the area. The type of mineraliz a ti o n displays many char ac te r i s tic s of iron oxid e -c o ppe r -g o l d systems . Type and amount of mineralization are still to be defined. Zinc, rare earths, possibly gold, copper and other metals are expected to occur in economic amounts. Part of the syenito i d s could act as potenti a l zinc sour ce for various styles of minera lization in the Katangan rocks. Mapping and samplin g along the transec t will probabl y help solve issues about hydrot hermal fluids, processes and different events that produced mineraliz ation. Table 4.2.2.4 the main featur es of the nine syenito i d circula r comple x e s that were discove r e d at the Oas farm. That includes estimat e d size of the bodies, composi t io n , heat product io n capacit y , associa t e d st ructur es and dikes, as well as age of emplace m en t . The map of Fig 4.2.2.1 pres en t s the main geolog i c a l obs erva t i on s of the ar ea. At least four of the circular bodies are made by high-heat producing syenitoids. Several of the comple x e s seem to have produced iron oxide-c o pp er - gold mineralization. The syenites of the Oas farm contain signific an t potent i a l for iron oxide-c opp e r - g o ld mineral iz a t i o n . More detailed geological maps, maps of alteration and studies of the associ a t e d minera l iz a t i o n were prepar e d and will be publis h e d elsewh ere . Most of the sample s from the Oas syeni te suite, in clud i ng mafic and felsic rocks, are endowe d with anomalo us zinc (See Table 4.2.2. 3 ) . None are truly enr ic h ed in copper . This does not includ e any of the mineralized samples; those were not a nalysed for the Greater Lufilia n Arc granitoid project. Assays for gold, copper, zinc and other metals will not be include d in this document . Extensiv e bodies of massive quartz occur througho u t t he Oas farm (see section 8.3.5.2) . These seem to be associated with a widespread event of silicif i c a t i on , and with quartzit e s . At the time of emplac ement, part of the Oas syenitoids were high-he a t produc i ng ro ck s . Four of the sampl es are especia l ly enriche d in thorium and they are listed on Table 4.2.2.5. The heat gener ating capacity of these rocks establis hed and maintained long-lived, large hydrothe rmal fluid circuits. That probably was a determin i n g factor in the mineral iz i ng capacity of the magmatic systems. Table 4.2.2.5 High heat producing rocks in the Oas farm, Namibia; estimated at 750Ma. Sample Uranium (ppm) Thorium (ppm) Potassium (%) Heat producing value (muW -m3) U/Th L - 6 7 0 17 46 3.35 4 . 1 6 6 0.370 L-675 10 78 6.41 6 . 6 0 3 0.128 L-697 15 51 4.59 4 . 6 2 8 0.294 L-699 15 50 4.73 4 . 5 7 9 0.300 2 1 5 2 1 7 Table 4.2.2.4 Main features of small syenitoid circular bodies found at the Oas farm, Namibia (See loca tion map, Fig 4.2.2.1) (Dated sample s are marked with an asteris k . An ?H? was added to the humber of high heat produci ng rocks.) Body Geological stations Number of samples Analysed samples Perimeter Shape Area Composition Dikes Heat production capacity Age Additional Notes A 0 0 0 Assumed Oval estimated 30 x 35 m diam eter S ye nito id Non e obs erved Unkn o wn Estimated Observed but not mapp ed nor samples collect ed. B 7 1 1 (L-69 8) Mapp ed Circul ar 75 m diam eter s ye nit e but not ana l yse d several gen eratio ns of mafic dikes Unkn o wn Estimated Exp los ive brec ciatio n. Man y quartz veins surrou nd hill. Breccia vein/dik e wit h hem atite and ang ular fra gments. C 3 1 1 (L- 697 H) Not well constrai ned Uncerta in M inimum 25 x 50 m S ye nite Not observ ed High Estimated Sye n ite cut by net work of magnetite-r ich veinlets . D 14 3 3 (L-69 3*, L-69 4, L-69 5) Mapp ed Oval 80 x 50 m Nep hel ine sye nit e Severa l L-79 5 alkal i gra nite + nep hel in e syen ite Lo w Dike L-69 3* is ~765;4.5 Ma T hree inde pen dent hills. Phot os. E 3 2 3 (L-66 8*, L-66 9, L- 670 H) 1/3 way arou nd Circul ar estimated 150 m diam eter estimated S ye nit e + nep hel in e sye nit e Not observ ed High L-66 8* is 762;1 2 Ma Intensel y fractu red and recem ented. F 14 10 (L- 678) 2 (L- 675 H, L- 676) Mapp ed Rou ghl y circular 60 m diam eter S ye nite Not observ ed Ver y hig h Estimated Abun da nt IOCG evidenc e. Massive magneti t e bod ies + vugs + sulfides. Abu nda nt magn etite- filled veins and stock works. L- 678 has xen olit h of pink gra nito i d. Photos. G 3 5 (L-68 5 to L- 688 *) 1 (L-68 8*) Not mapp ed ? More than 10 m; true size is uncerta in S ye nite Non e obs erved Lo w L-68 8* is 762;4.5 Ma Not ide ntifie d as ring comp le x duri ng fiel d work. Composit i o n simila r to body E. With brai ded quartz veins + hematit e + sulfides; diss. sulfides. H 1 5 1 (L- 699 H) Not mapp ed Rou ghl y circular 200 m diam eter estimated S ye nite Yes High ? Intersected by man y quartz veins wit h magn etite +sulfides. Ver y alter ed and weath ered, wit h abu nd ant gossans. Strong red-rock alterat ion. I 2 1 1 (L-71 6*) Not mapp ed ? Unkn o wn G neissic gran ite Yes Lo w L-71 6* is 745; Ma Not identified as a circul ar bod y in the field. Larg e red rock alterati on. Base ment 8 (L-69 1, L-71 2, L-713, L- 715 , L-1019, L- 102 0) Granite, alka li gran ite Yes Lo w ? Not well stu die d. 2 1 9 4.2.2.2.3 Geochemistry A significant portion of the rocks from the Oas farm is made of granite s and alkali granite s . The rest are syenites , nephelin e syenites and gabbroid s (Figs 4.2.2.2). 85% of the granitoid s from the Oas farm fall within the midalkaline field, while 15% of them fall in the suba lka l in e field (Table 4.2.2.6 ) . All midalka l i n e rocks make 74% of the samples. 18.5% are sulbalka l i n e and 7.5% ar e alkaline rocks. Rocks from this farm exemplify the problem of plutoni c rock nomenc l a t ur e . A suite of rocks that petrogr aphically is cons ide r e d to be syeniti c , plots as granodior itic and dioritic in the modified TAS diagram (Fig 4.2.2.3). The R1/Rs2diagram (Fig 4.2.2.5) show s them to be syenite s and nepheli ne syenite s . Table 4.2.2.6 Statistics of rock types, Oas farm, Namibia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type Number % Granitoids Groups a l k a l i gran i t e 7 25.93 Q u a r t z m o n z o n i t e 1 3.70 S ye n i t e 9 33.33 M o n z o d i o r i t e 1 3.70 M o n z o g a b b r o 1 3.70 Midalkaline Rocks A l k a l i gabbr o 1 3.70 85 . 0 0 74.07 Granite 3 11.11Subalkaline Rocks Gabb ro 2 7.41 15 . 0 0 18.52 Foid monzos ye n i t e 1 3.70Alkaline Rocks F o i d gabbr o 1 3.70 7. 4 1 Total 2 7 1 0 0 . 0 0 1 0 0 . 0 0 100.00 5 1 0 1 5 2 0 2 5 3 0 3 5 4 0 4 5 5 0 5 5 6 0 6 5 7 0 7 5 8 0 SiO2% 0 1 2 3 4 5 6 7 8 9 1 0 1 1 1 2 1 3 1 4 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM Khorixas Inlier, Namibia; Lufilian G.P. (Based on Middlemost, 1994, 1997 ) Sa m ples Pe trog raph ic fie lds L - 7 2 2 L - 7 2 8 L - 7 2 9 L - 7 4 0 L - 7 4 1 L - 7 4 2 L - 7 5 4 L - 1 0 2 1 L - 1 0 2 2 L - 1 0 2 3 L - 1 0 2 4 aL - 1 0 2 4 c L - 1 0 2 5 L - 1 0 2 7 L - 1 0 3 2 L - 7 5 9 L - 7 7 2 L - 7 7 3 L - 7 8 3L - 7 8 4 X - 2 7 X - 2 8 X - 2 9 X - 3 0 X - 3 1 X - 3 2 X - 3 3 Fig 4.2.2.2 4 0 4 5 5 0 5 5 6 0 6 5 7 0 7 5 8 0 SiO2% 0 1 2 3 4 5 6 7 8 9 1 0 1 1 1 2 1 3 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM Khorixas Inlier, Namibia; Lufilian G.P. (Based on Middlemost, 1994, 1997) S a m p l e s P e t r o g r a ph i c fi e l d s L-668 L-669 L-670 L-675 L-676 L-691 L-693 L-694 L-695 L-697 L-698 L-699 L-708 L-712 L-713 L-714 L-714a L-715 L-716 L-1016 L-1016a L-1019 L-1020 X-21 X-22 X-23 X-24 X-25 X-26 L-728 L-729 L-740 L-741 L-742 L-754 L-1021 L-1022 L-1023 L-1025 L-1027 L-1032 L-759 L-772 L-773 L-783 L-784 Fig 4.2.2.3 - 5 0 0 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti) 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 R 2 = 6C a +2M g +A l L-668 L-669 L-670 L-675 L-676 L-691 L-693 L-694 L-695 L-697 L-698 L-699 L-708 L-712L-713 L-714L-714a L-715L-716L-1019 L-1020 X-21 X-22 X-23 X-24 X-25 X-26 L-722 L-728 L-729 L-740 L-741 L-742 L-754 - 0 L-1022 L-1023 L-1024a L-1024c L-1025 L-1027 L-1032 LR25 LR23 LR20 LR5 LR4 759 L-772 L-773L-783L-784 X-27 X-28 X-29 X-30 X-31 X-32 X-33 R1R2 PLUTONIC ROCK CLASSIFICATION Khorixas Inlier, Namibia; Lufilian G.P. (After De la Roche et al, 1980) Pe tro gr ap hi c field s Sa mples Fig 4.2.2.4 - 5 0 0 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 3 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti) 5 0 0 1 0 0 0 L-66 8 L-669 L-670 L-675 L-67 6 L-69 3 L-69 4 L-695 L-69 7 L-69 8 L-69 9 L-712 L-713 L-714L-714a L-715 L-716 L-1019 L-1020 X-21 X-22 X-23 X-24 L-728 L-729 L-740 L-741 L-742 L-1021 L-1022 L-1027 L-759 L-772 L-773L-78 3 L-784 X-28 X-29 X-30 X-31 X-32 R1R2 PLUTONIC ROCK CLASSIFICATION Khorixas Inlier, Namibia; Lufilian G.P. (After De la Roche et al, 1980) Petrographic fields Sa mp les L -6 9 8 L - 6 9 3 L -7 8 3 L -1 0 2 1 Fig 4.2.2.5 Fig 4.2.2.5 - 9 0 0 - 8 5 0 - 8 0 0 - 7 5 0 - 7 0 0 - 6 5 0 - 6 0 0 - 5 5 0 - 5 0 0 - 4 5 0 - 4 0 0 - 3 5 0 - 3 0 0 - 2 5 0 - 2 0 0 - 1 5 0 - 1 0 0 - 5 0 0 5 0 1 0 0 1 5 0 2 0 0 2 5 0 3 0 0 3 5 0 Q=S i/3-(K +N a+2 C a/3) Q-P Plutonic Classification ( A f t er Deb on & LeFor t , 1983) Khorixas Inlier, Namibia; Lu filian Arc Granitoid Project (F i g 4. 2. 2 .7 show s enlar g em e n t of clus t er ) P et r o g r a p h i c F i e l d s S am p l e s - 1 4 0 0 - 1 3 0 0 - 1 2 0 0 - 1 1 0 0 - 1 0 0 0 - 9 0 0 - 8 0 0 - 7 0 0 - 6 0 0 - 5 0 0 - 4 0 0 - 3 0 0 - 2 0 0 - 1 0 0 0 1 0 0 2 0 0 P=K-(Na+Ca) L-668 L-66 9 L-670 L-675 L-676 L-691 L-693 L-694 L-695L-697 L-698 L-69 9L-708 L-712 L-713 L-714 L-714a L-715 L-716 L-1016 L-1016a L-1019 L-1020 X-21 X-22 X-23 X-24 X-25X-26 L-722 L-728 L-729 L-740 L-741 L-742 L-754 L-102 L-1022 L-1023 L-1024a L-1024c L-1025 L-1027 L-1032 LR25 LR23 LR20 LR5 LR4 L-759 L-772 L-773 L-783 L-784 Fig 4.2.2.6 - 5 0 0 5 0 1 0 0 1 5 0 2 0 0 Q-P Plutonic Classification ( Af t e r De b o n & L e F o r t , 1 9 8 3 ) Khorixas Inlier, Namibia; Lufilian Arc Granitoid Project P e t r o g r a p h i c F i e l d s S a m p l e s 0 - 4 0 0 - 3 5 0 - 3 0 0 - 2 5 0 - 2 0 0 - 1 5 0 - 1 0 0 - 5 0 0 5 0 1 0 0 1 5 0 L-668 L-66 9 L-670 L-675 L-676 L-691 L-693 L-694 L-695 L-697 L-698 L-699 L-708 L-712 L-713 L-714 L-714a L-715 L-716 L-1019 L-1020 X-21 X-22 X-23 X-25 X-26 L-728 L-729 L-740 L-741 L-742 L-754 L-1021 L-1022 L-1023 L-1025 L-1027 L-1032 L-759 L-772 L-773 L-783 L-784 Fig 4.2.2.7 0 2 0 0 GR AD GD TO SQ MZQ MZDQ DQ SQ MZ MZGO GO 0 0 . 1 0 . 2 0 . 3 0 . 4 0 . 5 0 . 6 L-6 68 L- 669 L- 670 L- 675 L- 676 L- 691 L- 693 L- 694 L- 695 L- 697 L- 698 L-6 99 L- 712 L- 713 L- 714 L- 714 a L-7 15 L- 716 L- 101 6a L-1 019 L- 1020 X - 21 X -2 2 X - 23 X -24 X -2 5 L- 722 L -72 8 L- 729 L -74 0 L-7 41 L -74 2 L - 7 L- 1021 L- 1022 L-1 023 L-1 024a L-1 024c L -10 25 L- 1027 L- 1032 L R 25 L R 5 L- 759 L- 772 L- 773 L- 783 L-7 84 MgB Diagram ( A f t e r Debo n & LeFor t , 1994 ) Samples from the Khorixas Inlier, Namibia Greater Lufilian Arc Granitoid Project Fig 4.2.2.8 X-26, L-708, LR-20, LR-23 L-1016 LR-4 L- 7 1 4 L- 7 1 2 L - 7 1 4 L- 1 0 2 0 L- 7 1 6 L - 7 0 5 L- 6 9 3 L - 6 9 8 0 0 . 1 0 . 2 0 . 3 0 . 4 0 . 5 0 . 6 0 . 7 0 . 8 0 . 9 1 F = % Feld s p ar s + musc o v i t e 1 0 . 9 0 . 8 0 . 7 0 . 6 0 . 5 0 . 4 0 . 3 0 . 2 0 . 1 0 Q = % Q u a r t z 1 0 . 9 0 . 8 0 . 7 0 . 6 0 . 5 0 . 4 0 . 3 0 . 2 0 . 1 0 B = % D a r k m i n e r a l s QBF ternary diagram (afte r Deb o n & LeF o rt , 19 9 4 ) Samples from the Oas Farm, Khorixas Inlier, Namibia Greater Lufilian Arc Granitoid Project R e f e r e n c e sa m p l e s (D e b o n & LeF o r t ) S a m p l e s L- 6 7 5 L - 6 9 9 L- 6 6 9 L - 7 1 3 L- 6 7 5 L- 6 7 0 L - 6 9 5 L - 6 9 4 L - 6 9 7 L - 6 7 6 L - 6 9 1 L - 1 0 1 6a L - 1 0 1 6 L - 7 0 8 L - 6 6 8 L- 1 0 1 9 Fig 4.2.2.9 2 2 8 The sample s from the Oas Farm that were analysed co uld be separated into four rock groups: 1) basement rocks, 2) massiv e intr us i on s of midalk al i n e and alkalin e ch aract er , 3) dikes that intersec t the second group, and 4) younger granito id s . These are listed on T able 4.2.2.7, along with their main geochemi c a l char ac t e r is t i c s and studies on environment of emplacement. Table 4.2.2.7 Sample grouping, Oas farm, Namibia (*dated samples. See acronym descrip t i o n on section 2.4.3.) Basement Sampl e Rock Name Debon & Le For t Mania r & Picco l i W h a l e n P e a r c e Mafic Rb/10H f Ta Rb/30H f Ta Nb-Ta L-712 alkal i grani t e peral u m iii leuco NaFe POG A V L-713 quart z s yeni t e metal u m v leuco NaFe A O-W 2-2 WP W OUT U L-714 Grani t e metal u m v leuco NaMg OP A V L-714a alkal i grani t e peral u m ii leuco NaFe A V L-715 Granite metalum iv meso Na-Kfe RRG-CEU G A O3/4 OUT U L-716 * Grani t e metal u m iv subleuc o NaFe C E U G - R R G A S2/4O2 / 4 VA- VA INV L-101 9 alkal i grani t e metal u m v suble u c o NaFe R R G A V2/4 WP- WP INW L-102 0 Grani t e metal u m v meso NaFe A W Mass ive Intrus ives Sampl e Rock Name Debon & Le For t Mania r & Picco l i W h a l e n P e a r c e Mafic Rb/10H f Ta Rb/30H f Ta Nb-Ta L-668 * Syeni t e metal u m iv meso NaFe RRG A O-W 2-2 wp ab WP- WP INW L-669 Syeni t e metal u m iv meso NaFe CEUG A W WP- WP INW L-670 Nephe l i n e s yeni t e metal u m iv meso NaFe RRG A O-W 2-2 ? OUT U-NE A L - 6 7 5 Syenit e peralu m i subleu c o NaFe CEUG A W3/4 wp ab OUT U L-676 Syenit e metalu m iv meso NaFe RRG-CE U G A W wp ab L-694 Nephe l i n e s yeni t e metal u m v meso NaFe RRG A W wp ab L-695 Nephel i n e s yenit e metalu m iv meso NaFe RRG-CE U G A O-W 1-1 wp ab L-697 Syenit e metalu m v meso NaFe RRG-CE U G A W3/4 wp ab WP- WP OUT U-NE A L - 6 9 9 Syeni t e metal u m iv meso NaFe CEUG A W X-21 Syenit e X-22 Quartz s yenite X-23 Quartz s yenite Dikes Sampl e Rock Name Debon & Le For t Mania r & Picco l i W h a l e n P e a r c e Mafic Rb/10H f Ta Rb/30H f Ta Nb-Ta L-691 Monzo n i t e metal u m iv meso NaFe RRG-C E U G A W wpt L-693 * alkal i grani t e metal u m iv meso NaFe RRG A W3/4 WP- WP INW L-698 alkal i grani t e metal u m v meso NaFe RRG-C E U G A O-W 2-2 OUT U L-708 Pyro xen i t e metalum v meso NaFe IAG-CA G A W? wp ab X-24 Nephe l i n e s yeni t e X-25 Gabb ro X-26 Satur a t e d olivi n e gabbro Quartz it es Sampl e Rock Name Debon & Le For t Mania r & Picco l i W h a l e n P e a r c e Mafic Rb/10H f Ta Rb/30H f Ta Nb-Ta L-1016 Quartzit e L-1016a Quartzit e Most samples that come from the Oas farm N-S transe ct are enriched in Nd, Pr, Ce, La, Nb, Zr, Sm, Nd, Pr and Y. They are also high in Na, Mn and Zn. Thes e make up a suite of rocks that are very similar to each other, and may have been emplaced at approximately the same time. Samples of syenite and nepheline syenite from the main cluster of ring complexesFig 4.2.2.1) show some additional similarities . Results from a simplified isocon diagram compar ison of each of these samples with all the rest are shown on the matrix of Table 4.2.2. 8 . The follow in g conclus i on s were reache d : the main group of samp le s is L-668 , L-669 , L-694 , L-697 and L-699 . Samples L-670 , L675 and L-676 are similar to each other. Samples L-676 , L-691 , L-693* , L-695 and L-698 are different from the main batch. L-698 a nd L-693* are very similar to each other, and differe n t from other rock s in the suite. They are also very similar to L-713 , L-715 a n d L-716* . In other plots, they are similar to L-1020 a nd L-1019 . L-716* w as dated and turned out to be younger than the syenite ring complex es . 2 2 9 Table 4.2.2.8 Correlation matrix of samples fr om the Oas ring complexes using the isocon diagram (Grant, 1986) and visual comparison. ( C on v e n t i o ns: B = bad, C = some change or variati on , G = good, VG = very good, ~ = reas ona b l e . ) L-669 L-670 L-675 L-676 L-691 L-693* L-694 L-695 L-697 L-698 L-699 L-668 G C C ~ C B G C G C G L-669 ~ ~ C C B G C ~ ~ VG L-670 ~ B B B B C B B ~ L-675 ~ B B ~ B B B ~ L-676 C B ~ ~ ~ B B L-691 B B C B B B L-693* C B B G B L-694 ~ VG B G L-695 B B C L-697 B G L-698 C L-712 , L-713 , L-714 a nd L-714a are all leucoc ratic. L-668 , L-669 , L-670 , L-675 , L-694 a nd L-697 make a straigh t line on the R1R2 diagram (Fig 4.2.2.5 ) . The same samples plot as a trend on the QBF diagram of Debon & LeFort (Fig 4.2.2.9). Samples L-668 , L-669 , L-670 , L-675 , L-676 , L-694 , L-695 , L-697 , L-699 , L- 708 ; all are in the ALKS suite of rocks on the QBF diagram (Fig 4.2.2.9). On the same diagram, L-693* , L- 698 , L-714 , L-715 , L-716* a n d L-1020 plo t on one of the ?quartz- poo r ? aluminou s types. L-694 and L-697 have very similar chemis tr y. L-669 and L-699 are also very simila r to each other. L-693* and L-698 are very different from the rest of the rocks in th e suite; they are extremely similar to each other. L-1019 seems to have significant hydrothermal alteration. On the R1/R2 diagram, L-716* forms a dense cluster of granit e s with L-715 (Oas farm), L-728 , L-729 , L-742 , L-1021 (Lofda l farm), L-759 , L-773 , L-783 and L-784 (Mes opotamie farm). See Fig 4.2.2.5. The minor element chemistry is uniform too. Thes e samples probably come from several suites of rocks, that formed at different times. All of these granites seem to hav e formed in anoroge n ic environ m en t s , accordi n g to the Whalen plots; the ones that produc e cohere n t result s from the Pearce diagrams are within-plate granites, and the ones that produc e coheren t results from the Mani ar & Piccoli procedure were formed in rift-related environments. They all formed in a simila r environmen t, from the same protolith, but at different times. Table 4.2.2.9 compiles most of the groups of rocks with similar chemic a l feature s from the differ e n t samplin g domains in Namibia, except for the Kamanjab Batholit h. There are many similarities between the various domains. Logarithmic major oxide and trace element diagrams of the groups of Syenites A and B have been plotted on Figs 4.2.2.10 and 4.2.2.11 to show their chemical similarity. 4.2.2.2.4 Zinc Enrichment All syenite s and gabbros from various Namibia n region s ar e enriche d in zinc, as show n on Table 4.2.2.9 . Part of the alkali granites and granites are also zinc-enr ic he d. A large portion of the rocks mentioned come from the Oas farm (See Table 4.2.2.3). 2 3 0 Table 4.2.2.10 Groups of sampl es from various Namibian regions. (Grouping ac cording to Table 4.2.2.9) (complete elemental analysis on Table A15, Appendix) Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI T otal Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h Sc Nd Pr Ce La Notc h 50 1 15.5 6 0.15 2 5 4.9 5.5 0.3 2 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 50 15 175 95 Basement granites Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI T otal Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h Sc Nd Pr Ce La L-715 72.1 0.48 13.0 2 3.49 0 0.09 0.48 1.12 3.88 4.88 0.12 0.5 100. 2 118 147 58 348 25 8 11 12 67 18 28 47 1230 <6 19 <10 39 88 154 44 L- 716 * 73.9 0.3 12.5 4 2.79 0 0.04 0.41 0.98 4.49 3.98 0.04 0.68 100. 1 69 164 38 332 16 8 11 12 51 16 19 57 1389 7 24 <10 42 11 134 66 L- 729 73.6 0.31 12.6 4 2.31 0 0.05 0.34 0.84 3.69 4.96 0.03 1.7 100. 5 113 82 46 281 24 <6 6 6 60 <12 58 957 L-759 74.1 0.03 14.4 7 0.47 0 0.04 0.02 0.7 3.55 5.54 0.06 0.94 99.9 109 124 20 16 7 <6 <6 <6 12 13 <12 185 649 <6 <15 <10 12 <12 L-773 74.8 0.06 14.9 8 0.87 0 0.02 0.11 0.8 5.35 3.07 0.04 0.41 100. 5 76 71 103 64 14 <6 10 8 43 20 <12 47 176 <6 <15 <10 25 <12 L-783 71.9 0.45 13.9 6 3.32 0 0.08 0.5 0.78 3.49 5.15 0.18 0.71 100. 5 223 85 54 273 22 <6 6 9 49 17 25 239 859 <6 27 <10 161 75 L- 784 71.8 0.39 13.2 3 3.59 0 0.06 0.56 1.31 3.67 5.07 0.09 0.7 100. 5 193 105 58 312 23 <6 7 7 59 17 23 63 1049 7 26 <10 37 99 155 51 L- 1021 72 0.43 12.8 6 3.47 0 0.05 0.24 1.1 4.37 4.02 0.07 0.53 99.2 83 92 84 464 33 <6 8 5 29 17 <12 250 1355 <6 18 <10 143 61 L-712 79.1 0.04 12.0 4 0.83 0 0.04 0.11 0.4 5.47 1.95 0.01 0.54 100. 5 33 159 12 17 7 <6 10 8 35 18 <12 47 662 <6 <15 <10 13 41 7 L- 714 77.6 0.05 13.1 9 0.73 0 0.03 0.17 0.85 6.33 0.76 0.02 0.67 100. 4 16 338 9 250 9 <6 9 8 40 23 <12 50 538 <6 16 <10 3 83 L- 728 75.1 0.16 10.3 5 2.83 0 0.14 0.22 2.2 6.61 0.86 0.06 2.04 100. 5 23 140 58 212 33 <6 10 15 45 18 14 67 581 5 21 15 82 20 171 73 L- 742 68.4 0.18 10 3.45 0 0.2 2.09 0.9 5.4 1.17 0.03 8.44 100. 3 59 181 41 310 26 11 13 32 227 19 18 44 802 <6 21 <10 33 52 79 44 L- 1020 70.8 0.58 12.6 8 4.01 0 0.1 0.76 1.57 5.17 3.14 0.09 0.31 99.2 70 173 52 445 22 <6 8 64 85 17 19 <12 1364 <6 19 <10 180 95 Q u a r tz i t es L-1016 77.3 0.1 1.04 2.18 0 0.47 2.02 6.71 0.5 0.09 0.13 8 98.6 6 124 8 15 4 <6 <6 56 14 <9 <12 351 33 <6 <15 12 24 <12 L-1016 a 79.4 0.1 0.8 2.49 0 0.45 1.96 5.74 0.55 0.13 0.04 7.5 99.1 5 140 6 37 4 <6 7 28 27 <9 13 15 57 <6 <15 10 23 <12 Syenite A Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI T otal Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h Sc Nd Pr Ce La L-668 62.6 0.89 17.3 2 4.83 0 0.14 0.72 1.8 6.42 4.79 0.36 0.59 100. 5 121 474 69 710 193 7 7 6 127 26 14 139 2037 7 22 <10 101 182 235 110 L- 669 64.3 0.61 16.7 6 4.66 0 0.12 0.36 1.46 6.43 4.8 0.23 0.74 100. 5 115 350 73 378 204 <6 9 7 146 28 <12 124 1647 9 31 <10 102 28 267 137 L- 670 57 1.45 15.1 4 11.0 8 0 0.21 1.42 2.33 6.69 3.35 0.53 1.32 100. 5 173 1219 73 1843 458 <6 9 9 85 42 <12 18 767 17 46 <10 27 72 219 42 L- 675 60.7 0.1 21.9 9 3.59 0 0.09 0.13 0.94 4.92 6.41 0.03 1.61 100. 5 125 384 123 1520 345 7 9 23 167 30 20 17 1321 10 78 11 140 592 844 440 L- 676 59.4 0.87 18.1 3 5.92 0 0.17 1.24 2.05 5.2 5.55 0.24 1.84 100. 6 226 634 58 553 139 7 7 11 177 26 19 31 1591 <6 19 <10 180 85 L- 694 59.2 1.09 17.0 7 5.91 0 0.17 1.01 2.48 6.84 4.89 0.36 0.54 99.5 106 633 39 333 93 7 <6 10 107 23 27 <12 1995 <6 <15 <10 166 87 L- 697 59.9 0.86 16.9 5.28 0 0.17 0.99 2.06 6.58 4.59 0.32 1.54 99.2 169 491 151 1363 432 8 9 5 129 26 <12 117 1444 15 51 <10 127 480 582 291 L- 699 63.4 0.28 17.2 8 5.27 0 0.2 0.34 0.93 7.4 4.73 0.12 0.56 100. 5 98 114 75 1246 307 <6 10 7 147 34 <12 126 458 15 50 <10 470 310 L- 1022 54.8 0.44 20.4 1 5.9 0 0.2 0.33 1.95 4.97 7.25 0.13 2.78 99.1 189 616 24 767 249 7 <6 11 171 36 14 <12 629 8 <15 <10 28 48 61 19 LL14 57 1 17 9 0 0 1 3 6 5 0 1 99.5 280 355 161 2052 364 4 5 133 4 0 1161 22 83 5 X - 21 60.8 0.87 16.9 7 1.13 4.1 0.16 0.99 1.94 5.65 5.27 0.22 1.78 99.9 Syenite B L-695 46.3 3.29 13.3 4 13.5 4 0 0.48 3.19 4.92 4.1 3.51 0.68 6.78 100. 1 197 399 53 329 54 27 22 89 120 19 353 28 639 <6 <15 26 64 30 L- 741 56.6 0.47 19.5 4 7.23 0 0.44 0.8 3.09 4.14 7.21 0.11 0.91 100. 6 169 548 49 640 337 <6 <6 14 164 34 14 18 1955 19 <15 <10 52 211 248 131 L- 1027 55.1 0.81 15.7 7 5.91 0 0.27 2.32 3.6 4.38 6.88 0.23 3.58 98.8 177 429 37 621 220 14 42 25 134 24 45 174 1043 <6 <15 <10 58 136 239 72 LL10 56.5 1.24 17.8 4 6.85 0 0.19 1.96 3.78 5.74 4.86 0.74 0.74 99.7 135 965 36 340 99 11 3 0 78 44 0 1366 9 25 1 LL15 62 1 16 6 0 0 1 4 6 5 0 4 99.7 118 328 31 305 47 10 9 0 73 125 22 1308 3 26 15 X - 24 51.3 0.4 19.0 6 5.95 1.05 0.42 0.82 4.79 6.75 5.19 0.3 3.38 99.4 Alkali granites Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI T otal Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h Sc Nd Pr Ce La L-693 71.4 0.48 11.6 5 6.47 0 0.14 0.19 0.77 4.62 4.46 0.09 0.31 100. 6 86 98 31 132 105 6 7 14 128 33 <12 60 241 2 9 <10 114 35 357 216 L- 698 71.7 0.46 11.4 5.84 0 0.1 0.1 0.85 4.91 4.1 0.1 0.4 99.9 77 45 50 329 124 <6 7 7 104 35 <12 207 157 <6 <15 <10 67 228 372 143 L- 713 71.3 0.16 14.3 6 2.37 0 0.05 0.08 0.32 5.76 5.66 0.02 0.41 100. 5 117 94 30 277 71 <6 8 9 53 25 19 49 909 <6 <15 <10 80 295 436 188 L- 714 74.5 0.12 14.6 3 0.94 0 0.04 0.12 0.59 8.15 0.94 0.05 0.41 100. 5 16 152 25 237 50 <6 8 <6 17 0 12 160 606 0 0 0 0 0 L- 772 72.6 0.03 14.2 9 0.43 0 0.03 0.03 0.05 2.34 10.1 0.02 0.67 100. 5 201 100 7 <8 4 <6 <6 8 28 13 <12 44 579 <6 <15 <10 21 <12 L-1019 72.2 0.41 13.1 7 3 0 0.11 0.24 0.79 6.18 3.79 0.08 0.41 100. 4 50 101 31 290 47 <6 10 9 62 17 <12 253 1351 2 17 <10 47 12 110 60 LL3b 70.3 0.04 16.9 1 0.47 0 0.01 0.24 0.37 2.44 9.09 0.09 1.2 100. 0 348 252 9 5 4 2 1 0 7 7 1 495 1 0 5 G a b br o i ds Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI T otal Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h Sc Nd Pr Ce La L-691 50.2 3.31 12.9 5 14.1 5 0 0.21 4.13 6.53 2.95 2.82 0.55 1.51 99.4 151 589 52 368 62 39 32 190 166 19 357 66 617 <6 <15 33 110 61 L- 708 47.2 0.47 8.72 11.2 7 0 0.53 13.1 14.2 1.46 1.77 0.04 1.79 100. 5 86 578 146 469 126 16 26 13 279 17 68 14 2096 <6 <15 23 258 97 L- 1032 46 1.99 15.4 7 14.0 7 0 0.33 6.8 9.26 3.22 0.75 0.42 1.94 100. 3 10 322 48 132 9 47 45 26 163 15 345 218 299 <6 <15 40 42 61 <12 40 L- 1023 47.5 0.82 15.7 11.3 9 0 0.21 7.63 11 2.78 0.87 0.09 2.31 100. 3 19 177 23 45 5 51 86 11 157 19 246 354 223 <6 <15 42 33 20 L- 1025 42.1 1.06 1.26 21.4 2 0 0.77 2.76 17.4 1.61 0.56 3.85 7.4 100. 2 30 1546 50 1312 ## 42 10 29 207 12 334 106 214 86 20 33 183 47 396 176 X - 25 47.5 2.22 14.4 7 3.74 8.09 0.05 6.73 11.6 1.24 0.77 0.3 2.8 99.5 X-26 48.8 1.03 12.2 1 3.62 6.54 0.15 13.7 9.63 1.77 1.1 0.59 1.16 100. 3 Carbonatites L-722 7.5 0.04 0.13 9.55 0 0.68 2.58 43.8 0 0 0.03 36.2 100. 5 7 210 260 119 13 23 <6 5 37 <9 194 12 145 6 27 54 16 10 <12 L-1024 a 7.58 0.07 0.57 9.33 0 0.79 5.76 37.2 0.03 0.15 0.23 38.8 100. 5 6 335 62 9 44 28 21 177 59 <9 23 <12 115 19 20 49 543 179 2058 1583 L- 1024c 5.56 0.06 0.2 9.37 0 0.84 6.08 39.5 0.01 0.04 0.23 38.7 100. 6 10 325 92 18 31 29 11 116 29 <9 24 <12 99 20 18 49 1786 1383 O ther L-713 71.3 0.16 14.3 6 2.37 0 0.05 0.08 0.32 5.76 5.66 0.02 0.41 100. 5 117 94 30 277 71 <6 8 9 53 25 19 49 909 <6 <15 <10 80 295 436 188 L- 754 53 1.59 13.3 2 16.1 8 0 0.28 6.53 7.5 0.32 1.02 0.3 0.15 100. 2 318 84 40 94 8 50 53 94 252 17 393 178 235 <6 <15 49 25 12 Granite F Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI T otal Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h Sc Nd Pr Ce La L-605 76.6 0.12 12.0 3 1.16 0 0.01 0.02 0.81 3.42 5.47 0.07 0.41 100. 1 198 99 7 89 7 <6 <6 9 19 13 <12 227 772 <6 42 <10 148 102 L- 791b 76.4 0.14 12.5 5 1.25 0 0.02 0 0.51 3.09 5.85 0.03 0.29 100. 1 270 74 83 70 65 <6 10 <6 15 22 16 234 332 8 17 <10 224 108 L- 793 74.9 0.33 12.3 9 2.15 0 0.08 0.24 1 3.28 5.24 0.14 0.37 100. 1 251 140 81 213 78 <6 7 7 34 19 22 390 435 12 61 <10 51 175 234 98 L- 797 75.1 0.21 13.0 5 1.92 0 0.04 0.08 0.51 3.62 4.63 0.08 0.61 99.9 225 107 23 199 38 <6 6 <6 33 21 17 372 658 6 37 <10 132 76 L- 802 73.3 0.23 14.5 6 1.83 0 0.05 0.29 1.08 3.46 4.55 0.13 0.84 100. 4 234 141 32 142 41 <6 6 <6 51 19 22 260 745 <6 15 <10 77 38 L- 812 75.6 0.08 12.8 9 1.27 0 0.03 0.25 1.29 4.03 4.17 0.09 0.71 100. 4 141 104 86 215 10 <6 8 9 67 13 <12 34 439 17 30 <10 93 55 L- 1043 72.4 0.34 13.6 2 2.4 0 0.04 0.57 0.57 2.76 5.77 0.1 1.27 99.9 276 85 71 207 17 7 9 51 30 14 28 <12 525 <6 44 <10 42 89 140 35 L- 1044 73.4 0.25 12.7 2 2.04 0 0.04 0.39 0.49 2.79 5.94 0.11 1.1 99.3 293 67 47 166 16 6 9 115 70 12 20 12 415 <6 36 <10 109 44 L- 1046 72.8 0.33 12.7 3 2.4 0 0.03 0.55 0.76 2.61 5.45 0.12 1.39 99.2 283 61 69 193 16 6 9 30 27 13 25 16 473 <6 42 <10 126 53 LL2a 75.7 0.02 14.9 8 0.67 0 0.01 0.06 0.12 3.62 4.86 0.04 1.36 100. 1 181 35 10 19 19 2 1 14 8 11 0 104 2 4 2 2 3 1 LL3a 75.9 0.03 13.8 7 0.68 0 0.01 0.05 0.39 2.87 5.93 0.01 1.19 99.8 156 182 13 29 0 2 1 14 4 5 3 659 0 7 1 X - 20 76 0.23 12.0 5 0.8 0.91 0.03 0.2 1.02 3.09 5.02 0.01 1.14 100. 5 Granit e G Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI T otal Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h Sc Nd Pr Ce La L-715 72.1 0.48 13.0 2 3.49 0 0.09 0.48 1.12 3.88 4.88 0.12 0.5 100. 2 118 147 58 348 25 8 11 12 67 18 28 47 1230 <6 19 <10 39 88 154 44 L- 810 73.9 0.06 14.0 5 1.11 0 0.04 0.16 1.04 4 5.44 0.04 0.5 100. 3 173 85 7 <8 7 9 10 13 50 14 <12 56 249 <6 <15 <10 24 <12 LL1 73.4 0.09 14.6 5 0.8 0 0.01 0.27 1 3.34 6.24 0.2 1.26 100. 0 150 176 17 42 6 3 3 13 11 6 1 1468 0 5 2 Granite I L-606 72.6 0.36 12.8 3 3.51 0 0.06 0.48 1.32 3.22 5.19 0.07 0.73 100. 3 185 105 38 202 17 <6 6 7 61 18 20 57 781 <6 38 <10 227 149 L- 729 73.6 0.31 12.6 4 2.31 0 0.05 0.34 0.84 3.69 4.96 0.03 1.7 100. 5 113 82 46 281 24 <6 6 6 60 <12 58 957 L-759 74.1 0.03 14.4 7 0.47 0 0.04 0.02 0.7 3.55 5.54 0.06 0.94 99.9 109 124 20 16 7 <6 <6 <6 12 13 <12 185 649 <6 <15 <10 12 <12 L-783 71.9 0.45 13.9 6 3.32 0 0.08 0.5 0.78 3.49 5.15 0.18 0.71 100. 5 223 85 54 273 22 <6 6 9 49 17 25 239 859 <6 27 <10 161 75 L- 798 72.6 0.26 14.0 7 2.13 0 0.08 0.26 1.09 3.42 5.17 0.12 0.91 100. 2 222 204 26 229 48 <6 <6 <6 40 20 16 285 1117 7 27 <10 211 102 L- 799 73.1 0.08 13.9 3 1.96 0 0.06 0.04 0.95 3.84 4.84 0.13 0.63 99.6 153 168 53 183 14 <6 7 11 19 18 29 326 727 7 <15 <10 102 36 L- 809 71.6 0.07 14.9 5 1.24 0 0.03 0.23 0.87 3.46 7.52 0.06 0.5 100. 5 253 92 19 <8 9 <6 7 11 56 16 <12 27 301 <6 <15 <10 29 <12 L-1021 72 0.43 12.8 6 3.47 0 0.05 0.24 1.1 4.37 4.02 0.07 0.53 99.2 83 92 84 464 33 <6 8 5 29 17 <12 250 1355 <6 18 <10 143 61 LL11 73 0 14 2 0 0 0 1 3 6 0 1 99.9 287 134 34 210 16 2 1 0 30 20 3 880 3 55 5 LL18 76 0 13 1 0 0 0 1 3 7 0 1 100. 1 178 84 8 55 3 0 8 5 4 316 5 4 1 LL4 74.7 0.1 13.5 1.59 0 0.03 0.1 0.8 3.49 5.74 0.02 0.41 100. 1 365 50 32 138 29 1 0 27 1 0 235 4 52 5 2 3 2 Fig 4.2.2.10 Logarithmic major oxide plot for the Syenites A and Syenites B groups in the Oas farm, Loftal farm and Ojtiwarongo environs, Namibia Fig 4.2.2.11 Logarithmic trace elem ent plot for the Syenites A and Syenites B groups in the Oas farm, Loftal farm and Ojtiwarongo environs, Namibia 2 3 3 Table 4.2.2.9 Comparison of sample groups from various Namibian regions (Bas ed mainly on geochemical simila rities.) Group Oas Lofdal Mesopotamie Summas Mts. Otjiwarongo AVMIN Felsic Volc. Grootfontein Okwa River Ugab River NW Zambia Hook Granite Age Environment S ye n i t e A L-676, L- 699, L-67 5, L-668* , L- 669, L-67 0, L-695, L- 697, X-21 L-1022 LL14 762?12 (L-668 ) Syenit e B L-694, X- 24 L-1027 , L-741 LL10, LL15 Alka l i Granite L-693* , L- 698, L-10 19, L-713, L- 714a L-772 B L-791a LL3b, L-1 039, L-1039a, L-1039c X-16, X-18, X-19 L-600A ~750 (L-6 93*) Rfit-related anoro g e n i c gtd. Gabbro L-708, X-25, X-26, L-6 91 L-1032,L - 1023,L-10 25 Base Granit e B L-1020, L-714, L-712 L-742, L-728* ~1750(L-728) Granite F X-20 L-791b LL2a, LL3a, LL17a L-812 L-043* , L-1044, L-1046 L-605 L-793, L-802, L-797, L-796* L-364, L-370 L-257, L -409 1887?39 (L- 1043) ~170 0 (L - 796) Granite G L-715 LL1 L-810 Granite I L-1021, L-729 L-759 L-758* A L L 1 1 , LL4, LL18 L-809, L-813, L-808* , L-815 L-1042 L-606 L-798, L-799 540 (L- 745) ~550 (L-8 08c) (L-758 ) 750?5 M a relic t at 1692?10 M a Anoro g e n i c undete r m i n e d envir o n m e n t Carbonat i t e L-1024a, L - 1 0 2 4 c , L - 7 2 2 L-411 Quartzite L-1016,L - 1 0 1 6 a Syenite C L-40 Base Granit e A L-716* L-729, L-1021 L-759 , L-773 ~745?15 (L - 7 1 6 * ) R i f t - R e l a t e d Anoro g e n i c Other L-713 L-754 L-729, L-1021 L-783, L -784, L-793 + schi s ts D 1692?10Ma (L- 758) W i t h i n -p l a t e Rift-R e l a t e d anoro g e n i c gtds L-789 L-1037, L-1038 , LJ1 Quartz pods 2 3 5 4.2.2.2.5 Quartzite from Oas Fa rm that might host mineralization. The chemic al analyses of L-1016 and L-1016a show high conten t of silica, CaO, MgO, Cu and high loss on ignition; extremely low K, Na and other oxides (Table 4. 2.2.3 ) . In thin section, the rocks are quartz it e s with partia l carbona t e cement and strong hydrot h er m a l overpr in t. The rock is light gray to white under the surface weathe r i ng crust (red-br ow n to dark gray color). Numero us quartz veins intersect the quartzites and in some areas signific a n t iron oxide minerali z a t i o n accompani e s the quartz . Extens ive exposures of the quartz ite are covered by hydrothermal breccias and stockwor ks. Fig 4.2.2.12 Field relationships of mineralized quartzites at the Oas farm , Namibia. Note size of the stockworking, quartz veins that intersect the quartzit es and the open vugs . Other descriptions in the text. Fig 4.2.2.12 is a sketch of field relationships ob serv e d around geolog i c a l statio n S170. The rock makes massiv e outcro ps , has a dark gray to brown surfac e w eathe ri ng color, rings like a bell when hammered , and displa ys abundant elongated vugs that are alligned . These look like elongated vacuoles in a lava. Parts of the rock contai n lensoi d fragme n t s of what seems to be a schistose or slaty material , after clay. Those fragments are seldom longer than five centimet er s . The rock?s indurat i o n makes it behave in a brittle way, and after fracturi n g , it becomes a good host for mineraliz a t i on . 4.2.2.2.6 Geochronology Three new isotop i c ages were produc ed from rocks at t he Oas farm during this projec t . Zircon s from samples L-716* , L-688* and L-693* were dated by U-Pb SHRIMP II techniques (Table 4.2.2.11). Table 4.2.2.11 Samples from the Oas fa rm ring complex cluster that were dated Sample Description Age (Ma) Notes L-688* S l i g h t l y- m a g n e t i c , bro wn -c o l o r e d fi ne- to mediu m - g r a i n e d s yeni t e with littl e visib l e quart z 762?1 2 Struc t u r a l relat i o n s h i p s indic a t e that the rock is older than L-689 . L-693* F i n e - g r a i n e d , me dium gra y, me ta l um i n o u s meso c r a t i c sodi c ferrif e r o u s , biotit e - r i c h , non-ca l c a re o u s alkal i grani t e , with stron g magne t i c conte n t 765?4 . 5 Struc t u r a l relat i o n s h i p s indic a t e that the rock is yo ung e r than L-688*. L-716* G n e i s s i c , medium - g r a i n e d , pink and black laye r e d , metal u m i n o u s suble u c o c r a t i c sodic ferri f e r o u s gran i t e with macr o s c o p i c potas s i u m felds pa r + q u a r t z + b i o t i t e and no app re c i a b l e magne t i t e 745?5 Youn g e s t kno wn intru s i o n at the Oas farm. The first intrusion of syenites ( L-688* ) was clos e ly follo w ed by an intr us ion of granite ( L-693* ) , and approximately 20 Ma later, by the intrus i on of alkali granit e ( L-693* ) . There might be at least two different minor younger intrus iv e events that intersec t the other plut on i c rocks, but they do not seem to be as relevan t for mineralization. A quartz syenite from the Oa s farm was dated by Hoffmann et al., 1996 at 756?2 Ma. 2 3 6 T h e protoli t h of intrusi v e rocks at t he Oas farm probabl y are granite s with ages of emplaceme n t that oscillat e in the range of 2192 to 2124 Ma, as indicated by inherit ed zircon s in samples from the Oas farm dated by Tegtmeyer & Kroner, 1985. Even though none of such rock s have been spec if i c a ll y dated, they could be part of the group of foliated granites and alkaline granites ob served at the farm. These might be correlative with the oldest rocks from the Kamanjab batho lith. Two granites in the nearby Lofdal and Mesopotamie fa rms were dated for the Greater Lufilian Arc projec t. These are L-758* and L-728 *. They produced ages of 750?5 Ma and 1750?5 Ma respec tively. Radiom e t r ic ages avail a b le for grani t o id s from the Oas fa rm in Namibia were plotted on the event diagram of Fig A38, along with other ages know n for the Khor ixas Inlier, the Summas Mountains and the Mesopotami e farm (Table A22.16). A minimum span of 113 Ma (Fig A3 8) , brok en into at least two discrete events of intrus io n took place. Ther e was one that is not so precis ely cons trained, from 853 to 827 Ma, and an almost continuo us series of intrus iv e events from 801 to 740 Ma (Table A22.16). This ev idence shows that the Oas farm ? consequentially the Khorixas Inlier - had a long-liv ed series of alkaline events of intrusion that took place in roughly the same place. The events of the Oa s farm are akin to thos e studie d for anoroge n ic alkali n e comp le xe s in vario us provi n c es worl dw i de. This is discussed on section 7.2. 4.2.2.2.7 Environment of Emplacement Table 4.2.2.7 show s the results of studies to devise the environ ment of emplacement for this important sample . The following is a descrip ti o n of the env iro n me n t s for the various groups of rocks. The basemen t granit o i ds observ e d at the Oas farm a ll formed in anorog en i c enviro n me n t s . L-713, L-715, L- 716, L-1019 and L-1020 have many similar i t i es and form ed in a rift-re l a t e d environ me n t . L-712 seems to have formed as a post orogenic granito i d in an anorogen ic environme nt , and L-714 as an oceanic plagiog r an i t e . These last two samples are cons ider ed to be the two oldest rock types in the Oas farm. The syenites and nephel i n e syenit e s and alkali granit es formed in a continu u m of continental epeirogenic uplift to rift related environments. The dikes formed mainly in rift-related environments. 4.2.2.2.8 Conclusions A basement of Paleopr o t er o z o i c gneisse s was intr ude d by a series of zinc -ric h midalka l i n e small anorogen i c comple x e s for a period that lasted from 801 to 740 Ma. Dike s of compos itions that vary from alkali granite to ultram a f ic and hypera lk a l in e and carbon a t i t i c intr ud e d the whole sequence during the midalkal i n e magmatis m . Several of the intrus ive events produced significan t hydr oth er m a l breccia t i o n . Mass ive iron oxide bodies were emplac ed along favour able structur es. Iron sulfides and po ssibly sulfides of zinc and copper, along with gold and silver were later depos ited on or around the magnetit e and hematit e bodies . Widespr e ad red-roc k and brow n- r oc k hemati t e alterat i o n and sodic altera t i on modifi e d the surrou n d in g rocks. Quar tz poddin g and some silicific ation replac ed in suitable redox sites in granitoids. All this took plac e in a continuum of continental epeirogenic uplift to rift related environments. At least nine circular midalkaline intrus ions were empl aced to make a ring comple x cluster at the Oas farm. The entire domain of the Oas syenites is prospective fo r iron oxide-c o pp e r - go l d mi neralization, and maybe for various types of zinc miner alizati o n . Economic rare earth deposit s and maybe thorium mineral enrichme n t s can probably also be found in association with the midalkal i n e and alkaline intrus iv e rocks. 2 3 7 4.2.2.3 LOFDAL FARM, NAMIBIA 4.2.2.3.1 Introduction The Lofda l farm is located in the eastern portion of the Khor ixas Inlier, to the west of the town of the same name in Damaral an d , norther n Namibia (Fig M20). The fa rm hosts a wide variet y of rock types. As observ e d on Figs 4.2.2.2 to 4.2.2.5, granites, nepheline syenit es, alkali gabbros and carbonatites occur togethe r and produce a complex set of minerals, mineralization, al teration and geolog y. This is probably a produc t of overpr i n t i n g intrusio ns over a long period of time. Older granites were intrude d by alkaline rocks in a rift environment. Major iron oxide bodies, sulfidation and emplac e me n t of brecci a pipes are relate d to the alkali n e plutonism. Repetitive explos ive hydrothermal events produced particu l ar hydroth e r m a l brecci a t i o n and what seems to be economic iron oxide-co ppe r - g o l d minerali z a t i on . This chapter will cover some aspects of geochem is t r y , environ m en t of emplac eme n t and geochro n o lo g y of the Lofdal area. A description of the field sampling will fo llow , and will clos e with some commen ts on carbon a ti t e s . 4.2.2.3.2 Geochemistry Table 4.2.2. 1.2 lists 21 repres e n t a t i v e sample s collec ted at Lofdal. Fifteen samp le s were analys e d for the Greater Lufilian Arc granito i d project, and six chemical anal ysis come from technical reports. Chemistry of only a small portion of the samples collect ed is availab l e . Most rocks were slabbed for macrosc opic studies ; none of the minerali z e d sample s have been assayed to date. 20% of the granitoids from the Lofdal farm fall within the midalkaline field, while 80% of them fall in the subalkaline field (Table 4.2.2.12). All midalkaline roc ks make 8% of the sample s . 58% are sulbal k a l i n e and 33% are alkali n e rocks. This suite of rocks is more enr ic h ed in alkali ne rocks than most of the others in the Greater Lufilia n Arc. Carbona t i t e s are extremely important. They accoun t for almost half of the total samples. The Lofdal farm subdomain is clearly domi nat e d by subalka l i n e and alkalin e rocks. Table 4.2.2.12 Statistics of rock types, Lofdal farm, Namibia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type Number % Granitoids Groups Midalkaline Rocks M o n z o n i t e 1 8.33 20 . 0 0 8.33 Granite 3 25.00 Gr a n o d i o r i t e 1 8.33 ga b b r o -d i o r i t e 1 8.33 Subalkaline Rocks Gabb ro 2 16.67 8 0 . 0 0 58.33 foid monzo s ye n i t e 3 2 5 . 0 0Alkaline Rocks p e r i d o t gabb ro 1 8.33 33.33 Total 1 2 9 1 . 6 7 1 0 0 . 0 0 100.00 Carbona t i t e 9 Total 21 Foliate d granitic rocks are repr es en te d by L-728* , L-729 , L-742 and L-1021 the various intrus io ns and the mineralization. The nepheline syenite L-1027 hosts minerali z e d magnetit e- cemented brecia pipes. L-740 , L- 741 , and L-1022 come from dikes that intrude granite s in different parts of the Lofdal farm. L-1023 , L-1025 , and L-1032 are gabbros with various composi t i on s and mag net ite conten t . Some of them intrude as dikes, others are large bodies that host various other intrusions. L-754 is an ultramaf ic lamproph y r ic rock (See Table 4.2.2.2). Many of the rocks that were analyzed carry signific an t amounts of Nd, Pr, Ce, La, Nb, Zr and Y. Some of them are also enrich ed in Zn. Losses on igniti o n also tend to be high in a large portio n of the samples studied (Table 4.2.2.13). All syenit e s and gabbros from the Lofdal and Oas farms di splay a particul ar enric hm en t in zinc , and part of the alkali granites and granites that were in truded by zinc-ric h rocks have it too. 2 3 8 Table 4.2.2.13 Chemical Analysis of Samples from the Lofdal Farm, Namibia ( c omp l e t e elementa l analys is are included on Table A12 in the Appendix ) Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 MnO MgO CaO Na2O K2O P2O 5 LO I Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U T h Sc Pb Sm Nd Pr Ce La Hf T a Eu Notc h 50.0 0 1.00 15.5 0 6.00 0.15 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 10 120 4 L- 722 7.50 0.04 0.13 9.55 0.68 2.58 43.8 0.00 0.00 0.03 36.2 7 210 260 119 13 23 <6 5 37 <9 194 12 145 6 27 54 17 16 10 <12 229 L-728 * 75.0 6 0.16 10.3 5 2.83 0.14 0.22 2.20 6.61 0.86 0.06 2.04 23 140 58 212 33 <6 10 15 45 18 14 67 581 5 21 15 24 17 82 20 171 73 6 3 3 L- 729 73.5 8 0.31 12.6 4 2.31 0.05 0.34 0.84 3.69 4.96 0.03 1.70 113 82 46 281 24 <6 6 6 60 <12 58 957 L-740 56.7 4 0.26 18.9 1 5.92 0.18 0.21 1.03 6.29 4.68 0.03 6.26 170 442 26 1803 563 <6 11 8 189 42 <12 27 617 27 18 <10 9 22 72 112 36 115 1 L-741 56.6 3 0.47 19.5 4 7.23 0.44 0.80 3.09 4.14 7.21 0.11 0.91 169 548 49 640 337 <6 <6 14 164 34 14 18 1955 19 <15 <10 15 52 211 248 131 127 2 L-742 68.4 1 0.18 10.0 0 3.45 0.20 2.09 0.90 5.40 1.17 0.03 8.44 59 181 41 310 26 11 13 32 227 19 18 44 802 <6 21 <10 3 33 52 79 44 72 1 L-754 53.0 2 1.59 13.3 2 16.1 8 0.28 6.53 7.50 0.32 1.02 0.30 0.15 318 84 40 94 8 50 53 94 252 17 393 178 235 <6 <15 49 25 12 L- 1021 72.0 2 0.43 12.8 6 3.47 0.05 0.24 1.10 4.37 4.02 0.07 0.53 83 92 84 464 33 <6 8 5 29 17 <12 250 1355 <6 18 <10 143 61 L- 1022 54.7 6 0.44 20.4 1 5.90 0.20 0.33 1.95 4.97 7.25 0.13 2.78 189 616 24 767 249 7 <6 11 171 36 14 <12 629 8 <15 <10 3 28 48 61 19 94 0 L-1023 47.5 1 0.82 15.7 0 11.3 9 0.21 7.63 11.0 2.78 0.87 0.09 2.31 19 177 23 45 5 51 86 11 157 19 246 354 223 <6 <15 42 33 20 L- 1024 a 7.58 0.07 0.57 9.33 0.79 5.76 37.2 0.03 0.15 0.23 38.8 6 335 62 9 44 28 21 177 59 <9 23 <12 115 19 20 49 2 50 543 179 2058 1583 0 n.d. 7 L- 1024c 5.56 0.06 0.20 9.37 0.84 6.08 39.5 0.01 0.04 0.23 38.7 10 325 92 18 31 29 11 116 29 <9 24 <12 99 20 18 49 1786 1383 L- 1025 42.0 6 1.06 1.26 21.4 2 0.77 2.76 17.4 1.61 0.56 3.85 7.40 30 1546 50 1312 1425 42 10 29 207 12 334 106 214 86 20 33 5 28 183 47 396 176 10 34 8 L- 1027 55.0 6 0.81 15.7 7 5.91 0.27 2.32 3.60 4.38 6.88 0.23 3.58 177 429 37 621 220 14 42 25 134 24 45 174 1043 <6 <15 <10 58 136 239 72 94 2 L-1032 46.0 4 1.99 15.4 7 14.0 7 0.33 6.80 9.26 3.22 0.75 0.42 1.94 10 322 48 132 9 47 45 26 163 15 345 218 299 <6 <15 40 109 42 61 <12 40 4 23 1 4.2.2.3.3 Description of outcrops from the Lofdal farm Field notes, correc t e d with results of geoche m is try and geochronology are included in Appendix A67. Coor di na t e s of geolog ic a l statio n s and sampli n g site s are also in Append ix A18. Fig 4.2.2.13 is a topogra p h ic a l map of the samplin g sites and geologi c a l stations . Fig 4.2.2.14 show s greater detail and coor dina t e s of the sampling area. The small map on the lower left portion of the figure shows relativ e locatio n of the various study ar ea s. Samples with chemical analysis have been underlined . Dated samples are marked with a star. 4.2.2.3 . 3.1 Dissolution of silicates in granitoids Many granito id s in the Lofdal farm display severe di ssolution effects. Both qua rtz and feldsp a r s have been partially dissolved out of the roc ks, to produc e a ?spongy? texture 1 . Sample L-726 is one of the clearest examples of that feature. Fig 4.2.2. 14 shows its location. The sample is a coarse- to fine-grained granitoid with abundant myarolitic cavities filled by brow n, dr uzy hematite. The rock is spongy, has extremely light density, and shows evidence of massive silicate leaching. Pa rt of the vugs were filled by spec ular ite. It is one of many simil a r rocks in t he enviro ns . Carbon a t i t e bodies and dikes, as well as ultramafic dikes, outcrop very few meters away; quartz pods 2 and quartz-f e l ds p ar pegmatit e s with go ssanous vugs are also pres en t in the area. The partial corrosion of the granitoids seems to have ta ken plac e in a hyperalk aline environ ment, related to the emplac ement of the carbonatites, under CO 2 saturation. This is a working hypothesis . Silica etching process descr ibed for the Lofdal farm we re observed in ot her locations during the Greater Lufilian Arc granitoid project. Granitoid ?corros i o n? was observ e d in the Kafue Flats area of Zambia . The etched granito i d s in that case are syenite s . Carbona ti t e s have not been reported there, but the host rocks are Katanga n carbona t es . Quar tz pods and small gabbroic bo dies are ubiquitous. Abundant massive iron oxide bodies and evidence of iron oxide-coppe r-gold mineral i z a t i on was observe d in the environ s . 1 Vuggin es s in calcal k a l i n e volcan ic s is a feature comm onl y sought during the explora t i o n of mineral deposit s in high sulfidat i o n environme n t s . ?Sp ong y ? rock and ?vuggy silica ? are terms used to descri be the textur e s of sub- vo l c a n ic and volcan ic rocks that have been etched in highly acid envir onments produced by the oxidation of pyrite. Feldspars and most of the other rock cons ti t u e n ts except for quartz are leac hed . The corros i o n features observed at the Lofdal farm are different. 2 T h e quartz pods are describ e d on the chapter on iron oxide-copper-gold mineralization. 2 3 9 2 4 0 2 4 1 4.2.2.3 . 3.2 Carbonatite dikes and iron oxide-copper-gold mineralization Numerou s mafic dikes and carbo na t i t e s were obser v e d in the easternmost portion of the Lofdal farm (Fig 4.2.2.14). Carbonatites outcropped as both dikes and la rge bodies . Severa l of the carbon a t i t es are associ ated with magnetite and sulfide mineraliz ation. The map of Fig 4.2.2.14 shows the ma in geologic a l stations and sampling sites. Field descriptions are included in Appendix A67.1. Several dike swarms were observ e d and sample d at the Lofdal farm, many of whic h are carbonatitic in composition. All of them have a NE -SW general strike, and roughly sub- ver ti c a l dips . Many of the dikes outcrop for over a hundred meters. Their widths vary wi dely from a few centimeters to over six meters. Some of such dikes might be respons i b l e for iron oxide-c o p per-gold mineralization. A carbon ati t e diatre me was found along strike one of the dikes; and magneti t e- s u lf i d e cement ed , coarse- g r a in e d polymi c t ic breccia s make most of the diatreme. Thes e dikes intersec t a se ries of quartz- f e l ds p a t h ic graniti c gneisse s ( L-742 and other sample s). Carbonatite dikes run sub- parallel to other ma fic and ultramafic dikes swarms. Some compos itions of dikes assoc i a t e d with carbo na t i t e s include: gabbro, alkali gabbro, syenite, alkali granite, phonolite, tinguaite and lamproph yres of variou s types. They extend for dozen s of kilomete r s along strike, as shown on the map by Frets, 1969. Thes e dikes sometim es produce anomal o us radiom e t r ic signat u r e s due to their high thoriu m conten t. According to Niku-Paavola, Siegfried, & Mari ano, 2002, thorium content may reac h up to 14.4% weight percent. An example of the type of features observed is descr ibe d below. Sheeted magnetit e veins in braided patterns with abundant sulfides were identifi e d . One of them is repres en t ed by sample L-738 . A fine-grained, foliated, pink granitoi d was intersec t e d by braided magnetit e + he matite + quartz + sulfide veinlets that vary in width from 1.0 to 0.3 cm. They intersect each other at un iform angles, making a trellis pattern, as shown on Fig 8.58. The vein system is approximately one meter wide. Almost every single one of the veinlets in the vein system contain s gossan ou s vugs with weathe r ed sulfid es. Magnetite in some of the veinlets is partially martitized. The surface expr ession of the vein system is a linear gossan. T he vein system extends for at leas t twenty meters along strike. Many sub-pa rallel vein syste ms occur in the region. The average foliation of the host rock is 130/76? N . The same orienta t i o n and similar features are often seen around this site. Fig 8.58 show two slabs from the sample, to illustrate the textures of mineralization. The rock is very similar to rocks from around the Hook Granite batholith, Zambia and to mineralized stoc kwor ks from the Tevr ede iron oxide- c o pp e r - go l d deposit in Namibia . Fig 4.2.2.16 Photograph of a slabbed carbona tite dike from the Lofdal farm, Namibia . Th e ho s t is a coarse-grained, foliated alkali granite. Note the irregular borders of the dike, with fragments of t h e crystals from the host rock ex tending towards the dike. There are chill margins from the dike into the granitoid. Millimeters for scale. 2 4 2 Fig 4.2.2.17 Photograph of a carbonatite dike with subparallel internal zoning and magnetite . This is one o f t h e iron-rich carbonatite dike s from the L o f dal farm, Namibia. There is abundant sulfidation that accomanies some of the massive iron oxides in the di kes and around th e m. T h e composition of t h e s e dikes is indicated on Table 4.2.2.16. For scal e, card is ten centimeters long . 2 4 3 2 4 4 (Photographs from the previous page) Fig 4.2.2.18 (upper photo) Clos e-up view of a magnetite-rich massive carbonatite body, Lofdal farm, Namibia . Sample L-722 came from this same intrusive bod y . N o t e t h e characteristic carbonate surface dissolution features. The white spots are the remains of HCl t es ts . S o me bo dies like this contain abundant gossans after sulfidation. They are described on t h e field no t e s and located on Fig 4.2. 2 . 1 4 . C hemical analysis of this sample is included on Table 4.2. 2 . 1 6 . Fig 4.2.2.19 (lower photo) Photograph of two subparallel carbonatite dikes. O n e o f t he m was sampled and makes Fig. 4.2.2 . 1 6 . T h e composition of t h e s e dikes is indicated on Table 4.2 . 2 . 1 6 . 4.2.2.3.3.3 Cross Section Thr ough Series of Ultramafic Dikes Many sub- para l l e l mafic and ultr amaf ic dikes were observed in the Lofda l farm. A series of seven sub- para l l el dikes was studie d along a 140 m long transec t that ran perped i c u la r to the main strike of the dikes (Fig 4.2.2.15 and Table 4.2.2.14 ). In othe r locations , dikes are clos er together and very abundan t . See field photos taken towards the west on Fig 4.2.2. 17 and 4.2.2.19 . The location of the ty pic a l cross secti on is indica t ed on Fig 4.2.2.14 . Detailed field descrip t i o ns are included in Appendix A67.1 and Table 4.2.2.14. L-742 is the host rock to the series of dikes studie d. Unfort u n a t e ly , samples L-743 , L-744 , L-745 , L-746 and L-747 were not analysed. These were other dikes, includ in g three carbon a t i te s ( L-743 , L-745 and L-746 ). Dozens of satell i t e dikes run subpar a l l e l to the main ones that were sampled. Fig 4.2.2.15 Cross section through mafic and ultramafic dikes, Lofdal farm, Namibia . This section is located on Fig 4.2.2.14. More description in text. 2 4 5 Table 4.2.2.14 Main features of cross section acr oss mafic, ultramafic and carbonatitic dikes, Lofdal farm, Namibia ( U nd er l i n e d samples were analys e d ) WPT Sample Composition Additional description Orientation Width Iron oxide Other 241 L-740 Peral u m i n o u s sodi c ferri fero us trach y phono l i t e Ver y fine - g r a i n e d , glass y, gra y- r e d d i s h to dark pink- br o wn ; no reactio n to HCl . It has c onch o i d a l fract u r e and sharp ed ges. 056?9 0 ? 1 m w/ diss fine magne t i t e 242 L-741 Metal u m i n o u s pota s s i c ferri fero us trach y phono l i t e Magne t i c , dark gra y to black , subvo l c a n i c . With extrem e l y fine-g r a i n e d matrix , pla gi o c l a s e porph yri e s , open vacuo l e s ; does not react to HCl; chlor i t i z a t i on . Nephe l i n e blade s 2-3mm wide, ra nge to 2cm long. 078?90? 243 Carbon a t i t e Black to dark brown wit h hemat i t i c bandi n g along th e folia t i o n , coars e hemat i t e clust e r s and gossa n o u s textur e. 60?/78 ? S Ver y ab unda n t iron oxides 244 L-742 Metal u m i n o u s sodi c magne s i a n bioti t e grani t e Ver y fine - g r a i n e d , mediu m gra y, folia t e d , with sligh t l y magne t i c chara c t e r . 245 L - 7 4 3 Carbon a t i t e Bro wn, ver y mag net i c , with intern a l flow ban din g . 085/52 ? S 1m abunda n t ea rth y goethit e after sulf i d e s 246 L - 7 4 5 Carbon a t i t e Strong l y ma gnet i c , ver y fine-g ra i n e d , medium gra y ; intern a l flow ban din g ; inters e c t s L-742 . Alter a t i o n halo around dike; sam ple has 2 ?quenc h e d ? ma rgin s . 095/4 9 ? S 4-5 cm none visib l e 247 L - 7 4 6 Carbon a t i t e Weather i n g surfa c e s show clust e r s of iron oxide - r i c h subst a n c e that do not weath er as much. The surfa c e is bro wn/ y e l l o w an d has a ver y irre g u l a r text u r e like lapie z corro s i o n in karst i c envir o n m e n t s . 064/83 ? S abundan t braid e d black magne t i t e bodie s that cont a i n sulf i d e s mini m u n lengt h = 400m 251 Carbona t i t e With abunda n t ir on oxide alter at i o n and red -ro c k alte rat i o n in the host rock s . Subve r t i c a l 25-30 cm 252 L - 7 4 7 Quartz vein With red iron oxide stain s , thin red-f i l l e d joint s , and some blac k -f i l l e d join t s . 050/90? 10-15 cm 4.2.2.3.3.4 Magnetite -Cemented, Polymictic Hydrothermal Breccia that Makes a Diatreme A magneti t e - c e m en t e d diatrem e was disc over ed at the Lofdal farm, along one of main farm roads . It is located on a saddle, as show n on Fig 2.2.2.2 0 , near the easternmos t corner of t he farm (See inset of Fig 4.2.2.14, and 4.2.2.1 3) . The diatrem e seems to have been a bl ow-up of a carbonati t e dike. Massive magnetit e and coar se sulfides cement the polymictic angular fragm ents of the diatreme. Fig 4.2.2.20 is a map of the diatreme . Field descrip tions of geolog ical stations and samplin g sites are include d in Appendix A67.2. The major portion of the diatreme is made by highly magnetic, coarse-grained, polymictic, angu lar hydro t h er m a l brecc ia s with gossan o us surfaces. Many of the clasts display corrosion edges and hydr othermal alterat i o n . The sulfide portion of the matrix was comp letely leached, to a point that no fresh sulfides are pres e n t . Coar s e massi v e , gossan o us magne t i t e was obse rved lying all ar ound over the diatreme. Typical descrip t i o ns and photogr ap h s of rocks from the diatrem e are include d in the chapter on iron oxide-c o pp e r - g o ld mineralization. Two types of rocks were identi f i e d as hosts to the di atreme (Fig 4.2.2.20). The first is a coar se-grain ed , metalumi no us mesocrat ic potassic ferrifer ou s nephel i n e syenit e, represented by L-1027 . It has abundant submill im e t r ic circula r vugs and contain s high K, Zr, Zn and Nb. It produced a 3.58% loss on ignition . The other host rock is a massive, very dark, green to black, foliated, metalumino us mesocratic sodic ferriferous undersaturated olivine ga bbro, represen ted by L-1032 . The average dip of its foliation is 65?SE. The rock has simil ar chemis tr y to L-754 a n d L-1023 . 2 4 6 2 4 7 A mafic dike with peculiar texture was observed on the northw es t e r n portion of the diatreme , as show n by sample L-1025 on Fig 4.2.2.20 (waypo ints W636, W639, and W640 ). It is a subver tical, black, magnetic, metaluminous sodic ferriferous undersaturated olivine gabbro dike, with extremely large radial pyroxene crys ta l s . The rock has a decime t r ic , radial , conic crys ta l st ructu r e . It might indicate paleo-verticality at the time of emplac ement. It trends in a general N-S direction. See photo on Fig 4.2.2.21. The sample has anomalous enric hement in U, Ti, P, Zn and V; very high Sr, Sr and Nb; low Al 2 O 3 , K, Na and Rb. It produced a 7.4% loss on igniti o n . Its copper conten t is also signif i c an t , and it contains 86.4 ppm uranium. The dike is two meters wide at times, but thins; it was followed for at leas t two hundred meters. The chemis tr y of this dike will be discus sed along with carbonatitic dikes in the next few pages. Fig 4.2.2.21 Large fans of elongated amphibole cryst als in an ultramafic dike, Lofdal farm, Namibia . T h e crystals are sometimes up t o t hirty centimeters long. Site of sample L-1025 . Analysis of this sample is included on Table 4.2.2 . 1 6 . S t e e l scratcher is 15 cm long. 4.2.2.3.3.5 Abandoned Lofdal Mine Several samples were collect e d from the abandone d Lofdal mine at UTM 0466547 / 77 55 9 8 0 , (Fig M21). These are numbered L-749 to L-753 . There is very little to see at the mi ne site. The mine exploited subver tical rare earth- b ea r i n g veins and pegmati t es strikin g 075?. Th at orientat i o n is sub-para l le l to most of the dike swarms in the region , as discus se d by Frets, 196 9. Among the abandoned machin er y was a Wilfley table, some crushers , water pumps, stor age equipmen t , as well as drillin g and pumping compres s o r s . Many exploration trenches and pits were found and they fo llow the main strike of the system. Abudant iron oxide and some charcoal lies on the ground around the pits. 2 4 8 4.2.2.3.3.6 Carbonatite Dikes 4.2.2.3.3.6.1 Introduction Maybe the mos t relevant types of ro cks present at the Lofdal farm are its numer ous dikes of mafic , ultr amafic and alkalin e nature. Among the dikes, ca rbonatites constitute a very impo rta n t portion . The dikes have a clear economic relevance, especially becaus e they might c ontain signifi c a n t rare earth element or base metal- precious metal accumula tions. This su b-chapter will discuss some aspects of carbonatit es at the Lofdal farm. M a n y carbona t i t e dikes and intrus iv e bodies were observed and sampled at the farm. Several of the carbona t i t e s are associa te d with magneti t e and sulf ide mineralization. Evident iron oxide-copp er-gold minerali z a t i o n was observed in at leas t two differen t si tes. Fig 8.58 was taken from a mineral iz ed frac tur e system confor me d by interwea v e d qu ar tz-magnetite-sulfide veinlets. Abundant gossans that remain after leachi n g of sulfid e s includ in g chalcop y r it e were sampl ed from each of the differe n t sites. Copper carbona t e and copper sulpha t e stains were observ e d in some case s. Free gold is thought to be present in gossans at most of the mineraliz ed sites. S e v e r a l dike swarms were observ e d and sample d at the Lofdal farm, many of whic h are carbonatitic in composition. All of them have a NE -SW general strike, and roughly sub- ver ti c a l dips . Many of the dikes outcrop for over a hundred meters. Their widths vary wi dely from a few centimeters to over six meters. Some of such dikes might be respons i b l e for iron oxide-c o p per-gold mineralization. A carbon ati t e diatre me was found along strike one of the dikes; and magneti t e- s u lf i d e cement ed , coarse- g r a in e d polymi c t ic breccia s make most of the diatreme. Thes e dikes intersec t a se ries of quartz- f e l ds p a t h ic graniti c gneisse s ( L-742 and other sample s). Carbonatite dikes run sub- parallel to other ma fic and ultramafic dikes swarms. Some compos itions of dikes assoc i a t e d with carbo na t i t e s include: gabbro, alkali gabbro, syenite, alkali granite, phonolite, tinguaite and lamproph yres of variou s types. They extend for dozen s of kilomete r s along strike, as shown on the map by Frets, 1969. Thes e dikes sometim es produce anomal o us radiom e t r ic signat u r e s due to their high thoriu m conten t. According to Niku-Paavola, Siegfried, & Mari ano, 2002, thorium content may reac h up to 14.4% weight percent. 4.2.2.3.3.6.2 Geochemistry Table 4.2.2.16 pres ents chemica l anal ys i s of three carbona t i t e s collec t ed at the Lofdal farm, along with six sample s compiled from reports on carbonatitic dikes in the envir o ns , a single carbon a t i t e from the Hook Granit e bathol i t h , and seven other dikes that are associ ated with carbonatites at t he Lofdal farm. They vary widely in major oxide and trace element compos i t i o n . Fig 4.2.2.2 2 is a logarit h mic plot of the carbonatites for visual compar i s on . Part of the carbon a ti t e s were plot ted on Figs 4.2.2.2, 4.2.2. 4 and 4.2.2.6 along with the rest of the samples for comparis on. Note on 4.2.2. 6 that the carbonat i t e s produce a linear trend. Dike chemis try has a wide range of compositions, as show n on Table 4.2.2.15 and Fig 4.2.2.22. Most of the sample s in the suite have high values for Fe2O3 and MnO, and low Na and K. Carbonatites obviously have high values for CaO. The only common trait between ca rbona t i t es sampled at Lofdal is that they have high CaO and Y content; the rest of the el ements vary widely in a large spec trum of values . Scandium is high, but not in all cases. Many samples from the suite of car bonat i t e s and carbonat i t e dikes from Lofdal are enriched in Cu. Ce and La are enriched in some but not all rocks. In the case of samples labeled LR, the total seems to have been recalc u la t e d to 100% withou t CO2 or water conten t. Maybe the values for major oxides are not read ily compar able to those coming from the rest of the Lofdal region. Anyhow, values for CO2, water and other vo latile s were not reported for the LR or AM sample s. 4.2.2.3.3.6.3 Economic Mineralization in Carbonatite Dikes From the data available, part of the carbon a t i t e dikes are enrich e d in the light rare earths, but there is no information on the heavy rare earth content for six samp les of carbonatite dikes from Lofda l. Evidence cited by Mariano, 2001 for studies of similar dikes from farms Lofda l 491 and Bergvill e 490, indicates that their Tb, Eu, and Dy conten t may be quite high. Based on cathodolo m i n i s c en c e spec t r a , he state s that the type of xenotime found in carbona t i t e vein at the Lofdal farm ?could be a good source material for Y, Tb, Eu and other mid atomic-n u mbe r and heavy lanthani de s ? . Y is anomalou s l y enri ched in all the carbona t i t e s sampled , except for L-411 , as shown on Table 4.2.2.16. Ce and La are enric hed in part of them and in some of the mafic dikes sample d . Mariano, 2001 states that sample AM1 was collec t ed from a ferrugi n o us carbona t i t e . No other elemen t a l data is available. Its high Y value derives from xenotime mineraliz a t i on . Studies done by Mariano on the sample 2 4 9 indicate that it contains ?an appreciab le quantity of Eu?, but the actual figures are not given. AM1 contains at least 2% weight xenotime, and other minerals include: m onazi t e , apatite , parisit e and thorite. Mariano states that xenotime is probably amenable to effective conc ent r a t i o n and separat i o n from other minerals includin g thorite. Accordin g to Mariano , 2001, ?primar y crystal l i z a t i on of xenotim e in a carbona t i t e is rarely encount e r ed , making the Lofda l occurren ce very unusual. The mineral churchite (YPO 4 ? 2H 2 O) whic h occurs in the Mount Weld laterit e of Austral i a is a product of supergen e weather i ng . It is fine-gr a in e d and inextric a b ly associat ed with ferric iron oxides and other deleter io us mineral compone n t s , while the Lofdal xenotime is relative l y coarse and should be amenable to concentr a t i on . ? He states that Eu content in that xenoti m e should be on the weight percent level. In other current deposits, minerals with that element contain less than 0.05 weight percent Eu. 4.2.2.3.3.6.4 High heat production properties in some of the dikes Part of the carbonat i t e and mafic dike s of the Lofdal farm carry high values of thorium, as indicated on Table 4.2.2.15. If th e areal conc en tration of those dikes is high, they may signifi c antly increa se the flow of heat, and power large hydrother m a l fluid flow cells. Table 4.2. 2 . 1 5 shows the heat produ c in g value for dikes in the Lofdal farm at the time of emplacemen t. The heat flow fo r the entire region due to t he presence of these dikes was evident l y high, and that does not take into cons ider a t i on the thermal anomaly produced by doming and rifting. Long-live d flow of hydrother m a l fluids were pr obably an important component of the iron oxide-copper- gold systems observed in the Khorixas Inlier. Thor ium - r ic h dikes may even be bulk-m i ne d for their thor iu m content in areas of high dike conc en tration. Table 4.2.2.15 High heat producing rocks in th e Lofdal farm, Namibia; estimated at 750Ma. Sample Uranium Thorium Potassium Time Heat producing value U/Th (PPM) (PPM) (%) (Ba) (muW -m3) L-1024a 19.00 20.0 0.1 5 0 . 7 5 1 . 9 7 3 0.950 L-1024 c 20.00 18.0 0. 0 4 0 . 7 5 1 . 8 4 9 1.111 L-1025 86.4 19.5 0.5 6 0 . 7 5 4 . 0 1 7 4.423 LR25 24 7730 0.0 1 0 . 7 5 5 3 5 . 0 1 7 0.003 LR23 15 130 0.10 0 . 7 5 9 . 4 5 0 0.115 LR20 0 36 0.04 0. 7 5 2 . 4 9 4 0.000 LR5 26 2347 0.5 3 0 . 7 5 1 6 3 . 0 8 0 0.011 LR4 28 1593 0.0 4 0 . 7 5 1 1 0 . 9 5 3 0.018 AM-1 11 1019 0.7 5 7 0 . 7 7 7 0.011 Fig 4.2.2.22 Major oxide logarithmic plot of carbonatite samples, Lofdal farm, Namibia 0.01 0.10 1.00 10.00 100.00 L- 411 L- 722 L- 10 24a L- 10 24c LR 25 LR 23 LR 20 LR 5 LR 4 SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 2 5 0 Table 4.2.2.16 Chemistry of carbona tites and dikes, Lofdal farm, Namibia (Major oxide values are expres sed in percen tage, va lues for all other elemen t s are in parts per millio n . ) Sample Notch L-411 L-722 L-1024a L-1024c LR25 LR23 LR20 LR5 LR4 AM-1 L-1025 L-740 L-741 L-1023 L-1022 L-1027 SiO2 50.00 8.09 7.50 7.58 5.56 4.673 6 . 1 3 8 2 . 8 7 5 7 . 6 6 6 2 . 1 3 3 4 2 . 0 6 5 6 . 7 4 56.63 47.51 54.76 55 . 0 6 T i O 2 1.00 0.09 0.04 0.07 0. 06 0.29 0. 0 6 0 . 0 2 0 . 3 0 0 . 1 0 1 . 0 6 0 . 2 6 0.47 0.82 0.44 0. 8 1 A l 2 O 3 15.50 0.85 0.13 0.57 0.20 0.34 1. 8 4 0 . 6 0 1 . 3 2 0 . 1 2 1 . 2 6 1 8 . 9 1 19.54 15.70 20.41 1 5 . 7 7 Fe2O3 6.00 0.57 9.55 9.33 9.37 5.85 1 4 . 0 1 2 . 9 1 6 . 1 3 3 . 4 2 1 . 4 2 5 . 9 2 7.23 11.39 5.90 5. 9 1 MnO 0.150 0.02 0.68 0.79 0.84 1.89 0. 4 5 0 . 3 8 2 . 2 4 3 . 1 2 0 . 7 7 0 . 1 8 0.44 0.21 0.20 0. 2 7 MgO 2.00 4.72 2.58 5.76 6.08 0.76 3 0 . 5 3 3 . 1 3 . 8 9 1 . 6 1 2 . 7 6 0 . 2 1 0.80 7.63 0.33 2. 3 2 CaO 5.00 43.80 43.77 37.24 39.51 70.8 4 0 . 6 4 5 . 0 4 8 . 8 4 8 . 6 1 7 . 4 4 1 . 0 3 3.09 10.97 1.95 3. 6 0 Na2O 4.90 0.04 0.00 0.03 0.01 1.58 2. 4 7 1 . 6 7 1 . 5 1 1 . 7 1 1 . 6 1 6 . 2 9 4.14 2.78 4.97 4. 3 8 K 2 O 5.50 0.35 0.00 0.15 0.04 0. 01 0. 1 0 0 . 0 4 0 . 5 3 0 . 0 4 0 . 5 6 4 . 6 8 7.21 0.87 7.25 6. 8 8 P 2 O 5 0.30 0.16 0.03 0.23 0.23 5.82 0. 1 8 0 . 1 5 8 . 0 9 0 . 6 6 3 . 8 5 0 . 0 3 0.11 0.09 0.13 0. 2 3 L O I 2.00 41.87 36.24 38.75 38.66 7.40 6. 2 6 0.91 2.31 2.78 3. 5 8 T o t a l 100.56 100.52 100.50 100.56 100.19 10 0 . 5 1 100.57 100.28 99.12 98 . 8 1 Rb 200 6 7 6 10 1 6 0 19 0 30 170 169 19 189 177 Sr 400 87 210 335 325 6765 941 1166 1669 1054 1839 1546 442 548 177 616 429 Y 60 4 260 62 92 12358 2633 152 4033 2761 8630 50 26 49 23 24 37 Zr 360 17 119 9 18 65 327 97 130 44 1312 1803 640 45 767 621 Nb 40 3.0 13.0 44.1 31.0 128 152 22 181 598 1 4 2 5 . 4 5 6 3 . 0 337.0 5.0 249.0 2 2 0 . 0 Co 30 <6 23 28 29 167 71 16 90 44 42 <6 <6 51 7 14 Ni 16 <6 <6 21 11 58 53 44 46 21 10 11 <6 86 <6 42 Cu 25 <6 5 177 116 166 41 31 89 0 29 8 14 11 11 25 Zn 85 16 37 59 29 899 53 79 45 99 207 189 164 157 171 134 Ga 26 <9 <9 <9 <9 0 0 0 0 -5 12 42 34 19 36 24 V 100 <12 194 23 24 191 62 115 36 0 334 <12 14 246 14 45 Cr 100 <12 12 <12 <12 50 86 85 114 0 106 27 18 354 <12 174 Ba 1300 23 145 115 99 469 25 32 393 0 114 214 617 1955 223 629 1043 U 20 <6 6.00 19.00 20.00 24 15 0 26 28 11 8 6 . 4 27.00 19.00 <6 8.00 <6 Th 37 <15 27.0 20.0 18.0 7730 130 36 2347 1593 1019 19.5 18.0 <15 <15 <15 <15 S c 20 45 54 49 49 7 19 0 0 0 33 <10 <10 42 <10 <10 Pb 20 2.4 0 71 10 91 438 3 3 0 4 . 8 Sm 50 17.16 50.29 673 0 0 65 5 0 2 7 . 7 8. 7 5 0 14.68 2.638 Nd 50 543.29 1335 0 0 1734 2003 748 183 22.20 51.69 27.54 58 . 3 5 Pr 15 15.61 178.89 0 88 0 486 0 4 7 . 1 7 1 . 8 8 210.8 47.69 1 3 6 . 1 Ce 175 12 10 2058 1786 3341 0 0 4909 6950 1726 396 112 248 33 61 239 La 95 <12 <12 1583 1383 2342 32 37 3846 5436 1061 176 36 131 20 19 72 Cs 3 0.06 0 0 25 18 3 0. 39 Hf 10 0.11 8 13 0 7 7 1 0 . 1 Ta 120 229.3 n.d. 35 449 42 75 2 1 9 9 3 3 . 6 1 1 4 . 8 127.0 94.38 94 . 2 5 As 100 0 0 24 6 49 93 78 Se 0 Eu 4 7.27 8.30 0.5 0 0 1.813 0.375 1. 6 6 3 G d 30 28.38 21.9 Tb 5 3.20 2.59 Dy 20 14.82 13.0 Ho 3 2.54 2.12 Er 9 6.75 5.37 Tm 35.5 1.02 0.85 Yb 7.5 0.263 7.22 7.25 0.1 3 8 1.863 1.063 Lu 1.6 0.863 1.10 1. 48 0.83 8 1.100 0.763 0.8 3 8 Be 0 0 0 0 0 Mo 75 5 2 21 74 Sn 27 0 0 0 12 Sb 3 0 0 73 0 W 368 109 14 124 137 183 Source of samples: L-411 : Hook Gra ni t e batho l i t h , Za mbi a , this docum e n t . L-722 , L-740, L-741 , L-1022 , L-1023 , L-1024a , L-1024c , L-1025 , L-1027 : Lof da l far m , Namib i a , this docum e n t . LR4 , LR5 , LR20 , LR23 , LR25 : Lof da l and Bergv i l l e farms , Nami b i a , (Niku - P a a v o l a et al., 2002) . AM-1 , Lofd al far m , Namib i a , Types of samples: L-740 , L-741 , L-1022 , L-1023 , L-1025 , L-1027 : mafi c and ultr a m a f i c dike s . AM-1 , L-411 , L-722 , L-1024a , L-1024c , LR4 , LR5, LR20, LR23 , LR25 : carbo n a t i t e s . 4.2.2.3.4 Environment of Emplacement All rocks from the Lofda l farm that were analys ed display anorogenic charac ter 3 . Several of the methods to evaluate environment of emplacemen t indicate within-plate origin for them (Table 4.2.2.2). From the evidence available, the basement granites, the undersaturated o livine gabbros that host a carbonatitic diatreme , and 3 W ha l e n ?s analy s i s for sampl e s L-1023 , L ?1032 and L-754 is not valid, because the proc edur e was designe d for granitoi d rocks 2 5 1 the numerous carbonatitic, midalkaline, alkaline and ultr amafic rocks from Lofdal formed in a continen tal epeirogenic uplift environment followed by incipien t rifting proc es s e s . Multip le recycl i n g of contin e n t a l crus t with mantle input has pr obably taken place during the Proteroz oic. 4.2.2.3.5 Geochronology A single sample was dated from the Lofdal farm during this project . Zircons from sample L-728 were dated using the U-Pb SHRIMP II method at the ANU, to pr oduce an preliminary age of 1750?5 Ma. Complete geochron o lo gi c a l data is not availabl e at the time of wr iting this document. Fig A38 is an event diagram with all radiomet r ic ages availabl e from the Khorixas Inlier. L-728 is part of the Base Granite B of Tables 4.2.2.7 ad 4.2.2.9 . It was collecte d in the easte r n mo s t portio n of the Lofdal farm, from a fine-grained, banded, dark pi nk to red-brown, fine-grained, metaluminous, subleuc oc r a t ic sodic ferrifer o us granite . Similar foliated granites host most of the younger intr usi v es and part of the mineralization at the Lofdal farm. L-742 , that hosts the carbonatite dikes at the site of the transect has almost the same chemis t r y as L-728 . L-738 illustrated on Fig 8.58 has the same physical features of L-728 and is located approximately 70 meters away from it. 4.2.2.3.6 Conclusions Alkaline and midalkal i n e rocks predomin a t e in the Lofdal farm. They intruded a series of ~1750 Ma foliated granites. A carbonatite diatreme in truded foliated ultr amafic rocks and nephel ine syenites. All of these rocks were emplaced in anorogen i c continen t a l extension a l environme n ts N70?E-t r en d in g dike swar ms were presen t in most of the Lofdal farm. Many dikes of widely varying composit i on s were found during fieldw or k . Some of them are carbonatitic , ultramafic, peralkaline and lamprophyric. It is extremely difficult to id entify the vari ous litholog i es and their associat e d minerals in the field. The effects of severe etching proc es s e s in granito id s by carbona t i t i c corrosio n were seen throu gh o u t the Lofdal farm. Zinc enric hement in many syenites, potential IOCG mine ra l iz a tio n associa t ed with carbon a t i t e s and at least one diatreme, as well as rare earth mineraliz a t i on as soci a t e d to alkalin e dikes and carbon a t i t e s are the economic mineral iz a t i on observe d . 2 5 3 4.2.3 OTHER SMALL OUTCROPS IN NAMIBIA AND BOTSWANA 4.2.3.1 INTRODUCTION 4.2.3.2 MESOPOTAMIE FARM, NAMIBIA 4.2.3.2.1 Introduction The Mesopota m i e 504 farm is located W of the Lofda l farm . It lies outside of the Khorixas Inlier, in a separate, fault-b o un d block (Fig M20). Various ty pes of granite s , includ i n g granit es wi th graph i c textur e s occur at the farm and seem to be respons ib l e for copper mineral iz a t i o n in the Copper Vallei deposit . Part of the granite s has been metamor p h os ed into gneisses . Most of the granito i d s intr ude a series of metapel i t i c (or metavolcan ic?) schistose rocks; in a few cases, the basement was made of gneissose granitoids. Mineralization observed at the Mesopo ta m i e farm conforms to the models of iron oxide-copper-gold deposits. A geologic a l model, with maps and samples of the mineral i z e d rocks is herein pres en te d . Five repr es en t a t i v e samples were analyz ed and they are listed on Table 4. 2.3.1. Chemistry of these rocks was plotted on Figs 4.2.3.1 and 4.2.3.2. As seen, all ar e granites. Several quartz pods were also mapped in the field. Sampling stations and sites of other geolog i c a l obs ervations are located on Fig 4.2.3.3. Table 4.2.3.1 Chemical analysis of sam ples from the Mesopotamie farm, Namibia ( c omp l e t e elementa l analys is can be found on Table A12, Appendix ) Sam ple SiO 2 T iO 2 Al2O 3 Fe2O 3 MnO MgO CaO Na2O K2O P2O 5 LO I T otal Rb Sr Y Zr Nb Co Ni Cu Z n Ga V Cr Ba U T h Sc Sm Nd Pr Ce La T a Eu Yb Notc h 50.0 0 1.00 15.5 0 6.00 0.15 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 50 50 15 175 95 120 4 8 L- 759 74.0 6 0.03 14.4 7 0.47 0.04 0.02 0.70 3.55 5.54 0.06 0.94 99.8 8 109 124 20 16 7 <6 <6 <6 12 13 <12 185 649 <6 <15 <10 12 <12 L-772 72.5 5 0.03 14.2 9 0.43 0.03 0.03 0.05 2.34 10.0 7 0.02 0.67 100. 51 201 100 7 <8 4 <6 <6 8 28 13 <12 44 579 <6 <15 <10 21 <12 L-773 74.8 3 0.06 14.9 8 0.87 0.02 0.11 0.80 5.35 3.07 0.04 0.41 100. 54 76 71 103 64 14 <6 10 8 43 20 <12 47 176 <6 <15 <10 25 <12 L-783 71.8 6 0.45 13.9 6 3.32 0.08 0.50 0.78 3.49 5.15 0.18 0.71 100. 48 223 85 54 273 22 <6 6 9 49 17 25 239 859 <6 27 <10 161 75 L- 784 71.8 3 0.39 13.2 3 3.59 0.06 0.56 1.31 3.67 5.07 0.09 0.70 100. 50 193 105 58 312 23 <6 7 7 59 17 23 63 1049 7 26 <10 11 37 99 155 51 42 1 4 There is possible IOCG mineraliz ation at Mesopotamie 504. Thes e mineraliz ations are as sociated to major E- W-tr e n d in g fractur e zones (Fig M20) and contain coppe r sulfides that surroun d masses of magneti t e and/or hematite. L-783 and L-784 were collect e d from the basemen t roc ks at Mesopot a m i e . They host mineral i z a t i o n and are cut by the other intrus ives . 4.2.3.2.2 Sampling and Geochemistry All geolog ical stations from the Mesopo tamie farm are located on the map of Fig 4.2.3.4. Field descriptions were updated with geochemi c a l and geochr ono l o g ic a l informat i on, and are included in Appendix A68. Samples collected from the Mesopo tamie farm can be grouped in four units as follows: A, L-758 a n d L-759 from a white granite with graphic textur e; B, L-772 from a light gray to white graphic alkali granite vein; C, L- 773 from a coarse-grained pegmatitic granitoid; and D, L-779 , L-783 a n d L-784 from an augen granite gneiss that probably makes the regional basement and could be the protolith to the granitods L-758 a nd L-759 . Chemic a l data shows that L-783 and L-784 are almost identical; these are roughly similar to L-758 a n d L-773 . L-772 is very differ e n t in all aspects from the other samp les. It is highly enric he d in K2O and depleted in CaO. The series of schists observ e d in variou s outcro ps through ou t the farm were probabl y formed as volcani c rocks at the same time as Unit D . Unit B is similar to L-713 a n d L-1019 from the Oas farm. The major oxide chemist r y of units C a n d D has similarities with samples from the Lofdal farm ( L-728 , L-729 an d L-1021 ) and the Oas farm ( L-715 a nd L- 716 *) . Fig 4.2.3.2 show s this on the R1/R 2 diagram . Thus the Mesopo t a m i e farm confor ms a series of rocks similar to those of the Oas and Lofdal farms. That ma kes sens e, since the three farms line in the Khorix a s inlier. 4.2.3.2.3 Environment of Emplacement All granitoids sampled at the Mesopotamie farm have an anorog e n ic origin. No signif ic a n t result s were obtained from the various methodo l ogie s to eval ua te environ ment of emplacement, except for L-773 and L- 784 . Both of them fall in the ?within-plate? category of Pearce et al, 1984. L-783 a n d L-784 come from the same basic rock unit. L-772 is an alkali granite and probabl y was formed as a rift-rel a t ed granito i d . The origin 6 5 7 0 7 5 O2% 7 8 9 1 0 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM Ugab River-Okwa River-Summas Mts.- Grootfontein-Felsic Volcanics, Namibia; Lufilian G.P. (Based on Middlemost, 1994, 1997) S a m pl e s Pe tr o gr a ph ic fie ld s L-793 L-797 L-798 L-799 L-802 L-600A L-602 L-605 L-606 L-789 L-791a L-791b L-1014 L-1042 L-1043 L-1044 L-1045 L-1046 X-16 X-17 X-18 X-19 X-20 II III Fig 4.2.3.1 Fig 4.2.3.1 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 = 4Si - 11(Na+K) -2(Fe+Ti) 5 0 0 X-16 X-17 X-18 X-19 X-20 L-793 L-797 L-798 L-799 L-802 L-600A L-602 L-605 L-606 L-789 L-791a L-791b L-1014 L-1042 L-1043 L-1044 L-1045 L-1046 R1R2 PLUTONIC ROCK CLASSIFICATION Ugab River-Okwa River-Summas Mountains- Grootfontein-Felsic Volcanics, Namibia; Lufilian G.P. (After De la Roche et al, 1980) Petrographic fields Sa mpl es II III Fig 4.2.3.2 Fig 4.2.3.2 2 5 7 2 5 8 of L-759 cannot be defined any further. Thus, probable environm ent s of emplac e m en t for the four rock units is as follows: B , C and D formed in rift-related environments ; A formed in an undetermined anorogenic environment. 2 5 9 4.2.3.2.4 Geochronology In principle, the only chrono logical relationships that can be established are that unit B intersec ts unit C , that units A and C inters ec t unit D . Other relatio n s h ip s between A and B , and A and C are uncer ta i n . As indicate d on Table A22.16, zircon conc en tr a t es from L-758 were dated to give an age of 750?5 Ma. Inherite d zircons in the sample gave an age of 1692?10 Ma. The sample was collec t ed from the NW corner of the farm, as seen on Figs 4.2.3.3. Since L-758 an d L-759 were taken from the same granitic body (unit A ) , we can assume that age and chemis try of both samples is the same. L-779 , L-783 a n d L-784 correlate well with sample s from other suites macros copically, micros copi cally and chemically (high Pr, Th and Rb). They behave as basement for the other intrusive rocks in the Mesopotamie farm. We w ill thus assign a temporary age of 1690 Ma to these rocks. Their striki ng similar i t i es allow us to give such an age to those rocks of group D . For the time being , groups B and C have not been dated in any way. 4.2.3.2.5 Economic Geology There are three distinct mineraliz ed areas at the Mesopotamie 504 farm. A ll have some char ac t e r is t i c s of iron oxide-copper-gold d eposits. These will be de scribed in chapter 8. Iron oxide-copper-gold mineralization at the Copper Valley deposit could have been produced by unit A or by a later mineral iz i ng event. 2 6 0 4.2.3.3 SUMMAS MOUNTAINS, NAMIBIA 4.2.3.3.1 Sampling and Geochemistry Some sample s were collected in the northern port ion of the Summas Mountain s, as illustrated on the map of Fig M22. Their chemistry is listed on Table 4.2.3.2 and is plotted on Figs 4.2.3.1 and 4.2.3.2. See location of samplin g sites on M22. Chemistr y of the dated volc anic rocks is not supplied by them. These rocks were probably emplaced in a rift-rela ted environment. Accordin g to Roy Miller, the rocks that make the Mitten Fold and all three of the outcrop s are made of the same grani toid rocks, but they are increasing ly sheared towards the south, to the point where they s eem to be a volcanic rock. All three have similar compositions (Miller, R., persona l communic a t i o ns , 2003). Table 4.2.3.2 Chemical analysis of samples from the Summas Mountains, Namibia (complete analysis of all elements on Table A12, Appendix) Sample SiO2 TiO2 Al2O3 Fe2O3 MnO MgO CaO Na2O K2O P2O5 LOI Total Na+K Notch 5 0 . 0 0 1 . 0 0 15.50 6.00 0.1 5 0 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2.00 L-789 6 3 . 9 1 1 . 3 8 14.35 7.45 0.0 7 1 . 1 3 1 . 0 9 4 . 8 7 5 . 2 1 0 . 4 1 0.55 100.42 10.08 L-791a 7 2 . 4 4 0 . 4 0 13.01 3.67 0.0 6 0 . 3 2 0 . 5 4 3 . 8 0 5 . 1 6 0 . 1 0 0.61 100.11 8.96 L-791b 7 6 . 3 8 0 . 1 4 12.55 1.25 0.0 2 0 . 0 0 0 . 5 1 3 . 0 9 5 . 8 5 0 . 0 3 0.29 100.11 8.94 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Sm Nd Pr Ce La Hf Ta Eu Yb Lu Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 50 50 15 175 95 10 120 4 7.5 1.6 L-789 125 29 66 715 149 <6 6 10 80 21 32 135 1019 8 15 <10 15 50 136 196 67 128 2.03 3.8 8 1 . 5 8 L-791a 141 25 97 685 130 <6 7 <6 35 17 <12 220 637 6 32 <10 109 23 37 63 18 2 7 0.438 5.688 1.400 L-791b 270 74 83 70 65 <6 10 <6 15 22 16 234 332 8 17 <10 224 108 Major WNW-ESE-, ENE-WSW-, and N-S? trending structures cut the rock s around the Summas Mountains and were unconfor m ab l y overlai n by Damara sedimen t a r y sequenc es includ i n g base conglom er a t es and turbiditic sequences. Several geochemical featur es of the three volcan ic rocks from the Summas Mountai ns include high Y, Nb and Cr, low Ca, and low metallic content. Table 4.2.3.3 Rock types and environment of emplacement for the Summas Mountains, Namibia ( S e e acrony m descrip t i o n on sectio n 2.4.3. ) Sample Rock Name Debon & LeFort Maniar & Piccoli Whalen Pearce Rb/10HfTa Rb/30HfTa Nb-Ta L-789 q u a r t z s yenit e metalu m i iv meso NaFe RRG-CE U G A O-W 2-2 OUT U L-791a a l k a l i grani t e peral u m ii leuco KFe RRG-C E U G A W3/4 WP- WP INW L-791b a l k a l i grani t e peral u m iv meso Na-KF e W The followin g is a direct transcri p t i on from the field notebook . L-786 , taken on WPT 342 at 967 m. Slightly foliated, light brown, very glass-rich, tr anslu c en t volcan i c rock. The foliation may be syn-sedimentary bedding . Fres h sample s are hard to find. Some vacuoles and porph yritic crystals are still present in the rock. Foliation plane is 100/45? N. L-787 Vugs with sulfides and gossanous textur es in volc anic rocks. Try to identify what the sulfides were using the methods of Blanchard, 1967. L-788 Another aspect of the volcanics, that are slightly foliated and contain goethite in vugs after sulfides . WPT 343 at 994 m. L-789 : Slightly magnetic, subvolcanic metaluminous sodic ferriferous quartz trac hyte with white porphyritic plagioc lase and open vacuoles .This rock formed in a rift-related environment. L-792 from WPT 343, Magnetic subvolcanic rock with compressional foliation. L-790 Fine-grained medium brown to r ed crystalline rock. Simila r to the ma trix of L-789 with specks of chalcopy r i t e and gossanou s spec ks. No crys tals or macroc ry s t a ls . WPT 344, 1028 m. L-791a : Finely laminated, pink/red fine-grained vo lcaniclastic, vitreous peraluminous leucocratic potassic ferrifer ous alkali rhyoliti c ash with conc hoida l fracture . Laminati o n = 180/67? W. This tuff formed in a rift-related environment. 2 6 1 L-791b was collecte d from another fine-gr a i ne d , laminate d , pink peralu m i n ous sodic to potass ic ferri f e r o u s alkali rhyolite. WPT 345, 951 m. Some clasts in the river bed c ontain quartz with magnetite/hematite inclus ions. The volcanic rocks oberved in the Summas Mountain s willl be compiled and correlat e d with other suites of Namibian rocks in the next few pages. The amount of sulfidation observed in volcan ic rocks from the Summas Mountains may be indication of economic mineral iz a t i on . Rhyolit i c magmas carry a lot of volatiles and metals , and they tend to be extremely explosive. Many high sulfidation and low sulfidat i on epitherma l systems wi th economic gold mineralization are hosted in rhyolitic tuffs. Other metals like tin, silv er and molybdenum might be pres ent too. None of the sample s from the Summas Mountains was assayed. 4.2.3.3.2 Geochronology Hoffmann, Hawkings , Isachsen , & Bowring, 1996 dated two volc an ic rocks in the Summas Mountains . They were given a U-Pb zircon age of 746? 2 and 747? 2 Ma (Table A22.16 ) . Their ages are within error of each other. As seen on Fig A38 they form part of magmatic and volc anic activity associated to the emplac ement of the Oas ring comple x clus te r . 2 6 2 4.2.3.4 UGAB RIVER OUTCROPS, NAMIBIA A well exposed series of granitoid s outcrops along two different intersection s of the Ugab River with main roads. Thes e are located south of the Khorixas Inlier, as shown on Fig M22. Field obser v a t i o ns are includ ed in Appendi x A69; a few photogr ap hs and diagrams are also include d there. 4.2.3.4.1 Sampling and Geochemistry Geolog i c a l stati o n s and sampl i n g sites are show n on Fi g M22. Only the sample s with a box were analysed, and their chemic a l analys is are listed on Table 4.2.3. 4 . As seen on Table 4.2.3.4 , most samples from the Ugab River contain high values of Rb, Nb, Cr, Sm, Nd, Pr, Ce and La. L-793 a n d L-797 contain high Th values; they are high heat producing gr anitoids, as shown on Table 5.4. Additional comments on geochemis try of the Ugab River and other sampling areas in Namibia with similar characteristics will be presented in the review of this chapter. Rocks with enrichment in Cr and Rb are not very common in nature. Only a handful of samples from the Greater Lufilian Arc geoche mical databa se have similar major oxide values to sample s from the Ugab River and are enriched in Cr and Rb. Thes e include: L-602 from the Okwa River in Botswana, L-754 from the Lofdal farm, L-783 f r o m the Mesopota m i e farm, L-791 from the Summas Mountain s , L-906 from the Kamanjab batholith, and L-1037 from the Otjiwaron g o envir ons . These rocks were found to be related , as indicat ed on Table 4.2.3.18 . Table 4.2.3.4 Chemical An alysis, Ugab River, Namibia (complete elemental analys is on Table A12 in the Appendix) Sampl e SiO2 TiO2 Al2O3 Fe2O 3 MnO MgO CaO Na2O K2O P2O5 LOI Total Na+K Notch 50.00 1.00 15.50 6.00 0.1 5 0 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2.00 L-793 74.92 0.33 12.39 2.15 0.0 8 0 . 2 4 1 . 0 0 3 . 2 8 5 . 2 4 0 . 1 4 0.37 100.14 8.52 L-7 9 7 75.11 0.21 13.05 1.92 0.0 4 0 . 0 8 0 . 5 1 3 . 6 2 4 . 6 3 0 . 0 8 0.61 99.86 8.25 L-7 9 8 72.64 0.26 14.07 2.13 0.0 8 0 . 2 6 1 . 0 9 3 . 4 2 5 . 1 7 0 . 1 2 0.91 100.15 8.59 L-7 9 9 73.13 0.08 13.93 1.96 0.0 6 0 . 0 4 0 . 9 5 3 . 8 4 4 . 8 4 0 . 1 3 0.63 99.59 8.68 L-8 0 2 73.34 0.23 14.56 1.83 0.0 5 0 . 2 9 1 . 0 8 3 . 4 6 4 . 5 5 0 . 1 3 0.84 100.36 8.01 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Sm Nd Pr Ce La Hf Ta Eu Yb Lu Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 50 50 15 175 95 10 120 4 7.5 1.6 L-793 251 140 81 213 78 <6 7 7 34 19 22 390 435 12 61 <10 119 51 175 234 98 1.8 28 0.938 6. 6 1 . 7 L-797 225 107 23 199 38 <6 6 <6 33 21 17 372 658 6 37 <10 132 76 L-798 222 204 26 229 48 <6 <6 <6 40 20 16 285 1117 7 27 <10 211 102 L-799 153 168 53 183 14 <6 7 11 19 18 29 326 727 7 <15 <10 102 36 L-802 234 141 32 142 41 <6 6 <6 51 19 22 260 745 <6 15 <10 77 38 Although only sample L-793 was analyse d for Pr in the Ugab River suit e, its values are significantly higher than the notch. The Pr enric hment is also known to many Namibia n samples , includin g most from the Summas Mountains , Mesopotamie farm, Oas farm, Lofdal farm, Grootfontein, Okajepuiko and Okwa River. In general, Zambian rocks do not display such high Pr values . Table 4.2.3.5 Rock types and environment of emplacement for the Ugab River, Namibia ( S e e acrony m descrip t i o n on sectio n 2.4.3. ) Sample Rock Name Debon & LeFort Maniar & Piccoli Whalen Pearce Rb/10HfTa Rb/30HfTa Nb-Ta L - 7 9 3 Granit e metaiv leuco Na Fe POG A W3/4 WP- WP OUT U L-7 9 5 * granite L-796* granite L-797 granite peraii leuco Na-K Fe RRG-C E U G A L-798 granite peraii leuco Na-K Fe POG A L-799 granit e peraii leuco Na-K Fe A L-802 granit e peraii leuco Na-K Fe N The suite of sample s from the Okwa River is very sim ilar to that of the Ugab River (See Table 4.2.13). The same anomaly of Th, Cr, Rb and rare earths is present. When suites I and II of Table 4.2.3.18 are plotted on the TAS diagram (Fig 4.2.3.1), they are very clos e; bu t when plotted on the R1R2 diagram (Fig 4.2.3.2), they make two separate clus ters. L-606 and L-798 are extremely similar. They plot almost on top of each other. 2 6 3 T h e s e two suites of rocks are very close. Based on geoc hem ic a l similar i t i e s , one can confidently state that the two domains may be linked together as a single entity. It is very improba b le that two di fferent suites of rocks, carrying the same major oxide and trac e element signatu r e s occur in two di ffere n t sites and not be related . They probably formed in the same environ me n t and from the same source rocks. That does not mean that they have the same age, but the possibility is large. Appendix A69 contains a transcription of all observati o n s , geolog ic a l statio n s and samplin g carrie d out at the Ugab River outcro ps . Notes were update d with chem ic a l analysi s and geochron o l og ic a l informa t io n . Coor dina t e s of stations and sample s are listed on Appendix A18. Table 4.2.3.18 compile s the suites of igneous rocks fr om the Ugab River, Okwa River and Summas Mountains with some from Otjiwar ongo and Gr ootfontein to evaluat e their chemical similarities and establish possible correlations . 4.2.3.4.2 Geochronology Zircons from two samples of that Ugab River suite ( L-795* and L-796* ) were approximately dated by U-Pb zircon SHRIMP II at the ANU (Table A22.16) Final result s are not available at the time of editing this document. L-795* , a gray, coarse, porphyritic granite with abundant biotite and magnetite clusters, gave an age of ~540 Ma; it also contain e d xenoc rys t i c zircons with ages around 1200 Ma. L-796* , a pink granite with red quartz clusters, zoned red plagioc l as e and no magneti t e , gave an age of ~750 Ma. That age came as a surprise, for the gray, foliated, porphyritic rock seemed to be older. There might be two generations of gray granit e s at the Ugab River outcrop s . Additional comments on geochronolog y of the Ugab Rive r and other sampli ng areas will be presen t e d in the review of this chapter. 2 6 4 4.2.3.5 OKWA RIVER OUTCROPS, BOTSWANA One of the few outcro ps of pre-Ka t an g an granit o id s in Bo tswana is located along the intersection of the main Trans-Ka l a har i road with the Okwa River. Sharad Master from the University of the Witwate r s r an d suggest e d visitin g that outcrop (Maste r , S., persona l communi cation, 2002). It is a reasonably well-exposed pavement outcrop; topography is almost flat, the river bed ha s very bad definiti o n , and no river banks are visibl e . According to Singletary et al., 1998, the Okwa River out crops of granit e and orthog ne i s s in the Qwangw ad u m Valley have given K-Ar ages of approximately 650-500 Ma. ?Pb/Pb ages for discord a n t zircons from the gneiss suggest a crystal l iz a t i o n age of approxi ma t e l y 2. 07 Ga and WR eNd(t) and T(DM) of -3.5 and 2.65 Ga, respec ti v e l y ? . Their data indicate s that reworked Arch ean crus t of Eburnian age is presen t in northwes t e r n Botswan a . They sugges t that the Okwa River gneiss re pres en t s baseme n t inlier s like those of the Damara belt to the southwest in Namibia and the Lufilian Arc to the northeast in Zambia. Geophysical evidence and regiona l struct u r a l trends that are know n beneat h the Kalaha r i semi-d es er t are consis t e nt with that model (Singletar y et al., 1998). Seven sample s were collect e d in the field, and four we re analysed. Their chemistry is listed on table 4.2.3.6 plotted on Figs 4.2.3.1 and 4.2.3.2. A transcrip t i on of the field notes ta ken on the outcrops is include d in the Appendix , as well as coordina t es of all samples collect ed . Their environ m e n t of emplac e me n t and geoch e m ic a l char ac t e r is t i c s ar e listed on Table 4.2.3.7. Table 4.2.3.6 Chemical An alysis, Okwa River, Botswana (complete elemental analys is on Table A12 in the Appendix) Sampl e SiO2 TiO2 Al2O3 Fe2O 3 MnO MgO CaO Na2O K2O P2O5 LOI Total Na+K Notch 50.00 1.00 15.50 6.00 0.1 5 0 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2.00 L-600A 76.09 0.13 11.83 1.93 0.0 4 0 . 0 7 0 . 4 5 3 . 8 5 5 . 5 5 0 . 0 6 0.40 100.40 9 . 4 0 L - 6 0 2 70.15 0.49 13.13 3.63 0.0 6 0 . 8 3 1 . 8 0 3 . 4 3 4 . 5 4 0 . 1 6 0.98 99.20 7. 9 7 L - 6 0 5 76.55 0.12 12.03 1.16 0.0 1 0 . 0 2 0 . 8 1 3 . 4 2 5 . 4 7 0 . 0 7 0.41 100.07 8 . 8 9 L - 6 0 6 72.56 0.36 12.83 3.51 0.0 6 0 . 4 8 1 . 3 2 3 . 2 2 5 . 1 9 0 . 0 7 0.73 100.33 8 . 4 1 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Hf Ta Eu Gd Yb Lu Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 10 120 4 30 8 2 L-600A 160 59 23 137 14 <6 6 14 29 15 <12 68 508 <6 43 <10 141 77 L-602 214 137 64 305 26 8 7 9 60 18 13 189 716 <6 36 <10 14 62 169 213 86 53 1 4 1 L-605 198 99 7 89 7 <6 <6 9 19 13 <12 227 772 <6 42 <10 148 102 L-606 185 105 38 202 17 <6 6 7 61 18 20 57 781 <6 38 <10 227 149 Table 4.2.3.7 Rock types and environment of emplacement for the Okwa River area, Botswana ( S e e acrony m descrip t i o n on sectio n 2.4.3. ) Sample Rock Name Debon & LeFort Maniar & Piccoli Whalen Pearce Nb-Ta L - 6 0 0 A alkal i grani t e metav leuco Na- K F? RRG-C E U G A L-602 granit e metaiv meso Na- K F? A O3/4 OUT U L-605 grani t e metav leuco Na Fe A L-606 granit e metaiv meso Na Fe RRG-CE U G A All rocks collecte d show high thorou m conten t. Two of them contain high chromium. Tentative lithologic and geochemic a l correlat i o ns are shown on Table 4.2.3.18 . 2 6 5 4.2.3.6 GROOTFONTEIN INLIER, NAMIBIA 4.2.3.6.1 Sampling and Geochemistry Outcrops of intrus i v e rocks were found southea s t of the Kombat mining area in the Grootfontein inlier, under sedimen t s of the Otavi sequenc e . Thes e were discove r e d under instruc t i o ns from Geolog i s t Arno Guenzel of Ongopolo Corpor ation (Guenzel, A., personal communica tion, 2003). General location of the outcrops is show n on Fig M25. Seven sample s were collect e d in the field, and five of them were analys ed . In addition to that, Mr Guenzel kindly supplied a series of granitoid samples from boreho les drilled into the basement of the Grootfontein Inlier. He provided approximate coordinates of the drill sites. A composite of those sampes was analys e d . The repres e n t a t i v e sample , L-1014 , is a coarse-grained , peraluminous mesocr a t i c sodic magnes i c biotit e granod i o r i t e . It has a specia l chemica l signatu r e : 1632 PPM Ba, 176 PPM Cr and low Ce, La and Pr. The only sample s with simila r geoche m i c a l featur es are L-985 , L-993 , L-994, L-999 from the Kamanjab batho lith. They are roughly similar in other aspects too, but don?t plot near on TAS or R1R2 diagram s . Chemic a l analysi s of the sample s is listed on Table 4. 2.3.8, Figs 4.2.3.1 and 4. 2.3.2 show their plots on geochem ic a l diagrams . A transcri p t i on of the field notes taken on the outcro ps is includ e d in the Append ix . Their environme n t of emplace me n t and geochem ic a l char ac t e r is t i c s are listed on Table 4.2.3.1 6 . Some Grootfontein sample s are enriched in K2O, Th, Rb, Y and Cu. Table 4.2.3.8 Chemical Analysi s, Grootfontein Inlier, Namibia (complete elemental analys is on Table A13 in the Appendix) Sample SiO2 TiO2 Al2O3 Fe2O3 MnO MgO CaO Na2O K2O P2O5 LOI Total Na+K Notc h 50.00 1.00 15.50 6.00 0.1 5 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2.00 L-1014 68.99 0.40 14.2 3.21 0.0 5 1 . 3 5 2 . 6 1 3 . 0 4 3 . 6 4 0 . 1 1 1.80 99.41 6. 6 8 L - 1 0 4 2 70.57 0.26 14.13 2.58 0.0 6 0 . 4 5 0 . 6 7 2 . 7 9 6 . 1 4 0 . 1 0 1.35 99.10 8. 9 3 L - 1 0 4 3 * 72.42 0.34 13.62 2.40 0.0 4 0 . 5 7 0 . 5 7 2 . 7 6 5 . 7 7 0 . 1 0 1.27 99.86 8. 5 3 L - 1 0 4 4 73.43 0.25 12.72 2.04 0.0 4 0 . 3 9 0 . 4 9 2 . 7 9 5 . 9 4 0 . 1 1 1.10 99.30 8. 7 3 L - 1 0 4 5 65.28 0.40 17.54 2.82 0.0 8 0 . 3 6 3 . 6 0 6 . 6 7 1 . 7 0 0 . 1 1 1.41 99.97 8. 3 7 L - 1 0 4 6 72.78 0.33 12.73 2.40 0.0 3 0 . 5 5 0 . 7 6 2 . 6 1 5 . 4 5 0 . 1 2 1.39 99.15 8. 0 6 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Hf Ta Eu Gd Yb Lu Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 10 120 4 30 8 2 L-1014 59 321 5 43.2 2.5 9 20 13 43 13 60 173 1632 <6 <15 <10 14 2.27 18.6 4.86 64 34 1.0 n.d. 1.76 1.76 0.4 .007 L-1042 317 68 65 161 17 7 12 20 29 14 16 <12 471 <6 35 <10 110 45 79 106 34 4 27 0 1 4 1 L-1043* 276 85 71 207 17 7 9 51 30 14 28 <12 525 <6 44 <10 109 42 89 140 35 2 37 1 9 2 L-1044 293 67 47 166 16 6 9 115 70 12 20 12 415 <6 36 <10 109 44 L-1045 90 471 107 246 24 5 7 48 18 20 24 <12 116 <6 57 12 12 15 48 154 16 298 0 2 2 L-1046 283 61 69 193 16 6 9 30 27 13 25 16 473 <6 42 <10 126 53 Table 4.2.3.16 Rock types and environment of emplacement for the Grootfontein Inlier, Namibia ( S e e acrony m descrip t i o n on sectio n 2.4.3. ) Sample Rock Name Debon & LeFort Maniar & Piccoli Whalen Pearce Rb/10HfTa Rb/30HfTa Nb-Ta L - 1 0 1 4 granod i o r i t e peraii i meso Na Mg IAG_CA G ?N L-1042 granit e peraii subleu c o K Fe POG A WP- WP OUT U L- 1 0 4 3 * granit e peraii subleu c o K Fe POG A O-W 2-2 WP WP OUT U L- 1 0 4 4 granit e peraii leuco K Fe POG A O-W1- 1 L-1045 quart z m o n z o n i t e metav suble u c o Na Fe A W3/4 OUT U L-1 0 4 6 granit e peraii subleu c o K Fe POG A O-W1- 1 4.2.3.6.2 Geochronology Zircons concen t r a t e d from a single sample of the Groo tfontein Inlier were dated by laser ablation ICPMS at the Memoria l Univers i t y in Newfound l a n d , Canada. L-1043* , a fine, felsic, porph yritic, almost un-folia ted, peraluminous, subleucocratic potassic ferriferous biotite granite gave a U-Pb age of 1939?64 Ma, with xenocrystic zircon s that dated 2544?78 Ma. Geochronological data for this sample was extremely complex to interpret, and further work may end up refining the age s (Table 4.2.1.15 ) . The relevanc e of this age will be discus sed in the next few pages. 2 6 6 4.2.3.7 ENVIRONS OF OTJIWARONGO, NAMIBIA 4.2.3.7.1 Introduction Very little outcrop of intrusive rocks is to be found in the environs of Otjiwaro n g o , Namibia (Figs M23 and M24). Most of the rocks are covered by carbonates, Kal ahari sand and calcrete. The presence of a significant batholith (appr oximately as large as the Kamanjab batho lith) under cover northeast of the town of Otjiwarongo is a fact known by a few geologists . Geophysicist Br anko Corner first detected the body of batholithic dimens io ns for AngloVaa l Namibia (Lombard , A., personal communication, 2003). The Otjikoto gold depos it is thought to have been produced by that plutoni c body. This chapter reviews samples from the environ s of Otjiwar o n go , and describ e s pegmati t i c apophy s es of the Otjiwa r o n go bat holit h . A single sample from Otjiwarongo pegmatites was dated . Geolog ists from AVMIN in Windhoek spent months looking for outcrops of intr usive rocks in that part of the world. They provided locations of their outcro ps and comple t e chemic a l analys i s of 18 such rocks and some petrogr ap h ic al details (Wilton , J, 2003, persona l communi c a t i o n) . These are labeled with the ?LL-? and ?LJ-? prefix on Table 4.2.3.1 0 . Seven samples were collect ed and analys ed from pegmat i t i c rocks that were cons ide r ed by geolog is t s from AVMIN Namibia to be pa rt of the Otjiwar ongo batholith (L-808 to L-815) (Lombard, A., 2003, personal communication). Six rock sample s collecte d in the field were added to AVMIN?s sample s to compos e the Otjiwar o n go suite, a database of 31 rock samples (Table 4.2.3. 1 0) . Figs 4.2.3.6 and 4.2.3.7 has them plotted on the R1/R2 diagram a nd Fig 4.2.3.5, on the modified TAS diagram. Rock composi t i on s are again bimodal . Granites dominat e , al thou g h alkali granit e , variou s quartz syenit e s and minor granodior i t e are also present. See T able 4.2.3. 1 3 . LL-9 and L-814 are roc ks of comple x petrol o g y or probab l y hydrothermally altered. 4.2.3.7.2 Field Description of Main Outcrops There are very few outcrop s of granito id s exposed in the environs of Otjiwaron g o . Some of the reason ab l e outcrops are out of bounds, because farm owners have locked their propert i es away from the public . The few outcrops that were visited are described below. The followin g is a transcr ip t i o n of samplin g field notes around Otjiwarongo, modified with laboratory results. Coor di na t e s of samples are in Append i x D. L-850 was sampled from a large outcrop along the main road from Okahand j a to Otjiwar ong o , 10 km before Otjiwarongo. Photo 4.2.3.8 ta ken towards the SE shows th e place where the sample was collected (hill on the left). See also Figs M23 and M24. The rock is a fresh, fine-gr ain e d , homogen e ou s , gray, peralum in ou s subleuc oc r a t ic ferrif er o us biotit e micro-g r a n i t e with occasiona l xenoliths of dark green amphyb o l i t e . The sample does not correlate well with any of the rest of rocks collected in the environs of Otjiwarongo. It probably formed in an anorogenic rift environmen t. Fig 4.2.3.8 Photograph of granitoid inselberg s on the road Okahandja-Otjiwarongo, Namibia . Sample L-850 was collected from the hill on the left of the im age. The o n e o n t h e back was observed bu t n o t sampled. This is the typical type of granitoid outcrop in most of Na mibia. Very few of them ar e present in the environs of Otjiwarongo. It is not clear if these granitoids intersect the Damaran s iliciclastic and ca lcareous rocks. An elongat ed whaleba c k ridge granit o i d outcrop locate d ju st north of Otjiwa r o ng o was visited with Geolog i s t John Wilton from AngloVaa l Mining in Windhoek . This wa s the best outcrop of granito i ds in many thousan d s of kilometer s . Its coordina te s are 20?27.16 9 ? S / 1 6 ?3 9 .1 5 9 ? E (See Fig M24). The entire outcrop seems to be a 5 5 6 0 6 5 7 0 7 5 8 0 8 5 9 0 SiO2% 1 2 3 4 5 6 7 8 9 1 0 1 1 1 2 1 3 N a 2 O % + K 2O % TOTAL ALKALI vs SILICA DIAGRAM Otjiwarongo environs-G rootfontein Inlier Namibia; Lufilian Granitoid Project (Diagram based on Mi ddlemost, 1994, 1997) S a mp l e s P e tr o g r a p h i c fiel d s L-850 L-1037 L-1038 L-1039 L-1039a L-1039c LJ1 LL1 LL10 LL11 LL13 LL14 LL15 LL16 LL17a LL17b LL18 LL2a LL2b LL3a LL3b LL4 LL5 LL9 L-808 L-809 L-810 L-812 L-813 L-814 L-815 L-1014 L-1042 L-1043 L-1044 L-1045 L-1046 Fig 4.2.3.5 Fig 4.2.3.5 0 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti)5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 R 2 = 6C a +2M g +A l L-850 L-1037 L-1038 L-1039L-1039a L-1039c LJ1 LL1 LL10 LL11 LL13 LL14 LL15 LL16 LL17a LL17b LL18 LL2a LL2b LL3a LL3b LL4 LL5 LL9 L-808 L-809 L-810 L-812 L-813 L-814 L-815 L-1014 L-1042 -1043 L-1044 L-1045 L-1046 R1R2 PLUTONIC ROCK CLASSIFICATION Otjiwarongo Environs, Na mibia; Lufilian G.P. (After De la Roche et al, 1980) P e t r o g r a p h i c fie ld s S a m p l e s Fig 4.2.3.6 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 3 0 0 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti) 5 0 0 L-850 L-1037 L-1038 L-1039 L-1039a L-1039c LJ1 LL1 LL10 LL11 LL14 LL15 LL16 LL17a LL17b LL18 LL2a LL2b LL3a LL3b LL4 LL5 LL9 L-808 L-809 L-810 L-812 L-813 L-815 L-1014 L-1042 L-1043 L-1044 L-1045 L-1046 R1R2 PLUTONIC ROCK CLASSIFICATION Otjiwarongo and Grootfontein Environs, Namibia; Lufilian G.P. (After De la Roche et al, 1980) P e t r o g r a p h i c fie ld s S a m p l e s Fig 4.2.3.7 Fig 4.2.3.7 2 7 0 t h i c k dike, with are several granito id facies, probabl y due to flow banding . The whalebac k ridge is elongat e d along 100?. Part of the large, flat lying ou tcrop was used as a quarry for road ballas t . The two main rock types observe d in the outcrop were sampled . L-1037 is a medium- to fine-gr a i n ed foliate d , light gray, peralum in o us mesocra t i c potassi c magnesic biotite quartzmonz on ite. One of the younger grani- t o i d s , collecte d from the norther n side of the railroa d , L-1038 , is a peralumin o us subleuco c r a t i c potassic magnes ic biotit e granit e . Several samples were collect e d from differe n t facies of a relativel y weathere d rock that makes another large granitoid outcrop located approxima t e l y 20 km north of Ot jiwar ongo . It is the only granitoid outcrop mapped in the 1:1,000,000 scale geological map sheet of Namibia (Fig M23) as well as in the 1:250,000 scale geological map sheet of Otjiwarongo. L-1039 is a pink, medium - gr a i ne d , peralu m i n ou s leucocr a t i c ferrif er o us alkali granite that weathers into a deep orange color on the surface. The entire outcr op probabl y has been subject to strong potassic alteration . L-1039 , L-1039a a nd L-1039c are vario us samples from the site. Sampl es LL31 , LL3b, LL28 were collected from other portions of the same outcrop. Euhedral magnetite crystals from 1 cm to 5 mm diamet er make cluster s that are dissem i n a t e d in some portions of the outcrop . Sample L-1040 contains them. It was collect e d for chemica l analys is and to compare with magnetite from other sources. The clusters s eem to be the product of albitization in the rock. 4.2.3.7.3 Pegmatitic rocks G e o l og i s t Anton Lombard , who worked at the Windhoe k exploration office of Anglo Vaal, suggested sampling several pegmatitic granitoid s intersec ted in boreholes dr illed by him. In his opinion, thos e rocks might be the only repres entatives from the covered Otjiwarongo batholit h. That batholith is cons idered to be the intrus ive body responsible for mineralization at the Otjikoto gold deposit. L-807 to L-815 come from boreholes NRD-1 and SCH-2 and were drilled on 1999 and 2000 by AVMIN (they are located respect i v e l y on stations 5000 and 5001 on Fig M24). The boreholes show domes of strongly- foliated igneous rocks intr uded by younger, underformed pegmatitic granito id bodies (Fig 4.2.3.10). The pegmati t i c apophys e s lie on top of small intrusi v e bodi es that came from the blind Otjiwarongo batholith. L- 808 to L-815 have chemica l analys i s as show n on Table 4.2.3. 11. Depth and field description of the samples is listed on Table 4.2.3.12. L-808 has complete chemic al analysis includ in g all rare earths . Table 4.2.3.11 Chemical Anal ysis, Otjiwarongo pegmatites, Namibia (complete elemental analys is on Table A13, Appendix) Sampl e SiO2 TiO2 Al2O3 Fe2O 3 MnO MgO CaO Na2O K2O P2O5 LOI Total Na+K Notch 50.00 1.00 15.50 6.00 0.1 5 0 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2.00 L-808* 70.53 0.14 15.35 1.50 0.0 5 0 . 4 2 1 . 7 1 4 . 8 0 3 . 6 7 0 . 0 7 2.04 100.28 8.47 L-8 0 9 71.56 0.07 14.95 1.24 0.0 3 0 . 2 3 0 . 8 7 3 . 4 6 7 . 5 2 0 . 0 6 0.50 100.49 10.98 L- 8 1 0 73.89 0.06 14.05 1.11 0.0 4 0 . 1 6 1 . 0 4 4 . 0 0 5 . 4 4 0 . 0 4 0.50 100.33 9.44 L-8 1 2 75.60 0.08 12.89 1.27 0.0 3 0 . 2 5 1 . 2 9 4 . 0 3 4 . 1 7 0 . 0 9 0.71 100.41 8.20 L-81 3 71.80 0.04 15.51 0.86 0.0 3 0 . 1 2 1 . 4 0 4 . 2 6 5 . 5 9 0 . 0 8 0.78 100.47 9.85 L-8 1 4 89.59 0.02 5.33 0.65 0.0 2 0 . 0 2 0 . 8 4 2 . 9 4 0 . 3 1 0 . 0 4 0.63 100.39 3.25 L-8 1 5 69.73 0.30 14.51 3.35 0.0 8 0 . 8 4 1 . 3 4 3 . 8 5 5 . 5 9 0 . 1 6 0.65 100.40 9.44 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta Gd Dy Er Yb Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 30 20 9 8 L-808* 140 89 12 29 14 <6 7 10 71 16 13 39 154 <6 <15 <10 32 2 9 2 26 <12 6 1 1 2 2 1 1 L-809 253 92 19 <8 9 <6 7 11 56 16 <12 27 301 <6 <15 <10 29 <12 L-810 173 85 7 <8 7 9 10 13 50 14 <12 56 249 <6 <15 <10 24 <12 L-812 141 104 86 215 10 <6 8 9 67 13 <12 34 439 17 30 <10 93 55 L-813 173 115 65 77 6 <6 9 13 23 14 <12 42 625 13 21 <10 63 22 L-814 23 38 5 <8 4 <6 7 10 54 <9 <12 77 50 <6 <15 <10 26 <12 L-815 214 122 43 268 25 <6 8 10 75 17 12 68 584 42 16 <10 68 29 A few gabbroid dikes were inter s ec t e d in the boreho le s ( L-807 a nd L-811 ) . These have not been analyse d , but are foliated and amphibo l i t i z e d (See photos in Fig 4. 2.3.9) . They probably are mid alkaline gabbroids , and were emplaced soon after the pegmatit es , in an anorogen ic environme n t . L-808* is a very coar se-grained, pink , peraluminous leucocratic potassic magnes ic graphic granite. L-808 to L-815 indicate chemis try of the pegmatitic in trus ives intersected in the boreholes. 2 7 1 Table 4.2.3.10 Chemical Anal ysis, Otjiwarongo environs, Namibia (complete elemental analysis is on Appendix A13) Sampl e SiO2 TiO2 Al2O3 Fe2O 3 MnO MgO CaO Na2O K 2O P2O5 LOI Total Na+K Not c h 50.00 1. 0 0 15.50 6.00 0.1 5 0 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2.00 L-808 70.53 0.1 4 15.35 1.50 0.0 5 0 . 4 2 1 . 7 1 4 . 8 0 3 . 6 7 0 . 0 7 2.04 100.28 8.47 L-8 0 9 71.56 0. 0 7 14.95 1.24 0.0 3 0 . 2 3 0 . 8 7 3 . 4 6 7 . 5 2 0 . 0 6 0.50 100.49 10.98 L- 8 1 0 73.89 0. 0 6 14.05 1.11 0.0 4 0 . 1 6 1 . 0 4 4 . 0 0 5 . 4 4 0 . 0 4 0.50 100.33 9.44 L-8 1 2 75.60 0. 0 8 12.89 1.27 0.0 3 0 . 2 5 1 . 2 9 4 . 0 3 4 . 1 7 0 . 0 9 0.71 100.41 8.20 L-81 3 71.80 0.0 4 15.51 0.86 0.0 3 0 . 1 2 1 . 4 0 4 . 2 6 5 . 5 9 0 . 0 8 0.78 100.47 9.85 L-8 1 4 89.59 0. 0 2 5.33 0.65 0.0 2 0 . 0 2 0 . 8 4 2 . 9 4 0 . 3 1 0 . 0 4 0.63 100.39 3.25 L-8 1 5 69.73 0. 3 0 14.51 3.35 0.0 8 0 . 8 4 1 . 3 4 3 . 8 5 5 . 5 9 0 . 1 6 0.65 100.40 9.44 L-85 0 71.15 0.3 8 13.69 2.97 0.0 5 0 . 4 7 1 . 5 6 3 . 0 9 4 . 9 6 0 . 1 0 0.48 98.90 8.05 L-10 3 7 67.15 0.4 4 16.05 2.51 0.0 2 0 . 7 7 1 . 3 3 2 . 9 9 7 . 4 9 0 . 1 5 0.46 99.36 10.48 L-1 0 3 8 68.09 0.4 4 15.77 2.42 0.0 2 0 . 6 9 1 . 3 9 3 . 0 3 6 . 4 5 0 . 1 7 0.40 98.87 9.48 L-1 0 3 9 70.93 0. 2 5 13.72 2.43 0.0 1 0 . 0 3 0 . 5 7 3 . 6 2 5 . 5 1 0 . 1 0 1.71 98.88 9.13 L-1 0 3 9 a 73.60 0. 1 0 13.76 0.98 0.0 2 0 . 0 6 0 . 4 7 3 . 6 7 6 . 1 4 0 . 0 3 0.53 99.36 9.81 L-1 0 3 9 c 70.50 0. 3 4 13.95 3.40 0.0 2 0 . 0 0 0 . 7 1 3 . 3 8 5 . 9 4 0 . 1 1 2.16 100.51 9.32 LJ 1 68.16 0 . 4 6 16.02 2.81 0.0 2 0 . 8 9 1 . 5 4 2 . 8 5 7 . 1 7 0 . 1 6 0.55 100.07 10.02 LL 1 73.41 0. 0 9 14.65 0.80 0.0 1 0 . 2 7 1 . 0 0 3 . 3 4 6 . 2 4 0 . 2 0 1.26 100.02 9.58 LL1 0 56.48 1. 2 4 17.84 6.85 0.1 9 1 . 9 6 3 . 7 8 5 . 7 4 4 . 8 6 0 . 7 4 0.74 99.67 10.60 LL 1 1 73.00 0. 0 0 14.00 2.00 0.0 0 0 . 0 0 1 . 0 0 3 . 0 0 6 . 0 0 0 . 0 0 1.00 99.86 9.00 LL1 3 62.00 1. 0 0 11.00 4.00 0.0 0 3 . 0 0 1 8 . 0 0 1 . 0 0 0 . 0 0 0 . 0 0 7.00 100.02 1.00 LL1 4 57.00 1. 0 0 17.00 9.00 0.0 0 1 . 0 0 3 . 0 0 6 . 0 0 5 . 0 0 0 . 0 0 1.00 99.52 11.00 LL 1 5 62.00 1. 0 0 16.00 6.00 0.0 0 1 . 0 0 4 . 0 0 6 . 0 0 5 . 0 0 0 . 0 0 4.00 99.73 11.00 LL 1 6 70.00 1. 0 0 14.00 3.00 0.0 0 1 . 0 0 2 . 0 0 3 . 0 0 5 . 0 0 0 . 0 0 0.00 99.49 8.00 LL1 7 a 73.00 0. 0 0 14.00 1.00 0.0 0 0 . 0 0 1 . 0 0 3 . 0 0 7 . 0 0 0 . 0 0 1.00 99.75 10.00 LL 1 7 b 66.00 1. 0 0 16.00 5.00 0.0 0 1 . 0 0 3 . 0 0 3 . 0 0 5 . 0 0 0 . 0 0 0.00 99.77 8.00 LL1 8 76.00 0. 0 0 13.00 1.00 0.0 0 0 . 0 0 1 . 0 0 3 . 0 0 7 . 0 0 0 . 0 0 1.00 100.07 10.00 LL 2 a 75.73 0. 0 2 14.98 0.67 0.0 1 0 . 0 6 0 . 1 2 3 . 6 2 4 . 8 6 0 . 0 4 1.36 100.11 8.48 LL2 b 69.71 0. 0 0 16.92 0.31 0.0 1 0 . 0 0 0 . 0 4 2 . 5 4 1 0 . 4 0 0 . 1 3 0.60 100.06 12.94 LL 3 a 75.92 0. 0 3 13.87 0.68 0.0 1 0 . 0 5 0 . 3 9 2 . 8 7 5 . 9 3 0 . 0 1 1.19 99.77 8.80 LL3 b 70.31 0. 0 4 16.91 0.47 0.0 1 0 . 2 4 0 . 3 7 2 . 4 4 9 . 0 9 0 . 0 9 1.20 99.96 11.53 LL 4 74.72 0. 1 0 13.50 1.59 0.0 3 0 . 1 0 0 . 8 0 3 . 4 9 5 . 7 4 0 . 0 2 0.41 100.08 9.23 LL5 75.94 0. 0 3 14.40 0.33 0.0 0 0 . 0 0 1 . 4 4 4 . 0 3 3 . 4 6 0 . 0 3 0.64 99.67 7.49 LL9 79.03 0. 0 2 14.86 0.39 0.0 0 0 . 0 1 0 . 0 2 0 . 3 0 5 . 6 3 0 . 0 0 3.19 100.25 5.93 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta Eu Gd Dy Er Yb Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 4 30 20 9 8 L-808 140 89 12 29 14 <6 7 10 71 16 13 39 154 <6 <15 <10 32 2 9 2 26 <12 6 1 1 0 2 2 1 1 L-809 253 92 19 <8 9 <6 7 11 56 16 <12 27 301 <6 <15 <10 29 <12 L-810 173 85 7 <8 7 9 10 13 50 14 <12 56 249 <6 <15 <10 24 <12 L-812 141 104 86 215 10 <6 8 9 67 13 <12 34 439 17 30 <10 93 55 L-813 173 115 65 77 6 <6 9 13 23 14 <12 42 625 13 21 <10 63 22 L-814 23 38 5 <8 4 <6 7 10 54 <9 <12 77 50 <6 <15 <10 26 <12 L-815 214 122 43 268 25 <6 8 10 75 17 12 68 584 42 16 <10 68 29 L-850 254 153 22 241 15 7 7 23 57 17 27 13 919 <6 46 <10 116 43 131 161 67 4.7 34 0.6 0.2 L-1037 204 190 22 149 16 <6 6 8 41 17 15 156 1143 <6 105 <10 288 157 L-1038 185 178 26 247 18 <6 8 13 39 16 14 162 975 <6 112 <10 316 175 L-1039 160 562 19 156 20 <6 7 21 11 18 <12 230 793 <6 26 <10 88 46 L-1039 a 168 205 12 38 2 <6 8 6 11 13 12 250 1060 <6 <15 <10 25 3 18 5 55 23 3 1 0 1 3 2 1 1 L-1039c 172 547 24 162 24 <6 7 29 12 18 <12 309 776 <6 32 <10 103 55 LJ1 196 191 24 259 17 4 30 42 15 0 954 1 95 4 LL1 150 176 17 42 6 3 3 13 11 6 1 1468 0 5 2 LL10 135 965 36 340 99 11 3 0 78 44 0 1366 9 25 1 LL11 287 134 34 210 16 2 1 0 30 20 3 880 3 55 5 LL13 12 701 42 128 6 9 26 3 58 101 66 448 4 5 10 LL14 280 355 161 2052 364 4 5 133 4 0 1161 22 83 5 LL15 118 328 31 305 47 10 9 0 73 125 22 1308 3 26 15 LL16 230 152 24 320 30 4 2 0 33 39 9 790 3 33 4 LL17a 202 57 12 29 9 2 5 8 4 6 22 0 5 3 1 LL17b 140 208 22 311 16 13 2 2 60 50 7 1167 4 18 9 LL18 178 84 8 55 3 0 8 5 4 31 6 5 4 1 LL2a 181 35 10 19 19 2 1 14 8 11 0 10 4 2 4 2 LL2b 356 67 7 4 1 2 1 0 2 0 1 20 5 0 2 0 LL3a 156 182 13 29 0 2 1 14 4 5 3 65 9 0 7 1 LL3b 348 252 9 5 4 2 1 0 7 7 1 49 5 1 0 5 LL4 365 50 32 138 29 1 0 27 1 0 235 4 52 5 LL5 180 89 47 48 11 1 6 4 0 0 151 5 11 1 LL9 256 26 9 33 9 2 2 1 3 12 3 28 5 2 3 2 2 7 2 Fig 4.2.3.9 Photographs of slabs from samples L807 and L-811 . T h es e s lightly d e f ormed mafic dikes with abundant plagioclase amygdules intersect the pegmatites of the Otjiwarongo Batholith. Scale in millimeters. Fig 4.2.3.10 Photographs of granitic pegmatites from the Otjiwarongo Batholith. N o t e graphic textures, amphibole needles and lack of deformation. A composite of th es e samples was dated. Dept hs are marked in blue. Bottom is to the left. F or scale, the core slabs are 5.5 cm wide. Table 4.2.3.12 Main details of samples from pe gmatitic granitoids, Otjiwarongo batholith, Namibia Sample Borehole Depth Field Notes Rock Name Remarks L - 8 0 7 NRD1 120.5 7 A l b i t i z a ti o n alkal i gabbr o ? See photo on Fig 4.2.3 . 9 L-808 * NRD1 161.7 9 P i n k pegma t i t i c grani t e s with graphic text ure peral leuco potas s i c magne s i c grani t e L-809 NRD1 162.4 2 P i n k pegma t i t i c grani t e s with graphic text ure meta leuco potas s i c ferri f e r o u s alkal i grani t e L-810 NRD1 161.8 1 P i n k pegma t i t i c grani t e s with graphic text ure meta leuco sodic to potas s i c ferri f e r o u s grani t e The rock was pre v i o u s l y cooke d and later intrud e d by pegma t i t e s . L-811 NRD1 172.2 8 S c h i s t o s e amphi b o l i t e alka l i gabbr o ? Scapo l i t e opens its space in the schi s ts with whit e plag i o c l a s e that flood s rock matri x . L-812 SCH-2 87.51 M i n e r a l i z e d grap h i t i c schi s t meta leuco sodic magne s i c grani t e 22 ppb Au, 36 pp m Pb, 76 ppm Cu, 69 ppm Zn L-813 SCH-2 82.94 G r a p h i t i c schist meta leuco sodic to potass i c ferrif e r o u s granit e L-814 SCH-2 158.6 8 A m p h i b o l e albit e schis t meta leuc o sodic ferrifer o u s , out of plot, high Si L-815 SCH-2 195.80 P e g m a t i t i c granit e meta me soc r a t i c sodic to potas s i c ferri f e r o u s granite 2 7 3 4.2.3.7.4 Geochemistry 76% of the granitoids from the Otjiwarongo region fall with in the midalkaline field, while 24% of them fall in the subalkaline field (Fig 4.2.3.5, Table 4.2.3.13). All mi dalkaline rocks make 71% of the samples, 29% of them are subalka l in e and none alkalin e . As no ted, there is a single quartzo l i t e . Table 4.2.3.13 Statistics of rock types, Otjiwarongo environs, Namibia The fifth column (granitoids) is the sum of underlined rock types. Group Rock type number % Granitoids Groups A l k a l i gran i t e 13 41.94 Q u a r t z m o n z o n i t e 5 16.13 S ye n i t e 2 6.45 Midalkaline Rocks M o n z o n i t e 2 6.45 75 . 8 6 70.97 Granite 7 22.58 2 4 . 1 4 Diorit e 1 3.23 Subalkaline Rocks Q u a r t z o l i t e 1 3.23 29.03 Total 3 1 1 0 0 . 0 0 1 0 0 . 0 0 100.00 Many samples from Otjiwar ongo are enriche d in K2O, some are enriched in Cr. Samples LL13 , LL12 , LJ1 were collect e d near the samplin g site for L-1037 , probably from the same large outcrop. All contain very high Th co nten t. They are extremely high heat produc i n g rocks due to abunda n t potassium and thorium. The analyses of LL12 and LL-28 were not available. LL13 is more mafic, it contains Cu, V, Mg, Ca and Ni. Very high Th, Cr, Rb, K alteration and high alumina. LJ1 with high Cu. LL13 low Th. Several samples were collected and analysed by Anglo Vaal from the same site where L-1037 and L-1039 w e r e sampled (Figs M23 and M24). LL3a an d LL3b have high K2O, but somewha t differ e n t chemis t r y . Although L-1039a has 29 ppm of Cu, LL3a a n d LL3b have muc h less and very much less Cr. Very low Th compared to medium Th values in L-1039 . Samples L-1039 an d L-1039c contain enough Th and K to be high heat produc er s (Table 4.2.3.10 ) . LL2b an d LL3b are very similar to each other; LL3a a n d LL2a are very similar too. Both types of rocks are exposed in two different outcrops that are approximately 10 km away from each other. That means that the same pluton extends furthe r north along the road (Fig M24). LL1 is similar to L-1-39a an d LL3a , except for the high Cr and Ba. L-815 is a very high heat producing granite. It c ontains high U. It has some simila ri t i e s with LL16 a nd L-1042 , but neither of them contain anomalous U. L-808 , L-813 a n d L-814 do not correlate with any of the other sample s. L-809 correlate s with LL-11 except in Th value A few samples from comple t e l y differe n t regions were found to have equivale n t geochem is t r y. They are listed on Table 4.2.3. 9 . Their chemic a l sim ilarity indicates a similar origin and environment of emplacement. That does not mean they have the same age. All the samples listed formed in anorogen i c contine n t a l extensi o n al environments. Table 4.2.3.9 Rocks from different regions that display very similar major oxide and trace element chemistry. Region Sample numbers G r o o t f o n t e i n Inlier L-1043, L-1044, L-1046 Mufulir a Gra nite L-166 Hook Granit e Bat hol i t h L-257, L-409 NW Zambia L-370, L-364, L-0 20, L-030 Otjiwa ro n g o enviro n s LL-4, LL -11, L-16 , LJ-1 2 7 4 S a m p l es from the environ s of Otjiwaro n g o could be grou ped into seven discrete groups based on their major oxide chemistry. The groups ar e shown on Figs. 4.2. 3.5 and 4.2.3.7. Other geoc he m ic a l diagrams did not produc e signif i c a n t results , becau s e the groups of samples clustered together and overprinted each other. Table 4.2.3.15 shows the various groups of samp les and the location s where they were sampled . 4.2.3.7.5 Otjiwarongo Batholith The Otjiwarongo batho lith may be respon sible for mineralization at the Kombat mine. All observations and critical reading of literatu r e availabl e on the mine lead to conc lude it formed as a deposit of the iron oxide- copper-gold family. Section 8.4.1.2 de scri b es this in greate r detail . Probab l y other copper deposi ts in the Kombat region have similar origin . All the occurrenc e s of gold that surroun d Kombat are hydroth er m a l and could be attribut e d to the hidden batholit h . It could al so produce mineralization of the sedime n t - ho s t ed gold type (so-called ?Carlin ?type??) in the Otavi carbonat e sequen c e . Several copper occurre nc es around Otjiwa r o n go and copper and gold occurr e nc es NE of the same town seem to be of hydrothe rmal origin too. In fact, isotopic signatu r es from the Kombat mine indicate that sulfides have a magmatic input (Pirajno, Kinnaird, Fallick, Boyce, & Petzel, 1993). This is a very significant intrus ive body to understand . Know ing more about it might lead to many major new mineral discove r i es in Namibia . The age of the Otjiwarongo Batholith is very significant, becaus e it indica t es that large-scale magmatis m took place at that time. It is also significant, because t he Otjiwa r o n go Bathol i t h is probab l y respon s ib l e for IOCG mineralization at Kombat and Otjik oto gold deposit in Namibia. 4.2.3.7.6 Environment of Emplacement All the samples from the environs of Otjiwarongo were emplac e d in anorog e n ic enviro nm e n ts , as indica t e d by the proc edu r e of Whalen et al. Few of the samples pr oduce coheren t results from the Pear ce and Maniar & Piccoli method s (Table 4.2.3.14 ) . Those that do, indica te continental within-plate rift-related magmatism or continental e peirogenic uplift. 4.2.3.7.7 Geochronology A zircon concent r a t e from composi t e sample L-808c* was dated to produce a preliminar y SHRIMP U/Pb age of 550 Ma. The radiom e tr ic age is dating one of the last magmatic events of the Ot jiwaro n go batholit h , and is the only geochrono logical cons traint on the batholith. T hat age correl a t e s well with the Zambia n Hook Granit e batholith, and the Damaran granitoids in Namibia. Ther e are very few radiomet r ic ages from rocks in this part of Namibia. 4.2.3.7.8 Discussion The eviden c e obtained from macrosc o pic descrip t i on and chemis try of the rocks colle c t e d from the enviro ns of Otjiwarongo lead to think that the basement rocks in that part of Namibia are very si milar to the rocks in the basement to the Grootfontein Inlier, the Zambian Copperbelt and northwestern Zambia , and probably have the same age. Table 4.2.3.1 5 groups the variou s samp les from the environs of Otjiwar ongo into several groups . Most of the groups are made of samples that come from more than one sampli ng site. The groups were plotted on Figs 4.2.3.5 and 4.2.3.7. Table 4.2.3.15 Tentative correlation table for samples from the environs of Otjiwarongo, Namibia ( L e t t e r s indicat e sites, roman numer als indicat e rock types.) B C A D Other LL13 anomal o u s , altere d LL9, altere d gran it e L-1014, granod i o ri t e L-814, alter e d gr anit e , quartz o l i t e L-808 L-1039, L-1039c LL13 II LL3a LL2a L-10 4 4 III LL4, LL5, LL 11, LL16, L- 810, L-812, L-850, L-1046 L-1043, LL18 V LL17a L-1039a, LL3b LL2b L-80 9 , LL 18, L-8 15, LL36, LL 16, L-1042 VI L-1038, L-1037, LJ1 L-813, L-815 2 7 5 The few samples collected that might come from the Otjiwar ongo Batholith were dated at circa 550 Ma. This age is probabl y one of the latest in a series of intrus i v e events that made the batholit h. The pegmatitic charac- ter of these rocks made it impossible to define their environmen t of emplacement prec isely. Nevertheles s, they formed in an anorogen ic environment. The age of most of the granit o i d s sample d in the enviro ns of Otjiwar o n go is uncerta i n . Several of them may be part of the basemen t to the Damara silici c la s t ic and carbona t e rocks that hav e been expos ed on surfac e due to tectonic uplift. Others may be inters ecting such sequence s . No relatio n s h ip s were directly observed in the field. Further indications of the geological setting of the granitoids may be possible, if funding for dating the granito id s bec omes availab l e . Table 4.2.3.17 Rock types and environment of emplacement for the environs of Otjiwarongo, Namibia ( S e e acrony m descrip t i o n on sectio n 2.4.3. ) Sample R ock Name Deb o n & L e F ort Maniar & Piccoli Whalen Pearce Mafic Rb/10 H f Ta Rb/30 H f Ta Nb-Ta L - 8 0 8 * Grani t e pegma t i t e Perai i i leuco K Mg IAG-C A G N S2/4 O2/4 VA- II INV L-809 Alkal i grani t e Metai v leuco K Fe IAG-C A G A L-810 Pegma t i t i c grani t e Metai v leuco Na-K Fe A L-812 Grani t e Metav leuco Na Mg A L-813 Granit e Metaiv leuco Na-K Fe A L-814 Quart z o l i t e , High silic a Metav i leuco Na Fe L-815 Pegma t i t i c grani t e Metai v meso NaK Fe A O-W1- 1 L-850 Grani t e Perai i i suble u c o Na Fe POG A O3/4 WP WP OUT U L - 1 0 3 7 Quart z m o n z o n i t e Perai i i meso K Mg A L-1038 Grani t e Perai i suble u c o K Mg A L-1039 Alkal i grani t e Perai i leuco K Fe CEUG A L-103 9 a Alkal i grani t e Perai i i leuco K Fe A S2/4 O2/4 VA- VA INV L-103 9 c Alkal i grani t e Perai i i suble u c o K Fe CEUG A LJ1 Gran i t e Perai i i meso K Mg A LL1 Grani t e Perai i leuco K Mg IAC+C A G A LL10 Nephe l i n e s yeni t e Metai v meso Na Fe A W wp ab LL11 Grani t e Perai i leuco K Fe A LL13 Out of plot, high Ca+Si Metav i meso Na Mg OP A V arc LL14 Nephe l i n e s yeni t e Metai v meso Na Fe RRG A W wp ab LL15 Syeni t e Metav meso Na Fe A LL16 Grani t e - g r a n o d i o ri t e Perai i i meso Na Mg A LL17a Grani t e Metav leuco K Fe A LL17b Gran o d i o r i t e Perai i i meso K Fe RRG A LL18 Grani t e Metav i leuco K Fe A LL2a Alkal i grani t e Perai leuco Na-K Fe A LL2b Quart z s yeni t e Perai leuco K Fe A LL3a Alkal i grani t e Perai leuco K Fe A LL3b Alkal i grani t e Perai leuco K Mg CCG A LL4 Grani t e Perai i i leuco K Fe POG A O-W1- 1 LL5 Granit e Perai leuco Na Fe A LL9 Granit e Perai leuco K Fe A 2 7 6 Table 4.2.3.14 Rock types and environment of emplacement for several Namibian domains ( S e e acrony m descrip t i o n on sectio n 2.4.3. ) Ugab River, Namibia Sample R ock Name Deb o n & L e F ort Maniar & Piccoli Whalen Pearce Mafic Rb/10 H f Ta Rb/30 H f Ta Nb-Ta L - 7 9 3 Granit e metaiv leuco Na Fe POG A W3/4 WP- WP OUT U L-795* Granite L-796* Granite L-797 Granite p e r a i i leuco Na-K Fe RRG-CE U G A L-798 Granite p e r a i i leuco Na-K Fe POG A L-799 Granite p e r a i i leuco Na-K Fe A L-802 Granite p e r a i i leuco Na-K Fe N Otjiwarongo Environs, Namibia Sample R ock Name Deb o n & L e F ort Maniar & Piccoli Whalen Pearce Mafic Rb/10 H f Ta Rb/30 H f Ta Nb-Ta L - 8 0 8 * Grani t e Perai i i leuco K Mg IAG-C A G N S2/4 O2/4 VA- II INV L-809 Alkal i grani t e Metai v leuco K Fe IAG-C A G A L-810 Granite M e t a i v leuco Na-K Fe A L-812 Granite M e t a v leuco Na Mg A L-813 Granite M e t a i v leuco Na-K Fe A L-814 out of plot, high Si Metavi leuco Na Fe L-815 Granite M e t a i v meso NaK Fe A O-W1- 1 L-850 Granite P e ra i i i subl e u c o Na Fe POG A O3/4 WP WP OUT U L - 1 0 3 7 Quart z m o n z o n i t e Perai i i meso K Mg A L-1038 Grani t e Perai i suble u c o K Mg A L-1039 Alkal i grani t e Perai i leuco K Fe CEUG A L-1039 a Alkal i grani t e P e ra i i i leuc o K Fe A S2/4 O2/4 VA- VA INV L-103 9 c Alkal i grani t e P e ra i i i subl e u c o K Fe CEUG A LJ1 Granite P e ra i i i meso K Mg A LL1 Granite P e r a i i leuc o K Mg IAC+C A G A LL10 Nephe l i n e s yeni t e Metai v meso Na Fe A W wp ab LL11 Grani t e Perai i leuco K Fe A LL13 out of plot, high Ca+Si Metav i meso Na Mg OP A V arc LL14 Nephe l i n e s yeni t e Metai v meso Na Fe RRG A W wp ab LL15 sye ni t e Metav meso Na Fe A LL16 Grani t e - g r a n o d i o ri t e Perai i i meso Na Mg A LL17a Grani t e Metav leuco K Fe A LL17b Gran o d i o r i t e Perai i i meso K Fe RRG A LL18 Grani t e Metav i leuco K Fe A LL2a Alkal i grani t e Perai leuco Na-K Fe A LL2b Quart z s yeni t e Perai leuco K Fe A LL3a Alkal i grani t e P e r a i leuco K Fe A LL3b Alkal i grani t e P e r a i leuco K Mg CCG A LL4 Granite P e ra i i i leuc o K Fe POG A O-W1 - 1 LL5 Granite P e r a i leuco Na Fe A LL9 Granite P e r a i leuco K Fe A Grootfontein Inlier, Otavi Mountains, Namibia Sample R ock Name Deb o n & L e F ort Maniar & Piccoli Whalen Pearce Mafic Rb/10 H f Ta Rb/30 H f Ta Nb-Ta L - 1 0 1 4 granod i o r i t e Peraii i meso Na Mg IAG_CA G ?N L-1042 Granite P e r a i i suble u c o K Fe POG A WP- WP OUT U L-1043* Granite P e r a i i suble u c o K Fe POG A O-W 2-2 WP WP OUT U L-1044 Granite P e r a i i leuc o K Fe POG A O-W1- 1 L-1045 Quart z m o n z o n i t e Metav suble u c o Na Fe A W3/4 OUT U L-1 0 4 6 Granit e Peraii subleu c o K Fe POG A O-W1- 1 Okwa River, Botswana L - 6 0 0 A Alkal i grani t e Metav leuco Na- K Fe RRG-C E U G A L-602 Granite M e t a i v meso Na-K Fe A O3/4 OUT U L-605 Granite M e t a v leuco Na Fe A L-606 Granite M e t a i v meso Na Fe RRG-CE U G A Summas Mountains, Namibia Sample R ock Name Deb o n & L e F ort Maniar & Piccoli Whalen Pearce Rb/10 H f Ta Rb/30 H f Ta Nb-Ta L - 7 8 9 Quartz s yenite Metalum i iv meso NaFe RRG-CEU G A O-W 2-2 OUT U L - 7 9 1 a Alkal i grani t e P e r a l u m ii leuco KFe RRG-C E U G A W3/4 WP- WP INW L-791 b Alkal i grani t e P e ra l u m iv meso Na-K Fe W 2 7 7 4.2.3.8 REVIEW OF OBSERVATIONS FROM THE OKWA RIVER, UGAB RIVER, GROOTFONTEIN AND SUMMAS MOUNTAINS OUTCROPS The outcrops of the Okwa River in Bots wana, the Ugab River and Grootfontein Inlier in Namibia that have been described in the previous pages are quite remark able. Especially given the scarci ty of outcro ps in Botswana. When geoche m i c a l data from the Ugab River, the Summas Mountains , Okwa River, Otjiwaron g o 1 , Grootfontein and the new Felsic volc anics are plotted on the R1/R 2 diagram (Fig 4.2.2.1) , several groups of similar rock types can be construc ted, as indicated on Table 4.2.3. 18. Groups II and III are common to the Okwa River, the Ugab River and the Grootfontein samp ling areas. Chemis t r y , microsc o p ic and macros c o p i c featu r es of both rock types from each of the sites is remarkably similar, and one of them was pres ent in the Summas Mountains, as shown on Table 4.2.2.10. That cannot be a coincid e nc e . These bodies of rock probably came from the same type of magma. Derived from melting similar rocks. They probably suffered the same geolog i c a l process es , and may have formed during the same events. Both of the foliated porphyritic granitoid s contain mafic elongated lenses of xenolithic mate rial that has been incomp letely assymilated by the magma. In addition, group III has two samples from the other do mains, the Summas Mountains and the felsic volcanic rocks from Frets, 1969. Apart from that, when compili n g the informa t i o n another si milarity was found between one of the samples from the Summas Mountains , three from the group of felsic volcanic s and some from the Otjiwarongo area, here listed as gro up V. L-789 correl a t e s well with sa mple s from the Otjiwa r o ng o area and confor m group VI. Samples X-17 and L-1045 differ signific a n t l y from the other groups and are listed on their own, apart as groups VII and VIII. The detailed chemistry of volcanic rocks from the Summa s Mounta i n s (L-791b ) matched with granit o id s from the Ugab River and the Okwa River samplin g sites. The high Cr, Nb and Y signatur es are unmistak a b le . The major oxide chemistry of the suite does not show anyt hin g specia l that can help to identify them positive l y from other rocks. Potentia lly all ro cks in the suite contain high values of Sm, Nd and Pr, but this was not tested for all the samples. As illustrated on the tabl e below, all rocks from group III contain high thorium values . No roc ks from the Ugab River on group III cont ain anomalous thoriu m, while those of the Okwa River and Grootf o nte i n do. The geoche m ic a l diagra ms devise d by Debon & LeFort did not produce any significant results. Since the rocks at the Ugab River were dated, (540 Ma) one could probabl y extend the same age to rocks from the Okwa River and Grootfontein. The ~750 Ma age from xenocrystic zircons in the granites dated from the Ugab River may be a key to the source of the t horium, the chromium or some of the other ?strange ? enric h me n t s . L-796, L793 and L-797 are the same type of rock with high Th. Maybe there was some special type of magma mixing that produced the Th enric hment. All samples from the Grootfontein Inlier (event L-10 44 ) have high copper. Two from Otjiwar on g o do so too, and they don?t come from the same suite. None of th e other sample s contain anomous copper . Maybe copper in thes e regions is secondary and was brought in afte r the granito ids were emplaced. This might mean that there is more copper to be found around the Grootf o n t e i n Inlier and the Otjiwar o n go batholi th . Copper might have been introduc ed along with the thor ium . Probably suites II and III both formed in post orogenic environmen ts. These environments may indicate both orogenic and non-anor o gen i c in the Whalen et al, 1987 plots. II and III are better identified on the R1R2 diagram. The TAS diagram mixes them, as shown on Figs 4.2.3.10. The new age obtaine d for a sample from the Grootfo n t e i n Inlier correlates well with rock type and ages from the Kamanjab Batholith. 1 The Otjiwar on g o domain will be describ e d in the followi ng ch apter . Neverthe less, it is treated in this review because of its strikin g similar i t i e s with the Okwa, Ugab and Grootfontein domains . 2 7 9 Table 4.2.3.18 Groups of rocks from the Ugab-Okwa Domain compared with others in Namibia ( U nd er l i n e d samples have chemic a l analysi s . The # symbol indicat es high heat produci n g granite s ) Suite Okwa River Ugab River Grootfontein Summas Mts. Otjiwarongo Felsic Volcanics NW Zambia I L-602# A Grani t e II L-606# M e d i u m - g r a i n e d grani t e not as foliat e d as L-605. A ARG- C E U G L-798# (f-m ediu m - g r a i n e d gra y granite witho u t pink felds . Ma y be facie s of ?pink ? grani t o i d ) A POG L-799 (m-c-g brown, porp h granit e with yellow quartz , magnet i t e + transp ar e n t to yellow plag) A L-802 (non -mag f-mediu m - g r a i n e d pink granit e that grad es from previo u s gra y gtd. With small spind l e - s h a p e d , biot- ri c h xenol i t h and coarse biotite ?e yes?) N L-795 * (c-g gra y porph gtd + biot + mag clust e r s ) ~540 Ma L-1042 c-g, porp h yr i t i c , folia t e d granit e ; copper ; A POG WP G LL-2a , LL3a III L-605# A c-g, folia t e d gr ani t e . Old L-793 ( c - g pink biotit e granit e with abund mag in clust e r s . Could be c-g facie s of pink gtd) L-797 (medium - g r a i n e d pink biotit e granit e with pink felds, rare mag + red qz ) L-796 * (pink gtd + red qz clust e r s , no mag + zoned red plag ), ~1700 Ma; L-794 , L-800 L-1043*# f -g , fels i c porp h yri t i c grani t e with littl e folia t i o n ; Cu; A POG WP; 1939? 64 Ma L-1044# f-g grani t e ; seems to cut throug h L1 04 2; Cu; A POG L-1046# c-g po rp h yr i t i c grant i e ; copper ; A POG L-791b (pi n k - rd f-l am, vitre o u s , f-g alkal i rh yol i t e tuff +conc h . Fract . ; A WPG; withi n plate granit e L850# , LL4# , LL11# , LL5 , LL- 810 , L-812# , LL14# , LL16# X-20 ? Rhyol i t e L-364 , L370 IV L-600A# l t pink, non-f o l porph . alkal i grani t e with fine matrix . Cu t by pink dike. A ARG-C E U G V L-791a ( p i n k - r d f-lam , vitre o u s , f-g, volca n i c l a s ti c alkal i rhyol i t e (ash?) +conch . fr act. ) ; A RR G- CEU G L-1039 relativ e l y we athe r e d c-g gtd; confo r m s large whale b a c k outcrop ; Cu L-1039a c-g gtd L-1039c c - g gtd; Cu LL17a , LL3b , LL2b, L-809 X-16, X-18, X- 19 ; alka l i rh yol i t e s VI L-789 ( ~ m a g sub v o l c a n i c quartz trach yt e with white porph y r i t i c plagi o c l a s e + open vacuo l e s ) ; A PPG-C E UG L-1038# m-f -g, foliat e d , lt gy gtd L-1037# m-f -g, foliat e d , lt gy gtd; ver y high Ht LJ-1# ; Cu; ver y high Th VII X-17 ; rh yol i t e VIII L-1045# c-g po rp h yr i t i c quartz m o n z o n i t e , Copper ; A LL17b IX L-1014 N IAC- C A G 2 8 1 4.2.4 WITVLEI, NAMIBIA 4.2.4.1 Introduction The Okatjep ui k o mineral i z e d site and its associa t e d grani toid rocks were visited by suggestion of Geologist Eckart Freyer, of the AngloAmerican exploration offi ce in Windhoe k (Freye r , E., 2002, person a l communi c a - t i o n ) . The site is located on Figs M26 and M19. Freyer offered informat i o n on a prospect he had recently been exploring , that displaye d some spec ia l char ac t e r is t i c s of iron oxide-c o p p er-gold mineralization. He found ore- grade gold and copper minera l iz a t i on on surfac e samp les (3.5 gAu/ton and multi percent Cu). The minerali- z a t i o n seems to lie underne a t h and beside the Witvle i sedimen t ar y - h o s t ed copper deposit . The latter deposit has been said to be very similar to thos e of the typical Zambian Copperbelt (Anhaeusser & Button, 1973; Borg, 1995; Borg & Maiden, 1986; Maiden, 1996; Mai den, Innes, King, Master, & Pettit, 1984; Maiden, Master , & Borg, 1986; Main, 1978; McManu s, 1994; Mendelsoh n , 1981; Mendelsoh n , 1986; Mendelso hn , 1989; Ruxton & Clemmey, 1986; Steven, 1992; and Steven, 1993). It is readily accessible by road, and has a railroad nearby (Fig M26) . Half a day of look ing at the scarce outcrops , mappi ng and sampling , and a day describi ng core from two boreho l es proved that Freyer was correc t in his apprec i a t i on : the Okatjep u ik o pros pec t could very well be an iron oxide-c op p e r - go l d deposit . Two borehole s drilled at the site were sampled and describe d at the explora- tion office of AngloAmerican in Windhoek. Part of t he sample s collec t ed were analys e d ; they are listed on Table 4.5.5.4 and plotted on Figs 4.2. 4.1 to 4.2.4.3. Although the number of samples is small, some special characteristics emerge; thos e will be described here. Parts of the Okatjepu i k o area have been explor ed by mining corporat i o ns for the past four decade s . Sedimentar y-hosted copper mineralization in the envir on s of the Okatjepu i k o farm has been know n all along. Fig 8.29 show s a few of the known mineral iz ed sites, in the environs of Witvlei , as shown on the Namibia n mineral deposit map. Several author s have describe d mi neralization from Witvlei to be ?typical? copperbelt- type depos its. Very little or no referenc e has been made on previous repor ts about gold, plutonic rocks associ a t e d with minera l iz a ti o n or iron oxide-copp er-gold mineralization. Se veral of the reports make general mention of mafic rocks as a source for primary copper mineraliz ation, but give few details about that issue. A large amount of additional petrographic, mineralo g i c , and hydrothe r ma l alterati o n informat i o n has been produce d , geoche m i c a l and geophys ic a l data from va rious entitie s has been proc es s e d , but will not be included in this document. Further discussion on Okatjepuiko and its associated ir on oxide-copper-gold minera l i z a t i o n is includ ed on sect ion 8.4.1.1 of this document. 4.2.4.2 Field Observations The Okatje p ui k o 154 farm was visited on October 10 th , 2002. Clear evidence of hydr othermal mineralization of Cu (and Au?) was observe d at the farm. Field descri ptions, updated with laborator y results are listed in Appendix A72. The coordinates of all geological statio ns and sampling sites are also in the Appendix . Geolog ical stations and sampling sites are drawn on Fig 8.2.5.4. Some of the rocks display round-cl a s t hydrother m a l brecciat i on overpr in t e d by extreme red-br ow n hematit e alteration. Samples L-644 and L-645 show those features . The origina l clas tic texture of the rock - a breccia cement e d by nephel i n e syenit e - has almost vanished . Both the matri x and clast s of the brecc i a were repla c ed by a pervasive brown-red hematite alteration. Fig 4.2.1. 21 illustrate s these features. The alteration process is gradational. Another significant geoche mical feat ur e of the suite of sample s is t hat felsic rocks associated with mineralization have very little magnetis m. They contain secondary, magnet ite-rich veinlets; but that is a hydrothermal overpr int and not a primar y feature. L-638 was selecte d for complet e chemic a l analysis . This rock is a pink, medium- g r a i n ed , metalum i n ou s leuco- c r a t ic potassic ferrife r ou s alkali granite with magneti t e veinlet s . It seems to be one of the intr usi v es respon s e- b l e for iron oxide-c o p pe r - go l d mineral iz a t i o n at Okatj e p u ik o , and formed in a rift-re l a t ed anorog e n ic environ - ment. Strong magnetism in the rock is due to the high density of magnetite veinlets. It also offers a clear gravime t r ic contras t with the neighb o ur in g rocks. 2 8 3 Table 4.2.4.1 Description of OP-1 Borehole, Okatjepuiko Project, Namibia. Depth in meter s . Depth Description Samples/Photos 0 . 6 2 Bro wn soil 3.85 Dark to light gree n, weathe r e d roc k fragme n t s that crumb l e easil y. Mediu m - g r a i n e d , we ath e r e d , mag ne t i c subv o l c a n i c , porp h yri t i c , p i n k to pink- w h i t e meta l u m i n o u s subl e u c o c r a t i c sodi c fe rri f e r o u s grani t e , wit h black crys t a l s 1-2 mm ?. L-816 * , 3. 21m 4 . 0 0 Same as above , with gra y tinct i o n . 6.00 Weat h e re d , brok e n frag m e n t s of gray, red and blac k "c la ye y" rock s (lam p ro p h yre s ? ) with tint e d surfa c e s . 7.02 Weathe r e d , brok en fragme n t s of yellow to gra y ro ck, as above, but more conso l i d a t e d , coars e grain e d to finer . All rock s from here to the surfa c e are we at h e r e d . 8.90 Dark gra y to gre en, fine-g r a i n e d , microp o r p h y r i t i c volc a n i c rock with 0.5 to 1 mm pl agi o c l a s e phen o c r ys t a l s and abund a n t green epido t e veinl e t s . 8.91 Red grani t i c vein with chlor i t e + epido t e rims. 13.00 Moder a t e l y mag ne t i c , dar, fine- g r a i n e d volca n i c rock with gree n veins . There is a pin k grani t i c vein from 12.13 to 12.14m . 13.13 Dense net wo r k of white and light green veinl e t s wi th chlor i t e and ep ido t e in a dark gra y tra p rock with white and fre en 5-10 mm ? am yg dul e s . Abunda n t hydr ot h e r m a l alt era t i o n . 15.52 Light e r , ver y fine - g r a i n e d intr u s i v e rock with no vei ns . Halo on cont a c t . 17.22 Mediu m densi t y green veini n g in a dark, fine- g ra i n e d dark gre en to black volca n i c rock. Conta i n s secon d a r y Cu mine r a l s 17.77 Dense l y veine d dark trap rock with epido t i z a t i o n in veins and vacuo l e s . 18.90 Dark trap rock, with light amygdu l e s ? 10 mm ?. Epido t i z a t i o n in veins and am yg d u l e s . 22.30 Weakl y mag ne t i c , dark trap rock with fine green ve ins in a mediu m densi t y veini n g pa tte r n . Ph 1,2 30.00 Dark gra y to blac k fine- g r a i n e d tra p rock with fine gr een veini n g and light patch e s of hydro t h e r m a l alter at i o n . Vacuo l e s are filled by some w h a t epido t i z e d pink and white pl agi o c l a s e . The rock is cut by shea r zone s that are fille d with ser pe n t i n e , epido t e and chlor i t e . Ph 3,4, C37 , 29.5m 30.01 Dense green vei nin g . 33.45 Dark rock with ver y littl e fine veini n g Ph 5 34.35 Interm e d i a t e to strong l y ma gnet i c dark green trap rock wi th subm i l l im e t r i c to mill i m e tr i c pink amyg d u l e s . Ph 6 54.00 Dark trap rock with inter m e d i a t e v eini n g densi t y; patch e s of white veins with yello w stain s ; occas i o n a l white am ygd u l e s ? 5 mm ?. Weakl y ma gne t i c due to disse m i n a t e d magn e t i t e . Ph7,8, L-818 , 29.5m 55.45 Denser da rk gra y trap rock with lar ger pink am yg du l e s . Ph. 9, 10, L-819 , 53.6m 60.80 Begin n i n g of pink grani t i c ve ini n g . Mixtu r e of mediu m - g r a i n e d gra y and pink grani t o i d s . L-820 , 57.37m ; L-821 , 60.17m 6 2 . 4 4 Mediu m - g r a i n e d , dark gra y intru s i v e rock with yello w to gree n veins and stain i n g . Inte n s e green stain (seco n d a r y copper carbon a t e and sulpha t e ) at 62.44m . 63.50 Moderately - to weakly-magnetic, f ine-grained, da rk gra y trap rock. With inten s e surfa c e malac h i t e stain i n g at 63.5m . 65.00 Mediu m - g r a i n e d grani t o i d with ink bandi n g . Inten s e green malac h i t e stain at 65.00m . L-822 , 63.75m 6 6 . 0 5 Dark gra y to blac k trap rock with light mottl e d pat ch e s of alter a t i o n and inten s e green Cu stain i n g . L-823 , 65.5m 6 6 . 7 0 Light e r trap rock with pink mo ttl e d patch e s of altera t i o n . 67.70 Medium - g r a i n e d , dark gra y intrus i v e ro ck with oxidi z e d coppe r gre e n speck l e s . 68.13 Pink, mediu m - g r a i n e d grani t o i d th at enclo s e s fragm e n t s of the dark gra y trap rocks . Cut by milli m e t r i c dark gra y vein s . Ph 11, 12 68.60 Mediu m - g r a i n e d , dark gra y intru s i v e s with littl e macro s c o p i c a l l y- d e t e c t a b l e hydro t h e r m a l alter a t i o n . Ph 11, 12 70.00 Weakl y mag ne t i c to non-m a g n e t i c , alter e d , mediu m - g r a i n e d , pink grani t o i d s with enclo s e d angul a r fragm e n t s of the trap rock. Inten s e yello w to green stain i n g and shear i n g at 69.45m . Ph 11, 12 74.80 Intens e l y altere d , green speckl e d , fine-g r a i n e d trap ro ck with gra y ve ins , green coppe r carbo n a t e and sulph a t e stain i n g . Some pinki s h and "quar t z e y " in clu s i o n s (=alb i t e ? ) . A bund a n t pu yrp l e ver y thin veinl e t s that make stoc k wo rk s . Ph 13, L-824 , 72.45m ; L-825 , 75.19m 76.61 Inten s e l y-f r a c t u r e d , pinki s h gra y grani t o i d , with some rounde d frag me n t s . Turqu oi s e c halc a n t h i t e stain i n g along part of the fract u r e surfa c e s . 77.52 Simila r as above, but with more whole, purpl y/ d a r k pink granit o i d rock mixed with gra y trap rock. L-826 , 77.1m 7 8 . 3 5 Dark gra y trap ro ck with black spott y miner a l i z a t i o n ; ve ini n g is maske d by some sor t of hyd ro t h e r m a l alter a t i o n (sodi c ? ). 85.00 Moder a t e l y to we akl y ma gne t i c , mediu m - g r a i n e d pink intr u s i v e that encl o s e s ve ry fin e-g r a i n e d dark gra y tra p rocks. There is gra din g bet wee n medium - g r a i n e d gra y an d pink zones . Ocass i o n a l green / y e l l o w stain i n g in the trap. Ph 14, L-827 , 79.11m ; L-828 , 80.63m 87.27 Dark gra y, fine- to medium- g r a i n e d trap ro ck . With occa s i o n a l whit e quar e t z vein l e t s . 87.55 Pinki s h stai n i n g of the mediu m to dar k gra y tra p ro ck. (= albit i z a ti o n ? ) 92.78 Non-m a g n e t i c to sligh t l y magne t i c , dark gra y tra p ro cks wi th sligh t green stain i n g . Very littl e disse m i n a te d magne t i t e . 100.00 Gra y trap rocks with pink angul a r fragm e n t s and pink subv o l c a n ci grani t o i d rock with dark gra y inclu d e d angul a r fragm e n t s . Ocass i o n a l yello wi s h - g r e e n stain i g of the dark gra y trap rock s , thin whit e vein l e t s , and also some very thin magne t i t e veinl e t s . Purpl e y-p i n k mediu m - g r a i n e d grani t o i d s with bl ack veins . 2 8 4 4.2.4.3 Description of the OP -1 borehole, Okatjepuiko Project Core from two boreho l es drilled into the Okatje p u ik o depos i t were observ ed and describ e d at the AngloAmerican office in Windhoek. Table 4.2.4.1 contains a rapid lit hological log of borehole OP-1. Table 4.2.4.2 lists main informat i o n on the samples collecte d from the boreho le . Sample L-816* was dated, and that will be discussed in the Geochronolog y section below. Figures 4.2.4.7 to 4.3.5.20 show photographs of core from the borehole. Table 4.2.4.1 refers to t he photogr a p hs in order, using number s 1 to 14. 4.2.4.4 Geochemistry Chemic al analysis from samples collecte d at the Okatj e p u ik o pros pec t show strong sodic altera t i o n , Cu en- richment, and general high Pr values (Table 4.5.5.4). All rocks from this area are also enriche d in Ni, Co, Zn, Cr and V. Th and U values are below the limit of detec tion. Values of Rb, Sr, Y, Zr and Nb are very low. Table 4.2.4.2 Samples collected from borehole OP-1, Okatjepuiko, Namibia (T he term ?trap rock? was us e d for mafic, fine-grai ne d rock s that could not be better ide n t ified macrosc o pical l y.) Sample Depth (m) Description L-816* 3.21 Medium - g r a i n e d , we athe r e d , ma g ne t i c , subvo l c a n i c , porph y r i t i c , pink to pink- wh i t e , metal u m i n o u s subl e u c o c r a t i c sodi c ferrif e r o u s granit e L-817 29.50 Dark gra y- b l a c k , fine- g r a i n e d intr u s i v e rock with va cuo l e s fille d by epido t i z e d pi nk and white plagi o c l a s e . Cut by shear zon es fille d with serpe n t i n e , epido t e and c hlor i t e . L-818 38.23 Dark gra y trap ro ck with inter m e d i a t e veini n g densi t y and occas i o n a l white am ygd u l e s ? 5 m m ?. Wea k l y magne t i c due to disse m i n a t e d magne t i t e L-819 53.60 Denser da rk gra y trap rock with lar ge r pink plagi o c l a s e am ygd u l e s L-820 57.37 Mixtur e of mediu m - g r a i n e d gra y and pink granit o i d s L-821 60.17 Mixtur e of mediu m - g r a i n e d gra y and pink granit o i d s L-822 63.75 Medium - g r a i n e d granit o i d with pin k bandin g L-823 65.50 Dark gra y to blac k trap rock with li ght mottl e d am yg d u l e s and inten s e green Cu staini n g L-824 72.45 Intens e l y altere d , green speckl e d , fine-g r a i n e d tr ap rock with gre y ve ins , green coppe r carbo n a t e and sulph a t e stain i n g . Some pink am ygd u l e s th at ma y be fille d by albit e . Abund a n t purpl e very thi n veinl e t s that make stoc k wo rk s . L-825 75.19 Light green -gra y trap rock with pin k am ygd u l e s and inten s e alter a t i o n L-826 77.10 Intense l y-f r a c t u r e d pink-gr a y rock , with some r oun d e d fragm e n t s . Chalc a n t h i t e st ainin g along part of fractur e surfa c e s . L-827 79.11 Modera t e l y to we akly ma gnet i c , medium - g r a i n e d pink intru s i v e with angul a r fra gm e n t s of trap rock L-828 80.63 Modera t e l y mag net i c , medium - g r a i n e d pink intr u s i v e with fragm e n t s of green- s t a i n e d gra y trap rock Table 4.2.4.3 Chemical Analysis, Okatjepuiko, Witvlei, Namibia (Total iron oxides were grouped under FeOt. comple te elemental analysis is on Table A13, Appendix) S a mpl e SiO2 TiO2 Al2O3 FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total Na+K Notch 50.00 1.00 15.50 6.00 0.1 5 0 2 . 0 0 5 . 0 0 4 . 9 0 5 . 5 0 0 . 3 0 2.00 L-625 74.31 0.32 12.49 2.19 0.0 4 0 . 4 2 0 . 9 4 5 . 7 2 2 . 0 0 0 . 1 0 0.70 99.23 7. 7 2 L - 6 2 6 75.44 0.32 12.53 3.15 0.0 5 0 . 5 7 0 . 7 1 5 . 9 9 1 . 0 4 0 . 0 6 0.63 100.49 7 . 0 3 L-633 51.27 1.55 16.00 10.81 0. 1 8 6 . 6 9 7 . 1 7 3 . 7 1 1 . 6 9 0 . 2 6 1.07 100.40 5 . 4 0 L - 6 3 5 62.14 0.98 15.43 6.05 0.1 2 3 . 2 9 3 . 2 8 7 . 3 7 0 . 2 2 0 . 1 5 1.00 100.03 7 . 5 9 L - 6 3 7 69.84 0.53 13.33 5.85 0.0 6 0 . 5 8 2 . 1 9 5 . 9 5 0 . 7 6 0 . 1 0 1.00 100.19 6 . 7 1 L - 6 3 8 77.05 0.18 11.68 2.36 0.0 4 0 . 1 4 0 . 6 2 4 . 2 7 3 . 7 3 0 . 0 2 0.42 100.51 8 . 0 0 L-641 50.76 2.24 13.78 12.16 0. 2 4 6 . 4 9 7 . 3 2 4 . 3 0 0 . 6 2 0 . 4 0 1.90 100.21 4 . 9 2 L-645 56.67 1.27 14.07 9.26 0.0 9 0 . 4 2 5 . 8 7 8 . 4 0 0 . 1 6 0 . 3 3 3.96 100.50 8 . 5 6 L - 6 4 8 72.50 0.35 12.81 4.25 0.0 5 0 . 6 9 0 . 6 4 7 . 2 7 1 . 3 2 0 . 0 6 0.59 100.53 8 . 5 9 L - 6 4 9 73.86 0.30 12.07 4.77 0.0 6 0 . 5 3 0 . 6 4 5 . 7 4 1 . 8 6 0 . 0 5 0.56 100.44 7 . 6 0 L - 8 1 6 * 74.57 0.30 12.43 3.00 0.0 6 0 . 3 9 1 . 3 7 6 . 0 2 1 . 9 6 0 . 0 4 0.44 100.58 7 . 9 8 Sample Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Hf Ta Eu Gd T b Dy Yb Lu Notch 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 10 120 4 30 5 20 8 2 L-625 43 78 49 280 30 <6 15 753 26 15 21 123 493 <6 <15 <10 125 54 L-626 18 64 50 263 30 <6 13 1078 41 17 21 53 609 <6 <15 <10 11 33 66 112 31 39 1 3 1 L-633 56 239 26 123 13 52 115 499 110 17 279 202 550 <6 <15 31 13 16 36 43 11 224 6 1 1 L-635 9 33 31 241 19 20 64 64 46 20 134 101 58 <6 <15 19 9 24 49 67 21 90 1 3 1 1 L-637 17 165 56 727 29 8 18 128 34 20 26 49 359 <6 <15 10 123 61 134 180 93 3 34 1 4 2 L-638 59 91 35 148 18 <6 9 95 29 15 14 66 751 <6 <15 <10 11 8 41 10 116 53 4 1 1 7 1 7 4 1 L-641 27 195 33 131 15 48 90 704 133 17 262 196 247 <6 <15 34 12 46 28 <12 L-645 5 67 38 214 17 9 21 6 21 19 113 185 87 <6 <15 26 49 22 L-648 25 69 21 248 12 6 17 1546 44 13 47 67 1144 <6 <15 <10 89 30 L-649 37 63 16 193 11 9 19 2238 37 11 50 78 1330 <6 <15 <10 74 19 L-816* 43 91 52 284 32 <6 13 104 62 17 18 81 386 <6 <15 <10 116 36 72 122 33 1 33 1 3 1 5 0 5 5 6 0 6 5 7 0 7 5 SiO2% 5 6 7 8 TOTAL ALKALI vs SILICA DIAGRAM Okatjepuiko, Witvlei, Na mibia; Lufilian G.P. (Based on Middlemost, 1994, 1997) S am pl es P et r o g r a p h ic fie ld s L - 6 2 5 L - 6 2 6 L - 6 3 3 L - 6 3 5 L - 6 3 7 L - 6 3 8 L - 6 4 1 L - 6 4 5 L - 6 4 8 L - 6 4 9 L - 8 1 6 Fig 4.2.4.1 Fig 4.2.5.1 5 0 0 1 0 0 0 1 5 0 0 2 0 0 0 2 5 0 0 R1 = 4Si - 11(Na+K) -2(Fe+Ti) 5 0 0 1 0 0 0 R 2 = 6C a +2M g +A l L-625 L-626 L-633 L-635 L-637 L-638 L-641 L-645 L-648 L-649 L-816 R1R2 PLUTONIC ROCK CLASSIFICATION Okatjepuiko, Witvlei, Namibia; Lufilian G.P. (After De la Roche et al, 1980) P e t r o g r a p h i c fie ld s S a m p l e s Fig 4.2.4.2 L - 6 4 8 L - 6 4 5 Fig 4.2.4.3 L - 6 3 3 L - 6 4 1 0 0 . 1 0 . 2 0 . 3 0 . 4 0 . 5 0 . 6 0 . 7 0 . 8 0 . 9 1 F = % Felds p a r s + musco v i t e 1 0 . 9 0 . 8 0 . 7 0 . 6 0 . 5 0 . 4 0 . 3 0 . 2 0 . 1 0 Q = % Q u a r t z 1 0 . 9 0 . 8 0 . 7 0 . 6 0 . 5 0 . 4 0 . 3 0 . 2 0 . 1 0 B = % D a r k m i n e r a l s QBF ternary diagram (afte r Debo n & LeF o r t, 199 4 ) Samples from the Okatjepuik o Farm, Witvlei, Namibia Greater Lufilian Arc Granitoid Project R e f e r e n c e sa m p l e s (D e b o n & LeF o r t ) S a m p l e s L - 6 3 8 L - 6 3 5 L - 6 2 6 L - 6 4 9 L - 6 3 7 L - 8 1 6 L - 6 2 5 2 8 8 Table 4.2.4.4 Statistics of rock types, Okatjepuiko environs, Witvlei, Namibia Based on the modified TAS diagram of Middlemost, 1994. The fifth column (granitoids) is the sum of underl i n ed rock types. Group Rock type number % Granitoids Groups A l k a l i gran i t e 1 9.09 M o n z o n i t e 2 18.18 3 3 . 3 3 Monzog a b b r o 1 9.09 Midalkaline Rocks A l k a l i gabbr o 1 9.09 45.45 Granite 5 45.45Subalkaline Rocks G r a n o d i o r i t e 1 9.09 66 . 6 7 54.55 Total 1 1 1 0 0 . 0 0 1 0 0 . 0 0 100.00 Although the number of samples analysed is too small to be repres entative, statisti c s on their compos i ti o n may be revealing. Two thir ds of the granitoids from the Okatjepuiko deposit fall within the subalkaline field, while one third are midalk al i n e granit o ids (Table 4.2.4. 4 ) . Midalk a li n e and subalk a l i ne rocks are roughl y equal in genera l figures . Gabbro i ds have been under - r e pr es en t ed in the curren t sa mpling; those are more abundant and they seem to play an importa n t role in the iron ox ide- copper-gold mineralization style. On ly a few of the multiple gabbr oid rocks obser ve d were sampl e d . Mafic rocks make over 70% of materi a l inter s ec te d at boreho le s OP-1 and OP- 2, and no mafic rocks from the borehol e s were analysed . Part of those rocks may turn out to be alkaline , includ in g nephelin e syenites . Table 4.2.4.5 Comparison of samples from the Okatjepuiko area, Namibia ( S e e acrony m descrip t i o n on sectio n 2.4.3. ) Sample Rock Name Debon & LeFort Maniar&Piccoli Whalen Pearce Mafic Rb/10HfTa Rb/30HfTa Nb-Ta L - 6 2 5 Granit e metaiv subleu c o Na Fe POG A V1/2 L-626 Grani t e perai i i meso Na Fe POG A OUTU L-6 3 3 Monzo- g a b b r o metaiv meso Na Fe N?Zn arc OUT U L- 6 3 5 Quartz m o n z o n i t e metaiv meso Na Fe OP A V2/4 wp ab OUT U L- 6 3 7 Granit e metaiv meso Na Fe OP A WP WP OUT U L - 6 3 8 Alkal i grani t e metai v leuco Na Fe RRG A S2/4 O2/4 VA- VA INV L-641 Monzo- g a b b r o metaiv meso Na Fe N?Zn V wp ab L-645 Nephe l i n e s yeni t e metav meso Na Fe RRG-CE U G A V wpt L-648 Alkal i grani t e metai v meso Na Fe A V L-649 Alkal i grani t e metai v meso Na Fe RRG N? V L-816* Granit e metav subleu c o Na Fe POG A WP WP OUT U A special feature that stands out on Table 4.2.4.5 is that all rocks displa y a sodic ferrif e r ou s nature . There is a greater propor t i o n of metalu m i n o us mesocr a t i c rocks. Fig 4.2.4.2 shows that the clus t e r of grani t e s has L-816* just in the center. The same is observe d on the TAS diagram (Fig 4.2.4.1). Chemistr y of these granites has been reasonably documented by six samples, listed on Tabl e 4.2.4. 6 . Compar i s on of thes e sample s show s a clear pattern. 2 8 9 2 9 0 Fig 4.2.4.5 Logarithmic major oxide plot, granitoi d samples, Okatjepuiko prospect, Witvlei, Namibia. Fig 4.2.4.6 Logarithmic trace elem ent plot, granitoid samples, Okatjepuiko prospect, Witvlei, Namibia. ( Values below t h e limit of det ection we re estimated to be half of the limit.) Table 4.2.4.6 Chemistry of granitoids from the Okatjepuiko Prospect, Namibia (Extracted from Table 4.5.5.4.) Sam ple SiO 2 T iO 2 Al2O 3 FeO t MnO MgO CaO Na2O K2O P2O 5 Rb Sr Y Zr Nb Co Ni Cu Zn G a V Cr Ba Sc Sm Nd Pr Ce La Hf T a Eu L-626 75.4 4 0.32 12.5 3 3.15 0.05 0.57 0.71 5.99 1.04 0.06 18 64 50 263 30 <6 13 1078 41 17 21 53 609 <10 11.5 33.3 65.5 112 31 L- 637 69.8 4 0.53 13.3 3 5.85 0.06 0.58 2.19 5.95 0.76 0.10 17 165 56 727 29 8 18 128 34 20 26 49 359 10 123 69.8 134. 1 180 93 3.31 3 L- 638 77.0 5 0.18 11.6 8 2.36 0.04 0.14 0.62 4.27 3.73 0.02 59 91 35 148 18 <6 9 95 29 15 14 66 751 <10 7.71 40.9 10.4 116 53 4.36 0.51 1.02 L- 648 72.5 0 0.35 12.8 1 4.25 0.05 0.69 0.64 7.27 1.32 0.06 25 69 21 248 12 6 17 1546 44 13 47 67 1144 <10 89 30 L- 649 73.8 6 0.30 12.0 7 4.77 0.06 0.53 0.64 5.74 1.86 0.05 37 63 16 193 11 9 19 2238 37 11 50 78 1 3 3 0 <10 74 19 L- 816 * 74.5 7 0.30 12.4 3 3.00 0.06 0.39 1.37 6.02 1.96 0.04 43 91 52 284 32 <6 13 104 62 17 18 81 386 <10 116 35.6 72.1 122 33 1.20 0 1.1 Av er age 73.9 0.3 12.5 3.9 0.05 0.48 1.03 5.87 1.78 0.1 33 90 38 311 22 5.8 15 41 16 29 66 763 7 64.2 42.7 70.5 116 43.1 2.96 21 0.9 0.1 1 10 100 1000 10000 L- 626 L- 637 L- 638 L- 648 L- 649 L- 816 A V G Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba Sc Sm Nd Pr Ce La Hf 0.01 0.10 1.00 10.00 100.00 L-626 L-637 L-638 L-648 L-649 L-816 AVG SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 2 9 1 A l l the sample s from the Okat jep u ik o suite, except for L-645 contain very high copper values , as seen on Tables 4.2.4.3 and 4.2.4.6. L-645 is a hydrot h er m a l brecc ia with an int ense overpr in t of hydrother m a l red iron oxide alteration Fig. 4.2.2.21. The high copper values are also shown on the logarith m ic plot of trac e element values for granito i d s in the Okatjep u ik o suite (Fig 4.2. 4.5). An important observation is that coppe r enric h me n t is seen both on mafic and felsic igneous rocks. A portio n of the anomal o us copper conten t in rocks from Okatjepuiko may have secondary origin, in the form of copper carbon a t es , sulfat e s and phos pha t e s hosted in joints and rock cleava g e . Nevert he l e s s , the major propor t i on of the copper has primar y hydrot h er m a l origin . It is hosted in sulfides, iron oxides and silicates that are main rock cons tit u e n ts . Detaile d studies to define the location of copper in the samples were not carried out. The major oxide logarithmic plot for Ok atjepuiko granito i d s shows that they have very uniform chemist r y . One of the main featur es is the high values for Na 2 O. That is probably an indication of hydrothermal sodic alterati o n . The general order of major oxide conc entr a t i o n is: SiO 2 , Al 2 O 3 , Na 2 O, FeOt, K 2 O, CaO, MgO, TiO 2 , P 2 O 5 and MnO. Average values for each of the major ox ides is listed on Table 4.2.4.6 and plotted on Fig. 4.2.4.5. The chemis t r y of trace element s for the suite of granito i d s is also rather uniform. Table 4.2.4.6 lists the values for trac e elemen t s and Fig 4.2.4. 5 show s their logari t h m i c plot. As illustrated, the variation for most of the elements occurs in a narrow range, often less than half of an order of magnitude. Copper is the metal with the greates t relativ e variati o n . Thoriu m values are surpris i ngly low, below the level of prec is e detection. Uranium is also very low. Cobalt values are relatively low, and certain l y far from econo mi c conc en t r a t i o n . The general order of abundanc e of some trace element s is the foll owing: Zr, V, Zn, Nb, Co. That elemental abundance is very char ac teristic and was not obser ved in the ot her sample suites from the Greater Lufilian Arc. The role of the abundant types of mafic and ultramafic rocks includin g alkali ne gabbro s , gabbr o s and lampro - p h y r es observe d in the Okatjepu i k o area is not well underst oo d. Those rocks might serve as source for various metals includ i n g : Co, Ni, Co, Cr and V. Ve ry few sampl e s of mafic and ultrama f i c rocks were analysed, and that information is probably not enough to produce relevant results. Furthe r studies on the mafic and alkali n e rocks should be carried out. 4.2.4.5 Environment of Emplacement Resul ts of some proce ss es to evalua te environm e n t of emplac eme n t for the various rock types are listed on Table 4.2.4.5. The proc edu r e develop ed by Whalen et al, 1989 indicates that all sample s analysed were formed in anoroge n ic envir o n me n t s . Most of the results from other methods produce conflic t in g results . There must have been a signific an t mixing of crustal rocks in t he formati o n of the granito i d s , because the Harris and Pearce diagrams indicate volcanic arc signatur e s . Nevert he l es s , post orogen ic envir o n men t and rift-r e la t e d environment seem to be prevalen t. The hydrothermal al teration that is evident in most rocks probab ly changed their chemis t r y to a point wher e traditi o n a l method s to evalua t e granito i d environm e nt of emplac e me n t are useles s . The granitoi ds from Okatjepu i k o were collected in a relati vely small area. The chemistr y of th e rocks is rather uniform as shown in the last few pages. They pr obably formed in a single tectonic environment; or in a slowly changing environment, such as incipien t rifting that took plac e after post orogenic collaps e. Further studies are curren t l y being done with neural web software to compare geochemistry of several thousand samples with Okatjepuiko rocks. This is expected to help define the tectonic envir onment of emplac e me n t for the granito i d s . 4.2.4.6 Geochronology A zircon concen t r a t e from a single sample in the Okatj e p u ik o area was dated at the ANU in Canberr a . Sample L-816* came from a subvolcanic, porphyritic, metalumino u s subleuc oc r a t ic potass ic ferrife r o us granite in borehol e OP-1. A compos ite of zircons from various parts of the same granito id was dated using radio me tr ic U-Pb SHRIMP II techniques. It gave an age of 1097. 6?5.9 Ma. Xenocrys tic zircons in the same sample indicat e d ages of 1194.6? 1 1 Ma and 1871?6. 8 Ma. The sample comes from one of the plutonic bodies respons i b le for copper and gold mineral i z a t i o n at Okatje p u ik o . The sequenc e of rocks that holds copper minera l i z a t io n at the Witvle i sedime n ta r y - ho s t ed copper deposi t was dated in the Ghanzi section, Botswana , at 1106 Ma, on a confor ma b l e , largely volcanic materia l [Schwar tz et 2 9 2 al, 1996] (See event 72 on Table A22.18 and on the event diagram of Fig A43). Subvolcanic intrusive rocks associat e d to IOCG minerali z a t i on at Witvlei (Okatjep u ik o farm) were dated in this projec t at ~1098 Ma. The question that immediately comes to mind is: Ar e these two types of mineralization related? 4.2.4.7 Other Events of the Same Age in the Region Many radio me t r i c ages are avail a b l e fr om Souther n Africa around 1098 Ma. Table A22.18 a selecti on of zircon U-Pb geochronolog ical data from that lapse of time. The event diagram of Fig A43 illustrates the density of ages and great tempor al continuity of the sp read of data available. Data from sample L-816* has been highlighted there for comparison. The last decad e has seen a very large amoun t of geochr o n o lo g ic a l data been produc e d on the circa 1100 Ma volcanic and plutonic belts of Souther n Africa, includin g t he southern portion of the Greater Lufilian Arc. It is common know ledge now that the time span of the grani toi ds and volcan ic s extends continuously from 1250 Ma to 1000 Ma as listed on Table A22.18 and show n on Fig A43. The plutonic-magmatic belt extends for several thousand s of kilometers along the border of the Kalaha ri Craton . It is not so well exposed under the Kalahari des er t, and that area is prec isely in the middle of the Greater Lufilian Arc granito i d project. Recent work in parts of the Irumide and Kibaran bel ts of Zambia and the D.R.Con go by DeWaele and co- wor k ers [De Waele, 2004; and De Waele, Fitzsi m o ns , & Nemchin, 2004 (as well as dozens of papers cited in the referenc e section ) ] have great ly enhance d the knowled g e of the circa 1100 Ma age span. The Namibia n and norther n South Africa counte r pa r t has had abunda n t work done in recent decades and literally hundreds of geochronological data are available (See referenc es in Table A22.18). The Ghanz i - C h ob e ridge in Botsw a na is an area that co rrelates well with the Witvlei granitoid and sedimentary sequence. According to Singletary et al., 1998 bimoda l volca n ic rocks occur in the north- e as t - t r e n d i ng Ghanz i - C h ob e ridge. They state that ?the Ghanzi- C ho b e Ridg e volcanics occupy a rift superimposed on a pre-exis ting Kibaran orogenic belt continuous with coeval terranes to the north in Zambia, and to the south in the Namaqua belt of South Africa? (Singletary et al., 1998). Mafic volcan ic rocks have been identi fi e d in the circa 1100 Ma belts in Namibia . Amygdal o i da l basalts , quartz i t e s , conglo m er a t es and acid volcan i c rocks in the Rehoboth-Witvlei area were intrud ed by granites of the Gams be r g Suite and numer o us diabas e and quartz porphyr y sills and dikes (Mille r , 1992). Underfo r m ed quartz -feldspa r porphyries and pyroclastic rocks of circa 1100 Ma are found in several location s, includ ing the Nuckopft and Guperas formations (Miller, 1992). Pfurr, Ahrendt, Hansen, & Weber, 19 91 publis h e d Rb-Sr ages of 1049? 2 8 Ma for volcan o- sedimentary units in the Rostock massifs of t he Southern Marginal Zone of the Damara Orogen, Namibia, and maximum U-Pb zircon ages of around 1200 Ma. In general , a period of granito i d emplac e me n t and volcan i c activit y between 1200-105 0 Ma is indicat e d by the results . That is prec isely what Fig A43 shows. Pf urr and co-work e r s furth e r state that the emplac ement of the ( circa 1100 Ma) igneous rocks is rela ted to collision - i n d u c e d rifting , comple mentar y to the Kibaran Orogenesis. Further SHRIMP geochro no l o g ic a l data from the Okatj ep u ik o deposit may help to better define the geologic a l evolution of this prospective area. 4.2.4.8 Evidence of Iron Oxide-Copper-Gold Mine ralization and Definition of a Mineralized Belt The Okatjep ui k o mineral iz a t i o n lies in the middle of a rectangular 3 x 6 km magnetic anomaly produc ed by a cluster of many small magnetic bodies of subvolcanic porphyritic intrusio ns . The Okatjepu iko pros pect lies in the center of the anomalous zone, just in the middle of a small granitic intr usio n. Ot her eviden ce of a suitab le environm e n t for the pres en c e of iron oxide- c o p pe r - go l d minera l iz e d syst ems in the envir o ns of Okatje puik o includ es dissemi n a t i o n of copper sulfide s in granite s and mafic lavas, explos ive brecciation, abundant pres e nc e of secon d ar y coppe r miner a ls and stockwo r k i n g . Gabbros as well as felsic intrus i v e rocks outcrop in the area. Subr ound e d- c l a s t hydroth er m a l breccias with in tense brown-r o c k and red-roc k (iron oxide) alterat i o n also outcrop . Vuggy massive magnetite and hematite fr agments occur as float; in fact, a strong magnetic anomaly guided exploration to the site. Among the types of hydroth er m a l alterat i o n observed are sodic alterat i o n and progres s i v e hematit i z a t ion that overprin ts previous text ures to a point where they are unrec ognizable. All of these ingredien ts point to an ir on oxide- co pp e r - g o ld mineraliz a t i o n at depth, under the previous ly identified sedimentary-ho sted copper deposit. Gold is not present in the sedimentar y-ho sted copper deposit; it probably remained undernea th in the original hypogene deposit. 2 9 3 Evidence of IOCG mineralization under at least one of t he sedimen t a r y - ho s t ed copper deposit s of Namibia is very importan t . The pres en ce of both hydrother m a l cop per and gold under the Witvlei deposit is relevant to understan d the regional metallog e n y , and could lead to a completely differen t source for copper in the Greater Lufilian Arc. The model of mineralization identified at the Okatjepui k o farm is not restrict e d to the environ s of Witvlei; it can be applied along the NE and SW extens io ns of a belt made of rocks with similar chemis try and age that occur along more than 600 km across Namibia and Botswana . The entire ?Kalaha r i Copper Belt?, as describe d by Maiden et al, 1984, could be pros pec t i v e for IOCG mi neralization. The belt has been given different names. This type of mineralization probably extends NW into the well defined Ghanzi-Chobe Belt, of Botswana (Modie, 2000); and SE into the Rehobot h and Helmer i n g ha u s e n areas of Namibi a . Borg, 1995 consid e r s that the belt is an aborted rift basin that underwent tectonic inversion. 4.2.4.8 Conclusions 1. The Okatjep ui k o prospec t has all the char ac t e r is t i c s of an iron oxide-c o pp er - gold deposit . 2. Sodic ferriferous felsic granitoids that are closely associated with fine-grained mafic rocks were emplac ed in an anor oge n i c environme n t into silici c la s t ic , ca rbon a t e and volc an ic sequenc es and they produc e d the iron oxide-c op p e r - go l d mineral iz a t i on . The chemis try of the granitoids is reas onably well defined. That of associa t e d mafic and ultrama f i c roc ks is not that well cons train e d . 3. There are many radiom e tr i c ages around 1100 Ma in the enviro ns of the Great er Lufilian Arc. There seems to have been a widespre ad , tempora l l y and spatially continuous volc ani c and pluton ic anorogenic belt from 1250 to 1000 Ma. 4. More than 90% of the samples analysed from the Okatjep u ik o suite contain highly anomalo us copper conc en trations. Both mafic and felsic igneous ro cks show that enric hment. Although a portion of the copper conten t is the produ c t of seconda r y migr at i o n in to joints and rock cleavag e , most of the copper has primar y hydrotherma l origin. It is hosted by sulfi de s , iron oxides and silicat es that are main rock cons tit u e n ts . 5. The fact that sample L-816* (and probably other granito ids like L-638 ) was emplac e d at 1097.6? 5 . 9 Ma is very significant. It proves the juxtaposition of an ir on oxide- copper-gold mineralization undernea th the sedimentar y-hosted copper deposit at Witvlei, Nami bia. This metallogenic event occurred at 1110 ma. Second ar y copper in the sediment ar y - h os t e d deposit probably came from the IOCG deposit that lies undernea t h . This idea may generat e a new conc ept for the origin of the Copperbe l t copper and cobalt deposits . That concep t is a major breakt h r o u gh . It could ch ange the geolog i c a l model of formati o n for the well- en d ow ed Zambian Copper b e l t , and could help devise new wa ys to explore for base metal deposits in the Lufilian Arc and elsewhere. Phenomena similar to that of the Witvlei - O k a t j e p u ik o pair might have taken place in many locations, throughout geological time. There is additional evidence of IOCG mineralization related to sedimen t - h os t ed copper in other parts of Namibia and Zambia. This topic will be dealt on Chapter 8, section 8.4.1.1 . 6. Finding IOCG and related sedimentar y-hosted copper mi neraliz a t io n at Witvlei is also signific a n t becaus e it opens an entire new age gap for the exploration of base metal deposits in the Lufilian Arc and in the surround in g environme n t , includ in g South Africa. 7. All the mineral i z ed rocks from Okatjep ui k o are pris tine . There is no significan t deforma tion involved. The mafic volc anic rocks show some foliation and shearing, but mineralization seems to have taken plac e after the deformation. Hydrother mal brecci at io n and other mineraliz a t i on features are un-de for med . This may be very useful to study mineralization and alteration processes. 2 9 4 Fig 4.2.4.7. Photo 1. Trap rock breccias from 18.20 t o 2 2 . 0 m; from borehole OP- 1 , O katjepuiko, Witvlei, Namibia. Notice abundant evidence of shearing. Part of the fractures in the mafi c rocks show s erpentinite. Fig 4.2.4.8. Photo 2. Enlargement with detail at 19.77 m from borehole OP-1, Okatjepuiko, Witvlei, Namibia. Note copper mineralizati on associated with hematite that fills part of the veinlets in a stockwork. 2 9 5 Fig 4.2.4.9. Photo 3. V o lcanic rocks with vacuoles and dens e v einlet n e t w ork. The s e occur around 26 t o 2 9 m of borehole OP-1, Okatjepuiko prospect, Witvlei Namibia. Fig 4.2.4.10. Photo 4. C l o s e- u p o f Fig 4.2.4. 8 . D e tails of pink zeol ites (?) and very thin white veinlets . Part of the v einlets and vacuoles are filled by albite. From borehole OP - 1 , O katjepuiko, Witvlei, Namibia. 2 9 6 Fig 4.2.4.11. Photo 5. Beginning of hydrothermal brecciation, 33 to 34 m, borehole OP-1, Okatjepuiko, Witvlei, Namibia. Also note signifi cant shearing in the mafic rocks. Fig 4.2.4.12. Photo 6. Clos e-up of photo 5, centered on letter M. Beginning of hy drothermal brecciation. 2 9 7 Fig 4.2.4.13. Photo 7. Breccia with abundant chlorite that fills open spaces and veinlets, after 34m, borehole OP-1, Okatjepuiko prospect, Namibia. Fig 4.2.4.14. Photo 8. 4 core fragments, marked with different alte ration types. Note overprinting of veining, part of which is albite. The base is to upper left. 47 to 50 m. Borehole OP-1, Okatjepuiko, Witvlei, Namibia. 2 9 8 Fig 4.2.4.15. Photo 9. Beginning of the pink granitoid 54-57 m. Note intrusive brecciation. Borehole OP-1, O katjepuiko. Fig 4.2.4.16. Photo 10. C lo s e- u p o f p hoto 9 , o n t h e pink granitoid . Borehole OP-1, Okatjepuiko, Witvlei, Namibia. Fig 4.2.4.17. Photo 11. Breccia with angular fragments of v o lcanic rock (68 m, 6 9 m and 70 m) . From borehole OP-1. 2 9 9 Fig 4.2.4.18. Photo 12. I n trusive rock in the middle line of core, surrounded by dark volcanic trap rocks. Upper left is bottom. Borehole OP-1, Okatjepuiko, Witvlei, Namibia. Fig 4.2.4.19. Photo 13. Core showing angular fragments of pink granitoid within dark gray trap rock, from 73- 75m. The third fragment is taped. Borehole OP -1, Okatjepuiko prospect, Witvlei, Namibia. 3 0 0 Fig 4.2.4.20. Photo 14. Core fragments from 79-82 m. At 79 m there are thin black, magnetite veinlets in stockwork. Angu lar fragments o f b lack volcanic rocks and pink granitoid. Borehole OP-1, Okatjepuiko, Witvlei, Namibia. 3 0 1 Fig 4.2.4.21. Slabs of strongly hema titized polymictic hydrothermal br eccias from Samples L-644 and L-645. T h e le f t p h o t o graph was taken from a dry slab, while the o t her two w ere taken from a wet slab. Wetting enhances the contrast of th e particles. The first two come from the sam e slab of L-644 ; the middle photo is a close- up o f t h e first. The t hird photo comes from L-645 . O n t h e s econd and third photos , n o t e t h e angularity and variability of t h e clasts. Th e matrix has been almost complete l y replaced by h e matite. Th e rock as a whol e has a deep red-brown color. Abun dant albite veining and strong albi tization account for the rocks ? induration. When hammered it produ ces a strong bell tinge. T his type o f rock forms large outcrops in the en virons of t h e O katje puiko prospect. Its s urface weathers to a deep brown color. In a few cases, the s urface is tinted by t hin layers of secondary cop per carbonates, ph os phates and sulp hates. That takes place, ev en when the copper content is very low. For scale, centimeter bars on the left, and millimeters on the middle and right photos. 303 5 THORIUM CONTENT OF SOME GRANITOIDS IN THE GREATER LUFILIAN ARC 5.1 Introduction As discussed on section 4.1.2.5, eight samples from the Kafue Flats area were found to contain extremely high values of thorium. Th enrichment in those rocks is more than ten times the average value for most granitoids in Zambia and Namibia. Abundance of Th in an igneous rock enables it to act as a long-lived heat engine. This can generate and focus hydrothermal fluid flow for a long time; and possibly is a key ingredient for the occurrence of certain types of iron oxide-copper-gold mineralization. A simple method to determine the Th content of a rock is using a radiometer. Such machines can directly measure radioactivity due to uranium, thorium and potassium. The tools may be taken to the field or flown. Field mapping of radioactivity in rocks could indicate localities with high counts and serve as a guide in the location of various mineral exploration targets. 5.2 High Thorium Samples Most of the samples collected by Pepper, 2000 (at Kalengwa, the Hook Granite and the Nchanga Granite, Zambia) contain anomalous Th. These are labeled with a P- prefix on Table 5.1. Pepper probably sampled granitoids in sites where significant mineralization was present and known. One conclusion derived from reviewing his work is that thorium enrichment is a key element for mineralization. High thorium values were observed in granitoids from northwestern Zambia, the Nchanga Red Granite, the Hook Granite, as well as in the Ugab River, around Otjiwarongo, Grootfontein and the Okwa River (Table 5.1). Table 5.1 High Thorium Values from Greater Lufilian Arc Granitoids (Sample numbers without a prefix are ?L-? samples. Those from the Otjiwarongo batholith labeled with a double consonant prefix were collected by AVMIN.) Region Samples Kafue Flats, Zm 208, 210, 212, 213*, 214, 215, 218 Hook Granite Batholith, Zm 012, 012A, 257, 409, 436, 439, P-39, P-50, P-53, P-57 Kalengwa, Zm 324, P-13, P-17, P-26 Kalene Hill/Mwinilunga, Zm 020, 030, 060, 364, 370, 377, 421 Nchanga Granite, Zm 151, 153, 154, 172, 173, P-28, P-29, X-34 Kamanjab Batholith, Nm 850 Ugab River, Nm 793 Oas Farm, Nm 670, 675, 697, 699 Otjiwarongo Batholith, Nm 1037, 1038, LJ1, LL11, LL14, LL4 AVMIN pegmatite, Nm 815 Grootfontein, Nm 1043, 1045, 1046 Okwa River, Botswana 600A, 602, 605, 606 Okatjepuiko, Witvlei, Nm None As indicated in earlier chapters of this document, chemical parameters of some syenites and alkali granites from the Oas Farm, the Hook Granite and the Otjiwarongo batholith are very similar to each other. Thorium enrichment in the Nchanga Granite is of a different nature from that of the Kafue Flats. The chemical signature of intrusive rocks there does not match its counterpart of the Hook Granite, Otjiwarongo Batholith and Oas farm. None of the Namibian Damara granites reported in the literature are known to have Th values as high as those found during this research project (Becker & Brandenburg, 1997; Becker, Diedrichs, Hansen, & Weber, 2000; Haack, Gohn, & Hartmann, 1983; Jung, Mezger, & Hoernes, 1998; McDermott, Harris, & Hawkesworth, 2000; and Seth, Okrusch, Wilde, & Hoffmann, 2000). Very little information was available on geochemistry of Zambian granitic bodies (Griffiths, 1978a; and Griffiths, 1978b) The mineral form in which the thorium enrichment resides was not studied during the Greater Lufilian Arc granitoid project. It is not clear if the high thorium content is a primary feature or a secondary overprint brought in with hydrothermal alteration. Note for example, the case of P-28 and P-29 from the Nchanga Granite. After searching for multi-element matches for geochemical parameters of thorium-rich samples from the Kafue Flats, best matches came from NW Zambia, the Hook Granite Batholith, the Oas Farm and Otjiwarongo. Results are listed on Table 5.2. Most of the rocks have a significant enrichment in Al, Na, Zr, Ce, La and some 305 306 are earths; part are also enriched in Y, Zn and Ga. Samples from the Hook Granite Batholith differ from the rest because they have high K and low Na values. Notably, no samples from the Kamanjab Batholith have a chemical signature precisely like that of the Kafue Flats thorium-rich rocks. Another surprising fact was to discover that none of the granitoids from Witvlei, Namibia carry anomalous Th or U. High thorium samples from the Nchanga Granite did not match the Kafue Flats? chemical signature. Nevertheless, they are highly enriched in thorium. P-28 is the only sample with a signature similar to rocks from the Kafue Flats, but its chemistry is intensely modified. Probably the high values of rare earths were brought to it by hydrothermal processes, at the same time as the sodium alteration took place. This topic has to be studied in greater detail. 5.3 Values for High-Heat Generating Granitoids Calculations were carried out to define the calorific properties of the rocks from the Greater Lufilian Arc that contain anomalous thorium. Heat generating capacity calculations involve K, Th and U, which are the radiogenic elements that contribute the most, and are listed in order of increasing importance. According to Klominsky, Partington, McNaughton, Ho, & Groves, 1996, high-heat-producing granitoids have the following values today: Equation No. 3A For comparison, a few A values of known batholiths are listed on Table 5.3. Table 5.3 Heat production values for various high-heat producing granitoids (in ?W/m 3 ) Granitoid A value Reference Cornubian Batholith, Britain 4.0 ? 5.7 Webb, Tindle, Barritt, Brown, & Miller, 1985; Lee et al, 1987 Bushveld granites 4.3 ? 12.8 McNaughton et al, 1993 Northern Australia 5.7 ? 6.3 Solomon & Heinrich, 1992 Young Intrusive Suite, Cullen Batholith, Australia 6.69 Klominsky et al., 1996 Early Intrusive Suite, Cullen Batholith, Australia 5.70 Klominsky et al., 1996 Transitional Intrusive Suite, Cullen Batholith, Australia 5.71 Klominsky et al., 1996 If a value of A?4 is taken as anomalous for heat producing in granitoids, ninety-nine of the granitoids sampled in the Greater Lufilian Arc are high-heat producers today using equation 3A. This is approximately a fourth of the samples analised and that is very significant. A table with estimated heat production value of all samples at their approximate age of emplacement is very useful to evaluate which of the regions were high heat producers throughout the geological history. Corrections must be made using the rocks? approximate age of emplacement. The formula to calculate these values comes from Gibson & Jones, 2002. The heat producing capacity of all the samples was estimated for the time of their emplacement using Equation No. 4. Precise age of emplacement is unknown for many of the igneous rock units studied in the Greater Lufilian Arc. Nevertheless, an estimate of their age has been made in order to obtain values for the heat production capacity [H(?)]. Table A76 in the Appendix lists results of the calculation for all samples from this project. Seventy of the samples collected from the Greater Lufilian Arc turned out to be high heat producers at the time of emplacement using that equation. Samples with the higher values from that table are included on Table 5.4. A= 0.081 (K2O) + 0.261 (U) + 0.072 (Th) A is expressed in ?W/m3, K2O is in %, U and Th are expressed in PPM. H(?) = [0.9929 x 0.0918 x M U x e(0.1551?) + 0.071 x 0.5726 x MU x e(0.98485?) + 0.256 x MTh x e(0.0498?) + 0.348 x MK x e(0.554?)] x ? x 10-4 H(?) = heat producing capacity of the rock in ?W/m3 MU = uranium content of rock in ppm MTh = thorium content of rock in ppm MK = potassium content of rock in percentage Equation No. 4 ? = density of rock in kg/m3 ? = age of rock in billions of years 307 308 6 GEOCHRONOLOGY 6.1 Introduction One of the main objectives of the project was to define the age of emplacement of key granitoids in the Greater Lufilian Arc. This chapter presents the main findings and results in this respect. The first section presents the new radiometric ages obtained. The second, describes the database of radiometric ages compiled for the project, and several diagrams devised to evaluate geochronological information. The third section discusses a few Re-Os ages that were obtained from sulfides in the Zambian Copperbelt. In mature, well-studied and mapped regions, a single age does not mean much. On relatively un-studied regions, a single age may represent the only evidence or a major geological event, and should be treated carefully. 6.2 New Radiometric Ages Twenty seven samples were selected for zircon U-Pb radiometric dating, and 38 new ages were obtained. 10 of them by laser-ablation ICP-MS techniques at the Memorial University of Newfoundland, Canada, by Marc Poujol and his research group; and 28 by SHRIMP II at the Australia National University1 by Richard Armstrong and his research group. Table 6.1 compiles all the new ages in chronological order, and Table 6.2 lists them by sample number. Raw data from each of the geochronological laboratories is presented in Appendix A77. The diagrams to interpret radiometric ages are presented in Appendix A78. A few of the tables and diagrams are missing, because they have not been produced by the ANU. As discussed in the introduction, a few of the ages sent to Australia have not been completely processed. The samples dated have been presented and discussed in each of the relevant sections of this document. The new radiometric ages helped to define ten discrete events of magmatism. These are listed on Table 6.3. Table 6.3 Events of magmatism identified in the Greater Lufilian Arc based on the new radiometric ages obtained Event of magmatism Time Lapse (Ma) Period No. of ages Associated Mineralization 1 534 - 555 Neoproterozoic 4 IOCG 2 742 - 770 Neoproterozoic 9 IOCG 3 875 - 885 Neoproterozoic 1 IOCG? 4 1091 - 1013 Mesoproterozoic 1 IOCG 5 1682 - 1710 Paleoproterozoic 2 - 6 1745 - 1755 Paleoproterozoic 1 - 7 1850 - 1890 Paleoproterozoic 9 Disseminated Cu 8 1920 - 1951 Paleoproterozoic 4 IOCG 9 1966 - 1986 Paleoproterozoic 1 Disseminated Cu 10 ~2500 Archean 2 - 6.3 Geochronological Database and Interpretation A total of 512 radiometric ages from Namibia and Zambia were compiled, including 38 produced for this project. The majority of those ages come from zircon U-Pb. Tables A21 and A22 present the compilation. Table A21 lists all the ages in chronological order, and Table A22 discriminates the data by country and by regions within the countries. The geochronological database serves as background for the evaluation of the new radiometric ages obtained. 1 The Australia National University will be refered to as ANU. 309 6.3.1 Event Diagrams Data from Table A22 was used to produce a series of event diagrams (Figs A23 to A49) that help to visually understand the temporal and spatial distribution of the dated events. The numbers on the lower portion of the event diagrams refer to numbers on the first columns of the corresponding tables in Appendix A22. The event diagrams have been used throughout this document to discuss aspects of the geology of the Greater Lufilian Arc. They were used to interpret the areas of study for the project. 6.3.2 Compilation of Event Diagrams In the event diagrams, intrusive events are just as important as the hiatus between them. The main event diagrams from the Greater Lufilian Arc were interpreted in terms of lapses of intrusion and hiatuses. That information was compiled in a series of correlation diagrams. The principal lapses of intrusion were labeled with letters. The correlation diagram for Zambia is Fig A79. The correlation diagram for Namibia is Fig A80. The complete diagram for the Greater Lufilian Arc is Fig A81. It was broken in two for ease of interpretation: Fig A82 is the first portion, from 3000 to 1400 Ma; Fig A83 is the second portion, from 1400 to 0 Ma. Many observations can be made from the correlation diagrams. A few of the lapses of intrusion occur throughout the Greater Lufilian Arc. Others are more restricted. One of the main observations is that there has been an equal amount of intrusive events through time. That can be deduced from observing the event diagrams for entire countries. Fig A35, the event diagram for all information from Zambia, has continuous events with very short hiatus. Fig A48 has longer hiatus. The geochronological data available for the Greater Lufilian Arc does not display any periodicity of intrusive events, nor displays a net increase or decrease in intrusive activity. The following are some observations from the geochronological correlation diagrams. 1. Tectonothermal event C is widespread in the Greater Lufilian Arc. 2. Hiatus of U is widely spread, as well as hiatus R and those of S1 and T, and V. 3. Intrusive events of local extension are: A, B, H, J, M, P, S, Y, Z, AC and AF. 4. In general terms, the geological history of the Mkushi, Mufulira, Copperbelt Basic, All Basement to the Coperbelt, and NW Zambia areas are very similar to each other. Evidence from geochemistry shows that they were emplaced in similar environments, and display equivalent tectonic and magmatic events. 5. The Zambian Lufilian Arc and Damara region of Namibia did not behave in a similar way from 2200 to 2000 Ma. They probably were independent entities. They also behaved significantly different from 1400 to 850 Ma. 6. Events D are important in the Kamanjab environs as well as in the whole of Namibia. 7. Geological history for the Khorixas Inlier and the Kamanjab Batholith are significantly different. They probably were not in the same geographic position all the time. The circa 750 Ma tectonothermal event is not known in the Kamanjab. Older basement is known in the Khorixas Inlier than at the Kamajab. This is discussed in more detail in section 4.2.1.13 8. Events K, M, N and O are not generally present in Namibia. Event N is present in the Kamanjab environs; M is present in Central Namibia. 9. Event L is important at the environs of Nchanga, as well as events E, D?, D and C. 310 311 312 6.4 NEW Re-Os AGES FROM COPPER MINERALIZATION IN THE ZAMBIAN COPPERBELT 6.4.1 Basic Data Re/Os ages on sulfides from copper mineralization collected in the Zambian Copperbelt, indicate that there is a significant overlap of mineralization with intrusion ages of granitoids described in this research project. A five-point isochron with analyses from chalcopyrite, carrolite and bornite from the Nkana, Chibuluma and Nchanga deposits, produced an age of 583?24 Ma, and a 187Os/188Os initial value of 1.22?0.13 (MSWD=0.67). This was indicated by Barra, Broughton, Ruiz, & Hitzman, 2004 and (Ruiz, J., personal communication, August, 2004). According to the authors from the University of Arizona, the sulfides have Os concentrations that range from 24 to 75 ppt and Re concentrations between 0.6 and 5.8 ppb (Fig 6.4.1). A later version of that age provided by Ruiz (Ruiz, J., personal communication, December, 2004) is 576?41 Ma based on seven points with a 187Os/188Os initial value of 1.37?0.32 (MSWD=4.0) (Fig 6.4.1). This is definitely not a chance issue. A growing amount of evidence points in the direction of a discrete mineralizing event at around 583 Ma. Barra et al., 2004 assume that the mineralizing event is related to the Pan African orogenic events. A Re-Os molybdenite age of 525.7?3.4 Ma was determined by the same group of researchers for mineralization at the Nkana mine. In this case, the molybdenite gave concentrations of 1789 ppb for Re and 325 for Os. This proves that there were at least two mineralizing events at Nkana. The other age reported by the working group of the University of Arizona headed by Ruiz is 825?69 Ma for copper mineralization at the Konkola deposit, with a 187Os/188Os initial value of 11.4?1.7 (MSWD=1.8) (Ruiz, J., personal communication, December, 2004). An earlier version of that age was 776?150 Ma with a 187Os/188Os initial value of 10.8?5.5 (MSWD=1.7) (Ruiz, J., personal communication, August, 2004). These new ages are quite relevant, because they may serve as evidence of an older age for deposition of the Katangan sediments, and as an age of mineralization. The geochronological information is within error of the ages recorded for some dikes sampled under the Nchanga open pit during this research project (L-172c and L-169). Armstrong, Robb, Master, Kruger, & Mumba, 1999 found that the Nchanga Granite was emplaced at 877?11 Ma. This age overlaps with that of copper mineralization at Konkola. Furthermore, there is Nchanga Granite-like chemistry in granitoids from the Konkola deep borehole. This indicates that there were at least three discrete mineralizing events in the Zambian Copperbelt. One centered on 825 Ma, a second on 583 Ma, and a third on 525 Ma. Table 6.4 presents dated events associated with three main copper events known in the Greater Lufilian Arc. Fig 6.4.2 illustrates the timing of the three events. 6.4.2 Discussion One of the questions that comes to mind after analysing the Re-Os ages is ?Could the waning anorogenic intrusive events related to the Nchanga Granite have produced copper mineralization at Konkola and Nchanga?? There might be a probable relationship between the anorogenic intrusion of the Nchanga Granite and copper mineralization at Nchanga and Konkola. Given the evidence, a magmatic-related origin seems reasonable for at least one of the copper-cobalt mineralizing events in the Nchanga and Konkola area. The presence of Nchanga-like intrusives in the Konkola deep borehole indicates that this possibility is very certain. There might be several high-thorium anorogenic granitic complexes like the Nchanga Granite that lie unidentified underneath the rift-related basin where the Katanga sedimentary sequence was laid. The deposition of the Katangan sequence of sediments must have taken place very soon after the intrusion of the anorogenic Nchanga Granite ring complex (dated at 877?11 Ma by Armstrong et al., 1999). There must have been rapid uplift or tectonic tilting in a rift environment to allow for the volcanic facies of the ring complex to be eroded, the lower Katanga deposits to cover the Nchanga Granite unconformably, and later for intrusive events related to the waning activity of the Nchanga Granite ring complex to intersect the recently deposited and mineralized (?) Kantangan rocks. Currently available resolution of radiometric ages to date mineralization, is not enough to develop a more specific sequence of events. But mineralization took place soon after the anorogenic events of intrusion. Mineralization probably took place around 760 Ma. That age is also within the error of Re/Os data provided by Ruiz and his working group at the University of Arizona, and is one of the ages for IOCG mineralization that comes out from the Lufilian Arc Granitoid project both in Zambia and Namibia. 313 Fig 6.4.1 Re-Os ages calculated by Joaqu?n Ruiz and collaborators at the University of Arizona. (Ruiz, J., personal communication, 2004.) 314 Two well-represented epochs of anorogenic granitoid intrusion that occur throughout the Greater Lufilian Arc and have been studied in this project are: (1) the sporadic, but widely distributed, small igneous intrusions at 750?50 Ma; and (2) the widespread and voluminous granitoid magmatism at 550?50 Ma (Table 6.4 and Fig 6.4.2). Both of these epochs are related to iron oxide-copper-gold mineralization. If we were able to associate the second period of IOCG mineralization (~550 Ma) to the copper-cobalt mineralizing event recorded by (Barra et al., 2004) for Cu-Co mineralization at several mines in the Copperbelt (583?24 Ma), we have one concordance between IOCG mineralization and so-called sedimentary-hosted Cu-Co mineralization. If we relate the ~750 Ma age of IOCG mineralization with the 825?69 Ma copper mineralization at Konkola, we have another concordance between IOCG mineralization and sedimentary-hosted Cu mineralization. This could mean that there is some sort of link between IOCG and sedimentary-hosted Cu mineralization in at least three discrete periods of geological time in the Greater Lufilian Arc (the Witvlei area and the Zambian Copperbelt) (Fig 6.4.2). That probably happened more often, but is not yet documented from enough locations to call attention of researchers. This three-legged coincidence might be more relevant than considered at first. It could mean that there is a direct tie between both types of deposits. Maybe the origin of copper in sedimentary-hosted copper deposits has a clear source in magmatic-related IOCG events. Maybe the rapid erosion of the surface expression of mineralized IOCG systems gave rise to the Cu-Co Sedimentary-hosted Cu deposits. The origin for cobalt in the Copperbelt and in other sedimentary-hosted copper deposits has been a mystery. Epigenetic IOCG mineralization certainly could provide copper, cobalt and other related metals. Zinc enrichment in anorogenic syenites and alkali granites may be the single source, or one of multiple sources, for the large economic zinc mineralization known in the Greater Lufilian Arc. As seen on Table 6.4 and Fig 6.4.2, the Copperbelt 1 series of events might have ocurred as follows: after the emplacement of the Nchanga Granite (event 11), large-scale hydrothermal convection of fluids was established and powered by the high-heat producing nature of the Nchanga Granite and other similar bodies like the Konkola Granite. Copper mineralization took place at Konkola and in the Copperbelt (10, 9), then dikes were emplaced into Katangan rocks (8), later came the regional event of intrusion and IOCG mineralization (7). Notice that the error of event 10 allows it to have taken place during an extensive time range. In a similar way, event 7 has a long range of time. Copper and cobalt mineralization could have taken place at any time after the emplacement of the Nchanga Granite and deposition of the Kagangan sediments. The dikes that intersect Copperbelt mineralization under the Nchanga open pit do not carry significant mineralization. They postdate the main event of copper mineralization at the Nchanga mine. There is close temporal association between the time of IOCG mineralization and that of sedimentary copper mineralization. The Copperbelt 2 series of events probably occurred as follows: Regional Cu-Co mineralization in the Copperbelt (6), resetting of radiometric watch at Konkola (5), regional IOCG mineralization (4), localized IOCG mineralization (3), copper mineralization at the Nkana mine (2), and mineralization of copper and cobalt in the Congolese Copperbelt. Again, event 6 could have taken place during a long lapse of time. 6.4.3 Conclusions Secondary copper in sedimentary-hosted deposits probably came from IOCG deposits. This is a new concept for the origin of Copperbelt Cu-Co deposits. At least three discrete time periods show that close temporal spatial association. 315 Table 6.4 Events associated with three main copp er mineralizing periods in the Greater Lufilian Arc. (Numbers refer to the events of Fig 6.4.2) # Event, Site, Type, Source Age (Ma) Error From To 1 Congolese Cu-Co mineralization (this report) 506.5 6.5 500 513 2 Cu mineralization at Nkana, Zm (Re-Os, Barra et al., 2004) 525.7 3.4 522.3 529.1 3 533Ma IOCG mineralization, Zm (shrimp, this report) 533 4 529 537 4 Greater Lufilian Arc IOCG mineralization (shrimp, this report) 550 50 500 600 5 Resetting age Konkola, Zm (shrimp, L-158, this report) 562 18 544 580 6 Copperbelt Cu-Co mineralization, Zm (Re-Os, Ruiz) 583 24 559 607 7 Greater Lufilian Arc IOCG mineralization (shrimp, this report) 775 50 725 825 8 Nchanga mine intrusives, Zm (shrimp, L-172c, L-169, this report) 765 3 762 768 9 Initial Cu Copperbelt, Zm (Robb, personal communication) 776 20 756 796 10 Konkola Cu mineralization, Zm (Re-Os, Ruiz) 825 69 756 894 11 Nchanga Granite, Zm (shrimp, Armstrong et al., 1999) 877 5 872 882 12 Witvlei IOCG, Nm (shrimp, this report) 1098 5.9 1059 1104 13 Kwebe Mills, Ghanzi, Botswana (Schwartz, 1996) 1106 2 1104 1108 Fig 6.4.2 Event diagram for three copper mineralizing periods in the Greater Lufilian Arc. 1 2 3 4 5 6 7 8 9 10 11 12 13 1100 1050 1000 950 900 850 800 750 700 650 600 550 500 M ill io ns o f y ea rs a go Copperbelt 2 Copperbelt 1 Witvlei 316 7 SOME ASPECTS OF ANOROGENIC INTRUSIVE ROCKS 7.1 INTRODUCTION Continental rifts are environments where granitoids, gabbroids and alkaline rocks may coexist short distances from one another. Extensional continental rift systems favor the formation of midalkaline felsic magmas. Both plutonic and volcanic rocks are produced from those magmas and may form characteristic ring complexes. Midalkaline mafic magmas also occur in the environs of the felsic magmas. A wide range of gabbroids, syenitoids and ultramafic rocks may form from the mafic magmas. The close association of such diverse rock types enhances magma mixing and there is potential for many types of mineralization. A model of rift-related intrusions was prepared by Kazmin & Byakov, 2000, and is included on Fig. 7.1. Note the different types of small intrusive bodies that originate from the same mafic magma chamber in the middle of the figure. Chemistry of each intrusive event is unique. Large mafic and felsic chambers may exist at the same time within very short distances, as illustrated. The chamber to the left is one of them. They occur much higher in the crust. With sufficient erosion from the upper layers of syn-rift sediments, the granitoids and mafic intrusive rocks may be exposed on surface. Carbonatites, syenites, gabbroids, alkali granites and granites coexist in this environment. They intrude pre-rift, syn-rift, and post-rift sediments. Fig 7.1 Schematic cross section of the Wonji Fault Belt: an example of a tectomagmataic belt in a continental rift. More details in text.Taken from Kazmin & Byakov, 2000. 317 Most of the rifting processes abort before oceanic crust is able to form. The rifting process may repeat itself in time, producing magmas with very similar chemical characteristics. If more felsic magmatic bodies like the one illustrated on the cross section of Fig. 7.1, occur along successive parallel cross sections, large volumes of granitods may accumulate with time. The ring complexes formed may eventually gain enough areal density to produce the ring complex clusters that are discussed in the next section. This chapter will begin by comparing granitoid batholithic bodies with three case studies of anorogenic ring complex clusters. It continues defining main characteristics of some ring complex clusters in the Greater Lufilian Arc. Finally, it describes the occurrence of multiple, small gabbroic bodies that are known to occur in anorogenic extensional settings and compares them with similar features observed in the Greater Lufilian Arc. 7.2 COMPARISON OF BATHOLITHIC GRANITOID BODIES WITH ANOROGENIC RING COMPLEX CLUSTERS 7.2.1 Introduction Similarities have been observed between some of the batholithic intrusive bodies in the Greater Lufilian Arc and clusters of anorogenic ring complexes described in the literature. This chapter presents those observations. Well documented African examples have been used as far as possible. 318 7.2.2 Nuba Mountains, Sudan Fig 7.3 shows the emplacement time span for a series of Sudanese rift-related ring complexes (Wooley, 2001). Table 7.1 shows the actual data. This example was taken from a large field of granitoids and alkaline rocks in the SW Nuba Mountains of Sudan, located west of the White Nile River, as shown on Fig 7.2. There were at least three discrete events of intrusion that took place in roughly the same location. These occurred from 531 to 497 Ma, from 275 to 216 Ma, and from 171 to 149 Ma. Taking into account the errors, the first event could have lasted for 38 Ma, the second for 59 Ma and the third for 22 Ma. There is no progressive advance of magmatism in any direction. Masakin Tiwal had two intrusive events separated by 275 Ma (Nos. 6 and 11 on Table 7.1). The old intrusions are separated from the main ?batch? of intrusions that occur from near 275-216 Ma. Table 7.1 Radiometric (Rb-Sr) ages from ring complexes, SW Nuba Mountains, Sudan chronologically sorted (from compilation of African alkaline rocks and carbonatites by Wooley, 2001. Numbers refer to those listed by Wooley.) # Name and Number of Site Age (Ma) Error From To 1 Jebel Demik 76 160 11 149 171 2 Jebel Lado 87 222 6 216 228 3 Jebel Tabaq 70 228 17 211 245 4 Jebel Talodi 89 229 15 214 244 5 Jebel Kadugli 79 238 12 226 250 6 Masakin Tiwal 85 239 10 229 249 7 Moro-Limon Hills 84 246 2 244 248 8 Jebel Keiga, Umm Dugo 77 248 4 244 252 9 Jebel Tuna, Kafina, Debkaya 81 251 7 244 258 10 Jebel Moro West 83 261 14 247 275 11 Masakin Tiwal 85 514 17 497 531 Fig 7.3 Event diagram for intrusions from the SW Nuba Mountains, Sudan. (Number of events from Table 7.1). 1 2 3 4 5 6 7 8 9 10 11 500 450 400 350 300 250 200 150 A g e in m ill io ns o f y ea rs Masakin Tiwal 319 Fig 7.2 Alkaline intrusions of the SW Nuba Mountains, Sudan. Note the varying average composition for each of the complexes. In a few locations, such as the Miri Hills, Masakin Tiwal and the Limon Hills, several ring complexes amalgamated together. (After Curtis & Brinkmann, 1985, in Wooley, 2001 p. 305.) 7.2.3 Central Nigeria ring complexes Another example of anorogenic ring complexes from Nigeria shows variations on the same topic (Bowden et al., 1987; Kinnaird, Batchelor, Whitley, & MacKenzie, 1985; and Kinnaird & Bowden, 1991). In this case, a cluster of granitic circular complexes was emplaced at the times shown on Table 7.2 and Fig 7.5. The time span is comparable to that of the Sudanese complexes previously described. The information available from Nigerian intrusions shows at least five discrete periods of emplacement, namely: 216-210, 194-180, 175-170, 167-164 and 158-138 Ma. The total time span for the groups of intrusions is 78 million years. If only the main portion is included, the span shortens to 34 Ma. Here, once more, there are some precursor events followed by a main batch of intrusions that were emplaced during a short period of time, and by a waning stage. This example has striking similarities to that from the Nuba Mountains of Sudan. Its dimensions (Fig 7.4) are roughly the same as those of the Kamanjab and Hook batholiths. In addition to that, the Nigerian complexes are mainly composed of biotite granite (Table 7.3). This cluster of complexes was already included in discussions about the Nchanga Granite on section 4.1.5.2. 321 Fig 7.4 Sketch map of cluster of anorogenic ring complexes in central Nigeria (after Kinnaird, 1985; Bowden, 1987 and Wooley, 2001). Ages in Ma. 322 Table 7.2 Radiometric (Rb-Sr) ages from Nigerian ring complexes Sorted chronologically from Wooley, 2001; numbers refer to those listed by Wooley. An arbitrary 3 Ma error was added to starred sites (Afu, Mada, Tibchi, Ningi-Burra, Fagam and Dutse) from Bowden et al., 1987. Name and number of site Age (Ma) Error From To 1 Afu* 141 3 138 144 2 Mada* 147 3 144 150 3 Sara-Fier & Pankshin 38 153 7 146 160 4 Sara-Fier & Pankshin 38 154 4 150 158 5 Jos Bukaru & Shere 31 164 4 160 168 6 Jos Bukaru & Shere 31 165 2 163 167 7 Amo & Pukuba 33 165 3 162 168 8 Ririwai 13 171 2 169 173 9 Tibchi* 171 3 168 174 10 Banke 14 173 2 171 175 11 Banke 14 173 3 170 176 12 Dutzenwai 15 173 3 170 176 13 Kundaru 16 173 3 170 176 14 Ririwai 13 175 5 170 180 15 Kundaru 16 175 16 159 191 16 Ririwai 13 176 5 171 181 17 Dutzenwai 15 177 3 174 180 18 Ningi-Burra* 183 3 180 186 19 Zaranda 25 190 15 175 205 20 Fagam* 191 3 188 194 21 Dutse* 213 3 210 216 Fig 7.5 Event diagram graph for ring complexes in Central Nigeria. (Number of events from Table 7.2). 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 220 210 200 190 180 170 160 150 140 130 A g e in m ill io n s o f y ea rs 323 Table 7.3 Chemistry of biotite granit es from Nigerian anorogenic ring complexes (from Bowden et al., 1987) Complex Sample SiO2 TiO2 Al2O3 Fe2O3 FeO FeOt MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Cu Zn V Ba Th Pb Ce La Hf Li Be Sn Notch 50.00 1.00 15.50 6.00 0.15 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 25 85 100 1300 175 95 Amo AMN24 72.60 0.29 14.07 0.90 1.73 2.63 0.07 0.43 1.01 3.36 5.74 0.07 0.47 100.74 185 100 63 246 57 61 9 362 27 22 144 59 6 34 5 8 Ririwai RN75 75.90 0.11 12.85 0.33 1.05 1.38 0.05 0.02 0.24 3.91 4.31 0.01 0.88 99.66 979 15 696 399 214 120 376 0 109 111 56 296 234 28 391 7 40 Pankshin PAN112 73.90 0.15 14.88 0.43 0.80 1.23 0.02 0.67 0.43 3.98 5.17 0.02 0.61 101.06 192 28 117 234 88 0 80 25 22 195 189 7 25 8 19 Jos Bukuru JON147 73.20 0.18 14.18 0.67 1.19 1.86 0.02 0.08 0.73 3.45 5.32 0.03 0.98 100.03 296 38 227 330 118 126 0 264 41 38 251 218 8 32 14 39 Banke B34 76.00 0.10 11.74 0.37 0.89 1.26 0.02 0.09 0.83 3.78 5.77 0.04 0.24 99.87 574 4 115 141 158 60 12 39 40 74 114 64 5 205 9 145 Mada MD333 75.40 0.10 13.33 0.01 0.96 0.97 0.02 0.04 0.34 4.26 4.53 0.01 0.20 99.20 620 0 139 129 78 9 68 0 0 66 70 79 28 9 158 8 0 Ningi NG208 75.70 0.20 13.18 1.48 0.01 1.49 0.03 0.09 0.44 3.41 5.10 0.01 0.66 100.31 318 29 75 186 80 70 2 151 63 57 156 83 7 13 16 34 Tib` chi T15A 74.30 0.08 11.74 0.33 0.89 1.22 0.02 0.01 0.26 3.88 4.59 0.01 0.64 96.75 502 1 86 166 132 7 61 3 0 69 37 153 166 7 122 12 Dress DR11 76.70 0.14 13.36 0.00 1.16 1.16 0.03 0.05 0.33 4.41 3.58 0.02 0.34 100.12 966 0 87 81 119 103 4 0 61 47 149 88 9 558 15 76 Dutsen DW1 78.03 0.06 12.14 0.33 0.89 1.22 0.01 0.09 0.52 4.59 3.56 0.01 0.42 100.65 389 22 356 207 205 77 0 71 42 16 275 169 10 138 10 10 Faban FG5 77.44 0.08 11.99 0.37 0.87 1.24 0.02 0.07 0.49 3.89 4.45 0.01 0.34 100.02 347 3 189 161 148 42 0 43 39 27 117 64 8 67 13 10 Kudaru KD12 76.50 0.10 12.83 0.35 0.84 1.19 0.02 0.07 0.46 4.17 4.39 0.01 0.34 100.08 283 4 144 147 96 48 0 4 36 41 62 27 6 56 9 7.2.4 Kanye-Gaborone ring complexes, Botswana As shown on Table 7.4 and Fig 7.7, the Gaborone anorogenic ring complex cluster that lies in between Botswana and South Africa formed at least during a period of 20 Ma (Grobler, 1996). If we take into consideration event 12, then the lapse of time increases to approximately 72 Ma. There seems to have been a precursor event (13) 160 million years before. Other U-Pb radiometric ages that are not so well constrained (events 14 to 17) indicate that there might be other moments of intrusion before and after the main known lapse from 2840 to 2768 Ma. These precursor and tailing events are not well studied, and the entire ring complex cluster could very well have formed during a longer time. Only a relatively small portion of the ring complex cluster is exposed, and radiometric ages are available from that eastern portion. The possible extension of the ring complex cluster to the east is estimated by Grobler in some 300 km. Main features of the complex are shown on the map of Fig. 7.6. Fig 7.6 The Botsalano ring complex and other possible ring intrusions in the Gaborone-Kanye igneous terrane, Botswana and South Africa (after Grobler, 1996). 324 Table 7.4 Geochronological data available for Gaborone anorogenic ring complex cluster, Botswana and South Africa . Data from (Grobler, 1996). # Site Age (Ma) Error From To 1 Mmathethe Granite 2775.2 7.4 2767.8 2782.6 2 Lobatse rhyolite** 2780 5 2775 2785 3 Kanye Formation rhyolite 2780 6 2774 2786 4 Plantation porphyry (Lobatse) 2781.1 1.9 2779.2 2783 5 Thamaga rapakivi granite 2782.2 5 2777.2 2787.2 6 Main phase of Kgale granite 2783.1 2 2781.1 2785.1 7 Gaborone Granite granophyre 2783.1 1.2 2781.9 2784.3 8 Kanye Formation rhyolite 2784.7 1.7 2783 2786.4 9 Kanye Fm. rhyolite 2784.8 1.8 2783 2786.6 10 Spherulitic porphyritic 2784.9 1.9 2783 2786.8 11 Rhyolite and granophyre 2785.1 1.1 2784 2786.2 12 Majwana Granite (Kubung) 2830 10 2820 2840 13 Gaborone Granite Derdepoort* 3010 10 3000 3020 14 Plantation porphyry 2630 100 2530 2730 15 Platberg group 2643 100 2543 2743 16 Gaborone Granite Derdepoort 2825 100 2725 2925 17 West Kubung diorite 2932 250 2682 3182 * an error of 10 Ma was added for plotting and comparison. ** an error of 5 Ma was added for plotting and comparison. Fig 7.7 Event diagram for Gaborone anorogeni c ring complex cluster, Botswana/South Africa. Data comes from Grobler, 1996. (Number of events from Table 7.4). 7.2.5 Comparison of the three ring complex clusters Finally, a direct comparison of the event diagrams from the three anorogenic ring complex clusters just reviewed helps to understand their similarities better. Fig 7.9 presents event diagrams from the Nuba Mountains, the central Nigerian ring complexes and the Kanye-Gaborone complexes of Botswana. They have been leveled to a common central time point and plotted at the same scale. If one takes into consideration sampling errors, that not all of the ring complexes present in each of the clusters has been dated, and that several different dating techniques have been used, the three diagrams can be said to represent equivalent geological processes. Precursor events more than 200 Ma before the main group of intrusions are present in both the Sudanese and Botswanan clusters. Volcanic and plutonic rocks of roughly the same composition occur together in all three complex clusters, and in most of the world?s ring complexes. The amount of volcanic rocks decreases with successive levels of erosion, to a point where only granitic rocks are left and all volcanic rocks are eroded. 0 1 2 3 4 5 6 7 8 9 10 11 12 13 3050 3000 2950 2900 2850 2800 2750 A g e in m ill io n s o f ye ar s 325 326 Individual anorogenic complexes tend to have circular outcrop, hence the name ?circular? or ?ring? complex. Clusters of ring complexes tend to have the shape of isosceles triangles in plan view. This can be considered the model for anorogenic ring complex clusters. Clusters identified in the Greater Lufilian Arc will be compared with it in the next pages. 7.2.6 Model for the origin of batholithic-size granitoid bodies in anorogenic environemnts. New ideas on the origin of granitic bodies have been proposed by numerous working groups and individuals during the last fifteen years. Some review articles on the subject include Clemens & Mawer, 1992; Glazner, Bartley, Colemena, Gray, & Taylor, 2004; Hutton, 1996; and Vigneresse, 1995. The existence of batholithic size magma chambers is physically impossible. Long-term amalgamation of very small magma chambers, amalgamation of numerous consecutive dikes, and granitic magma transport by fracture propagation seem to be the most energy efficient systems to accumulate large volumes of granitoid rocks and account for the majority of batholiths. The three, reasonably well-documented, case studies of anorogenic complex clusters described in the previous section form the basis for the genetic model for batholithic-sized anorogenic bodies proposed here. Many African ring complexes are made of midalkaline granitoids. If such ring complexes intrude very near each other as shown on Fig 7.2, batholitic size bodies may form. Larger magma bodies develop underneath the ring complexes, and once lithified, subsequent erosion can expose them. This process explains the formation of large plutonic bodies like the Hook Granite and the Kamanjab batholith in anorogenic rift-related environments. The process could also help to explain the large compositional variety of batholiths like the Hook Granite. They did not form during a single event, but by amalgamation of multiple small discrete plutons, each with its own chemistry. Regional heat re-sets the geochronological clocks of some rocks, and continuously metamorphoses older intrusions. This method is proposed as origin for granitoid batholiths in anorogenic environments. Fig 7.8 shows a cluster of granitic ring complexes (unit E) overprinted by a cluster of quartzmonzonitic ring complexes (D) and later by a third cluster of alkali granite ring complexes (C). Two more generations of ring complexes (B and A) came later. The end result is complex geology, abundant thermal metamorphism and hydrothermal alteration of the older plutons, as well as widespread opportunities for magma mixing processes to occur. Each event of granitic ring complexes produced contemporaneous vulcanism of equivalent composition. Depending on the level of erosion of the ring complex cluster, one will find only volcanic rocks, a mixture of volcanic and plutonic rocks, or only plutonic rocks in ring complexes. The shapes, and internal and external characeristics of granitic plutons are purely arrival phenomena dictated by local structure, kinematics, and stress states [Clemens & Mawer, 1992, p. 339]. But in the case of large granitoid ring complex clusters, there seems to be an underlying mechanism that leads to the formation of isosceles triangle shapes. The triangular shapes of the Kamanjab and Hook Granite batholiths, as well as their size, are comparable to those of the three ring complex clusters described in the previous section. Fig 7.10A shows the outlines of the five entities drawn at the same scale, and rotated for simpler comparison. At first glance, the outlines of the Kamanjab batholith and Hook Granite batholith show many similarities. Their area is approximately the same. Both display a roughly isosceles triangular shape; if one is laid over the other, the silhouette of their perimetral triangles is almost the same size and shape. In the position that the two outlines are laid, both bodies are composed of a principal large, elongated portion and several other smaller portions separated from the main body by a fracture that is parallel to one of the longest sides of the triangle (Fig 7.10B). Both bodies have small satellite intrusions that fall outside of the main triangular outline. The outlines of the Nuba Mountains and the Central Nigerian ring complex clusters also display several similarities. In both cases, the main portion of the cluster can be circumscribed by an isosceles triangle of roughly the same size and shape. In both cases, there are fractures that run parallel to the longest side of the triangle that separate the ring complexes. Again, both clusters have small satellite intrusions that fall outside of the main triangular outline. The Central Nigerian ring complex cluster a large number of ring complexes that fall outside the main triangle. 327 Fig 7.8 Plan view of what might have taken place to produce one of the granitoid ring complex clusters identified in the Greater Lufilian Arc. N o tice that if a series of five different generations of granitoid ring complex s tructures intrude and inte rsect each other, a complex assembly of igneous lithologies can form. Each of the s e parate intrusive ev en t s ( A t o E ) was m ade of a few ring complex es widely s pread in the area. In the hy p o t he tical case, each generation of ring comple x es has a uniform litholog y . A chance orientation for a geological transect along X- Y results in the ge o l og y s h o w n. Interpretation of that geology based on the single transect is quite complex, e s p ecially if the o u tcrop density is not g o o d . Th e g e o l og y o f t he H oo k Granite Batholith and the Kamanjab Batholith are very much like this. The Kanye-Gaborone ring complex cluster is less well defined than the other clusters, shows the general triangular shape, but it also has three additional ring complexes that significantly modify its overall shape. 328 Fig 7.10 Comparison of the outlines of various African ring complex clusters. (All scale bars are 100 km long). Note that most of the ring complex clusters may be circumscribed by an isosceles triangle of similar dimensions. The outlines have been rotated for evaluation. All north arrows kept their original orientation. 329 7.2.7 Ring Complex Clusters in the Greater Lufilian Arc The anorogenic granitoid-magmatic events that produce ring complex clusters seem to have a consistent time span of ~110 Ma. This is seen on many locations of the Greater Lufilian Arc, as shown on Table 7.6 below. The Sudanese Nuba Mountains, Nigerian and Gaborone granite ring complex clusters have been included in the table for comparison. Table 7.6 Compilation of Anorogenic Complex Cluster Periods in th e Greater Lufilian Arc # Name Time Lapse Magmatism Central Age Number of Radiometric Ages Precursor Events Tailing Events Areal Extent Event Diagram (page) Example or main body 1 Nigeria ~75 Ma Granite 170 21 1 New Jos Bukuru 2 Nuba Mts., Sudan ~70, 120Ma Granite 250 11 1 1 New Masakin Tiwal 3 Hook Granite ~110 Ma Granite, alkali granite 500 8 ? 138 Hook Granite batholith 4 West Lusaka 2 ~120 Ma Syenite 550 16 ? 139 Hook Satellites 5 NW Zambia 2 ~100 Ma Quartz syenite, gabbro 720 7 2 137 Peter Mann's pluton 6 Kafue Flats ~140 Ma Granite 750 10 yes 139 Lusaka Granite 7 Khorixas 1 ~110 Ma Syenite, nepheline syenite 760 8 no no 150 Oas Syenite 8 Khorixas 2 ~105 Ma Granite, quartzmonzonite 1800 3 ? 2 150 Khorixas Inlier 9 Irumide ~100 Ma 1870 10 2 New 10 NW Zambia 1 ~110 Ma Granite 1920 7 ? 137 L-030 11 Kamanjab ~110 Ma Granite, quartzmonzonite 1925 8 2 yes 149 Kamanjab batholith 12 Mufulira ~120 Ma Granite, tonalite 2000 7 141 Mufulira Granite 13 Mkushi-Serenje ~100 Ma Granite 2050 9 2 New 14 Kanye-Gaborone, Botswana and South Africa ~72 Ma Granite-rhyolite 2800 17 1 Maybe 200 x 120 km (may be 300 x 150 km New Gaborone and Jwaneng At least ten of those anorogenic complex cluster periods have been documented in the Greater Lufilian Arc during this project. That represents the regions with enough geochronological data to produce meaningful results, and is definitely an incomplete list. The gaps in the event diagram of Fig 7.11 are time periods with less reliable data and do not necessarily mean that anorogenic ring complex clusters only formed in particular moments (See Fig A81, for example). What should be understood from the diagram is that the process has been taking place on what is now the African plate, at least during the past 2.8 billion years. If the information from Table 7.5 is considered as totally representative of reality, then three main periods of anorogenic ring complex cluster formation are in evidence in the Greater Lufilian Arc: one from 2100 to 1820 Ma, a second from 815 to 670 Ma, and a third from 610 to 445 Ma. That is just a partial observation. In addition to that, Fig 7.11 shows that two of the regions have had two completely distinct periods of anorogenic ring complex cluster formation. The events from the NW Zambia region are separated by 1095 Ma, while the events from the Khorixas region are separated by 933 Ma. In both cases, the clusters of ring complexes formed in roughly the same areas. This may be another recurrent feature of the ring complex clusters that probably has not been made evident due to scarce geochronological information. The two clusters from West Lusaka are not illustrated on Fig 7.11. They trail one after the other, separated by 50 Ma (Fig A25), and Nos. 5 and 6 on Fig 7.12. The end of West Lusaka 1 is the beginning of West Lusaka 2. 330 Table 7.5 Compilation of ages from various ri ng complex clusters in the Greater Lufilian Arc No. Name Central Age Difference From To Lapse 1 Central Nigeria 170 37.5 208 133 75 2 Nuba Mountains, Sudan 250 60 310 190 120 3 Hook Granite 500 55 555 445 110 4 West Lusaka 550 60 610 490 120 5 NW Zambia 2 720 50 770 670 100 6 Kafue Flats 750 70 820 680 140 7 Khorixas1 760 55 815 705 110 8 Khorixas 2 1800 52.5 1853 1748 105 9 Irumide 1870 50 1920 1820 100 10 NW Zambia 1 1920 55 1975 1865 110 11 Kamanjab 1925 55 1980 1870 110 12 Mufulira 2000 60 2060 1940 120 13 Mkushi-Serenje 2050 50 2100 2000 100 14 Gaborone Cluster, Botswana 2800 36 2836 2764 72 Fig 7.11 Event diagram of Anorogenic Complex Cluster periods in the Greater Lufilian Arc (With three additions from Botswana, Nigeria and Sudan for comparison) Gaps may be due to incomplete information more than to periods of quiescence. More thorough compilations of geochronological data from the African Plate are necessary to complete the picture. 0 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 Number of each event 2800 2400 2000 1600 1200 800 400 0 M il li o n s o f ye ar s b ef o re p re se n t 331 The event diagrams for some of anorogenic ring complex clusters were leveled to allow for direct comparison of their features. Fig 7.12 includes event diagrams from nine clusters plotted at the same scale, and centered on a uniform arbitrary age datum (230 Ma). Note that there are many similarities. Precursor and trailing intrusions occur in many of the clusters. 110 Ma seems to be the common duration for most of the clusters. Fig 7.12 Comparison of event diagrams from various anorogenic ring complex clusters from the Greater Lufilian Arc. Ages of the various complexes have been leveled to allow for comparison. Original data is on Table A22 and modified ages are on Table 7.7. Data from Sudanese, Nigerian and Kanye-Gaborone clusters were also included. Reference numbers of the event plots: 1, Nuba Mountains, Sudan; 2, Central Nigeria; 3, Kanye- Gaborone, Botswana; 4, Hook Granite batholith, Zambia; 5, West Lusaka 1, Zambia; 6, West Lusaka 2, Zambia; 7, Mufulira, Zambia; 8, Kamanjab batholith, Namibia; 9, Khorixas Inlier, Namibia. Note, for example, that clusters from the Hook Granite, West Lusaka 1, West Lusaka 2, and the Kamanjab batholith show very similar shapes, total length and distribution. Data available for the Mufulira and Khorixas Inlier clusters has some similarities. There are precursor events more than one hundred million years before the main Kanye, West Lusaka 1, West Lusaka 2, and Mufulira clusters. The ring complex clusters require long-lived mantle plumes that remain relatively still in one place for at least the 110 million years. In several cases, anorogenic complex clusters formed in roughly the same place with 800 million years of difference or more. Examples of this have already been mentioned in the Khorixas inlier and NW Zambia. Another series of such events with a long hiatus is the basement to the Nchanga Granite. 525 500 475 450 425 400 375 350 325 300 275 250 225 200 175 150 M ill io ns o f y ea rs 1 2 3 4 5 6 7 8 9 332 333 Very few of the old anorogenic complex clusters remain as discrete entities. Most of them have been broken up. For example, the Khorixas-Ugab-Mesopotamie-Summas domain in Namibia is very fragmented. 7.2.8 Conclusions Clustering of multiple anorogenic ring complex intrusions can form batholithic size bodies. Clusters of anorogenic granitoid ring complexes have been produced from Archean times and up to the past 140 Ma in what is now the African Plate; they probably have been forming all through the period in between, including the present. Eastern African examples in the rift valleys indicate that similar processes are still active today. A few normal faults with vertical displacement of over two kilometers expose syenites and granitoids underneath recent trachitic and rhyolitic vulcanism. Many young ring complexes have not been eroded enough to expose their ring shape roots and lie under volcanic fields. Ring complex clusters have the following characteristics: 1) Multiple ring complexes of varying chemical composition and size that might intersect each other. 2) Volcanic and plutonic rocks of roughly the same composition occur together. 3) Successive magmatic events of varying composition allowed for abundant opportunities of magma mixing and recycling of crustal materials. 4) The plan view geometry of ring complex clusters is roughly that of an isosceles triangle. 5) Less voluminous precursor and waning events of magmatism may occur. 6) The principal chemical composition of the magmas is midalkaline, but may ocassionally vary to alkaline and subalkaline. In extreme cases, it may be peralkaline and can even produce significant carbonatitic rocks. 7) Isolated bodies of mafic and ultramafic rocks often come in the latter stages of the process. At least ten clusters of ring complexes were identified in the Greater Lufilian Arc. They all display the general characteristics listed above. Their event diagrams show roughly the same parameters that have been identified in African ring complex clusters from the literature. Total duration of ring complex cluster cycles averages 110 Ma. Several cycles of ring complex clusters have repeatedly occurred in roughly the same location in at least three different localities. These repeated cycles were separated 1095 Ma in NW Zambia, 933 Ma at the Khorixas area, and 50 Ma in West Lusaka. The relevance of these observations on ring complex clusters are far reaching. They will probably be useful to help understand Proterozoic geology and the formation of contintental crust. 334 7.3 COMPARISON OF LUFILIAN SMALL BASIC INTRUSIONS WITH EXAMPLES FROM THE LITERATURE The ubiquitous presence of abundant small gabbroic and midalkaline bodies in portions of the Greater Lufilian Arc was intriguing. These rocks intersect any lithologies, including siliciclastics, carbonates, granitoids and various metamorphic rocks. Parts of Nigeria have rocks with similar characteristics being formed today in rift- related environments. The following pages describe an example that can help understand the origin of the mafic bodies of the Greater Lufilian Arc. The map from the Filiya area in eastern Nigeria (Fig 7.13) shows hundreds of small bodies of mafic and alkaline rocks that were emplaced into various rock types from 10 to 20 millions years ago. Some of the bodies form plugs or needles that ?vary geomorphologically from small mounds several meters high to substantial peaks. Tangale peak, for instance, rises to more than 600 m above low sandstone hills.? (Wooley, 2001, p. 247). Many smaller bodies have not been mapped. These numerous bodies of small intrusives were emplaced in an anorogenic environment within a continental plate that is being rifted. Fig 7.13 Sketch map of basalt, trachyte and phonolite plugs of the Filiya area in eastern Nigeria (after Carter et al, 1963 in Wooley, 2001, p.248) Note that several ENE-WSW linear trends can be identified. These are typical intrusive features that form in rift environments. Some of the plugs behaved as feeders to volcanoes and others as feeders to dikes and sills. Many of these bodies were emplaced along weak structural zones and may be roughly aligned (Fig 7.13). They take place as the continental crust thins due to 335 extensional tectonics and the mantle reaches nearer to the surface. Fig 7.1 shows an example of what happens underneath an active rift zone today. This is very similar to the abundant bodies of mafic rocks and syenites that are known from parts of the Greater Lufilian Arc. The only difference is that the level of erosion in the Lufilian Arc is deeper than that from Nigeria. Regions like West Lusaka and northwest of Solwezi, Zambia, display abundant such small bodies of gabbro, syenite and other alkaline intrusions. In some cases, gabbroic bodies are a few kilometers in diameter, and may even amalgamate into larger ones. Very few Katangan age volcanic rocks associated with the small mafic intrusions remain. For example, see Figs 8.8, and 8.9 to 8.11. By analogy with the Filiya mafic bodies, the following is an explanation for a large part of the widespread small gabbroic bodies in the Greater Lufilian Arc: They were emplaced as mafic plugs in large, within-plate areas that are being subject to incipient rifting. The mafic plugs could intersect the sedimentary cover of the plate, including marine and continental deposits. A portion of the mafic bodies are eclogite facies oceanic rocks that represent an ophiolitic melange. 3 3 7 8 IRON OXIDE-COPPER-GOLD MINERALIZ ATION IN THE GREATER LUFILIAN ARC 8.1 INTRODUCTION Large mineral deposit s of the iron oxide-c o p pe r - g o ld fa mily are thought to be pres ent in the Greater Lufilian Arc of western Zambia and norther n Namibia . This ch apter reviews main features of the deposit type and describ es evidenc e for such deposi t s in the region , in cludi n g iron oxide bodies, hydr oth er m a l breccias and alteration features . As Foster et al, 2001 state, ?Pan-A f r ic a n seque nc es of Afric a have tended not to be the first priority for mineral exploration when assessed agains t the historic al perspe c t i v e of explora t i o n succes s es and minera l produc t i on in Archean, early Proterozoic and P haneroz oic terranes. However, recent advances in unde rstanding of the evolution of Pan-African s equen c e s and a number of recent explor a t ion succes ses suggest that Pan-African terranes merit more attentio n than wa s previous ly accorded to them.? 8.2 SOME NOTES ON IRON OXIDE-COPPER-GOLD DEPOSITS Iron oxide-c op p e r - go l d (IOCG) miner a l depos i ts compr i se a recently-identified ty pe of mineral depos its. IOCGs are know n to have formed in Meso- and Neo- Proterozoic rocks of Australia, Canada, Brazil, Scandinavia, the United States, China and Russia. P han e r oz o ic depos i ts occur along the Andea n chain in Chile and Peru. Brazili an examples of Archean age are also known. The relatively recent international recognition of the deposit family is expecte d to result in many more mi nera l iz ed provinc es in the ranges of geolog i c a l time and geogra p h ic a l distrib u t i o n , includin g Africa . A brief overview of this deposit family is given below , based on publishe d informat i on and personal obser v a t i o ns of some minera l iz e d system s (Oresk es & Einaudi, 1990; Hitzman, Oreskes, & Einaudi, 1992; Bart on & Johnson, 1996; Kerrich, Goldfarb, Groves, & Garwin, 2000; Jens en & Barton, 2000; Partington & Williams , 2000; Barton & Johnson, 2000; Haynes , 2000; Hitzman, 2000; Pollard, 2000; Piche & Jebrak , 2003; Sillitoe, 2003; Sillitoe, 2002; Hitzman, 2004a; Barton & Johnson, 2004b; Barton & John son, 2004a; and Wall, 2004). Most of these deposits are located in zones of extens ional tectonics, occur mainly along past rift zones or aulacogens and ar e situated along major structur es. Table 8.1 lists a few of the major IOCG deposits with their principa l feature s . Most are related to felsic a nd mafic intrusi v e rocks of so-called ?anorogen i c ? type . There is no direct relationship with intrus ive rocks in m any of the small deposits and in the ?distal? portions of mineralized systems. The size of the alteration and minera li z a t i o n footprin t of IOCG systems is very large, typical diamete r s are in the order of hundr eds of kilome t e r s . Fig 8.1 Cartoon to illustrate the developmen t process of an iron oxide-copper-gold system. T h e e mp lacement o f massive iron oxide bodies takes place fi rst, and later sulfidation nucleates around or within the massive iron oxide. The t w o processes s ee m t o b e indepen den t , and are not n ecessarily related. Massive iron oxide may have a different origin from the s u l fidation process. Three of many alte rnatives for the origin of massive iron oxide are: 1) t h e iron oxide may ha ve been de p osited as a banded iron formation, 2) h y drothermal emplacement of iron oxide by replacement of granitoids, 3) hy drothermal emplacement of iron oxide by selective replacement of layered rocks. At a smaller scale, oth er origins include 4) disseminated magetite in a granitoid rock, and 5) massive sodic altera tion of a biotite-bearing granitoid that turned biotite into magnetite. T h e cartoon sho w s pyri te (light gray) and chalcopyrite (d arker gray), but su l fidation may be on l y pyrite, or may include ot h er copper sulfides like born ite. As s ho w n , s u l fidation may occur as large bodies in the contact betwe en massive iron oxide bo dies and thei r host rocks, or disseminations within the iron oxide bodies. In s ome cases, significant addition of rare ea rth ele me n t s takes place. Thes e processes can take place at many scales. Massive iron oxide bodies can be kilometers in diameter or a few millimeters. In general terms, the minerali z ed deposits contain an iron oxide nucleus (magnetite and/or hematite) that was replac ed by pyrite and chalcopy r i t e . Magnetit e might have been demagnetized into martite and/or hematite; and later, part or all of the iron oxides are replac ed by sulfides (Fig 8.1). The Salobo depos it, located in the 3 3 8 C a r a j ?s provin c e of Braz il is a good example to explain here. Location of Caraj? s is outlined on Fig 3.1. As observed on the schemati c map of alterati o n and mineral iz ation from its 250 m level (Fig 8.2), note the ir on oxides in the center and nuclea ti o n of copper conten t around it. Both iron and potassium alteration increa se their intensity towards the middle of t he system, which is controlled by a ma jor fracture. Mineralization cons ists of a sub-vertical lensoid body 6km long and approxim ately 100m wide. This is hosted in hydrothermal breccia s and metagr a y w ac k es that hav e been almost entirely replac ed by iron oxides. The deposit is a tabular body, but was clearly emplaced hydrothe rmally (Goad, Mumin, Duke, Neale, & Mulligan, 2000; Haynes, 2000; Lindenmayer, 1994; Linden mayer & Fyfe, 1994; Mark, H. S., Williams, Valenta, & Crookes, 2000; Pollard, 2000; Requia & Fontbo te, 2000; Requia, Stein, Fontbo t?, & Chiaradia, 2003; and Souz a & Vieira, 2000). The deposi t has not been mined due to high metall u r g i c a l co sts derived from the comple x composition of its copper ore. Light rare earth elemen t s (LREE) and gold are someti m e s pres en t in econom i c quanti t i e s in iron oxide- co pp e r - go l d deposits . Uranium conten t might be signifi cant; many other metals like silver, cobalt, and mangan es e may occur in econom ic concen t r a t i o ns . Cop per mineralization seems to be associated with flow of meteor ic fluids and redox reac tions on or around t he iron oxides as described by (Bar ton & Johnson, 2000). LREEs may be associated with apatite. Fluorine is another element that may be present in ec on omic quantities. The Brazilian Alem?o IOCG deposit, also located in the Caraj? s Province (Fig 3.1, general location on Fig 3.3) contains signific ant fl uorine. Note that gold, copper, c obalt, thorium, uranium, potass ium and fluori n e nuclea t e around and in the iron oxide bodies that are marked with a star. The origin of gold and LREEs is not very clear, and current views on this issue are polemic (Barton & Johnson, 2000; Hitzman, 2004a; Barton & Johnson, 2004b; and Wall, 2004). The caus es of hydrothe rmal alteration , disolu tion of silicates and transporta tion of metals are other uncertain issues (Piche & Jebrak, 2003 ). In some cases , evaporites formed in sabkha, playa or salt lake envi r o n me n t s are cons i d er e d to be an impor t a n t sourc e of halogens for the highly- a lka l i n e and/or F-rich solution s ; basinal brines and/or mixing with sea water may also play a role (Kirkham , 2003; Barton & Johnson, 2000; and Warren , 2000). The origin of elemen t s like cobalt , nickel , zinc and probab l y also copper and gold in many IOCG systems seem to be assoc i a ted with mafic (and ultramafic ?) rocks, in a manner not yet completely understood. Fig 8.2 Generalized geological map of the Salobo Deposit, Caraj?s, Brazil. Note size and distribution of the copper and g ol d mineralization around iron oxide bo dies. Also n ote the ?banana? shape of the orebo dy in plan view. Other notes in text. T he Caraj?s district is located on Fig 3.1. 3 3 9 Zoned hydrothe r ma l alterati o n takes place in almost all mineralized IOCG deposits. Various alteration patterns depend on depth of emplace me n t and host rock chemist r y . In general terms, from shallow to deep levels, these generall y are: albitiz at i o n , scapo lit iz a t i o n , potassic alterati on , serici ti z a t i o n and silicifi c a t i o n (Figs 8.4 and 8.5). Bear in mind that alterat i o n patterns and types vary immens e ly from deposit to deposit , dependi n g on the composi t i on of intrus i v e s and host ro cks. At times large quartz -only rocks occur on the surface above IOCG mineralization. This seems to be produc ed by leaching of silicates in the center of the systems to allow for the emplac ement of iron oxide bodies, and precipitation of the silica farther out. Massive hematitization and so-called ?r ed-roc k ? (?brow n rock?) alterati o n ar e widespread and affect most types of host rocks. Regiona l sodic altera t io n marks zones of hydroth e r m a l circula t i o n around the mineral iz e d deposit s . Textura l replaceme n t s of rock cons tit u e n ts ar e common. Ther e seems to be a particular or der of hydrothermal alteration and mineralization in the ?typical? IOCG deposits. First comes a strong albitization of the country rock. Then high temper ature Fe ? K ?Ca alteration; this is repr es ented by biotite- ga rnet-K feldspar- amphibo le-clinopyroxene-magnetite. Mineralization and low temper ature alteration come last (sulfides ? magnetite ? hematite?car bonate ?s er i c i t e /c h l or i t e ) . The last phase of sulfidat i on may contain both Cu and Au. Explosive brecciation occurs in most of the know n deposits. An important portion of the larges t orebod ies shows evidenc e of multiple explos ive fragmentation (Tabl e 8.1). This is quite evident at the Mantoverde mine and its environs in Chile (Astud i l l o , 2003; Geolog? a , 2003; Zamora & Castillo, 2001; also personal observations), at Candelaria mine in Chile (Sillitoe, 2003; Sillitoe, 2002; Marschik, Leveille, & Martin, 2000 ; also personal obser va t i o ns ) , at the Raul-Co n de s t abl e mine, Peru (Injoque Espino za, 2002; and personal observations), as well as at the Olympic Dam mine in Australia (Ferris, Schwarz, & Heithersay, 2002; Ores kes & Einaudi, 1990; Reeve, Cross, Smith, & Oreskes, 1990; Reynolds , 2000; and Skirrow, Bastrakov, Davidson, Raymend, & Heithersay, 2002). Geometry of the mineralized bodies varies substantia lly; by far the commonest deposits are veins. Some are massive replacements that grade into stockwor k s , others are breccia pipe s or diatreme s, others are tabular bodies that run conc or da nt with rock foliation or stratifi c a t i o n . Compo s i t e depos it s compr is i n g veins , brecc ia s , stockw o r k ed zones and replac e m e n t m antos are common (See Table 8.1). 3 4 0 Fig 8.3 Simplified geochemical log of borehole ALM-FD09, from the Alem?o deposit, Caraj?s, Brazil . Massive iron oxide b odies in this iron oxide-copper-gol d dep osit are marked with stars on th e right of the l og. Not e that so me of the b o dies are over fifty met ers thick. For sca le, tick marks o n t he left of th e l o g are set every fifty met ers. Iron oxides s erved as site for nucleation of economic mineralization at this site . Note pres ence of fl uorine. Slightly mo dified from Ro n ze , Soares, dos Santos, Barreira, & Proterozoic, 2000. 3 4 1 Fig 8.4 E xamples of hydrothermal alteration zonation in IOCG deposits formed in volcanic and plutonic host rocks. N ote that most alteration affects large vol u mes of rock, par ticularly sodic alteration. Note t hat the breccia pipe may be cemente d by massive magnetite or he m atite. A pproximate location of Olym pic Dam and Ernest Henry d ep osit s is show n for better comprehension. Taken from Nisbet et al., 2004a. Fig 8.5 Examples of hydrothermal alteration zonation in IOCG deposits formed in sedimentary sequences. Based on examples from th e W ernecke M o unt ains in the Yukon, Canada. Note that total vertical ext e nsion of the diagram is 5 km and its widest portion is also 5 k m. Alt eration and mi neralization are greater in reac tive rocks like carbonates. From Hit zman et al., 199 2. 3 4 2 Table 8.2 Details of selected IOCG deposits and prospects, Greater Lufilian Arc, Africa 3 4 3 TABLE 8.1 DATA FOR SOME IR ON OXIDE-COPPER-GOLD DEPOSITS Deposit T (x10^6) Cu (%) Au(g/t) Ag(g/t) Mineralization Styles Associated Metals Age References R a u l - C o n d e s t a b l e , P e r u >500 0.7 0. 5 5 V e i n s , m a n t o s , d i s s e m i n a t i o n s Co,Mo , Z n , P b , A s , L R E E ~ 115 I n j o q u e , J., perso n a l commu n i c a t i o n , 2002 Mina Justa , P e r u 209 0.86 m i n o r p r e s e n t I r r e g u l a r vein- l i k e repla c e m e n t bo d y ~155 R i o Tinto , 2003 i n Silli t o e , 2003 Marco n a , P e r u >1000 50-60 % F e Repla c e m e n t ma nto s + veins Cu,Ag , A u 150 In j o q u e , 1989 Cande l a r i a , C h i l e 470 0.95 0 . 2 2 3 . 1 9 B x , s k a r n As,Mo , P b , Z n , L R E E 114 Ma r s h i k et al, 2000 Mant o s Blan c o s , C h i l e 500 0.6 B x s , s t wk s , v e i n s Ag Urruti a , J., pe rson a l commun i c a t i o n , 2003 Susan a , C h i l e >100 ? Diat r e m e bx Ag Espin o z a et al, 1996 Manto Verde, C h i l e ~300 >450s u l f 0.6 0.53su l f B x , f a u l t zones, d i a t r e m e LREE 117 Zam o r a & Castil l o , 2 0 0 1 , Person a l Commu n i c a t i o n s , Urrut i a , J., 200 3 Santo s , C h i l e 19 1.7 0.4 V e i n , b x Ag Marshi k & Fontb ot e , 1996 Punta del Cobr e Distr i c t , C h i l e ~120 1.5 0. 2 - 0 . 6 8 S t r u c t u r a l zone Zn,LR E E , M o ~115 M a r s h i k & Fontb ot e , 2001 Minit a Despr e c i a d a , C h i l e 3 16 Vei n s Mo,U 114 Es p i n o z a et al, 1996 Cerro Negr o,Ch i l e 249 (49 ) 0.4(0.71 ) ~ 0 . 1 5 B x , m a n t o s , s t wk s , v e i n s Atna Reso u r c e s Pres s Rele a s e , 2002 Teresa de Colmo , C h i l e 70 0.8 tra c e B x pipe Hooper & Cor rea , 2000 Salob o , B r a z i l 789 0.96 0 . 5 2 5 . 5 V e r t i c a l , t h i c k , m as s i v e FeOx lense s , b x Co,Mo, N i , R E E , U 2579? Linden m a ye r & Texeira , 1 9 9 9 ; Req uia et a l, 2003; Souza & Vieira , 2000, 2004 Alem?o , B r a z i l 170 1.5 0.8 2 B x bodies Mo,U EprotZ c B a r r e i r a et al, 19 99 Igarap e Bahia, B r a z i l 23.4 2.9 B x EprotZ c Ta v a z a et al, 199 8 Sosse g o , B r a z i l 355 1.1 0. 2 8 H yd r o t h e r m a l veins and bx bodies Co,Ni Eprot Z c Fa n t o n , 20 01; Le vei l l e , 2001 Crist a l i n o , B r a z i l ~200 1.4 0. 2 5 S t wk Co,Ni Eprot Z c Hu h n et al, 1999 Pojuc a , B r a z i l 58 0.9 S tr a t i f o r m re pla c e m n t , Fe stone - h o s t e d vein s Au,Co,N i , M o , Z n EprotZc W i n t e r , 1994 Pahtoha v a r e , S we d e n 1.15 2.1 0.9 B x Co EprotZc L i n d b l o m et al, 1996; Freit s c h et al, 1997 Bidjo v a g g e , N o r wa y 3 1.8 0. 5 V e i n , s t wk REE,U , T e , C o , N i EprotZ c B j o r k yk k e et al,1 98 7 ; Ettner et al, 1993 Aitik, S we d e n 606(+8 5 0 r s ) 0.37 0. 2 3 V e i n , b x Mo,U 1.87Ga W a n h a i n e n et al, 2003 Ol ym pi c Dam,Au s t r a l i a 2000 1.6 0.6 D i a t r e m e bx com ple x Co,Ag, U , R E E MprotZ c Re e v e et al, 199 0 Ernest Henr y, A u s t r a l i a 166 1.1 0.5 4 B x matri x and re plac e m e n t in shear zone net wor k Co,Mo, R E E MprotZ c R ya n , 1998 Mount Ellio t , A u s tra l i a 2.47 3.7 2. 1 S k a r n , b x in bri tt l e fault s Co,Ni Mprot Z c Fo r t o ws k i & McCra k e n , 1998 Starra , A u s t r a l i a 7.4 1.88 3. 8 S h e a r z o n e - c o n t r o l l e d Fe stone- h o s t e d Co MprotZ c Ro t h e r h a m et al, 1998 Osborn e , A u s t r a l i a 11.2 3.51 1. 4 9 B x , s h e a r z o n e - h o s t e d Fe stone Ag,Co, M o , B i , T e , S e , H g , S n MprotZ c A d s h e a d et al, 1998 Gree nm o u n t , A u s t r a l i a 3.6 1.5 0.7 8 V e i n , s t wk and re plac e m e n t Co MprotZ c K r e m a r o v & Ste wa rt , 1 9 8 8 Elois e , A u s t r a l i a 3.1 5.5 1. 4 V e i n , b x , s t wk in shear z o n e Ag,Co,Ni , Z n MprotZc B a k e r , 1998; Gol d Gazette, Feb. 1995 Warreg o , A u s t r a l i a 5 139kT( 2 . 6 ) 1 . 5 M o z ( 2 ) Fe stone - h o s t e d in fold limb Bi Ep rot Z c Go u l e v i t c h , 1 9 7 5 ; Wedek i n g & Cove, 1 9 9 0 Notes: bx = brec ci a , stwk = stockwo rk , Fe stone = ironst o n e , mPro t Zc = MesoP r o t e r o z o i c , eProt Z c = Earl y Prote ro z o i c , rs = total reso u r c e s , sulf = sulf i de rese rv e s . 3 4 4 Fig 8.6 Geological Map of the Kamanjab Batholith, Namibia. Not e t he fracture zon e s drawn in light blue. E - W - trending fractures control copper, iron, zinc and gol d mineral occurrences. For reference, light blue u nits are Katangan-age sedimentary rocks including carbonat es and siliciclastics. Light orange is com pos ed by meta-sedimentary and metavolcanic rocks. Light green are v olcanic rocks. Dark or ange is made up of granitoid ro cks of the Franzf ontein suite. No te the various mineralized sit es at th e Khorixas Inlier, the Meso po tamie farm, the Gelbinge n Farm, Kop permyn and Otjavasandu (T evrede). T here is active drilling at the last site to explore a large C u and Au mineralized a rea. Taken from th e Mineral Map of Namibia, 199 8, 1:1 ?0 00,0 00 scale, pu blishe d by the G eol ogical Survey of Namibia, Windh oek. 3 4 5 3 4 6 8.3 IRON OXIDE-COPPER-GOLD SYSTEMS IN THE LUFILIAN ARC IOCG systems occur on and around the granit o id massif s of the Lufilian Arc (Fig 8.7). Proper environments for develo p me n t of those systems are widely spread thr oughout. Massive iron oxide bodies with associated sulfides and other mineral iz a t i o n seem to have formed by replacement and infill of the host rocks. Thes e can be of various types, includin g true granite s, syenites, carbonatites, quartz ?pods 1 ?, albitiz e d schists , volcanic l as t i c deposits and carbonat es . ?Pregna n t? granito i ds have produce d ext ensive hydrotherma l alteration and variab le iron oxide mineralization, especia l l y when intrud i ng reac ti v e rocks like carbon a t e s , black shales or carbo na t i t e s . Large bodies of hydroth er m a l iron oxide rocks are found near the intrusi v e contac ts . Many types of mineralization geometries are know n, includ i n g brecci a pipes as well as tabula r vertic a l and horiz o n t a l breccio i d bodies (Stohl , 1972; Stohl, 1977; Hitzman, 2001; Phillips, 1959; and Phillips, 1958a). Subvolcanic porphyritic intrus ives and apophy s es of the main massif s accoun t for most of t he mineralization. In general terms, the margin s of plutons or their distal satellit e bodies seem to be better environ m e n ts for IOCG systems. The followi ng pages will describ e relation s h ip s between granitoid and iron oxide bodies , types and featur es of iron oxide bodies, hydrothe rmal iron oxide alteration , hy droth er m al breccia t i on in Lufilia n Arc IOCG systems , structural control and particular alteration features . 8.3.1 RELATIONSHIP BETWEEN GRANITOIDS AND IRON OXIDES Evidence of clos e temporal and spatial relationship s betwee n the iron oxide bodies and granit i c rocks is widely spread througho u t the Lufilia n Arc. An associati o n of four types of rocks is common in many parts : iron oxide bodies (of both magnetite and/or hematite), small gabbr oic bodies , small outcrops of red- alte r e d fels ic or syenitic intrusives and quartz bodies (See Figs 8.8 to 8.11). So me localit i es show coarse magneti t e- b ea r i n g intermed i a t e intrusi v e rocks with weak copper minera lization. This is seen on outcrops near Otjiwarongo, Namibia ; it occurs in some rocks of the Hook Granite Massif and in sites around Kasemp a and the Kafue Flats region of Zambia. At times, magnetite fills thin vein s in the intrus ives; thes e may grade into sheeted veins and/or stockworks. Coarse magnetite is often associated with sulfides. Magnetite ?clusters? up to 1 cm in diameter in gran it o i d s and subvol c a n ic rock s may produce a black and white ?dalma t i a n rock? texture in some intrusi v e rocks lo cated NE of Otjiwar o ng o , Namibia. The origin of this type of texture is not very clear. It mi ght be produc e d by immisc i b l e iron ox ide ?droplets? in the magma, by iron oxide nuclea ti o n and growth , or as a secondary alterati o n that over prin ts previous intr us ive textures. The last alternat i v e seems more plausibl e , bec ause prelimin a r y macros c o p ic and petrogr a ph i c studie s show that magnetite is emplac ed after all of the other minerals of the rock. As a working hypoth es is , part or all of the silicates seem to dissolve in orde r to make space for the iron oxides . This may take place during sodic alteration (albitization) of the rock, where biotite acts as nucleus for the replac eme n t of magneti t e . Throughout the Lufilian Arc, small gabb roic bodies (i.e.: dikes, plugs and sills) seem to be associ a t e d with most copper and gold occurre nc es related to iron oxide bodies , in a manner not yet well underst oo d . The same seems to be true in most wester n South Americ a n IOCG deposits (Injoq ue , Atkin, Harvey, & Snelling, 1988; Injoque, 2002; Sillitoe, 2003 and per sona l observat i on s ) . Figs 8.8 to 8.11 illustrate the type of small mafic bodies that occur. Subvolc a n i c dacitic porphyr i t i c intrus i v e s in the Andean IOCG systems are called ? ocoitas? . 1 A description of the quartz pods is included below in the chapter Particular Alteration Featur es (6.4.4.2.). 3 4 7 Fig 8.8 Quartz bodies, gabbros, felsic granitoids and iron oxide bodies that outcrop together east of Solwesi, Zambia. T h e s e are all small bodies of rocks that occur together in a rift environment. T h e d ou b l e line that cuts across from left to right is the main ro ad from Kitwe to Mwinilunga; Kitwe to the east, Mwinilunga to the w e s t . H os t rocks in this case are Katangan carb onates and siliciclastic units. Co mpare this map with that from Filuya, Nigeria on section 7.3, t hat show s many small mafic bodies. For scale, tick marks are separated 1 km. I n t erpreted from public 1:100,0 0 0 scale geolo gical map sheet p u b lished b y t h e Zambian Geological Survey Organization, Lusaka. Fig 8.9 Quartz body and metamorphos ed gabbros that outcrop to gether to the northeast of Mwinilunga, Zambia. Host rocks are gneisses from the domes. O utcrops are out lined in darker color. Th e double brok en line is a tertiary open road. For scale, tick marks are separated 1 k m. Interpreted from pub lic 1:1 00,00 0 scale g eol ogical map sheet p ublishe d by the Zambian Geol ogical Survey Organization. 3 4 8 Figs 8.10 and 8.11 Young gabbroic bodies that inters ect all rock types to the northeast of Solwesi, Zambia. Most of the bo dies are too s mall to map at this scale. Many quartz b odies and fl oat of magnetite are also pres ent, but they w ere not identified b y cartographers. Sm all fe lsic intrusives also outcrop, but are hard to find due to w eathering. F or scale, tick marks are separated 1 k m. Interpreted from pu blic 1:1 0 0 ,000 scale g eol ogical map sheet pub lished by the Zambian Geolo gical Survey Organization. Fig 8.11 is an en largeme n t of Fig 8.10. Many smal ler quartz bo dies and felsic intrusives that outcrop are too small to be mapped. Gabbroic rocks are younger th an all Katangan un its mapped here. Work on gabbroic rocks from the Lufilian Arc is conti nui n g . As a working hypothes i s , gabbros and dior itic rocks are thought to be the source of copper, cobalt and other metals like zinc, nickel, molybdenu m and 3 4 9 p l a t i n u m group metals that are enriche d in some IOCG deposits and pros pec t s . Gabbroi ds may be one of multipl e sour ces . Gabbros predate main mineral i z a t i o n in some of the deposits with reas onabl e geochron o lo gi c a l data. They could have been altered by large hydrot h er m a l IOCG systems driven by more felsic plutons , enrich e d in sodium and silica and depl eted in metals. Barron, Broughton , Armstron g, & Hitzman, 2003 carried out resear ch along the same lines, and Kapenda, Kampun zu , Cabanis, Namegabe , & Tshimanga, 1998; and Kampunzu, Tembo, Matheis, Kapenda , & Huntsma n- Ma p i l a , 2000 also evalua t e the relevanc e of small mafic igneous rocks in the Lufilia n Arc. 8.3.2 IRON OXIDE BODIES Iron oxide bodies in the Lufilian Arc occur as cement for hy drothermal breccias and filling for numerous fract ur e zones (Brand t , 1955; Cikin , 1968; Dawson, 1982; Drakulic, 1984; Drakulic, 1984; Johns, 1982; Moore, 1964; Phillips, 1958; Phillips, 1959; Stohl, 1972; and Stohl, 1977; also personal observations near Lusaka and in the Kafue flats region, Zambia). Nambian geologic a l literatur e contains very few descript i on s of iron oxide bodies, althou gh massive hematite and m agneti t e bodies have been ob serve d by the author at many location s . Host rocks of ir on oxide bodies in the Lufili an Arc genera l l y displa y sodic and sodic- c a lc ic alteration. Part of the iron oxide bodies carry associ a t e d sulfid e minera l iz ation, including pyrite and copper minera l s like bornit e and chalco p yr i t e (Dawso n , 1982; Cikin, 1968; Burnard et al., 1990a; Burnard et al.,1990b; Burnar d et al, 1993; and Hitzman, 2001). So me of the know n IOCG deposits and pros pects in the region contain very partic ula r chem ic al signatures. These may be marked by abundance of one or more of the following : uranium, LREE minerals, phosphorus, cobalt, barium minerals, silver, platinum group elements, titanium minerals and vanadium, apart from copper a nd/or gold. Some deposits do not contain any copper. A significant number of the previous elements have affinity to mafic and ultramafic rocks. Two iron oxide sample s from the Greater Lufilia n Arc were analysed and they are described on the chapter about the West Lusaka-Kafue Flats area, Zambia (4.1.2.4.4). In location s of western Zambia, large iron oxide bodi es displa y a particu la r geomor ph o l og i c a l expres s i o n . They protrude as needles up to a hundred meters above the average elevation of t he plateau. An example of this can be seen on Fig 8.12 which depicts a magnetit e hill lo cated just to the west of Lusaka and very near to the site of the Nampund w e (or King Edward) pyrite mi ne. Gabbros and red syenites occur in the environs. Some of these iron oxide bodies carry disseminated sulf ides. Similar hills oc cur near Kasempa, to the NW of Mumbwa and also in the Democr a t i c Republ ic of Co ngo. The Namibia n counte r pa r t of Zambian iron oxide bodies does not form such structu r es , probabl y due to less rainfal l . Fig 8.12 Hill of massive magnetite that outcrops west of Lusaka, Zambia . As show n here, massive iron oxide bo dies in this part of the Greater Lufilian Ar c produce thes e interesting ge omorpho logi cal features. They stand o ut up to 1 20 meters abov e the average flat plateau. In the foreground, rolling hills are s yeniti c intrusive bodies. Small gabbroic bodies are also foun d in the environs. A bundant hydrothermal breccias with su lfide mineralization occur here too. Iron oxide bodies emplac e themselv es after the dissolut ion of the host rock takes place. A gradual change from normal rock into iron oxide has been observ e d , progres s i v e advance induced by hydroth e r m a l dissolu - tion of silicates and replac emen t by iron oxide. Probably fluori n e- r ic h soluti o ns play an import a n t role in the proc es s . 3 5 0 Progressive iron oxide alteration over pr ints textures of granitic rocks, sedimentar y rocks and hydrothe r m a l breccia s ; sometim e s to a point where the origina l ro ck is unidentifiable. This was observed ar ound many intrusive bodies; ther e is a gradual change from unaltered rock to similar rock with the ?black and white texture? or the ?magnetite diseas e? (Fig 8.13) that progressively becomes a 100% magnetite rock. Red hematite also produce s similar alterat i on features , as show n on Fig 8.14. Fig 8.15 shows some aspec ts of the progress i v e alterati o n . Core fragmen t s were taken from portions of exactly the same host rock, along a borehol e , at interva l s separat e d every three meters. As show n, progres s i v e iron oxide overpr in t i n g is an example of how iron oxide can make its spac e in a rock by dissolv i n g its space ou t. The intr usive body that produced the alteration is located towards the hematit e - e nr i c h m e nt . It was a subvolc an i c porphy r i t i c rock. In this cas e, the hos t roc k to alteration is a polymic t ic , round pebble hydr othermal explos ive breccia. These breccia s will be discus s e d furthe r in this chapter . Equivale n t gradual change was observed in several granitoids. Another interesting iron oxide miner alization feature is illustrated on Fig 8.37. Fig 8.13 Magnetite ?disease? in a felsic granitoid that is very light pink when fresh . Progressive magnetite replacement of silicates near mineralized IOCG systems in the Lufilian Arc. This type of hy drothermal alteration grades from very slight to completely pervasive. From borehole MB - 3 4 , Kasempa area, Zambia. Fo r scale, ticks are millimeters. Fig 8.14 Hematite ?disease? that overprints a polymictic hydrothermal breccia . Note small roun d clusters of red he matite t hat nucleate and grow until th e e ntire vo lu me of t he rock is replaced by minute he matite crystals. So metimes the previous texture is complete ly oblit erated, and original proto lith cannot b e recogn ized . All compo nents of the previous rock have b ee n replaced by a massive, non-s el ective process . T h is type of hydroth ermal alteration increases towards the IOCG mineralization, and towards the intrusive bodies res p onsible for the alteration/ mineralization. From b orehol e MB-34, Kasempa area, Zambia. For scale, centimetric/millimetric lines. 3 5 1 Fig 8.15 Progressive ?red-rock? hydrothermal alte ration in round-pebble hydrothermal breccia . T he fresh est rock 2 in th e l ow er core gradually changes into an entirely d ee p red rock in the upp er one. T his is an example of hydroth ermal iron oxide alteration. It can take p lace in almost any ty pe of rock, o bliterating previous textures and all f eatures. Sometimes previous quartz fractures se e m t o be leached aw ay and nothing is l eft be hind except for th e massive red mass full of disse minated h ematite crystals. A fragment in the l o w er core has ?he matite disease?. N ot e t he p oly mictic character of the breccia and rounding o f some clasts. Fragments are alte red in v ery different ways as se en. T h e large fragment to the left of the s econd core from th e botto m s how s concentric hematite alteration advancing inward. R ou n ding of clasts will be ex plained in the fo ll owing item. Core fragments w ere tak en every 3 m to s how variation, but a compl ete alteration continuu m occurs in outcrop and core. From b orehol e M B-34, Kasempa area, Zambia. See d etails in text. Diameter of core is 5 cm. 8.3.3 BRECCIAS Multiph as e hydrot h er m a l breccia s with strong K-iron al teration (biotite-seric ite-magnetite-hematite) and pyrite occur on or around iron oxide bodies in the Greater Lu filian Arc. Sometimes thes e breccias have a matrix of metallic hematite and/or magnetite, with evidence of explosive hydrothermal activity. Initial Na feldspathization (albitization) is overprinted by bi otit i z a t i on (potas s ic altera t i o n) . Round- c l as t breccia s cement e d by ir on oxides are a common featur e in some portio ns of the IOCG systems of the Lufilian Arc. Figs 8.15, 8. 16 and 8.17 show polymic tic round-peb ble hydrothermal breccias that surround subvolca n ic porphyry t i c intrus io ns in IOCG systems in northwestern Zambia. Clas ts of various intrusi v e , sedimen t a r y and metamor ph ic rocks are presen t . Packing is very dense and almost all clas ts are rounded. It seems that corrosion of extremel y alkaline or acid hydrot h er m a l soluti on s etched angular rock fragmen ts, rounding them. 2 The ?freshes t rock? is slightly altered. Its fragme n t s and matrix contain minute dissemi na t e d chlorit e and amphiboles. As illustrated, part of th e clasts displa y ?hematite disease?. The varied chemis try of the clasts reac ts in different ways to the types of hydrothermal alteration. 3 5 2 Fig 8.16 Typical features of polymic tic, round-pebble hydrothermal breccia. T his t ype of breccia seems to form by extreme corrosion of hyper-alka line fluids that move around in IOCG syst ems. Fragments t hat were previously angular are corroded. Clasts display sev ere packing and ma trix is mainly smaller, more resistant grains. Note variable grain size and composition. From b orehol e MB-34, Kase mpa area, Zambia. See details in text. Fig 8.17 Aspect of poly-brecciated polymicti c round-pebble hydrothermal breccia. T he large fragment to the upp er left of the ph otograph is compos ed of angular peb ble s and p oly mictic fragments, includ ing angular fragments o f chalcopyrite and pyrite. It has bee n round ed itself and make s up a large clast of the n e w breccia. The roun d fragments also contain s ulfide and magnetite clasts. F or scale, millimetric ruler. N ote that so me fragments are more angular in this portion of core. From boreho le MB-34, Kasemp a area, Zambia. Read more details in text . Round fragme n t s in hydrot h e r ma l breccia s have been mis-id en t i f i e d in the past as ?Grand? and ?Petit Conglo m er a ts ? , as ?tecto n ic brecci as ? and as ?sedim en t a r y breccias ? (Johns, 19 82; Cailteux, 1995; Stohl, 1972; Pollard, 2000; and Binda, 1995). Part of the angular hydr o t h er m a l brecc i as and st ockworks observed at the Komba t mine, Namib ia , were mis- in terp r e te d as ?coll a p s e breccia s ? . See chapte r on the Kombat mine in the next pages. 3 5 3 8.3.4 STRUCTURAL CONTROL Structural control of IOCG deposits is held by intrus iv e - h os t rock contac t s , more reac ti v e strati g r a ph i c units, crus tal scale fractur es like the Mwembez h i disloc a t i on in Zambia, and local fractures in brittle rocks. We will now review aspects of rock frac turing to control IOCG , and major E-W controll i n g structur es in the Lufilian Arc. 8.3.4.1 ROCK FRACTURING TO CONTROL IOCG MINERALIZATION Albitization and silicific ation enhance rock brittleness, t hey allow rocks to fracture and become good hosts for IOCG mineralization. Quartzites also behave in a brittl e manner and produce favorable sites for new minerals. Densely-fractured rocks sometimes ho st rich mineralization. Figs 8.18 and 8.19 from northern Namibia illus- t r a t e that. Fig 8.19 shows a three- d i men s i on a l network of irregula r frac ture s that grades into a hydrother m a l jigsaw breccia and later into an angula r transp or t e d brecci a . Fractur e s in the stoc kwor k of Fig 8.18 are formed by three distin c t families of joints that are roughl y perpe n d ic u la r to each other . Both stock w o r k syste m s accoun t for hundreds to thousands of cubic meters of ir on oxide mineralization with sulfides , akin to IOCG mineralization. On both cases, note that mineraliz ation takes plac e from the fractures into the host rock. Fig 8.18 Typical angular stockwork mineralization in a foliated granitoid host rock. T his pattern of fracturing is produced by three su b-p erpendicular joint families and allow s for very large vo lu mes of IOCG mineralization. S ee tex t for further details. Scale in centimeters. Fig 8.19 Typical irregular stockwork mineralization in a felsic non-foliated granitoid. T his pattern of random fracturing d oes not see m to follow any rule. IOCG mineralizati on is hoste d by this type of stockwork, and it grades from fresh, undisturbed rock through hy drothermal jigsaw brecci as and into breccias with comp lete l y displaced clasts. From one of the mineralized areas along the N-S transect, Oas fa rm, Namibia. Scale in centimeters and millimeters. 3 5 4 8.3.4.2 E-W STRUCTURES A regiona l model on the nature of granit o i d s and their metallogenic significan ce at Mesopo tamie, Lofdal and Oas farms in Namibi a was put togethe r , as show n on Fi g 8.6. Most of the miner al i z a t i o n observe d in or around the Kamanjab Batholith and the Khorixas Inlier seems to be controll ed by subparal l e l regional E-W- tren d i ng major fault systems. The term E-W struct u r e s is used here somewh a t loosely. Most of the structures that fall under that denomination are actually N68?E; t hey follow the general trend of the Lufilian Arc. Rifting and later collisio n fronts had roughly the same relative orientat i o n . The major control l i n g structu r e of the Luiswishi, Shituru and Kamoya mine s in the Democratic Republic of Congo is also an E-W trending fault. Main orientation of the minera l iz a t i on and planar iron oxide bodies at these sites almost coinci de s . The Otjiko t o gold deposi t NW of Otjiwarongo, Namibia is also related to a system of thes e E-W trending faults. These E-W structur es may be long-lived crus tal frac tures that remain in plac e since the onset of rifting . They probably were reactivated through time as varying types of structu r es , includ i ng strike- s l ip faults and normal faults. Structur es that original l y were normal faul ts associ a t ed to the ri fting events, could have been reac ti v a t e d into thrusts during basin invers io n . Henry, Clenden i n , Stanist r ee t , & Maiden, 1990 discuss some aspects of these featur es and the origin of ma in faults in central and northern Namibia. Most of the fault systems may not be accurate l y mapped due to lack of out crop in parts of the Lufilia n Arc. Recent mapping in NW Zambia by Key et al., 2002, shows abundan t previou s l y un-iden t i f i e d E-W thrus t faults. An E-W structure connec ts the northern part of the Summas Mo untain s (Fig 8.6) and repeats the lithology. It may be a fracture of simila r orientation to t he previous l y describe d , t hat acted as thrust fault repeatin g stratigr a ph y . Various types of mineraliz a t i on observe d in the Kamajab Batholi t h are also associa te d to those E-W structures (Fig 8.6). The southern portion of the Tevrede fa rm (NW of Kamanjab Batholith, Fig 8.6), site of IOCG deposi ts under explor a t i o n , seems to be controlled by that ty pe of struct u r e . Another one seems to enter the Gelbing e n farm and controls mineral iz a t i o n there. These E-W fractures are quite eviden t in the publis hed geolog ical maps (Fig 8.6), for they allign copper, iron and gold mineralization (Schneider & Seeger, 1999; Burnett, 1999; Burnett, 2000; and Ajagbe, 2001). A N-S fractur e control s gold mineral iz a t i o n to the W of the Kamdescha Farm in Namibia. The main frac tures that control the Kombat mine and its satellit e deposits in the Otavi Mountains of Namibia also run E-W. This may be a regional feature that is relevant for intrusio n and control s the migrati o n of mineralizing fluids (Fig 8.6). The Mwembez h i Disloc a t i on in Zambia is anothe r major NE -SW struct u r e that contro l s granit o id intrus io n and associa t e d mineral iz a t i on (Simpso n , 1962; Simpson & Stillman, 1963; DeSwardt & Simpson, 1972; Abell, 1976; Griffiths, 1978; Krishnan, 1978; Unrug, 1983; Coward, 1984; Kasolo & Foster, 1991; Hans on , Wardlaw, Wilson, & Mwale, 1993; and Molak, 1995). See country map of Zambia on Figs M1 and 4.3. The Kasempa area, in Zambia, also has important E-W structures that control magmatis m and metallogeny. Several other major frac ture s run parallel to the Mwembezh i Disloc at i o n , includin g the Mkus hi and Serenje faults. Some of the E-W faults cut across the batholiths , limit them, serve as conduits for the extrusion of granitoid rocks, and control mineralization. They played a very important role in the emplacemen t of granitic rocks throughout the Lufilian Arc and have not been adequately studied. The Mwembe zh i Disloc at i o n , one of Zambia?s largest structur al features , has not been well mapped, described or understood. 8.3.4.3 PLANAR FEATURES OF IRON OXIDE BODIES Iron oxide bodies may display layering and/or bedding. Sometime s discrete massive iron oxide bodies are interlayer ed with plane- structured units that are presumably derived from s hales and other types of bedding. At first sight, these planar features may look like band ed iron formations ; they ar e produced by selectiv e replac ement that confor ms thick, extensive, stratabound ir on oxide bodies. Some of those bodies have been mis-ide n t i f i e d as banded iron form ations in the Lufilian Arc. Neverthe l es s , they show a close spatia l (and tempora l ?) relation s h ip with hydroth er m a l magneti t e- b ea r ing intrusi v e bodies, and displa y relict round-p eb b l e hydr ot h er m a l breccia t i o n . The Kasumba l es a body of Zambia is an example of these features (Fig 8.20), as de scribed by Stohl, 1972; Madi- Lugali, 1975; and Bala-Bala & Madi-Luga l i , 1979. Surpris i n g l y , none of the Congoles e aut hor s knew about the writin gs of geolog is t s workin g on the same tabula r body in the Zambia n side of the border , and viceve r s a . Dikelike magnetite and/or hematite veins occur as feeders to the tabular conforma b l e iron oxide bodies. 3 5 5 The age of the iron oxide mineralization at Kasumb alesa, in the borde r betwe en the D.R.Con g o and Zambia, is clearly older than the Grand Cong l o merat , because large fragmen ts of iron oxide with the same featur es as Kasumb a l es a are seen inside the Great Conglo m er a te that lies on top of the tabular iron oxide layer (Stohl, 1972; Watts, 1991). This is very significant. Ther e might be a relati o n s h i p between the gabbro ic bodies that occur in the lower Roan and the iron oxide bodies , as seen to the east of Solwes i and elsewhe r e . Another simila r exampl e was found at the Kamoya Cu-Co mine in the Democratic Republic of Congo. Ongoing research at the northern wall of the main pit show ed that a tabular iron oxide body indicated to be a banded iron formati o n had at least three diagona l br anche s of iron oxide and cuts diagona l l y across stratification. It is thought to have been emplac ed along a faul t zone that cuts indurat ed volcan i c ash. In some cases, the iron oxide body carries sulfide s . Almost a ll of the secondar y coppe r mi nera l iz a tio n at the deposi t lies west of the iron oxide band (below it). Stohl, 1972 shows that the iron oxide body at Kasumbal es a is intersected by quartz -tou rmaline- iron oxide veins (Fig 8.20). In the D.R.Congo an in parts of Zambia, the Grand Cong l o merat is very magnetic, becaus e it contains the eros iona l product of magnetite layers. T hese are simila r to some veins seen near the Hippo mine (Cik in, 1968; O'Brien, 1958; and Page, 1974), Zambia and others near the Gelbingen farm in Namibia. Fig 8.20 Schematic geological section across the southeast margin of K asumbalesa Hill, Zambia. V ertical and horizontal scales are eq ual. From Stohl, 197 2. Note th e stra tiform layer of massive hema tite, here in terpreted as hydroth ermal replacement of iron oxide within favourable b eds with a suitable redox setting. Also note the unconformity, and angular fragments of massive iron oxide and vein material. A stratiform magnetite- hematite body occurs in the Ka semp a area of Zambia. Fig 8.21 pres en ts evidenc e of this, as shown on aeromagn e t i c images proc esse d by BHP-Billiton. A doubly plunging syncline is very evident in the maps of that area, as show n on Fig M9. The Kanton ga IOCG prospec t also is associa t e d to a tabular iron oxide replac ement body (Fig 8.22) The deposit is associa t e d to mafic intrus i v e rocks, apophys es of the Hook Granite Batholith. Note the lateral extension of the bodies. 3 5 6 Fig 8.21 Stratiform body of magnetite in the Kasempa area of Zambia. T his typ e of tabular replacement of iron oxides in sedimentary be ds is observed in nu merous loca tions through o ut the Greater Luf ilian Arc. Taken from Nisbet, 200 4b; the image was originally deve lop ed b y BHPBilliton. Fig 8.22 Cross section of stratiform body of magnetite at the Kantonga IOCG deposit, Zambia. Interlayering of discrete, massive iron oxide bodies with mafic sills. T hick, extensive, strata-boun d iron ox ide b odies w ere produced by selective replacement. T here is a close spatial (and te mporal?) relations hip with hy droth ermal iron oxide-bearing intrusive bodies. Part of the iron oxide bo dies display relict round- p ebb le hy drothermal brecciatio n. Note the pink diatreme cemente d by magnetite. From Hit zman, 20 04b. 3 5 7 8.3.5 PARTICULAR HYDROTHERMAL ALTERATION FEATURES Particular hydrothermal alteration f eatures observed in the Lufilian Arc will be described below. Alteration from nearby mineralizing systems over prin t each other. Sodic alterat io n is wide spr e a d and very importa n t in the iron oxide- copper-gold systems of the Greater Lufilian Ar c. Scapo li t i z a t i o n and albitiz a t i o n were observe d in various types of rocks around the IOCG systems. At times, alteration ext end s a few hundred kilome t e r s away from the center of the systems. Sodic alteration will not be discussed here. 8.3.5.1 TOURMALINE ALTERATION A special type of hydrotherma l alteration was observed in the wester n Kamanjab Batholith, and around Otjiwar o n go , Namibia (Figs 8.6 and 8.33). Monoton ou s bands of black tour mal in e and quartz , each five to ten mm wide produce the ?zebra alteration? pattern. This alte ration was seen to occur in silicified quartz ites and some time s in albitiz e d schi s ts and silic i c la s tic rocks . Portions of the western Hook Granite Batholith also displa y patterne d black tour mali ne in red granites and syenite s. In this case, the tourmaline occurs as braided and sheeted veins. Yet in other cases, tourmal in e was fo und to be the matrix of hydrothe r m a l breccias . No chemic a l analys i s of thes e rocks has been carried out to date, but it is expected that copper and maybe gold may be associated with tourma liniz ation. Significant bor on enric hmen t is another of the ?typical? alteration patterns of some IOCG mineraliz a tion. 8.3.5.2 QUARTZ ?PODS? Quartz pods are a partic ula r featur e that has been identif ied in most of the Lufilian Arc study region of Zambia and Namibi a . The term ?quart z pod? (here shor te n ed as QP) is an informa l name coined by the author for massive or sugary quar tz bodies of varying dimens ions. F eatures are very different from those of vein quartz and pegmat i t ic quartz bodies ; what seems most differ e n t is their geomet r y . The shape of quartz pods appear s to be roughly cylindrical, outcrops of undeformed bodies ar e round to elliptical, and their diameter varies from a few to several hundred meters. Some mapped bodies of quartz exceed four kilometers in diameter . There is geophy s ic a l evidenc e of even larger bodies . Quartz pods occur near intr us i v e bodies and around iron oxide- copper-gold mineralized systems. Most of the pods are made of white quartz, but color may vary greatly. Example s show change from milky white to dark gray smok ey tones and to light pink or yellow tints. These colors are probably due to abundant gas, salt, iron oxi de and sulfide micro- inc l u s i on s . Both transluc en t and milky varieties of quartz occur togethe r. Different por tions of a single body may be saccaro id a l and/or massive . Quartz pods are seldom mapped in publish e d geological maps of Zambia and Namibia. Identifyin g them in the field and studying their physical-chemic al feat ures may aid in the exploration of iron oxide- copper- g o l d mineral iz a t i o n . 8.3.5.2.1 Description of Quartz Pods Quartz pods seem to be a partic u l a r charac t er i s t ic of the Lufilian Arc, and may somehow be related to rift environments. They occur in many different types of rocks includ i n g limesto n es , dolos to n es , granit oi d s , various schists and gneisses. The author has seen t hem occur in an extensi v e region, roughly 2000 km by 300 km; QP are also expec ted to be found in SE Angola, the Katanga pr ovince of the Democratic Republic of Congo, and NW Bots wana (See Fig 8.23). The author tried to locate them wher ever they weree spotted , sampled them for regional comparis on, and whenever time allowed, walk ed around them with a GPS to study their surfac e geometry (Fig 8.24) Se veral dozens of QP were intersec ted along the roads. Points of interse c t i on were recorded , and cons tit u t e a simple measume n t of the size and abundanc e of quartz bodies in the Lufilian Arc. That ch ance sampling is not re presentative, but it is all availa ble for the time being. A few of the QP were sample d with the hope to find partic ula r c hemic al or physical features of use in explor at io n . Prelimi n ar y results describ e d here are a by-prod uc t of field samplin g for a regiona l projec t on granito ids in portions of the Greater Lufilia n Arc. Fig 8.24 Types of quartz pod outc rops observed during fiel d work, Greater Lufilian Arc Granitoid Project. Q P w ere encountered along th e main roads (thick black line) w hile sampling f or granitoid rocks in Zambia and Namibia. A few of the perimet ers (gray poly go ns) w ere measured by walking with a GPS. 3 5 8 3 5 9 In many locations, QP have been found to host IOCG minera lization. At times QP themselves acted as brittle rocks to hold massive magnetite and/or spec ular hematite mineraliz ation with accompanying sulfides. This is show n on Fig 8.26 D-H. The Egue farm, located NE of Otjiwarongo, Namibia and in the environs of the Otjikot o gold deposit has a massive quartz body, 500 meters in diameter. After ca rryi ng out airbor n e and field geophy s ic s , the Namibi a n division of Anglo Amer ican drilled in the center of th e body sear chin g for metallic minerali z a t io n and could not find the bottom of the quartz body. A borehole 325 meters deep was collared in quartz and finished in quar tz with minor dissemin a t ed pyrite. In this case, the qu artz pod seems to be associ a t e d with the Otjiwa r on g o Batholith, a large granitoid entity that lies beneath Ka lahari sand, Katangan carbonat e s and calc rete . The Otjikot o gold deposit , current l y being develop e d by AngloVa a l , is located a few kilometers away from the QP; the Kombat copper mine also seems to be related to the Otjiwarongo Batholith. Both mineralizations have recently been classified by the author as iron ox ide-co pp er - gold deposits . There might be more of these deposit s under cover. Someti m e s the count r y rock is defor me d upwar d ar ound QP, as if they had somehow intruded themselves forcefully in a fashion similar to that of diapirs (Fig 8.25). This behavi o r was observ e d in outcrop s locate d to the west of the University of Nami bia, Windhoek , as show n to the autho r by Dr. David Roberts o n from the same university. Fig 8.25 Sedimentary bedding and/or foliation that bends around quartz pods. In some locations, country rocks have b een se e n to fold around the quartz b odies. T he reason fo r this be havior is unkn ow n. It might b e due to differential compaction of the various b e ds and n on-compaction of q uartz p ods, or dissolution of water-sol ubl e salts in the country rock. The diagram has no particular scale. Some publishe d map sheets of Zambia have QP on them . Very few references specific ally describe these bodies ; maybe they were conside r e d to be simple quart z veins of minor importance. There is very little mention of quartz bodies in Namibian geological literature. Two Zambian locations displa y well-exp o s e d QP. One is located west of Kitwe along a road near the Congol es e border . Anothe r lies east of Solwes i and is show n on Fig 8.8. Both occur in cluste r s and have bodies that are more than 500 meters in diameter. 8.3.5.2.2 Four Rock Association A four-fold rock association is observ e d in many parts of the Lufilia n Arc. This is made up by small bodies of gabbro or diorite , small bodies of red-tin t e d felsic in strusi v e rocks, massive iron oxide bodies (magne ti t e and/or hematit e ) and quartz bodies. All of these seem to occur in rift environ me n t s , and their origin is not yet comple tely understood (See Fig 8.8) . Explaining the ubi qu i t o us pres e nc e of these four rock types might provide ideas for the origin of iron oxide-c o pp er - gol d mineralization in the Greater Lufilian Arc, and more importan t l y , may give clues for mineraliz a t i o n elsewher e . 8.3.5.2.3 Particles Enclosed in QP On some locati o n s , the large quartz bodies contai n isol ated spherical ir on oxide (h ematite and/or magnetite) inclus i on s that vary in size from a 10 cm diamete r to 1.5 cm diamete r as shown on Fig 8.26D. It seems that the iron ?bubble s ? occur inside the quartz as if they were immiscib l e subs tan c es or xenocrys t s . At times, hemati t e or magnet i t e cubes occur in quartz (See Figs 8.26A, B and C). Sometimes xenoliths of any type of countr y rock are includ e d within the quartz bodies . Shapes of these xenoliths vary wi dely. Many questions still remain unanswered : Can the FeOx spheres in quartz be a product of immiscib l e fluids , or incomple t e assymilation of previous euhedral iron oxide minerals ? W hat are the relation s h ip s with gabbroic bodies , small syenitic bodies and iron oxide bodies? At times the brittle char acter of quar tz allows it to be host for braided or sub-pa rallel sheeted veinlet systems filled by hematite and sulfides (Fig 8.26H). Numerous field examples show braided veins, stockworks and various breccias where quartz is both the host rock and the single componen t of clasts . Figs 8.26 3 6 0 D-H illustrate that well, at the scale of a hand samp le. Similar features were observed on sample s from Tevrede , a rich copper and gold IOCG prospe c t in the northwest Kamanjab region, Namibia (www.boulde rmining.com). Fig 8.26G is a slab of massive milk y quartz that is hos t to brecciation and specular hematite mineraliz ation with iron and copper sulfid e s . This is a fragmen t from a quartz pod that behaved in a brittle manner and offered a good host for IOCG mineralization. 8.3.5.2.4 Studies that can be Done on the QP Investigations on the QP might reveal interesting chem ical signatur es that will probably contribute to the field explorat i on of IOCG deposits in southe rn Africa. On -goin g resear c h on QP includ es detail e d macros c op i c analysis of features , measurement of radioact i v i t y and fluoresc e nc e under variou s waveleng t h s , cathodo l u m ini s c e nc e studies , detaile d determin a t i o n of s pecific gravity, chemical analysis , bibliogr a ph i c a l review , studie s of H and O isotope s , rare earth conten t, halogen conten t, fluid inclus ion studies to detect salinity and temper ature of emplac emen t, decrepitation st udies to evaluate detailed chemical compos it i on of the fluid inclus ions , metallic content, study of the contacts with iron oxide inclus io n s , and study of the braided veins, their contacts with quartz and chemical char ac teristics. The three- d im e n s io n a l geomet r y of quartz bodies might be studie d in a few well-k n ow n outcrop s using seis mic profiling, elec tric al resistivit y profile s , vertica l electric a l soundin gs and electric a l tomogra ph y . Detaile d IP profiles may also contribute significantly. Four sites for this have been identified in the Greater Lufilian Arc. They are all easily accessib l e along main roads. 8.3.5.2.5 Practical Applications of the QP The fact that QP are related with iron oxide-copp er-gol d mineralized systems is very significant. Their positive identif i c a t i on as part of IOCG syst ems might become a major breakthr o ug h in mineral explora t i o n . If as thought , the detaile d chemica l signatur e of quartz bodi es from mineralized IOCG systems is found to be somewha t anomalo us and charac t er i s t ic , chemic a l analys is of outcrop p i ng quar tz bodies and of large areas with quartz float may provid e a new ex ploration tool. Positive field identif i c a t i on of IOCG-r e l a te d QP could help to select prospective areas for IOCG deposits. Abundant float of white quartz in a circular area may be detecte d easily on arid regions . Outcro ps of these quartz bodies offer a good color contrast with the country rock; thus black and white air photograp hs may be an aid to their location . The large outcrop area of so me QP can make them identif i a b l e in ASTER images and on other remote l y - s en s e d images . Large QP in part of the Kamanjab Batholith in Namibia are evident on ASTER and hyperspec tral airbor ne images. 8.3.5.2.6 Hypothesis About the Origin of QP The origin of the QP is not well understo o d . Many hy potheses for their occurren ce come to mind. They may be a type of silicific ation alteration that is not yet well documented in the literature. The idea of hyper-alkaline fluids dissolvin g silica in one place and producing t he quartz bodies in anothe r place was briefly proposed by Behr, Ahrend t, Porada, Rohr s, & Weber, 1983 while studying chloride -rich inclus ions in QP. Sabkha enviro nm e n ts near rift system s certai n l y could produc e ve ry saline fluids. But how can the space for the pods come to be? How did silica get in place? The most reasona b l e working hypothes i s based on field observations, is that QP are produced by extremely alkaline fluids rich in HF that dissolve silica in rocks replac ing it by iron sulfides (Fig 8.27). Silica migr ates further out and precipit a t es quartz bodies . But again, the questi o n is how can the spac e for quartz bodies be produc ed ? How could one detec t fluori n e in fluid inclus ions if the way to diss olve silicate s involves HF? Fig 8.27 Schematic diagram to s how process of quartz pod formation. Space for the emplacement of massive magnetite bodies was diss olv ed out from th e h o s t rocks. Silica from the dissolved mi nerals migrated outward from the site and later became massive quartz p ods in favorable e mp lacement sites. All th e process is carried out by warm hydroth ermal fl uids. T his process may occur at varying scales. T he radius of magnetite b odies and quartz p ods may be up to a few kilome ters long. 3 6 1 Fig 8.26 Various features of iron oxides in quart z pods (QP) of the Greater Lufilian Arc . A and C are cubic fragments of magnetite h o sted by a QP. B is a sub-roun ded fragment of magnetite f oun d inside a QP. D, portion of a sulfide-rich, magnetite-fille d stockwork hoste d in a QP. E and F are sulfide-rich, magnetite stockworks hosted in QP. Field of view is 1 5cm. G is a hydrothermal angular clast brecci a cemente d by magnetite t hat is host ed in a QP. Clasts are made of quartz fragments. H is a series o f closely- packed, subparalled sheete d veinl ets hosted in a QP. A and E have scale marks ev ery mm; B and D, every 2mm. 3 6 2 8.4 SOME KNOWN IOCG-LIK E DEPOSITS AND PROSPECTS The Greater Lufilian Arc of Zambia and Namibia is a pros pe ctive zone for the exploration of economic IOCG mineralization. Below is a descrip tion of some operating deposi ts and prospec t s that are very akin to IOCG syste ms . Mines and occurr e nc es in the Demo cr a tic Rep ublic of Congo that are cons idered to be of IOCG origin will be described later. Table 8.2 compiles some of the main IOCG deposits . Fig 8.7 illustra t es the location of the main deposits and prospe ct s . 8.4.1 NAMIBIAN DEPOSITS AND PROSPECTS 8.4.1.1 OKATJEPUIKO PR OSPECT, WITVLEI, NAMIBIA An un-dimens i o ne d IOCG deposit exists under the Witvlei sediment ar y - h o s t ed coppe r deposit at the Okatjep u ik o farm, Namibia. As seen on Fig 8.29, seve ral authors describe mineraliz a t i o n from Witvlei to be a ?typica l? copperbe l t deposit (Borg & Maiden, 1986 ; Maiden, Innes et al, 1984; Steven, 1993; Ruxton & Clemmey, 1986; and Anhaeusser & Button, 1973; and Moodie, 2000). Eckhart Freyer of Anglo Americ an explorat i on in Namibia offered abundant informat i o n on the deposit and the region (Freyer, E., personal communic a t io n s , 2002, 2003). See general location on Fig M26. More details are include d on section 4.2.2.6 . Fig 8.29 Geological map of the Witvlei site, and location of the Okatjepuiko IOCG prospect. As show n, the main road (in red) from Go babis to Windho ek cuts across the map. Ther e is also a railroad that runs parallel to that road. Farm bou ndaries are marked by po lygo ns. Note the ?Malachite Pan? and Witvlei Pan that are lo cated around the mineralized area. Th e belt of dark rocks t hat runs NE-S W extends un d er cove r into B otswana, and f urther s outhw e st in Namibia. Not e the roun d and sygmoid symb ols that indica te tabular copper mineralization. More details in text and on section 4.2. 2.6.. Rich gold and copper mineral iz a t i o n (3.5 gAu/ton and multi percent Cu) has been found on surfac e samples (Freyer, E., persona l communication, 2003). A subvolc anic porphyritic intrusive rock seems to produce mineralization. Gabbros as well as felsic intrusive rocks outcrop at t he Okatjep u ik o area. Subroun de d - c l as t hydroth er m a l breccias with intens e brown (iron oxide) alteratio n al so outcrop. Massive magnetite and hematite fragments occur as float. In fact, a strong magnet ic anomaly guided exploration to the site. Gold is not present in the sedim entary-hosted copper deposit; it probabl y remaine d underne a t h in the origina l hypogene deposit. All of these ingred ients point to an iron oxide-c op p e r - go l d mineral iz a t i o n at depth. 3 6 3 Evidence of IOCG mineralization under at least one of t he sedimen t a r y - ho s t ed copper deposit s of Namibia is very importan t . The pres en ce of both hydrother m a l cop per and gold under the Witvlei deposit is relevant to understan d the regional metallog e n y , and could lead to a completely differen t source for copper in the Greater Lufilian Arc. This type of mineralization probably extends NW into the Ghanzi-C h ob e Belt, of Botswana (Moodie, 2000; and Steven, 1993). Other belts of similar age in the region can be pros pe cted for IOCG mineralization. Another possibl e case of IOCG under a sediment a r y - hosted deposit might exist in Zambia. The Kalumbila, sedimen t ar y - h o s t ed copper (nickel- c o b al t ) deposit in NW Zambia described by Steven & Armstrong, 2003 is closely associated to small granitoid and gabbroic intrusions, and might be underlain by an IOCG deposit. 8.4.1.2 KOMBAT MINE, OTAVI MOUNTAINS, NAMIBIA The Otjiwarongo Batholith, intrusive bo dy that measures approximately 200 km by 40 km wide, is thought to exist undercover below carbonates and Mesozoic sands to the NE of Otjiwarongo, Namibia. Geophysical evidence produced by Dr. Branko Corner for Anglo V aal supports the presence of that hidden batholith (Cor ne r , B., persona l communi c a t i o n , 2003). It may be respons i b le for the know n abundan t copper and gold mineralization in the region, including the Kombat mine, Uis West, Asis North, and others in the Kombat distric t . The mine is owned and operate d by Ongopo l o Co rporation, a Namibian-ba sed mining compan y. It has been active since the 1960?s, and is one of the major co ppe r produc e r s in the count r y . The reserv e databas e has been increased progressively with time to allow fo r further undergr ound development. Five or six year ?s worth of reserves are all known, but new ones are found as the mine is exploited. Ongoing investigations at the Kombat copper mine in t he Otavi Mountains of Namibia (See location on Figs M25, M19 and 8.33) show physical features that are akin to the iron oxide-cop per-gold (IOC G) deposit type (Table 8.2) . Brecciation and stockworks of hydr other ma l origin hos t mos t of the ore-gra d e rocks at the mine (Fig 8.30). Primary copper mineralization always occurs near or around large bodies of iron oxides (Innes, 1983; Galloway, 1988; Deane, 1995; Innes, 1986; S onge, 1957; Pirajno & Joubert, 1993; and personal observations). Figs 8.31 and 8.32 illustrate this well. No direct rela tionship with granitoid rocks has been establis hed to date. Frank Melc her (Melcher , F., pers on a l communic a t i o n , 2003 and Melc her et al, 2003) state that sulfur isotopes for the Kombat mine are in the 30-24 d 34 S range, whic h indicat e s an igneou s input. That had been previous l y establis h ed by (Piraj no, Kinnaird, Fallick, Boyce, & Petzel, 1993). Field observati o n s and critical reading of literatur e ava ilable on the mine lead to conc lude it is a deposit of the IOCG family (a copper-rich end-member). Probably ot her copper deposit s in the Kombat region have similar origin. All the primar y occurrences of gold that surr ound Kombat are hydrotherma l and could also be attribu t e d to the hidden bathol i t h (Figs M25 and 8.33). The same igneous body could also produc e minera l iz a t i o n of the sediment-hosted gold (so- called ?Car lin type?) in the Otav i carbon a te sequenc e (descr ib e d on chapte r 6.5.5.) . The several portions of the Kombat mine ar e controlled by a regiona l E-W fault as well as the other copper deposits in the region. Copper sulfides nuclea te around iron oxide bodies of differe n t shapes and sizes. This is shown on Figs 8.31 and 8.32 and others. 3 6 4 Fig 8.31 Diagram taken from Deane, 1995 to reinterpret origin of the Kombat mine, Namibia. T his three- dimensional picture of a typical ore l ens at the mine s ho w s that large iron oxide b odies with minor manganes e act as nucleus for pyrite and copper sulfide mineralization. Note the scale for dimensions o f t he magnetite bo dies that are marked with the small dots. T he large dots are a fine hydrothermal breccia that is ca lled ? Otavi sandston e ? at the mine. It see ms to be th e residual of carbonate disol ution by acid fl uids. Coarse-grained breccias and stockworks are indicated b y the material with triangles. Massive mineralization of copper sulfides is marked in b lack. The dep osit has tectonic overprinting and foliation, t hat re-mobilized and sheared bot h host rocks and mineralization. 3 6 5 Fig 8.30 Typical mineralization at the Kombat Cu mine, Namibia . T his p hotograph sh ow s the ty pe of stockworking that occurs at the mine. It contains basically bornite, chalcopy rite and pyrite. Large vol u mes of three- dimensional fracturing like the o ne de picted account for most of the rich mineralization at the mine. Massi ve bodies of sulfides are found in parts of the breccia voids. As described in the te xt, the origin o f mineralization see ms to b e associated to the Otjiwarongo batholith and e verything indicates that it is an IOCG deposit. Fig 8.32 Underground map that shows core of iron oxide bordered by copper mineralization at the Kombat Mine, Namibia. Note that underground ex posures show manganese-rich iron oxide bodies ? in violet- (so metimes massive, sometimes ?banded ? and ?b e dde d ?), surrounde d by hydrothermal breccias. High grade mineralization is marked in red, and the thick red line indicates economic mineralization. Note that all the copper sulfi des occur around the iron o xide bodies. T his map is one of many cross s e ctions and maps produced by mine geo lo gi sts that show similar features. Since the p urpose of miners is n ot to map iron oxides, thes e ar e s eld o m de picted in three-dimensions. T his diagram was extracted from internal report s reviewed at the mine library. 3 6 6 8.4.1.3 OTJIKOTO GOLD DEPOSIT, NAMIBIA Otjikoto is another deposit that seems to be associate d to the Otjiwarongo batholith. It occurs in the northe rn portion of the Lufilian Arc in Namibia. Fig 8.33, a ge neraliz ed map produced by the AVMIN geolog ical staff based on compila t i o n , field mapping and geophys ic al interpr e t a t i on , show s general geology in the environs of Otjikot o . The Kombat mine is also shown there for lo catio n and general context . Miner alization at Otjikoto has direct associa t i o n to magnet i c iron oxide bodies and is control le d by E-W fractur es , paralle l to the main Lufilian Arc elongation. The mineralized sheeted vein system is preferentia lly hosted within albitized pelitic and silicicl ast i c rocks in marble s of the Karibib Form ation. Just as discussed previously, hydrotherma l proc es ses that indurated the host rocks at Otjikoto enabled them to fracture in brittle fashion. According to Wilton, Lombard, & Philpot, 2002, ?individual veins range from 1 to 10 cm in width. Ther e is an apparent strong correla t i o n between vein density and grade. Vein miner a l og i es compr is e variou s propor t i on s of pyrrhotite, magnetite, pyrite, with associ a t e d large rounde d almand i ne garnet s , amphib o le and free gold.? Metamorphic foliation overpr ints mineralization. A signi ficant component of the mineralization at Otjikoto compris es coarse gold. Tourma l in i z a t i o n is one of the obs erved types of hydr otherma l alteration. Other metals of mafic affinity are associated to the deposit. The charact er is t i c s describe d ab ove point to classify the Otjikoto deposits as a gold-rich member of the IOCG family. A very aggress i v e drilling campaig n was carried out at the deposit during 2003, and pilot mining will soon be advanc e d . It could soon become a large undergr ou nd mi ne. Very little public informat i o n on the deposit was made available. Fig 8.33 Simplified geological map of the Otjikoto gold deposit, Namibia. T his map was produced by the Namibian office of An glo Vaal and pu blished in Wilt on et al., 200 2. Dark lines indicate ex ploration licences; broke n lines are magnetic lineaments; most of the rocks are different f orms of carbonates, marbles and calcareous silt stones. Th ere are almost no o utcrops in the entir e area, except in the norther n portion of the map, und erlain by Otavi limeston es. No te location of the Kombat mine and main roads. 8.4.1.4 MESOPOTAMIE FARM, NAMIBIA The Mesopota m i e farm, located in the southwes te r n corner of the Kamanjab Batholit h in Namibia has significant known copper mineralization of IOCG type (Figs 8.6 and M20 for location). Various granitoids, includ in g graphic textur e alkali granites occur at the fa rm and seem respon s ib le for the copper minera l i z a t i o n of the Copper Vallei deposit. Massive iron oxide bodi es emplac ed along E-W vein systems and relate d sulfida t i on accoun t for the copper mineral i z a t i on . Gold is though t to occur along with the copper. Hydroth er m a l breccia s were mapped and many quartz ?pods? were al so identified during reconnaissance work at the farm. 3 6 7 Fig 8.34 Mineralized quartz pod with magnetite and chalcopyrite. Sample L- 7 56b from the Mesop otamie farm, Namibia. Sulfides w ere prese nt in the vugs along veinlets and esp ecially in the low e r left portion of he matite, The chapter on the Mesopotamie farm (4.2.2.4.2) cove red most of the geologic a l backgroun d of the area. Aspects of iron oxide- copper-gold mineralization at the farm w ill be discussed here. The old mine located on the northwes t e r n corner of the Lofdal farm farm exploit e d oxidized copper sulfide s by crus hin g , leachin g and prec ipi t a t i n g copper on iron scrap. A large proportion of the gold, bismut h and other metals were probably not recovered. The small oper ation seems to have run bankrup t after finding hard to proc ess sulfide ore in the pits. Dozens of explora t i on pits were observed ; no lar ge, old pits were found. Very small dumps indicate a small total extracted volume of rock. The type of miner alization at this deposit seems to be of iron oxide- co pp e r - go l d type. 8.4.1.4.1 Copper Valley mineralization on the NW portion of Mesopotamie 504. According to the bibliogr aphical compilation carried out by Schneider & Seeger, 1992, the Copper Valley deposit , located on the northwes t er n corner of the farm Mesopotami e 504, is made by discontinuous quartz lenses with sporad ic concentrations of galena, chalcoci te and native gold. Such veins appear to be confined to subs id i ar y faults and shear zones. Host rocks to t he mineraliz ation are locally altered to chlorite-ser icite schist, talc, brown carbonate and epidote (Songe, 1958 in Schneider & Seeger, 1992, p. 2.3-9). Six trenche s were opened up in a group of Cu-bea r in g quartz veins prior to 1924. ?Durin g the period 1950 to 1952 more than 1000 tons of handcob b ed ore grading 20 to 30% copper were produc e d by open cast mining . ? The discon t i nu o us quartz veins, ?up to 60 m in length and 1 to 1.5 m in width, carry spor ad ic conc en t r a t i o ns of chalcoc i t e , chalco p y r i t e and sparse pyrite. They strike mainly parallel to the N-NW trending foliation of the gneiss and schist or transe c t the stru ct u r a l grain at right angles . Althou g h the ore near surfac e has been worked out, open-cast mining may be resumed with a very low stripp i n g ratio as the dip of the major quartz body is slightly steeper than that of the slope on whic h it crops out.? (Schneider & Seeger, 1992, p. 2.3-9). Many miner a liz e d specimen s were coll ec ted at the Copper Valley mine site ( L-760 to L-770 ). Some of thes e include crus hed material from an old silo, finely crus hed and leac hed tailings , and grab samples from the 3 6 8 d u m ps . Gossano us vugs after sulfides with copper carbona t es , quartz and hematit e are ubiquit o us . Abundan t fragmen t s of quartz veins with hemati t e networ k s and re mnants of sulfides were observed . In many cases, hemati t e blobs are the site for nuclea ti o n for chal copy r i t e and bornite (Fig 8.35). For example, L-771 is a fragmen t from a quartz vein that enclos es an angula r part ic l e of the schisto s e host rock; it contains vuggy veins and gossanous boxworks after sulfides. Fig 8.35 Mineralized samples from the Copper Vallei mine, Mesopotamie farm, Khorixas Inlier, Namibia. Q uartz pods with magnetite, chalcopyrite and pyri te. A and C are photographs of e x po s e d s urfaces, while B and D are slabs. Note t h e abundant sulfidation, that normally comes tog e t her with magnetite. T h e d e ns e v eining is typical of samples fou n d at the old pi ts and mine site. A, sample L-766a; B, L-765j; C, L- 765c; D, L-765g. Scales in millimeters. Some specimens collected from the refuse pile are good examples of the entire mineralized system ( L-774 to L-778 ) . These include vuggy quartz veins with dusty c halcoc i t e and Cu carbon a t es ; quartz veins with fine hematit e veinlet s , iron oxide dust, gossano us vugs and Cu carbon ate s ; and quartz veins with dense hematit e stockworks that grade into hydrotherma l breccias with vugs after su lfides and intense Cu carbona t e stains. Figs 8.34 and 8.35 show aspe cts of the mineralization. 8.4.1.4.2 Kruger?s Deposit on th e NW portion of Mesopotamie 504. ?Kruge r ?s deposi t lies in augen- g n e is s of the Huab Co mple x on a steep mounta i n slope clos e to the Copper Valley pros pect near the northwestern boundary of the fa rm Mesopo t a m i e 504. The copper occurs in a quartz vein that strikes NNE and dips 50 to 55? E. The leng th of the vein is 45 m and its maximu m thickne s s 2 m near the center of the deposit. A narrow sheet of phyllit ic schist adjoins the vein, while the hanging wall is silicified. Mineraliz ation is locally rich where the ve in thickens. The copper miner als are mainly malachite, shattuck i t e , chrysoco l la and occasiona l dioptas e , acco mpanied by hematite, spec ular ite and limonite. Bornite has been noted at only one place.? (S chneide r & Seeger, 1992, p. 2.3-9). ?An ore sample from one of the coppe r occurren c e s on the farm Mesopo t am i e 504 (probab l y from Copper Valley) contain s a surpris i ng variety of mineral s . These include native copper, cuprite , chalcoc i t e , malachi t e , azur ite , chrysoc o l l a , planche i t e , a very rare blac k mineral with a spinel-t y pe structu r e , a yellowis h - gr e en 3 6 9 mineral clos e to calciovolborthite, native bismuth, bism ite, bismutite, beyerite, clinobisvanite, the newly named mineral namibite, galena, scheelite, cuprotungstite, i odagyrite and embolite. The deposit has been opened by trenches over a strike length of 25 m.? (Schne ider & Seeger, 1992, p. 2.3-9). 8.4.1.4.3 Mineralization on the NE portion of Mesopotamie 504. ?In the granitic gneiss on the NE part of the farm, spor ad ic Cu-Pb- B i - A u - Ag minera l iz a t i on in lentic u l a r quartz pods occurs in fault zones striki n g east and dipping st eepl y north. Handco b b ed chalcoc i t e concen t r a t es have been repor t ed to carry 68.5 g/t gold, where as galen a conc en t r a t es contain e d 685 g/t gold. Numerou s trench es and pits, one open cast and one 12-m-de ep shaft were excavat e d during previous explora t i o n . Some metallurgical testwork has been carried ou t.? (Schneider & Seeger, 1992, p. 2.3-9). Additio n a l Cu-rich mineral iz a t i o n as socia t e d with gold is know n to occur in the nearby Korecha s 381 and Navarr e 383 farms. These occurr e nc es were not visit ed, but might also be related to IOCG. Field notes collected at the Mesopotamie farm are included in the Appendix. 3 7 0 8.4.2 ZAMBIAN DEPOSITS AND PROSPECTS Zambian deposit s like Kalengw a , the Dunrob i n mine (gol d), Sanje (iron ore), Kansanshi mine (copper, gold) Nampundw e mine (pyrite , copper and minor gold) , Kantong a (copper , gold and uranium? ) and Kasumba l e s a (iron, gold?) on the D.R. Congo border with Zambia and ot hers , also displa y some char ac t e r is t i c s of the IOCG deposits (See Table 8.2). Relation to intrusive rocks at thes e deposits is not evident. The first three are fractur e- c on t r o l l e d and display evidenc e of strong hy drothe rmal activity. Intrusive rocks that heated the systems are thought to be nearby and under cover. 7.4.2.1 EVIDENCE OF IOCG MINERALI ZATION UNDER THE ZAMBIAN COPPERBELT Evidence of IOCG mineralization under, or very near sedimentary-hosted copper mineralization has been found in several sites of the Zambian Copperb e l t . The chapters on the Nchanga Granite (4.1.5.2), Mufulira (4.1.5.7) and Chambishi (4.1.5.6) already discussed part of these issues. Below are some additional comment s on the topic. Mendels oh n , 1961 and Garlick , 1973 pres ent evidenc e of iron oxide-c o pp e r - g o l d mineral iz a t i o n in several sites of the basement to the Copperbelt. Portions of the Mulias hi porphyry and the Nchanga Granite are probab l e sour ces for at least part of the copper in t he sedime n tar y - h os t e d copper deposi t s of the Copper b e l t . Very little publicly-available research has been carried out in this field. Descrip t i on s of the IOCG pros pe c ts are shor t and lack detail. Neverth e l ess , several of such oc curre nc es contain primary copper sulfide s and gold . Gray?s quarry, the Maunga, Nsato and Kafue Areas are some of the zones in the basement to the Copperbelt that contain evidence of iron oxide- c op p e r - go l d mineral iz a t i on . These mineral i z ed areas are associa t ed with magnetite and hematite, most of them carry spec ular i t e and tourmali n e . They occur in stoc kwor k s , veins or shear zones. The associa t io n quartz- hematite-tourma line-chalcopyrite is recu rre n t in surfac e occurr e nc es . At the Nsato area, ?a linear magnetic anomaly, whic h may be associa t e d with a granite contact or a basic dike, was outlin e d by geophy s ic a l surveys. The follow-u p work and di amond drilling reveale d veins and disseminations of chalcopyrite and bornite in biotit e schist s and impure schist o s e quartz ite s . The copper mineral s occur as isolated grains in the matrices and as veins along joints and planes of schisto s i t y . Seams and scattered grains of magnetit e and hematite are fairly common. Neither the extent nor the source of the mineral i z a t i o n are known? (Mendels o h n , 1961 , p. 34). The magnetic anomaly could be due to tabular body of magnetite that nucleates sulfidation. Also, ?In several localit i es , copper minerals have been discovere d near granite , pegmati t e , and basic intru- s i v e s . Minor amounts of malachi t e , chalcop y r i t e , and bo rnite are present along joints, quartz veins, and as disseminations in the country rock. In a few localities the host rock contains scattere d grains and veinle ts of magneti t e and spec ula r i t e , and has been silicif i ed , feld spa t h i z e d and seriti z ed . ? (Mende ls o h n , 1961, p. 33). The Miku and Chondw e areas contai n both copper and gol d minerali z a t i on that is not well document e d in the report by Pienaar in (Mendelsohn, 1961 ). 8.4.2.2 DUNROBIN GOLD MINE, ZAMBIA Very little information is publicly available from the Dunr obin mine. It was a medium-s c al e operati o n that mined only oxide mineral iz a t i o n from open pits and minor undergr o u nd works. The origin of the deposit is not well understood. From reconnaissance work carried out, IO CG features that were seen include: very important role of iron oxide bodies to nuclea t e sulfid a t i o n and gold; particu la r hydroth er m a l alterat i o n features ; very clear structural control for mineralization is evident in the pits; there are some copper show ings in the environs, strong hydr oth e r ma l alterat i o n and brecci a t i o n were observ e d in and around the main mine; free gold was observed in some of the gossans. Mineraliz ation is ho sted by carbonates thought to be correlative with Katanga n units like the Lusaka Formati on . Typical hydr othe r m a l veins of the Dunrob in mine are sh ow n on Fig 8.36. Note the interbr a nc h in g and braidin g of these quartz veins with massive magnetit e and hema tit e . These iron oxide mineral s served as nuclei for pyrite and other sulfide s wher e gold is hosted. Simila r featur es were observed at various scales. The host rock around these veins is almost entirely transformed by brown-rock (hematite) alteration . Note the 35 cm steel mallet for scale. 3 7 1 Fig 8.36 Mineralized quartz-magnetite-sulfide veins at the Dunrobin gold mine, Zambia . N o t e s t e e l hammer for scale. Most of the host rock is heavily altered by he matitization. More details in text. Fig. 8.39 Explanation diagram for Fig 8.37. Progressive hydrothermal mineralization around quartz- magnetite-sulfide veinlets at the Dunrobin gold mine, Zambia. 3 7 2 Fig 8.37 Progressive hydrothermal alteration aro und mineralized quartz-magnetite-sulfide veinlets at the Dunrobin gold mine, Zambia. N o t e s t ee l scratcher for scale. Potassic alteration in very thin veinlets , and silicification are ov erprinted by later gold-b earing quar tz-magnetite veinlets. Progressive hematitization of the host rock takes place away from the second generation of veinlets. M o s t o f t h e h o s t rock is heavily altered by h e matitization that gives it a deep brown color. Origina lly the rock was a felsic granitoid. More details in text. 3 7 3 Fig 8.38 Concentric iron oxide banding around mineralized veinlets at the Dunrobin gold mine, Zambia . Host rocks in this case are Katangan carbonat es, probably correlatives of the Lusaka Formation. This pa rticular type of alteration and mineralization produces large volu mes of brow n, gossanous rock. W hen w eather ed, coarse free g old can be easily extracted. Parts of the main ore grade materi al at the mine see m to have be e n of this type. Professor Allan Clark of Queen ?s University in Kingston Ontario calls the texture here de picted ?riglites ? (Personal communication, 200 4). According to him, th e texture is also called ?Racoon tail? banding. Riglites are a common feature in some skarn de posits, and have also bee n de scribed in Mississi ppi Valley T ype Z n-P b d ep osits. T he same structures have bee n called ? piedra famelicana? in Spanish de posits b y Prof essor Ll uis F ontb ot? from th e University of Gen eve , Swit zerland. Fig 8.37 illust r a t e s another aspect of gradua l host rock hematiti z a t i o n . In this case the rock is granit i c ; numer ous veinlets intersect it conforming a series of phacoids . Note progress i v e hematite impregna t i o n in the host rock. At times this alteration comple tely obliterates the original texture and main mineralogy of the host rock. Zones of denser veining ar e completely brow n. The accompa n y i ng diagram illustr a t e s various other features of the veinlets and their hy drotherma l alteration. A metallic scratcher is used for scale. The sketch of Fig. 8.39 serves to understand t he variou s featur es of alteration and mineralization on Fig 8.37. Another interesting aspect of the in tense iron oxide alterat i o n that takes plac e around mineral i z e d veins of the Dunr obin mine is show n on Fig 8.38. Concent r ic iron ox ide alteration that spread s out from contiguous veins replac es the host rock and produc es a particu l a r banding in the rock that in a way is similar to Leisegang rings. Extensive volumes of similarly altered rock ar e found around and within the Dunr ob i n gold mine. Here too, a progressive disolution of the host rock and replac ement first by iron oxides and later by sulfides seems to be the governi ng rule. Gold comes late, with pyrite and other sulfid e s that are emplac e d on top or within the previous ly deposited hematite. Note steel ru ler with centime t e r s and inches for scale. 3 7 4 8.4.2.3 NAMPUNDWE PYRITE MINE The Nampundw e mine, previous l y called ?King Edward Mine ? is a pyrite mine currently exploit e d as a sour ce of sulfur for smelti n g proces s es by the private corporation KCM at Nc hanga. As observed on Fig 8.40 it is emplac e d in Katanga n carbona t es and silicic l as t i c s of the Lusak a Formati on , just west of Lusaka. Very few referenc es discuss the geology of this deposit in detail (Bur nard, Vaughan, & Sweeney, 1990a; Burnard, Vaughan, & Sweeney, 1990b; Burnar d, Sweeney, Vaughan, Spiro, & Thirlw all, 1993; Phillips , 1958a; Reeve, 1963; Simpson, 1962; Stohl, 1977; and Tembo & Porada , 2002). The deposit has been mis-id e n t i f i e d as a sedimentar y exhalative mineraliz ation (Burnard et al., 1990a; Burnard et al., 1990b; and Burnard et al., 1993). Its associat i on with large iron oxide bo dies of hydr oth e r m a l origin is certai n (Figs 8.12 and 8.40); part of the deposit is spatiall y related to the large magnetit e hill show n on Fig 8.12; small bodies of gabbro and felsic intrusives occur in its environs; it is basically a pyrite deposit, but contai ns minor chalcop y r i t e and gold; many copper and gold occurr e nc e s are known around the deposi t . A working hypothe s is is that the Nampundw e mine is a pyrite-ric h end-memb er of the IOCG clan of deposits. Similar types of mineralization are known in the Marcona area and Ra?l-Co n de s t able mine of Peru; bot h are currentl y being mined and explored for their iron oxide-c op p e r - go l d potenti a l . Fig 8.40 Geological map around the Lusaka West area, Zambia. Note dark dots that indicate iron oxide mineralization and lighter on e s that indicate copper and go l d mineralizati on. T he Nampundw e pyrite mine is l ocated n ear the l ow er third left portion of the map. Most of the ro cks shown are carbonates. Note P eacock a nd Cheta copper prospects, as well as Sanje iron de p osit o perated by Zambian collieries. Do ub l e lines are main roads. Small sq uares are sampling sites for intrusive rocks, that are not mapped. The pho tograph of Fig 8.12 was tak en in one of the iron oxid e hills. More details in text. Compilation ge ol ogical map from Billiton. Special ge ophysical tests w ere carried o ut at the Input sites. 8.4.2.4 KASEMPA REGION PROSPECTS, ZAMBIA The Kasempa region of Zambia has IOCG minera l i z a t i o n associate d to small bodies of alkalin e gabbros and syenites that intrude Katangan limes tone s . The chapter on that portion of Zambia describ es its main geolog y. Hydro t he r ma l brecc ia t i o n and vario us forms of iron ox ide alteration are widespread . Massive bodies of iron 3 7 5 o x i d e have been identif i e d and sampled . Large magnet ic and gravim e tr i c anomal ie s as well as soil geochemis try Cu, Co, Ag, As and Au anomalies have been identified. Numerou s compa n i es have carri ed out signi f ic a n t explo r a t i on in this part of Zambia, includ in g Roan Selectio n Trus t, Phelps Dodge, Iscor, Billiton and Anglo Vaal. Part of the aeromag ne t i c anomalie s were drilled . The most promisin g anomaly is the Chitamp a pros pe c t , wher e boreho l e MB-34 was drilled in the 1970?s. Various aspects of breccia t i o n , hy drothermal alteration and mi neralization at the borehole will be described in this chapter. The Kasempa area is not definitively expl ored , and many of the anoma lie s identifi e d have not been followed up. See the chapter on the Kalengwa- K a s e m p a ar ea for descript i ons on samples from part of the boreholes drilled by Billiton at Kasempa. The Lufupa prospec t of the Kasempa area in Zambia al so displa y s sedime n t ar y - h o s t ed copper minera l iz a t io n . It is located near IOCG prospects and iron oxide- ce mented brecciation and veining. It was drilled by Roan Selection Trust. 8.4.2.5 IOCG PROSPECTS AND MINES AROUND THE HOOK GRANITE BATHOLITH, ZAMBIA The northwestern portion of the Hook Granite Batholith contains abundant mineralization of various types. As show n on Fig 8.41, zinc , silver , copper , gold and iron deposi t s occur in a wide area. Mines like the Hippo mine (Cik in, 1968), Blue Jacket, Lou-Lou and others were well know n in the early twentieth century. All of them are akin to the iron oxide- co p pe r - g o l d type. Some are enriched in silver or lead or zinc or copper , but they are all associ a t e d to iron oxide bodies and round- p e bb l e hydrot h er m a l breccia t i o n . The region has been called the Mumbwa distric t by some authors , an d the ?Great Concessi on ? by others . Two samples of iron oxide bodies were analyse d from this area and they are enriche d in Zn, Cu, Ce and other minerals (See complet e descrip t i o n on section 4.1.2 about t he West Lusaka-Kafue Flats ar ea). Fig 8.41 Geological Map NW of Mumbwa, H ook Granite Batholith, Zambia . Black squares and shapes are massive iron oxide b odies. Gray dots are copper oc currences and mines. Part of the m contai n silver and g old. Dark gray rocks are syenitic intrusions and light gray on es are granitic intrusions . T hese granitoid bodies se e m to b e apoph yses of the H o ok Granite Batholith (in very light gray, up per lef t corner), or s m all ring compl ex es . T he t ow n of M u mbwa lies jus t in t he lo w er right corner. The thin d ou ble line is the main road. The N- S th ick light gray line is the easter n limit of the Kafue National Park. More details in text. Co mpilation map from Billiton. 3 7 6 M a n y small IOCG pros pec t s have been explor e d around the Hook Granite in Zambia during the past ten years. None have been proven large or rich enough to warrant large-sc a l e mining. Ther e are numerous massiv e iron oxide and copper occurr en c es in and aroun d the Hook Granite Batholith. Katangan siliciclas tics and carbonates that are intruded by various bodies of the batholith accoun t for iron oxide, gold and coppe r mineralization. Sites like the Luiri Hills, Shimyoka, Kamiyobo , Kitumba, Kantonga , and Lou Lou pros pects are just a few of the mines and pros pec t s around Mumbwa and west of Lusaka that c ontain IOCG mineralization and deter mi ne a large pros pec t i v e provinc e (Fig 8.41). Small copper, silver , zinc and lead mines oper ate d in the area during the century . There is abundan t eviden c e of replac e m e n t mineral i z a t i o n in breccia s accompa n y the intrusio n of syenites and alkali granites . The foll owi ng are referenc es that describe d various types of mineralization in the area: Brandt, 1955; Brandt, 1956; Nisbet, Cooke, Richards, & Williams , 2000; Nisbet, 2004a; Nisbet, 2004b; O'Brien, 1958; Phillips, 1957; Ph illips, 1958a; Phillips, 1958b; Phillips, 1959; Sikazwe, 1999; and Simpson, 1962. See also the map of IOCG mi neralization in the Greater Lufilian Arc (Fig 8.7) For example, the Shimyoka district contains several cubic k ilome ters of 0.2% Cu, as def ined by Billiton in the late 1990?s . During the 1990?s Billit o n ?under t o ok a large program of exploration at Ki tumba-Kantonga, following up initially on INPU T and Aeromagnetic survey s flown by the United Nations, wh ose drill results included 100m averaging 0.98% Cu at the Sugarloaf prospect.? Sign ifi c a n t reconn a i s s an c e work was carrie d out, includin g rock chip and soil geochem i s t r y , airborn e and ground - b as ed geophys ic s followe d by drilling . ?They outline d extensive areas of anomalous geochemistr y and IO CG style alteration and brecciation of Kundelungu metas ed iments and Hook Granite syenite s , the mos t interest i ng areas being the Kitumba and Kantonga Prospects.? (Nisbet, 2004b). ?At Kitumba , an 8x3 km sized, Cu-Au anomalou s serici t e - he m a t i t e alterat i o n system was outli n e d , assoc i ate d with significan t aeromagnetic, IP, and CSAMT anomalism. Hemati t e - q ua r t z - s er ic i t e - ap a t ite - b ar i t e - s i d er i t e alteration assemblage s are described, sugges ting the sy stem is a ?shallow level? sy stem comparable in size and alterat i on assembl age s to Olympic Dam. Drillin g interse c t ed wide, low grade Cu-Au mineral iz a t i on , a typical interce p t being of the order of 125m @ 0.2% Cu.? (Nis be t , 2004b) . Fig 8.42 shows a simplif i e d geolog i c a l map of Kitumba , its widesp r e a d breccia bodies and hydrot h er m a l altera t i o n . Note compar is on of various feature s with the Olympic Dam and Ernest Henry deposits, at the same scale. Very large, ridge- p r o d uc i ng ring dike s, with an approxim a t e diameter of 40 km, make up the norther n portion of the Hook Granite, just north of Kitumba. This is evident on the airbor ne geophysical image pres en ted by Nisbet, 2004a (Fig 4.5) . These are portions of large anorog e n ic ring comple x e s . ?At Kantong a, intense aeromag ne t i c anomali es are asso ciat e d with several large Cu soil anomalies . Drilling intersected brecciated Kundelungu metasediments and Hook syenite s , with extensi v e albite - g ar ne t - e p ido t e - actinolite- magnetite-Ks par-calc ite- apatite alteration. Sulf id e s were domina n t l y pyrite , with minor chalco p yr i t e . The alterati on assembla ge s suggest the Kantonga system was formed at deeper levels to Kitumba, probably more akin to Ernest Henr y? (Nis be t , 2004b) . Fig 8.22 sh ows a cross sectio n throug h t he main mineralization at Kantonga. Note the dimensions of alteration, the widespr ea d iron oxide alterati o n and the tabular bodies of magnetite. Explosive hydr othermal breccia t i o n and round-p ebb l e hydr oth er m a l breccias are a common feature at Kantonga. 3 7 7 Fig 8.42 Generalized geology of the Kitumba prospect, Kafue Flats, Zambia. H y drothermal breccias and massive iron oxide bodies with abundant sulfide mineraliz ation is what makes this large hy drothermal IOCG system. Note that the size of the mi neralized brecciation and alteration is approximately th e same as that of th e O l y mpic Dam deposit in Australia. Ernest He nry has also bee n included at the same scale for reference. Figure from Nisbet, 2004b. 8.4.2.6 KALENGWA COPPER MINE, ZAMBIA The Kaleng w a mine is though t to be one of the majo r exponen ts of iron oxide- c op p e r - go l d deposits in Zambia. It was one of the most profita b l e copper deposit s in the co untry, and paid for its own infr as tructure in a remote location , separate d from the rest of the main Copper belt (See location on Figs 8.7, M8 and M1). Few reports on the depos it are public ly available today. Initially proven reserv es were of 600,00 0 tons at 16% Cu, accordi n g to Ellis & McGregor , 1967. Total productio n accordi n g to Hitzman & Broughto n , 2003, was 1.9 million tons of 9.44% Cu, 50 gAg/t. Hydr othermal brecciation, as well as gabbros and monzodiorites seem to have played important roles in the formation of the orig inal deposit. Most of the mined copper minerals came from a massive chalco c i t e body enric hed by superg en e co nc en t r a ti o n ; copper oxides and a few sulfid e s were found near the surfac e (Fig 8.43). The deposit was comple tely blind; no part of it outcropped. Discovery of Kalengwa was produc ed by straightforward geochemic al explor ation. The deposi t was hoste d by Katang a n silic i c la s t ic rocks an d limes ton e s . It cons iste d of a tabular body of round- p e b b le hydroth e r m a l brecci as , calc ar eo u s conglo me r a t e s , sandst o n es and siltst o n e s repla c ed by prima r y copper sulfides (chalcopyrite, bornite and chalcocite) surroun d ed by a large halo of red-roc k and brow n- r o c k (hematit e ) alterati o n (Fig 8.43). An associat i o n of syenites and granites seems to have produced the mineralization. Ongoing research on samples from the mine includes detaile d chemica l analysi s of various intrusive rocks in its environs. See the chapter on the Kalengw a- Ka s e mp a area for descri p t i on s of part of that resear ch. 3 7 8 Fig 8.43 Cross section and map of the Kalengwa mine open pit, Zambia. Note the body of mafic intrusives t hat is considered to have produced the mi neralization. Total production from the mine was 1.9 million tons @ 9 . 4 % C u with 50g/ t A g . Taken from Ni sbet, 2004b ; Nisbet, 2004b and Woodhead, J. Personal communication, 2004. 3 7 9 8.4.3 OTHER LUFILIAN ARC IOC G PROSPECTS AND DEPOSITS 8.4.3.1 QUARTZITE-HOSTED DEPO SITS, GELBINGEN FARM NAMIBIA Some pros pec t s associat ed with the large intrusiv e bodies in the Lufili a n Arc, have gold- and copper - r ic h surfac e sample s . These occur around larger magmat i c bodies . Small apophy s i s of subvol c an i c porphyr i t i c intrus i v e bodies are respon s i b le for gold, iron and sulfid e mineralization. In some cases, very small intrus ive bodies are the only evidence of magmatism (Fig 8.44) . Abundant magnetite- and hematite-filled frac tu res carry gossans after copper and iron sulfides. All of this is hos ted in brittle quar tz ites . Thes e featu r es were observed at the Gelbingen farm in Namibia. Figs 8.45 to 8.48 illustrate some of th e breccioid mineralization. Part of t he region was previously explored for its zinc conten t; that may be associated to the IOCG environ m en t . Large bodies of quartz - so-cal l e d ?quartz pods? - are pres en t in extens i v e areas. No eviden ce of zinc mineralizati o n was seen during the recon- naiss ance visit. Sedimentar y-exhalative Zn-Pb deposi ts have been sought througho u t parts of norther n Namibia , especia l l y around the Gelbinggen farm, but companies that focuse d on those exploration targets for decades, over- l o o k e d coppe r - g o l d hydroth e r m a l minera lization and its high potential. Very small subvo l c a n ic porph yr i t i c intrus i v e bodies outcrop in few places and seem to be introd uc i ng minera l iz a t i on and altera t io n . Unmapp ed , region a l E-W struct u r e s contro l bot h intrusions and mineraliz ation. Fig 8.44 Angular hydrothermal breccias and the subvolcanic , porphyritic, rhyolitic intrusive that is responsible for their formation. Both p hotographs are at approximately th e same scale. Rul er in millimeters. Col lected at th e Gelbinge n farm, Namibia. Stockwor k s of magneti t e veins with sulfida t i o n were observe d in the environ s . T he photog r ap h of Fig 8.49 is typical of the alteration and mineraliz ation seen. Quartz it e - h os t e d IOCG mineral iz a t i on was also observe d on the western border of the Kamanja b Batholi th , in associa t i o n with N-S- tre nd in g major f ault systems . All char ac t e r is t ic s are similar to those just described from the Gelbingen farm on the north-eas tern borde r of the batholith (Fig 8.6). 3 8 0 Fig 8.45 Another aspect of hydrothermal breccias cemented by massive magnetite from the Gelbingen farm, Namibia . 14 cm marker for scale. Note slight deformation in bre ccia clasts. Black is magnetit e. Part of the vugs w ere originally fille d by sulfides. T his particular breccia is associ ated to large b o dies of carbonatitic dikes and diatremes. More details in text. Fig 8.46 Sulfide-bearing hydrothermal breccia-vein cemented by magnetite that intrudes quartzites. . Located in the Gelbinge n Farm, to the northeast of the Kamanjab Bat holith, Namibia. The brittle behavior of quartzite produced extraordinary rock fracturing and IOCG mineralization in various lo cations of the Lufilian Arc. This is an example of these breccia bodies . T hey are associated with small porphyritic subv olcanic intrusives of inte rmediate composition. ( N ote smaller breccia veins that extend to th e central and low er part of the the photo. T hey are more e nriched in su lfides than the thicker vein above.) Se e text for more details. 3 8 1 Fig 8.47 Three close-up aspects of the mineraliz ed breccias from the Gelbingen farm, Namibia. Sample B had strong calcanthite staining o n its surface. Al l scales in millimeters. In this case a ll clasts are made of quartzite. T h e matri x is magnetite and sulfide-rich silica. Some outcrops of this breccioid material may reach twenty meters in l ength. N o assays have b ee n carried o ut at the mo ment of editing this d ocument. Fig 8.48 Another aspect of sulfide-bearing hydrotherma l breccia cemented by magnetite that intrudes quartzites. T hese w ere ob served in the Gelbinge n farm, Namibia. Note type of clasts and clear cut contacts with the w hite q uartzite. Angu lar fragments are exclusively made of w hite quartize , and to a less er extent by milky w hite quartz. M ultigram gold- bearing samples w ere collected n ear this site. Again, brittle behavior of th e quartzite e nhanced the f ormation of physical traps for IOCG mineralization. T he matrix of this breccia cont ains many s mall angular fragme nts in a fractal distribution. Hammer for scale. More details in text . 3 8 2 Fig 8.49 Network of sulfide-bearing magnetite veins that form a stockwork in Pan African felsic granitoids . Fifteen-centimeter marker for scale. These s t ockworks grade into magnetite-cemented dikes, magnetite-rich carbonatite dikes on one direction and in to hy drothermal breccias on the other. Granitic rocks have been w hitened by albitization; that probably increased their brittleness. Very little iron oxide alteration stems away from this web o f v einlets , as seen here. Large volumes of rock display similar features in specific portions of t h e G e l bingen farm. 3 8 3 8.4.3.2 DEPOSITS ASSOCIATED TO ALKALINE ROCKS AND CARBONATITES Highly alkaline rocks includ ing syenites, lamprophyre di kes and carbonatites seem to have been emplaced in rift environ me n t s during late Pan African times throug h o u t the Lufilia n Arc. Most of these rocks conta i n anoma lo us zinc, coppe r and rare earth s . Gold is known to occur in some syste ms , but is thought to be present in many others. IOCG mineralization is pres ent at the Lofdal and Oas farms in the Khorix as Inlier . Below are examples from some of the pros pects associated to such rocks. NeoProt e r o z o i c syenit i c and carbon a t i t i c magmas are associ a t ed with hydrot he r m a l brecciat i o n , diatreme s , massive iron oxide bodies and iron oxide-fi l l e d veins in parts of Namibi a and Zambia . Figs 8.50 and 8.51 illustrate brecciation and mineraliz ation as soci a t e d to carbona t i t e s in the Lof dal farm, Khor ixas inlier, Namibia. Portio ns of the iron oxide bodies carry signific a n t vugs and gossans afte r sulfide mineralization. In some occasi o ns fres h bornit e is observ e d on surfac e . Fig 8.52 shows a magneti t e-pyrite-chalcopyrite vein system from other parts of the Lofda l fa rm, Khorixas Inlier, Namibia. Fig 8.53 illustrates typical polymictic hydrothermal breccias ce mented by magnetite, t hat carry abundant vugs and were previously filled by sulfides of various types. This is part of a ca rbonatitic diatreme from the Lofdal farm, Namibia. Several features of IOCG mineralizat ion were observed in these breccioid bodies. Ongoing work using techniq u es pres en t ed by Ronald Blanch ard to study gossans and boxwor k wil provid e more detail s on prec ursor sulfides . Bornite, chalcopyrite and pyrite boxwor k s have been identi f i e d . Note the roundn es s of clas ts due to corros i on , and haloes of alterat i o n that ri m the clasts. Most clas ts are touc hing each other; this indicates dense packing and lack of matrix that seem s to be charac t e r is t i c of round- p e bb le hydrot h er ma l breccias . For scale, the card has marks in centimet ers and inches . Fig 8.50 Aspects of hydrothermal breccias associated to a diatreme body 450 m by 150 m in outcrop, Lofdal farm, Khorixas Inlier, Namibia. T he poly mictic breccias are cemented by massi ve magnetite and abundant coarse sulfides. Note corrosion of the fragment s. T his ty pe of rock generated positive to po graphy. Similar bodies probably can be detected with airborne magneto metry and gravimetry. Steel ha mmer included for scale. More d etails in text. 3 8 4 Fig 8.51 Polymictic hydrothermal breccia cemented by magnetite that is associated to an extremely explosive IOCG system in the Lofdal farm, Namibia. Note d ens e packing of fragments, variable clast size, t heir rounding and alteration haloes of iron oxide. Note the wide variety of clast types that includ e gn eiss, b edd ed vo lcanic rocks, sandsto ne, various granitoids and schists . T he abundant op en v ugs are a si gnificant feature. Most of t hese carried s ulfides and have bee n l eached. T his type of rock is like a spo nge: an ideal host fo r mineralization. Slight roun ding of clasts is interpreted to have b ee n produced by hyp er-alkaline hy drothermal solutions. Various lithol ogies w ere attacked to different d egrees. Rock foliation or be dding also produced anisotropic reactions to chemical attack. Abrasion bet ween clasts also must have contributed to roun ding. More notes in text. F or scale, card with centimeters and inches; the arrow is oriented n orthward. F i g 8.53 show s yet anothe r aspect of hydroth er m a l bre ccia pipes associa t e d to carbona t i t e diatrem e s in the Loftal farm. A slabbed surface of a polymictic hydrot h e r ma l brecc ia cemen t ed by magnet ite show s angul ar clas ts and smaller angular clas ts that make up the matrix. Note conc en t r i c potassic alterat io n in the rims of each of the clasts . Clasts of igneous rocks and strati f i e d volcan i c and sedime n t ar y rocks can be seen here. Figs 8.54 and 8.55 are other images of vuggy, polymic t i c , round-p e b b le hydro th e r ma l brecc ia s cemen t ed by mangnet i t e in a breccia pipe that occurs in carbona t i t e env iron ment. Again, note corros ion of clasts thought to have been produced by extremely alkaline fluids. See the conc entric alteration rims on ever y clas t. Also note the dense packing , where clas t-t o - c l as t contac t is the rule. Angular clas ts are more common in portio ns of the di atrem es . Fig 8.56 illust r a t es a case of slight clast imbric ation. Some clas ts display corros ion, the matrix is made of smaller clas ts, and the cement is magnetite. Additional IOCG mineralization of the Lufilian Arc include series of granites , nephelin e syenites , alkali gabbros and carbonatites that occur together and produce a complex set of minerals, mineralization and geology. These occur in the Oas farm of t he Khorixa s inlier, Namibia . They are thought to have been produce d by overprinting of intrusions over a long period of time ; in a rift environmen t, alkaline rocks intruded previous granit es and mafic rocks. Major iron oxide bodies , sulfi d a t i o n and emplac e me n t of brecci a pipes are relate d to the alkaline plutonism. Repetitive explos i v e hydr oth er m a l events produced pa rtic ular hydr othe rmal brecciation and what seems to be economic IOCG mineralization. Some syste ms under evalu a t ion contain significant amounts of rare earths, Zr, La, Nb, as well as Cu, Au and Zn. 3 8 5 Fig 8.53 Slab of magnetite-cemented angular polymictic hydrothermal breccia. From Sample L-748 , collected in a carbonatite diatreme of the L ofdal farm, Namibia. This is part of the same bre ccia body w here the previous ph oto graph was taken. Note corrosion of clasts and concentric alteration of their rims. Also note h eterogen eity of clast composition, varying clast size and angularity. On the surface this ro ck is very gossanous, because it carries abundant sulfides. F or scale, centimeters. T he image has bee n digitally e nhanced to increase contrast betw een rock types. More details in text . Fig 8.52 Sulfide-bearing magnetite-hematite veins associate d to ultramafic dikes from the Lofdal farm . A t times they produce s tockworks, braided vein, and sheete d vein s yst ems. Cop per carbonates are found among the gossans that occur wherever this type of IOCG miner alization o utcrops. T he host rock in this case is a true granite. Sometimes t h e country rock is heavily altered by iron oxides. Only slight re d-rock alteration spreads o ut from th e veins, as illustrated here . F or scale, steel hammer in foreground. More details in text. 3 8 6 Fig 8.54 Another aspect of heterolithic round-pebble hydrothermal breccias cemented by magnetite. Taken from a carbonatite diatreme of t he Lofdal farm, Namibia. Note d ense packing and most grains touching th eir neighb ors. T his type of material cannot flow on its ow n in the current st ate. It has denser packing than a box full of spheres. Alkaline corrosion is int erpreted to have produced clast rounding. T he initial proportion of matrix in the breccia must have b ee n much greater, and fragments must have b ee n angular. So me vugs carry sulfides. Clasts have multipl e compositions. F or scale, card with centimeters and inches; oriented n orthward. Fig 8.55 Dense packing in heterolithic round-pebble hydrothermal breccias associated to IOCG systems in the Lufilian Arc. P hoto taken from a carbonatite diatreme, Lof dal farm. No t e iron oxide impregnation in th e rims of the round clasts. Compo sition is h eterogen eo us, altho ugh n ot apparent. Note clast size variation. Cem ent is magnetite. Scale in centimeters and inches; arrow points northward. This type of breccia has bee n called sedimentary ?conglo merate?. It is clearly a hy drot hermal breccia, associated to a highly explosive hydrothermal system . I t s clasts were corroded by abrasion and by chemical attack of magmatic-related (or magmatically-drive n) fluids . Abun dant v ug s w ere fille d by sulfides that are now leached. 3 8 7 Fig 8.57 I O CG Mineralized Fracture System, that branches from a series of sub-parallel carbonatite dikes in the Lofdal farm, Namibia . S lab of Sample L-738k . N ote th e type of rhomb oidal quartz-magnetite v eins that intersect an albitized foliated granitoid; th e h ost rock was embrittled by so dic alteration. T his type of material forms part of a vein system that is approximately a met er wide and contains abundant vugs after sulf ides. The same structures occur at different scales, from hand sp ecimen to 1:50 00 and 1:1 0,00 0. No samples from th e site have b ee n assayed for Au, Cu or other ele ments . On the botto m, anoth er slab from a nearby rock ( L-738m ) t hat shows similar feat ures. Left , w e t s lab; right dry slab. Note magnetite and sulfide di sse mination, as well as red he matitizati on towards the upp er part of both slabs. 3 8 8 Fig 8.56 Angular fragments in a polymictic magnetite- cemented hydrothermal breccia from an IOCG mineralized body that is hosted by a carbonatite diatreme from the Lofdal farm, Namibia. A and B s how de nse round-clast packing and abundant voids in the matrix that were previously f ill ed by coarse s ulfides. Note t hat most large clasts display corrosion and concentric alteration. Note s light imbrication o f the fragments on C , to produce a shingl e breccia towards t he upp er right. Vugs with pyrite, very gossanous surfaces. Co pper s ulfides w ere identified in so me of the gossans that fill large vugs bet w een tabular breccia fragmen t s. Angular fragm ents in the l eft side of the pi cture display dens e packing and evident transportation. T heir str ong angularity is evidence of trans portation over a short distance. D sh ow s a wide variety of clast types, including metasediments with fine bed ding. More d etails in text. In all fo ur photo graphs, the arrow points north, and th e card show s bot h centimeters and inches. Other study areas of the Lofdal and Oas farms contain significan t potential for IOCG mineralization. Massiv e magneti t e and hematit e was observed in many sites, and abundan t gossans after sulfides were sampled and mapped . Carbon a t i t e dikes and intrus i ve bodies are asso cia t e d with magneti t e and sulfide mineral iz a t i on . Fig 8.57 was taken from a mineral i z e d fractur e system conformed by interwea ved quartz -magnetite- sulfide veinlets . Abundant gossans that are relict after sulfides includ i ng chalcop y r i t e were sampled in the enviro n s . The sulfides previous ly presen t in gossans and boxwork were positively identified using techniques described by Blanchard, 1968. Free gold is thought to exist in most of the mineralized sites. 8.4.3.3 IOCG MINERALIZATION IN THE DEMOCRATIC REPUBLIC OF CONGO Although the primar y focus of the Greater Lufilian Arc gr anitoid project was not the Democratic Republic of Congo, several field observations were made, they ar e relevant to iron oxide-copper-gold mineraliz ation, and will be discussed below. Tabular iron oxide bodies occur at the Luiswis hi, Shituru and Kamoya deposits located in the Katanga province , D.R. Congo. These tabular iron oxide bodies that intersect Katangan sedimentary rocks of the Lower Mwashya have been mis-identifi e d as itabir i t e s . On-goin g resear c h at those sites indica t e s a hydrother m a l origin for the iron oxide bodies . In all th ree cases , struc t u r a l l y cont rol l ed iron oxide bodies are not conc or dan t with stratification, and branch 3 . These bodies have traditio na l l y been cons idere d to be banded iron formati on s ; the author of this paper believes that they were emplaced under a brittle environment, after the sedime n ts were lithif i ed . This observ a t i o n is rele vant, because it could imply that Luiswishi, Shituru and Kamoya are all iron oxide-copper-gold deposits. Further wo rk on this is current ly being carried out. The Likasi mine, in fact the entire discrict incl udin g Shituru mine, contain s gold in pyrite. The dumps of Shituru contain 2 gAu/ton. According to Doug Jack (Jack, D., persona l co mmunication, 2003), tailings of Likasi, that were under evaluation by First Quantum Minerals in July 2003 for their re-treatment, contain 1.59 gAu/ton. The Kamoya deposit contains gold, but average content is less t han 0.01 g/Au/ton. In addition to this , the Kakontwe limestone s and dolomites at several Congoles e sites have been replac ed by iron oxide of hydrothermal origin. Historically, gold has not been systematic all y evalua t e d or recover e d in t he copper /c o ba l t - r ic h deposi t s of Katanga. 3 Massive, tabular hematite bodies that bifurcate or branch were observed and document e d in at least three different locations in the D.R.Congo. The bodies also cut across strati g r a p h ic marker s. Thes e two features do not occur in banded iron formati o ns , whic h are deposit ed as sedimentary beds. The best explanation for the occurren ce of the iron oxide tabular bodies just descr ibed is that they were hydrotherma lly emplaced along fractur es , in the fashion of veins (S ee section 8.3.4.3). They definitely ar e not BIF. The lateral extension of tabular iron oxide bodies in The D.R.C. could be explai ned if they were emplac ed along a regional fracture. 3 8 9 T h e Kisan g a iron oxide pros p ec t that wa s visited in the D.R. Congo on July 23 rd , 2003 is emplaced in Kakontw e limest o ne and seems to be a hydr oth er m a l brecci a with megacla s t s imperf ec t l y cement ed by goethi t e . The rock has massiv e red-roc k iron oxide alte ration. Many polymic tic, angular , clas t-supported hydrothermal breccias were found to be cemented by iron oxide. Most of the rocks that outcrop in the quarry contain irregu l a r angular vugs after pyrite. Ther e is ir on oxide stain (goethite-limonite) along most joints, but not on the fragmen ts themsel v es . Ther e is no evidenc e of copper at the quarry, but gold may certainly be present. Ongoing research on sample s fr om the site will be presented soon. Prelimin ar y observa t i o n of the D.R. Congo mineral oc curren c e map shows that there are many iron oxide mineralizations spread out in a very large area. 70 of these are mapped in the sout hern Shaba area. Most are massive bodies with no particu la r orienta t i o n . Four out of five tabular FeOx bodies have NE-SW orientation. These are Kasekele s a , located W of Kolwes i , Kabom po , an un-name d occurre n c e in the headwat e r s of the Lualaba river near the Zambian border, and an occurrence located north of Kiabana. There is a clear alignment of ?tabular ? copper and c opper- c ob a l t deposit s that runs NW-SE. It extends from the Etoile mine, Rwashi, Luwis hi, Kibolo, Kippo, Kishia 5, Shituru, Likasi, Kambove. Several un-named occurrrenc es are also present. In total, the aligned and subpar allel tabular mineraliz ations mapped are 12. Three massiv e iron oxide occurr e nc es are also pres ent along the same alignmen t, the NW-SE feature follows the regional structural trend and extends for 300 kilometers. The NW part of the lineament cuts across regional stratigr a ph y . It seems to have been controlled by a deep-tapping thrust fault. The evidence of hydr othe rmal mineralization associated with the copper and cobalt deposi ts in the D.R. Congo that was discus s e d above, clearly points towards an important input of IOCG systems in the mineralization. No granitoid s nor mafic intrusives were observed during a two- week field visit mainly dedicated to stratigr a p hy of the Katangan rocks. Neverthe l es s , a la rge volume of volcan ic rocks was observ e d . Most of the sediment a r y Katangan sequence in the region is allochtonous; it was transp o r t e d northw a r d hundred s of kilometers by thrusts. It is improbable that complete IO C G syste ms (inclu d i n g intru s i v e rocks ) will be found in the Congo, due to the tectonic disrupt io n . Only distal facies hosted in the upper volc an ic and sedime nta r y sequenc es will be pres en t . The roots of the systems we re left behind to the south. Remobilization of the metals from primar y IOCG mineralization and other so urces, probably took place during the Lufilian orogeny to produce the copper and copper-cobalt deposits known today. 3 9 0 Fig 8.58 General gravimetric map overlain by selected samples and metal values, Tevrede property, northwestern Kamanjab batholith, Namibia. T he image is self exp lanatory. Note dimensions of the mineralized area, high conte nt of copper and g o ld in s o me samples and site of the anomalies. T his is part of an ongoing expl oration project for IOCG. Drilling was carried out in this and other locations, but results are not yet kno w n. T he circular features de picted probably d efine a ring compl ex. Image pu blished by th e Bo ul d er Mining C orporation of Canada, www . boul dermining.com. 8.4.3.4 ACTIVE EXPLORATION PR OJECTS IN THE LUFILIAN ARC At the time of writing this document (August, 2004), at least two small mineral exploration companies are activel y investi n g in ground and airbor ne geophys ic s , soil and rock sampling and diamond drillin g of gold and copper - r ic h prospec t s in the northw e s te r n Kamanj ab Batholith and around the Hook Granite, the Kaleng wa area and the Zambian Serenje area and other sites in eas tern Zambia with excellent results . Fig 8.58 is a gravity map from the Tevrede projec t of BAF EX Exp loration, a junior explor ation company that carries out successful ac tivity in the northwestern part of the Kamanjab Batholit h , Namibia (Fig 8.6) . Preliminar y results from soil and rock sampling are plott ed on top of the gravimet r i c map. Note the significant dimens ions of the mineralized area. Evidence from pub licly available information on the prospect indicate that it is a large and well-en d ow e d IOCG system. Part of the mineralization is hosted in felsic intrusive rocks that have been hydrot h er m a l l y breccia t e d and cement e d by magnetite. Stockwor ks a nd braided magnetite-quartz- s u l f i d e veins were seen in sample s at the headqua r te r s of BAFEX in Windhoe k (McKen z ie , Chris, persona l communic a t io n s , 2002, 2003). If drillin g campaign s carried out during the last months of 2003 were successful, there will probably be a new gold an d copper mine in this part of Namibia. 3 9 1 8.5 RELATIONSHIP BETWEEN IOCG AND SEDIMENTARY-HOSTED Cu MINERALIZATION The origin of sedimentar y-hosted Cu mineraliz ation ma y be secondary, derived from primary mineraliz ation in IOCG systems . Severa l IOCG systems that lie unde r s edimentar y-hosted Cu deposits probably gave or igin to their copper mineral i z a t i o n . ?Exotic mineralization? is the term given to some very large copper deposi t s hosted in Quaternary or Upper Tertiary sediment a r y rocks and/or in permeable volc an i c rocks in the environ s of large Chilean copper deposits (Munchmeyer, 1996; Munchmeyer & Urqueta, 1974; Camus, 2003; and Dold, 2003). Both copper porph yr y and iron oxide-c o p p er - g o l d deposit s are know n to be the source for source for exotic copper accumula tion in nearby porous rocks. The natur al oxidation of pyrite and chalcop y r i t e in primar y coppe r deposi ts libera t es copper , iron and other metals from the hypogene mineraliz a t i on . The upward flow of groundwater, produ ce d by strong evaporati o n regime s in arid regio ns leac h es copper from hypog ene copper - r ic h depos i t s , leavi n g insol u b le subs t a nc es like gold behind. Copper- r ic h fluids are then transpor t e d into favourab le porous and permeab l e litholo g i es with a suitable redox contras t where the metal prec ipi t a t es . The process just described takes plac e today, and its rates of copper accumula t i o n have been estimate d by Dold, 2003 for several locations in the Atacama desert of Chile. The same process might have taken place in many loca t i on s durin g the Meso and NeoPr o te r oz o ic to gener a t e exotic copper accumulations in adequate environment s. Presence of organic matter in blac k shales or carbonates might have provided the redox change required for copper seconda r y minerals to precip i t a t e . Subsequent metamorphism and tectonism could hav e transformed the transported copper sulfides, phospha t e s , sulphat es and carbona t e s that were ho sted in the sediments into other mineral forms. Similar pheno men a might have taken place along the Gr eater Lufilia n Arc. The rapid exposur e of IOCG deposit s formed previous to rifting could have been erod ed at great speed during rifting , and their product s conc en t r a t e d in second a r y traps withi n sedime n t s in t he rift basins. Exotic copper accumulations could have occurred in favorable porous and permeable lithologi es where suitable redox contrasts took place. 8.6 SEDIMENTARY-HOSTED GOLD MI NERALIZATION IN THE LUFILIAN ARC There is potential for hydrotherma l sedime n t a r y - h os t e d gold (? Carl i n type?) minera l iz a t i o n in the carbona t es and dirty limes tones that lie on top of th e Otjiwarongo Ba thol i t h . This region is roughl y shown on the map of Figs 8.33 and M25. Other parts of t he Lufilian Arc show evidence of this type of gold mineralization. Some of them are areas east of Sesfon t e in in Namibia (Figs M19 and 8.6); the region where the Lusaka Formati o n (dolomites, silicicla stic s and limestones) is intruded by small granitoid bodies to the west of Lusaka, Zambia (Fig 8.40, see also section 4.1.2) ; and the environs of Tshoosh a (tow n pr eviously called Kalkfontein) in Botswan a , along the Trans ka l a ha r i road. The Navacha b gold mine in Namibi a displa y s many simila r i t i es to the sedimentar y-hosted gold mineralization at the Pinzon deposit in Nevada, U.S.A. 8.7 PECULIARITIES OF ZAMB IAN AND NAMIBIAN IOCG SYSTEMS In wester n Zambia and northern Namibia, the IOCG pr os pects and evidence of mineralization seem to differ from the published literature on the depo sit type. First of all, rocks of mo st of the mineral iz ed systems have not been subject to high temperatures and strong meta morphic deformat i on . In general, they tend to be undefor med. Most of the original hydr otherma l textures are pris tine . High tempera t ur e gradien t s due to nearby plutons seem to be the only major alteration so ur ce. Neverthe l ess , it can be said that the circa 550 Ma and 750 Ma events that produc ed IOCG mineraliz a t i on were t he last major tectonot h e r m a l process es , after whic h there has been relative stability. Some alteration featur es that are not commonly desc ribe d in the literat u r e on IOCG deposits have been identified. Some of thes e are: quartz ?pods?, round clas t hydr othermal breccias , co rros i on of the fragme n ts in some of the magnetite-matrix brecci as and progr ess i v e hematiti z a t i o n of the count r y rock to allow for emplac ement of iron oxide bodies of any size. The riglite al teration is not associated to IOCG in the literature. Very few metallic sulfides are visibl e on the surface in the Lufilian Arc. At times, black chalcocite is mis- iden t i f i e d as black moss or as Mn-iron oxides. This mineral has commonly been overlo ok ed, and seems to be the most common copper sulfide on t he surfac e in Namibian territory. 3 9 2 8.8 CONCLUSIONS 1. Most IOCG mineralization in the Lufilian Arc s eems to be related to mafic midalkal i ne and ultramaf i c intr u s ives that occ ur at the same time as fels ic mi dalk aline intrusives. Relation ships between both rock types to produce mineraliz ation are not well unders tood. In the few well documented cas es available, mafic and ultramafic rocks, intr uded before the main mineralization, and they might be contributing a significant portion of the metals, including Cu, Zn, Co, Mo, Mn, PGEs and even Au. In others, syenites or alkali granites are the main mineralizing intrusives. 2. In the Lufilia n Arc, subvolc an i c porphyr i t i c intrus i v es and apophys i s of ring complex e s that are separat ed from the main ring complex cluster s account for most of the IOCG mineraliz ation. 3. Iron oxide is a major component in IOCG systems. It occurs as massive magnetite, massive hematite, or disseminated fashions of both. Emplacement of these iron oxide s at macrosc o p ic , mesos c o p ic and microscop i c scales is thought to have been produced by gradual replac eme n t of the host rock. The process seems to involve silicate disolution by hy per-alkaline hydrothermally-driven solutions. 4. Sometimes iron oxide bodies display structural c ontrol, and they are emplaced along faults, joints and stockworks. At other times, they are emplaced in space dissolved out from si lica t e (intru s i ve and silici c las t i c ) or carbon a t e rocks. The second proces s of emplac e m en t is not fully understood at the time of writing this document. 5. Most of the massiv e iron oxide bodies do not disp la y sulfidation nor any other metallic mineralization. They are consider ed ?barren? . Only a few of the bodies of massiv e iron oxide became minera l iz e d for reas ons not well understood. 6. E-W-tren din g regiona l fractur e systems that run pa rallel to the elongation of the Greater Lufilian Arc play an important role in IOCG mineralization. They acted as routes for intrusi on , channels for fluids and control for ore depositi on . Such structur es are generall y para llel to the main Lufilian Arc trend, and could have been norma l syn-rift faults that reac tivated throughout geol ogic a l histor y. Some N-S-tren d in g structur es are also mineralized and they are sub-pe rpendicular to the main trend of the Lufilian Arc. 7. Hydrother m a l alterat i o n patterns in IOCG systems vary widely. They seem to be dependan t on the types of intrusive rocks that produce them and rocks that host them. Sodic alteration of various types is ubiquitous and its role in IOCG proc ess es is not well unders t oo d . Evaporites presen t in the Katanga-Damara sedimentary sequenc es were probab l y one of the source s of sodium . 8. Massive , three- d i m en s io n a l quartz pods are emergin g as a type of alteration that is associated to IOCG systems in the Greate r Luf ilian Arc. They seem to be a special ty pe of silicification. Hyper-alk aline, hydrothermal solution s seem to be involved in th e transportation of silica and emplacement of the quartz pods. 9. Round-p eb b l e hydr othe r m a l brecci as are another feature that occurs often in and around IOCG systems throughout the Greater Lufilian Arc. They seem to hav e been produc ed by hyper- a lk a l i ne soluti o ns that corroded previous l y angular hydrother m a l breccia. In some cases, they act as good hosts for sulfid e mineralization. 10. Many minera l deposi t s and pros pec t s found in the Lufilian Arc are being interpre t e d as IOCG. These include the Dunr obin, Nampundwe and Kaleng wa mines in Zambia; Luiswis hi, Shitur u and Kamoya in the Democrat i c Republic of Congo; and the Kombat, Cop per Vallei, Otjikot o , and Tevrede deposits in Namibia , among others. Many new pros pe cts with IOCG char acte r is ti cs are emer g i ng . Some larg e distr ic ts like the Kitumb a - K an t o n g a area and the Kasemp a - K a le n gw a distri ct in Zambia, and the Lofdal-O as in the Khorixas Inlier of Namibia are promis ing for the future. The Otjiw aro n go Batholit h has potentia l , but involve s explorin g under cover. 11. An iron oxide- c o pp er - go l d deposit seems to lie underne a t h a sedimen ta r y - ho s t ed ?Copper b e l t - t yp e ? copper deposit at the Okatjepuiko farm, near Witvlei, Namibia . The IOCG mineral i z a t i on seems to have been the source of copper for the sedime ntar y - h o s t ed copper deposit . If this can be proven, a new model for copper mineralization in central Africa might emerge. 12. There are several locatio ns where IOCG and sedimenta r y hosted Cu mineral iz a t i o n seem to be associa t e d . Part of these occur in the Zambia n Copper b e l t , and may be one of the sour ce s for second ar y Cu mineralization in the Coppe rbelt. 3 9 3 13. The main IOCG events that have been identified took plac e during seven discrete time period s. From younges t to oldest these are listed on Table 8.3. This is a first attemp t to temporally cons train the IOCG mineralization in the Greater Lufilian Ar c. The possib le IOCG events that took plac e in the basemen t to the Zambian Copperbelt (at Chambishi, Mufulira, the main Copper be l t , Konkol a and Nchanga ) are not very well defined or constrained geochronolog ic ally. The tentativ e age of ~825 Ma is derived from interpreta tions discus s e d on sectio n 6.4 of this report . Other possib le IOCG miner alization in the basement to the Copperbelt are discus s ed in this chapte r and on sectio n 4.1.5. Table 8.3 Discrete periods of iron oxide-copper-gold mineralization that took place in the Greater Lufilian Arc. 4 IOCG mineralization at Sasare is included here for comple teness. The source of information about mineralization and geochronolog y in that part of Zambia cannot be made public. Period Main representative mineralization ~ 4 60 Ma Sasar e 4 , Zambia ~533 Ma Hook Granite Ba tholith satellites, Zambia ~550 Ma Otjiwarongo, Namibia; Kafue Flats, Zambia ~746 Ma Kalengwa-Kas empa , Zambia; Khorixas, Namibia ~825 Ma Copperb e l t , Zambia (possib l e , see section 6.4) ~1078 Ma Witvlei, Omitiomire, Namibia ~1937 Ma Kamanjab Batholith, Namibia 3 9 5 9 CONCLUSIONS 9.1 Main Granitoid Terranes in the Greater Lufilian Arc The nature of the granitoid terran es in the study area of the Greater Lufilian Arc can be summariz ed as follows : 1. Foliated alkali granite, quartzmo nz on ite and grani te were emplac ed at 1900?100 Ma. They are pres ent beneath the Katanga Supergr o up in the Copperb e l t, the Mkus hi- S e r en j e area, NW Zambia, and the Domes region (Zambia ) ; Kaokola n d , central Namibia , the Kamanjab Batholith and Grootfontein Inlier (Namibia). The environment of emplac ement for these rocks has not been well identified, but tends to be anorogen i c . This period may be broken in to at least four discrete events. 2. Generally poorly outcropping pre-Katanga gr anito id and felsic to mafic volcan ic s were emplac e d at 1100?50 Ma. They are pres ent south of the Copperb el t , and west of Lus ak a (Zambia) ; around Omitiomi r e , Kaokolan d and the Witvlei area (Namib ia ) . These roc ks surro u nd the Kapva al Cr aton continuously from Namaqualand in South Africa, to the Irumide Belt in Zambia . They were emplaced in anorogenic continen t a l rift?rel a t e d environme n t s . 3. Sporadic, but widely distributed, small igne ous intrus i on s were emplace d at 750?50 Ma. They comprise granite, alkali granite, syenite and gabbro with felsic and mafic volcan i c s , as observe d in the Copperbe l t , Kalengwa- K as e m pa and NW Zambia (Zambia) ; Khorixas Inlier and Summas Mountains (Namib i a) . These bodies intrud e Roan and Nguba Fo rmat i on lithol o g ie s but are genera l l y overla in by (Upper ) Kunde l u n gu sedime n t s and their Namib i an equi val e n ts . They were emplace d in anoroge n ic rift- related and continental epe irogenic uplift environments. 4. Widespr ea d and volumin o us granit o id magmat is m (Pan African ) was emplac ed at 550?50 Ma. It is well pres er ved in the environs of Otjiw ar o n g o , central Namibia , Kaokola nd , and in west-cen t r a l Zambia (includi ng the Hook Granite Batholit h ) , but also sporadically detec ted in NW Zambia. The Otjiwarongo batholith, a covered pluton in Namibia, may be similar to the Hook Granite batholi t h in size, rock type and age. Thes e rocks were emplaced in continental epei roge n ic uplift and rift-re la t e d environme n t s . This period may be brok en into at least three discrete events. 5. Several, more restricte d magmatic events occur du ring the las t 2000 Ma in the Greater Lufilia n Arc . Examples of this are the Nchanga Granite in Zambia (880 Ma); magmatis m at 1700 Ma in the Khorixa s Inlier, Namibia; and at 1600 in the Kamanjab Batholith. The Zambian Lufilian Arc and Damara region of Namibia behaved in a different way from 2200 to 2000 Ma; they were indepen d e n t entitie s . They also behaved sign ificantly different from 1400 to 850 Ma. Geological history of the two main portions of t he Greater Lufilia n Arc is cons iste n t from circa 800 Ma to the presen t, and especially during the last 600 Ma. 9.2 Polycyclic Geological History Most areas studied in the Greater Lufilia n Arc show polycycl ic geolog ic a l histories . Repea ted anorogen i c intrusiv e events are a common denomina t o r . Source rocks for the various melts come from previously-formed intrusive rocks and siliciclas tics. Prolonged crustal histories have resulted in superimposition of events. Two Namibian examples illustrate this. In the Otjiwar ongo environ s, Neoproterozoic granites intruded anor ogenic Paleoproterozoic granites, and both were intruded almost in the same location by two large Mesozoic alkaline comple x e s . At the Oas farm, a Mesozoic mafic feeder pipe cuts through 750 Ma alkaline intrusion s that had intrud ed Paleop r o t er oz o ic anorog en i c granit o i ds . Melts and sedime n t a r y rocks have been re-work e d in each of the areas; a lot of magma mixing and crus tal contami nation processes were involved in the formation of the granito id s . 9.3 Rock Types The majority of the rocks from the Greater Lufilian Arc t hat were analysed had midal kaline character. Table 9.1 compiles statist ic s on sample composi t i on and alkali n i t y that were carried out in all samplin g domains . Any rock that plotted outside of the fields of the m odified TAS diagram was not included in the statistics. 3 9 6 Table 9.1 Rock type statistics of all sa mples analysed from the Greater Lufilian Arc Group Rock type number % Granitoids Groups A l k a l i grani t e 102 22.1 3 Q u a r t z m o n z o n i t e 83 18.00 S ye n i t e 32 6.94 M o n z o n i t e 17 3.69 6 3 . 9 3 Monzo d i o r i t e 10 2.1 7 M o n z o g a b b r o 12 2.60 Midalkaline Rocks A l k a l i gabbr o 20 4.3 4 59.87 Granite 99 21.48 G r a n o d i o r i t e 33 7.16 3 6 . 0 7 Diorit e 6 1.30 Gabb ro-di o ri te 3 0.65 Q u a r t z o l i t e 4 0.87 Subalkaline Rocks Gabb ro 6 1.30 32.75 foid sye ni t e 11 2.3 9 f o i d monzo s ye n i t e 4 0 . 8 7 f o i d monzo - d i o r i t e 2 0 . 4 3 f o i d gabbro 12 2.60 Fo i d o l i t e 3 0.65 Alkaline Rocks P e r i d o t gabbr o 2 0.43 7.38 Total 4 6 1 9 9 . 5 7 1 0 0 . 0 0 100.00 C a r b o n a t i t e 10 Total including carbonatites 4 7 1 The database of 471 sample s was brok en into domain s as indicat e d on Table 9.2 . R oc k type perce n ta g es for each domain is listed on Table 9.3. Table 9.2 Number of samples from each rock type for domains of the Greater Lufilian Arc. 3 9 7 Table 9.3 Percentages of each rock type for domains of the Greater Lufilian Arc. 60%, 33%, 7% is the percentage relationship of midalka l i n e to subalkal i n e to alkaline rock groups for the entire project (Fig 9.1) . 64%, 36% is the percentag e relatio ns hi p of midalkal i n e to subalka l i ne granito i d s . Carbonatites make 2.1% of the total sample s. If the suite of mafic rocks collec t e d are cons ide r ed repr es entative of reality, then mi dalka l in e gabbroi ds make 66%; alkalin e gabbroi ds , 18%; and subalka l in e gabbroids, 17%. Fig 9.1 Distribution of rock types and comparat ive composition of rock alkalinity in the Greater Lufilian Arc granitoid project. Based on the names of the modified TAS diagram of Middlemost, 1994a. Note the absolute domination of alkali granite, granite and quartzmonzonite. Toge ther thes e rock types account for almost 62 % o f all samples st udied. That is also clear on Fig. 9.2. 0.00 5.00 10.00 15.00 20.00 25.00 alkali granite granite quartzmonzonite granodiorite syenite alkali gabbro monzonite monzogabbro foid gabbro foid syenite monzodiorite diorite gabbro quartzolite foid monzosyenite gabbro-diorite foidolite foid monzo-diorite peridot gabbro 3 9 8 Fig 9.2 Composition of the samples collected in the Greater Lufilian Arc. T h e u p per pie diagram groups rocks according to t h eir alkalinity, sens u Middlemost , 1 99 4 . T h e l o w er diagram breaks the samples into their respective rock types . Midalkaline rocks predominate, whatever the point of vi ew. That corres ponds with the continental extension, anorogenic environment that has ruled formation of plutonic rocks in the Greater Lufilian Arc. The average rock type distribution for the entire Great er Lufilian Arc closely rese mble s that of the Hook Granite Batholith, as indicated on Table 9.3. 9.3.1 Mafic, Ultramafic and Alkaline Rocks Mafic, ultrama f i c , carbona ti t i c and alkalin e intrus i on s ar e well repr es ented , albeit volumetric ally minor, in most domains of the Greater Lufilian Arc that were studied. In certa i n cases , these rocks might be implicat e d in mineral i z i ng proc es s e s (Kalengw a deposit , Lofdal rare earth mineral iz a t i on and Lof dal carbonatites ). These rocks occur in anoroge n ic epeiroge n ic uplift and rift-re l a t e d envir on m e n t s . Mafic ro cks are under- r e pr es en t e d in the geochemical datab as e, becaus e they were not the primar y sampling target. The widesp r e a d small gabbro ic bodies in the Greate r Luf ili a n Arc were emplac ed as mafic plugs in large, within-p l a t e areas that were being subjec t to incipien t rifting. The mafic plugs could intersec t the sedimenta r y cover of the plate, includ in g marine and contine n t a l deposits . A modern day analogue of the same proc es s takes place in the envir ons of Filiya, Nigeria. 9.3.2 Rock Associations in Anorogenic Environments A frequent field observation is the per sist en t cluster i n g of small bodies of red- al t e r e d granito i d s , gabbro id s , massive magnetite-hematite and quar tz pods that are linked to ages around 550 and 750 Ma. The four -rock associa t i o n seems to be a char ac t e ristic of continental extension ano rogen i c environme n ts . It is spatia ll y related to iron oxide-c opper-gold mineraliz ation. A recurren t feature observe d in most outcrops of the study area is the pr esence of two or more contrast i ng types of pluto n i c rocks . In some ca ses gabbro i ds and granit o i ds ; in othe rs, syenitoids and granitoids; even three or four types of granites and alkali granites. Many of the small areas also contain mafic, ultrama f i c and alkalin e plugs and dikes of varying composi t i on , such as lamprop h y r es , carbon a t i t e and nephel in e syenit e . alkali gr anite gr anite quar tz monz onite gr anodior ite s y enite alkali gabbr o monz onite monz ogabbr o f oid gabbr o f oid s y enite monz odior ite dior ite gabbr o quar tz olite f oid monz os y enite gabbr o- dior ite f oidolite f oid monz o- dior ite per idot gabbr o 3 9 9 T h e multi p l ic it y of rock types in a small area seems to be another char ac teristic of continental extens ion anorog en i c enviro n me n t s . 9.3.3 Quartz Pods Quartz pods have been identified throughout most of t he Greater Lufilian Arc region. They differ from veins, boudina g ed veins and pegmati t i c quartz units, particu l a r l y in geometry: outcrop s of undeformed bodies are typically round to elliptical, and vary from a few to several- hundred meters in diameter . Dimensio ns of some quartz pods exceed four kilometers in diameter and ther e is geophysical eviden ce of even larger ones. They seem to be a special type of silicific ation. Hyper-alk ali ne, hydrothermal solutions seem to be involved in the transpor t a t i o n of silica and emplac e me n t of the quartz pods . Quartz pods are emerging as a type of alterat i on that is associated to IOCG systems in the Greater Luf ilian Arc. Improved identification in the field and an increase d understa n d in g of their physico -chemic al features may aid in the explor ation of mineral deposits. 9.3.4 Iron Oxide Bodies Masive bodies of magnetite and/or hematite at macros c o p ic , mesosc o p ic and micros c op i c scales emplac e d themselves by gradual replacement of the host rock. The proces s seems to involv e silica te dissolu t i o n by hyper-alk aline hydrothermally-driven solutions. 9.3.5 Round-Pebble Hydrothermal Breccias Round-pebble hydrot hermal breccias occur often in and around IOCG systems th roughout the Greater Lufilian Arc. They seem to have been produced by hyper-alk aline solutions that corroded previous l y angular hydroth er m a l breccia s . In some cases, they act as good hosts for sulfide mineraliz a t i o n . 9.4 Ring Complex Clusters Clus ters of anorogen ic granitoi d ring complexes have been produced all along from Archean times to the pres ent. Clusteri n g of multip le anorogen ic ring complex intrusio ns can form batho lit h i c size bodies. At least ten clusters of ring complexes were identified in the Greater Lufilian Arc. Ri ng complex cl usters have the followin g char ac t e r is t i c s : 1) Mult iple ring complexe s of varying chemical composit i on and size that might interse c t each other. 2) Volcanic and plutoni c rocks of roughly the same compos ition occur togethe r. 3) Successive magmatic events of vary ing compos ition allowed for abundant oppo rtunities of magma mixing and recycli n g of crustal materials . 4) The plan view geomet ry of un-tectonized ring complex clusters is roughly that of an isos cele s triangle . 5) Less volumino us prec urso r and waning events of magmatis m may occur. 6) The princip a l chemica l compos i t i o n of the magmas is midalkaline, but may ocassionally vary to alkaline and subalkaline. In extreme cases, it may be peralk alin e and can even produc e carbon a t i t i c rocks. 7) Isolate d bodies of mafic and ultramafic rocks often come in the la tter stages of the process . 8) Total duratio n of ring comple x clus ter cycles aver ages 110 Ma. Several cycles of ring complex clus ter s have repeated l y oc curre d in roughly the same location in at least three differen t localiti e s . Thes e repeated cycles were sepa rated 1095 Ma in NW Zambia; 933 Ma at the Khorixas area, Namibia; and 50 Ma in West Lusak a, Zambia . 9.5 Tectonic Environment of Emplacement The tectonic environment of emplacement for part of t he rocks collected is not yet well constrain e d ; active resear ch is curren tly being carried out to address th is issue. Nevertheless, several clear patterns are emerging : 1) The largest portion of granitoi ds collec t e d are midalk a l in e rocks that formed in an anorog e n ic contine n t a l epeirog e n ic uplift environm e n t . 2) Next co me thos e formed in rift environments. 3) Another signif ic a n t group of rocks formed in a post orogen i c gr anitization environment. 4) Continen t-continent collision environments were not positively identified. 5) Sub duc t i o n a l magmat i s m seems to have been very restric te d both in terms of time and areal extens ion. Ther e is ev idence of minor such magmatis m in Paleop roterozoic rocks of Kalene Hill and in portions of the Kamanjab Ba tholith. In any given area, two or more of these settings may be superimp os e d . Anor ogen i c continen t a l ex tension is the main geologi cal process of the Arc. Comple te Wils on cycles were not identifi e d in the doma ins of the Greater Lufilian Arc that were studied . The dominan t magmatic proc ess, as eviden ced by the volume of extrude d rock, is anoroge n i c continen t a l epeirogenic uplift, closely-fo llowed in time by a rift-re lated granitoid emplacement. Coalescing and overprinting aulac ogens seem to be the main type of geolog ical event in the arc. 4 0 0 The environment of emplacement of Pa leoproterozoic rocks that occur thro ughout the Arc cannot be identified using the established methods for granitoid envir onment of emplacemen t. Intense sodic alteration and hematit i z a t i on were observe d in part of these rocks. Another alteration proc ess is a net enric hment in potassium that is evident by the abundant biotite and alkali feldspar over growth. Part of th e rocks showed diffus e crys tal margin s and abunda n t blue quartz phenoc r y s tals. Incipient migmatitization of these rocks may have modified their chemistry to a point wher e they don?t fit tr aditional proc edures to evaluate granitoid environment of emplac ement. The alteration processes just mention e d seem to have taken place before ~880 Ma, becau se the environment of emplacem ent of younger rocks can be identified. 9.6 High Thorium High values of thorium were found in part of the granito ids of NW Zambia, Kafue Flats, Hook Granite Batholith (Zambia ) , Oas farm and Otjiwar o n go environ s (Namib i a ) . They are high-heat pr oducing rocks. The anomalous thorium content in some granitoids of the Greater Lufilian Arc indu ced and maintained long-lived, large convec tive cells of hydrothe rmal fluid flow . High-th or i u m granito id s in all five domains have a parti cul ar trac e element chemica l signatu r e that is not common, and probabl y were subject ed to analogo us geolog i c a l process es at differe n t points in time. 9.7 Correlation of Granitoids Granitoid rock suites with clos ely matching chemis tr y and macros copic features have been found to form in the same region, two or three times with up to a thous and million years of age diffe renc e . Source rocks and environm e n t of emplac e me n t for the anoroge n ic intr usi v e events were the same: for that reason, magmatic products turned out equivalent. These features preclu de lithological or detailed geochemic al correlation. Rocks from the suites of Muliash i Porphyr y and Mufulir a , Zambia are an example of this. They both have pink and gray granitoids with similar compositions, but the ages of the rocks are completely different. Several lithological correlations have been developed for granitoid s in variou s domains of the Greater Lufilian Arc. The rocks cannot be properly correlated until mo re geochronological information is available. 9.8 Main Findings in Specific Domains 9.8.1 Hook Granite Batholith, Zambia Information currently available on geophysics, geochr onology, rock distribution an d geoche mistry from the Hook Granite Batholith fit quite well with an intrac on tinental, anorogenic, ring complex cluster origin. The batholith is mainly composed by midalkaline granitoid s. Alkali granites , quartzmo n z o n i t es and granites make up 70% of all rocks. 9.8.2 Nchanga Granite, Zambia The Nchanga Granite has all the char acteristics of an anorogenic granite ri ng complex. Chemistry of its rocks crosses the midalk a l i n e to subalk a l i ne fields . Parts of t he pluton are made of high heat produci n g granit e s that maintain ed a long-lived circulat i on of hydrother m a l fl uids. The Nchanga Granite might have contribu t e d to the origin of copper in its environs. 9.8.3 Kamanjab Batholith, Namibia Sixteen suites with more than two contrast i ng rock types were identified in the Kamanjab Batholith. No two suites are identica l , and they are made by a large variet y of rock types. This multip licity of rock types at a given site is one of the charact e r is t i c s of anorogen i c environme n t s in the Greater Lufilian Arc. There is no direct proof of the pres enc e of ring comp lexes at the Kamanjab Batholith. Nevertheless, several sources of evidence point to the batholith as a cluster of ring comple xe s . Among other s, thes e are: 1) the lack of continui t y in the rock types along traverses; 2) the pres ence of mult iple rocks types in at least fifteen discret e sites; 3) General anoroge n ic charac t e r of most of the rocks; 4) three quarters of the rocks in the suite are midalka l in e ; 4) the size and shape of the batholith, as well as its event diagra m has simila r i t i e s with other ring complex clus ters . 4 0 1 9.8.5 New Temporal Constrain to Katangan Sedimentation G r a n i t ic dikes emplac e d at the Nchang a mine area in anorogen i c extens i on a l environ m e n ts were dated at ~765 Ma. They provide the youngest age of deposition for that portion of the Katanga sediment a r y sequen ce at Nchanga (Roan sedimen t s ) , and might provi de a significant brac ket age for mineralization. 9.8.6 Khorixas Inlier-Kamanjab Batholith Geolog ical history for the Khorixas Inlier and the Kamanj ab Batholith are significantly different. They probably were not in the same geograph i c positio n all the time. Older basemen t is known in the Khor ixa s Inlier than at the Kamajab. The two regions seem to have had a common geolog ic a l history for the past 550 Ma. 9.8.7 Long-Lived Fractures E-W-tre nd i n g region a l fractu r e systems that run paralle l to the elongation of the Greater Lufilian Arc play an important role in the emplac emen t of magmatism and IOCG mineraliz a t i o n . They acted as routes for intr us ion , channe ls for fluids and contro l for ore deposi t i o n . Those structures are generally paralle l to the main Lufilian Arc trend , and could have been norma l syn-rift faults that have been reac ti v a t e d through o u t geologic a l history . Some N-S-tre n d i ng structu r es are also mineral iz ed and t hey are sub- per p en dic u l ar to the main trend of the Lufilian Arc. 9.9 Metallogeny Various types of mineral iz ati o n were seen to be asso ciated with intrusive rocks along the Greater Lufilian Arc (Table 9.4) . These include rare earth minerali z a t i o n as socia t e d to alkali ne dikes and carbona t i t e s in the Khorixas Inlier, sedimentary-ho sted gold (so-called ?Car lin?-style deposits), several low-sulfidation hydrot h er m a l gold occurr e n c e s , low su lfida t i on hydroth er m a l copper deposti s , epigen eti c copper vein deposits, alkaline porphyry molybdenum (-copper?) styl e mineral i z a t i o n , sedimen t a r y - h os t e d copper- c ob a l t deposits , and a wide variety of iron oxide-cop pe r - g o l d and relate d deposi t s and prospe c ts . Severa l Paleoproterozoic rocks throughout the Greater Lufili an Arc are enriched in copper. Some Mesoproterozoic syenites and alkali granites are enriched in zinc . The si gnific a nce of the latter observa t i on remains unclear . Paleopr o t e r oz o ic copper - r ic h rocks could be the source of metal for later events. Incipient migmatitization of those rocks could have remobilized t he copper. Copper is probably bei ng recycled. Very little skarn mineralization was observed in Ka tanga n carbona te s , even though they ar e intruded by multiple pluton ic episo d es . Possib l e excep t i o n s occur around the Hook batholit h . The Samba deposi t is not conside r ed to be a copper porphyr y ; it is a low sulfida t i o n epither m a l copper mineral iz a t i o n host ed in pyroclas tic rocks that were sheared during regiona l metamor ph i s m . 9.9.1 Metallogenic Epochs At least eight discret e periods of mineral iz a t i o n can be interpr e t e d from Table 9.4 (The same are simplif i e d on Table 9.5) . Wher e possib l e , radiome tr i c ages have bee n used to place the various events. Most have been assigned to specific ages by correl ation or association. Six deposits could not be placed chrono lo g ic a l l y and are included at the bottom of the list. There is a wi de-sp r e a d series of mid- alk a l i n e intrusi on s emplac ed around 750 Ma that produces a variety of mineral deposi t s . Another such event (separ a te d in at leas t three different phases: 500- 513, 550 and 583 Ma) took place around 540?40 Ma. Five less well defined events took place as indicated on Table 9.5. From old to young, they occurred at ~1970, ~1930, ~1866 , 1097-105 9 and ~460 Ma (See Tables 9.4 and 9.5). The dominant depos it type is iron oxide-cop per-gold mineralization. The age of sedimentary-ho sted copper mineralization in the Copperbe lt is currently being re-evaluated using Re-Os dating at the University of Arizona. Three tentative ages for them are 796-756, ~583 and ~550 Ma. The main events of sedimen t a r y - h os t e d gold mineral i z a t i o n in Namibia are ~750 Ma in the environ s of Sesfontein, ~550 Ma in Eastern Na mibia. The age of the Zambian de posits and prospects could not be estimated. At least two distinct events of diss emi na t e d copper mineral iz a t i on associa t ed to midakaline granitoid intrusives were identified in the Kamanjab Batholith. The first took place around 1975 Ma and the second around 1928 Ma. 4 0 2 4 0 3 Table 9.5 Simplified Classification of Metallogenic Events in the Greater Lufilian Arc By Alberto Lobo-Gu errero, M.Sc., Min.Ex., December, 2004 Economic Geology Research Institute, Univer sity of the Witwatersrand, Johannesburg Commodities Location Deposit Type Age * Environment A u Sasare , Zm IOCG 460 ACR Cu,Co,Ni, Au,U,Fe Kansanshi, Zm + some southe r n Congo l es e Fe + Cu- Co deposi t s IOCG + Kansanshi veins 500-513 Eo Extension Mo Marink as Kwela Mo porphyry 520-560 E ACR Cu,Au,Fe, REE,Ag,Zn,Pb Hook Granite batholith satellite bodies , Zm IOCG ~533 E1 ACR Cu,Au Otjiwarongo, Otavi Mts., Nm; Kafue Flats, Zm IOCG + Sedimentary- h o s t ed Au + Navachab , Nm ~550 E2 ACR Cu,Co (U) Copper b e l t and Congol ese Cu- Co minera l iz at i o n hosted in sediments; remobilization and mineralization Sed- ho s ted Cu (epigene t ic overprin t ) ~ 5 83 E3 Event related to Verang i a n Glacia t i o n ? Cu,Co,Ni,Au Kabompo Dome, Zm IOCG, sed-ho sted Co- Ni -C u ~730 I CEUG Cu,Au,REE, Ag,Mn Kalengwa-Kas empa area,Zm Oas, Lofda l, Mesopotamie, Nm IOC G ~745- 75 6 I ACR Cu,Co Initial copper mineralization in the Zambian Copperbe l t (and Katang a ?) Sed-ho s t ed Cu 756-79 6 I-J ACR Cu,Au Witvlei, Nm; Mkus hi,Zm; Omitiomire,Zm IOCG + Intrus ive related mineralization 1 0 5 9- 1 0 9 7 L ACR Au,As ,Bi,Sb Karibar e mb i and Kililamirombwe, Zm Sed- ho s ted Au L or younger L ACR Cu,Au? Kamanjab Batholith, Nm IOCG, hydrotherma l Cu dissemi n ati o n 1866 U enviro nm e n t cannot be identif i e d - probab l y CEUG Cu,Au? Kabompo Dome, Mwinilunga, Lumwana, Zm Schis t- h os te d Cu 1928 U ? Cu, Au,Fe,F,REE Kamanjab Batholith, Nm; Mwinilun g a , Zm (?) IOCG 1930 U ACR Cu,Mo Samba, Zm Schist- h os t e d Cu 1965 V ? Cu,Au,Ag? Kamanjab Batholith, Nm Hydrot he r ma l Cu dissemination 1975 V CEUG NOTE: ACR = Anorogenic continental rift. CEUG = continental epeirogenic uplift granitization. * Letters in the fifth column refer to labels for magmatic events in geochronolog ic al correlation diagrams (Figs A79 to A83). White and gray colorati o n serves to separate major metalloge n i c times. 4 0 4 9.9.2 Iron Oxide-Copper-Gold Mineralization The iron oxide copper- g o ld (IOCG) styl e of minera l iz a t i o n is far broader in terms of both spatial distribut i o n and age of emplacemen t than previous ly thought. IOCG deposit s have been identif i e d in both Namibia and Zambia. In Namibia, for example, the IOCG deposit Tevrede is curren tly being explor ed by junior mining corpor ations in the northwes tern portion of the Kamanjab batholith; in addition, the Kombat copper mine in the Otavi Mountains and Otjikoto, a gold deposit in the environs of Otjiwarongo, s eem to be IOCG depos i t s . Several IOCG-li k e mineral i z e d areas were identif i e d at the Oas, Lofdal, Mesopo t a m i e and Gelbinge n farms as outliers to the Kamanjab Batholith. Zambia also has se veral known IOCG depos it s like the Kalengw a copper- silver mine, the Kitumba and Kantonga copper depo sit s and others around the Kasempa area. The Nampundwe pyrite mine as well as Dunr obin gold mine also have IOCG char ac teristics. Quartz ites are good hosts for mineralization. This wa s observ e d in severa l Namibi a n areas, includ i n g the southe r n part of the Oas farm, the Gelbing e n farm and the western portion of the Kamdes cha farm, bordering the Kamanjab Batholith. Quartz ites fracture in a bri ttle manner that is ideal for hydrothe rmal brecciation. Equivalent rocks might host mineraliz ation in Zambia . The main IOCG events that have been identified in t he Greater Lufilia n Arc took place during eight time periods . Thes e are listed on Table 9.6. The possible IOCG events that took plac e in the basement to the Zambian Copperbelt (at Chambishi, Mufulira, the main Copper be l t , Konkol a and Nchanga ) are not very well define d or constr a in e d geoc hr o n o lo g ic a l ly . Table 9.6 Periods of iron oxide-copper-g old mineralization in the Greater Lufilian Arc. Period Main representative mineralization ~ 4 60 Ma Sas are, Zambia ~533 Ma Hook Granite Ba tholith satellites, Zambia ~550 Ma Otjiwarongo, Namibia; Kafue Flats, Zambia ~746 Ma Kalengwa-Kas empa , Zambia; Khorixas, Namibia ~825 Ma Copperb e l t , Zambia (possib l e , see section 6.4) ~1078 Ma Witvlei, Omitiomire, Namibia ~1937 Ma Kamanjab Batholith, Namibia The rocks of many IOCG deposit s and prospec t s in the Greater Lufilia n Arc are pristin e . There is no signifi c an t deforma ton involved. Hydr othermal bre ccia t i o n and other mineraliz a t i o n f eatures are un-defor m ed . This may be very useful to study mineralization and alteration processes. 9 . 9 . 3 Association of Sedimentary Hosted C opper Mineralization with IOCG Mineralization A significant finding is the juxtaposit ion of iron-oxide-copper-gold minera lization undernea th the sedimentary- h o s t ed copper deposit at Witvlei , Namibia . This metall ogenic event occurred at 1110 Ma. Secondary copper in the sedimentary-ho sted deposit might have come from the IOCG deposit that lies undernea t h . This idea may generat e a new conc ep t for the origin of the Copper b e l t - K a t an g a copper and cobalt deposits . The concep t also opens an entir e new age gap for the explor a t i on of base metal mineralization in the Greater Lufilian Arc and the surrounding environment, includ in g South Africa. There is additiona l evidence of IOCG mineraliz a tio n related to sediment - h os t ed copper in other parts of Namibia and Zambia, includ in g the Chambish i area and parts of the basement to the Copperbelt. At least three discrete time periods show IOCG miner alization in close temporal spatial associa t i on with sedimen t ar y - h o s t ed copper deposits . The first took pl ace around Witvlei from 1108 to 1059 Ma. The second and third oc urred in the basement to the Zambian C opperbe lt from 882 to 725 Ma and from 607 to 500 Ma. 4 0 5 10 BIBLIOGRAPHY Abell, R. S. (197 6) T h e G e o l o g y o f t h e L u k o me zi River Area - Ex planation of De gree Shee t 1 5 2 6 N W Q uarter (Geol o g i c a l Repor t 33) , Repub l i c of Zam bi a , Minis t r y of Mines and I ndus t r y , Geolo g i c a l Surve y, Lusak a , Zam bi a . Adamso n , R. G. , & Teichm a n n , R. F. H. (1 986) The Matchl e s s C upre o u s Pyrit e De po s i t , South West Afric a / Namib i a , In C. R. 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(1989 ) K-A r, Rb-Sr and Geoc h e m i c a l Inve s t i ga t i o n s int he Mooir i v i e r Compl e x , South West ern Windh o e k Distr i c t and Nort h - W e s t e r n Malta h o h e Distr i c t , Namib i a , C o m mu nications of t h e G e o l o gical Survey o f Namibia , 5: 69- 75. Ziegler , U. R. F., & Stoesse l , G. F. U. (1990 ) Isotop e Geolog y and Geoch e m i s t r y of th e Rehob o t h Basem e n t Inlie r , Na mib i a / S.W. Africa; A Multi m e t h o d Case Histo r y, B u l l e tin der Vereinigung Schweizerisches Petroleum - Ge o l o g e n u n d - I n g e nieur , 56 (130 ): 13-33 . Ziegle r , U. R. F., & Stoesse l , G. F. U. (1991 ) Ne w Constr a i n t s on th e Age of the We ener Int rus i v e Suite, the Gamsbe r g Gra nit e a nd th e Crust a l Evolu t i o n of the Reho b o t h Basem e n t Inlie r , Namib i a , C o m m u nications of t h e G e o l o gical Survey o f Namibia , 7: 75-78. Ziegler , U. R. F., & Stoesse l , G. F. U. (1993 ) A g e D e t erminations in the R e h o b o t h Basement I n lier, Namibia , Geol o g i c a l Surv e y of Namib i a , Windh o e k , Namib i a , Spec i a l Publi c a t i o n , Volum e 14. Contact information of the author Last Name: Lobo-Guerrero Sanz Name: Alberto e-mail addresses: ageo@iname.com ageo@logemin.com Paper mail address: Calle 127A No. 53A-28, office 309 Bogota, Colombia Home address: Calle 109 No. 13-98 Bogota, Colombia Business telephone: +57-1-6435364 Home telephone: +57-1-6586040 PRE- AND POST-KATANGAN GRANITOIDS OF THE GREATER LUFILIAN ARC ? GEOLOGY, GEOCHEMISTRY, GEOCHRONOLOGY AND METALLOGENIC SIGNIFICANCE Volume 2, Appendices By Alberto Lobo-Guerrero Sanz Supervisor: Professor Laurence J. Robb A thesis submitted to the Faculty of Science University of the Witwatersrand, Johannesburg For the Degree of Doctor of Philosophy Johannesburg, March 12, 2005 v ABSTRACT This document reports observations , findings and conclusions of the re search pro ject entitled ?Pre- and Post-Katangan Granitoids of the Gr eater Lufilian Arc - Geology, Ge ochemistry, Geochronol ogy and Metallog e n i c Signific a n c e ? . The pro je c t, structur ed and sup er vised by Pro f essor Laure nce Robb, was designed to study granitoids that comprise the Greater Lufil ian Arc. Its main aims were to define the vario us grani toids, and study their role in Katanga n orog enesis and mineral izati on. Main fieldwork was concentrated in northwestern Zambia and northern Namibia. The Greater Lufilian Arc is a curvilinear belt of Ne oprot e r o z o i c Kat ang a n sedime n t s that was deform e d during the Pan African oroge ny in Zambia and the De mocr at i c Repu blic of C ong o, and the westwa r d extension of similar rock sequences into Botswana, Angola and Namibia. The mobile belt of the Greater Lufilian Arc also comprises a dominantly Pale o prote rozoic basement of defor med granitoids, and a diverse suite of Pan-African gra nitoi ds that intrude t he Katanga n sequences. A total of 1500 samples were collected in the fiel d; 351 plutonic rocks were anal ysed. 157 chemical analysis wer e compiled from vario us well-docume nted sources, to reach a total of 508 samples anal ysed in the databa se. 38 new zircon U-Pb SHRIMP II and laser ablation ICP-MS ages were pro duced. The majo rity of intrusive rocks from the Greater Lufilian Arc that were an alysed (60%) had midalkaline characte. 33% were suba lkaline and 7% were alkal ine. Mafic rocks are cl osely associat e d to felsic rocks in most domains of the Arc. Two thirds of the gabb roid s were mid alkaline, 1/6 alkaline and 1/6 subalkaline. The average rock type di stribution for the entire Lufilian Ar c closely resem bles that of the Hook Granit e Batholith in Zambia. A frequent field obser va tion is the persistent clustering of small bodi e s of red-alt ered gra nitoids, gabb roids, massive magn etite-hematit e and quartz pods that are link ed to ages aro und 550 and 750 Ma. The four-roc k association is related to iron oxide- c oppe r-gol d (IOCG) miner aliz ation, and seems to be a character i s t i c of c ontinental extension anoro genic envir onment s. Another recurrent featur e observed in most outcrops of the study area is the presence of two or more contrasting types of pl utonic rocks, includin g mafic, ultramaf i c and alkaline plugs and dikes. The multipli c i t y of rock types in a small are a seems to be a charact e r i s t i c of cont inental exten s ion ano rog e nic envir onment s. Quartz pods, hydrothe rmally-empl a ced iron oxid e bodies and roun d-pe b ble hyd rothe rmal breccias are features that occu r often in and around IOCG system s throughout the Greater Lufilian Arc. The main granitoid perio ds of empla c ement pres ent in the study area of the Arc are li sted on Tabl e 1. Several mor e restricted events occurred at 1700, 1600, 880 and 460 Ma. Table 1 Main Granitoid Terranes in the Greater Lufilian Arc Age (Ma) Rock types Location Environment of Emplacement Notes 5 5 0 ?50 Granite, alkali granite, quartz monzon ite, syenite, gabbr oids Otjiwarongo, central Namibia, Kaokoland, Damaran intrusives (Namibia), Hook Granite, NW Zambia (Zambia) Continental epeirogenic uplift The period may be brok en into 3 discrete events. 750 ?50 Granite, alkali granite, syenite and gabbroids with fels ic and mafic volc anics Copperbelt, Kalengwa- Kasempa, NW Zambia (Zambia); Khorixas Inlier and Summas Mountai ns (Namibi a ) Rift-re la t e d and continental epeirogenic uplilft. Intrude Roan and Nguba Litholog i es ; overlain by Kundel un g u and equiva l e n t sedime n t s . 1 1 0 0 ?50 Granitoids and fels ic to mafic volc an ic s South of the Copperbelt, West of Lusaka (Zambia); around Omitiomire, Kaokoland and the Witvlei area (Namibia ) Continental rift- r e l a t e d environments Surrou n ds Kapvaa l Craton from Namaqu a la nd to Irumide Belt in Zambia 1 9 0 0 ?100 Foliated alkali granie, quartz mon z on i t e and granite Copperbelt basement, Mkushi- S e r e n je , NW Zambia, Domes region (Zambia); Kaokoland, central Namibia, Kamanjab Batholith, Grootfontein Inlier (Namibia) Not well defined; probabl y formed in an anoro ge n ic continental extension environment Period can be brok en into 4 discrete events vi The Zambian Lufilian Arc and Damara re gion of Namibia behav e d as indepe n d e n t enti t i e s from 2200 to 2000 Ma. They also beh aved significantly differen t from 1400 to 850 Ma. Geological history of the two main portion s of the Gre ater Luf ilia n Arc is consist e n t from circa 800 Ma to the presen t, and especially during the last 600 million years. Most areas studied in the Arc show pol ycyclic geological histories. Repeated anor oge nic intrusive eve nts are a common denomin ator. Prolonge d crustal histor ies have resulted in superimposition of events. Granitoid rock suites with closely matching chemistr y and macroscopic features have been found to form two or three times in the same regi on, with up to a thousand million years of age difference. These features preclude lithologi cal or detailed geochemical correlation of plutonic rocks. At least ten clusters of ring comple xe s were identi f ied in the Arc. Cl ustering of multiple anoro genic ring complex intr usions can form batholith i c size bodie s . Cl usters are made by amalgam atio n of multiple ring complex e s of varyin g chemic a l compos i t i o n and si ze. Most of their rocks are midalka l i n e . Volcani c and plutonic rocks of roughly the same composit i o n occu r together. Total duration of ring complex cluster cycles avera ges 110 Ma, and their pla n view geom etry is roughl y that of an isosceles triangle. Information currently available on geoph ysics, geochron olog y, rock distribution and geochemistry from the Hook Granite Batholith (Zambia) fit quite we ll with an intracontinental, anoro genic, ring comple x cluster origin. The Nchanga Granite (Zambia) has all the characteristics of an anor oge nic granite ring complex, and might have contributed to the origin of copper in its environs. Several sour ces of evide nce indicate that the Kamanja b Batho lith (Namibia) is an ano rog en i c cluste r of ring complexes. Volcanic and pluton i c rocks of simila r compos i t i o n make the batho l i t h . Geolo g i c a l hist ory for the Khorixa s Inlier and the Kamanjab Batholith are significantly different. Complete Wilson cycles were not ide ntified in the st udy areas of the Great er Lufilian Arc. The domi nant magmatic process, as evidenced by the vol ume of extrude d rock, is anorog enic continental epeir oge nic uplift, closely-f o l l o w e d in time by a rift-rel a t e d granit o i d emplac e m e n t . C oalesci n g and overprin t i n g aulacoge ns seem to be the main geol ogical event in the Arc. Incipient migmatitization and alter a tion of Paleopr oterozoic rocks modi fied their chemistry to a point wher e their enviro nment of em placement cannot be i dentified by traditional geochemical means. The anomal ous thorium content in some gra nitoids of the Greater Lufilian Arc induced and maintai ned long-lived, large convective cells of hydrotherm al fluid flow. E-W-trendin g regional fracture systems, that run para llel to the elo ngation of the Arc, play an imp o rtant role in the emplacement of magm atism and IOCG mineralization. Thos e structures are gene rally par allel to the main Lufilian Arc trend, and could have been no rmal syn-rift faults reac tivated multiple times during geolo gical history. At least eight discrete periods of mineralization were ide ntified in t he Gre ater Lufilian Arc. There is a wide-spr ead series of midalkaline in trusions emplaced aroun d 750 Ma that prod uces a variety of mineral deposits. Another eve nt took plac e around 540?4 0 Ma. Five less well defined events oc curred at ~1970, ~1930, ~18 66, 1097- 10 59 and ~460 Ma. The domin ant dep osit type is iro n oxide -coppe r -gol d mineralization, but other types of mi ne ral deposits are present in the Arc. At least two di stinct events of disseminated coppe r mi neralization associated to midalka lin e gra nitoid intrusives were ide ntified in the Kamanjab Batholith; the firs t took place arou nd 1975 Ma and the second aro und 1928 Ma. The main IOCG events that have be en identified in the Great er Lufilian Arc took place during eight time perio d s . The rocks of many IOCG de posi t s and prospe c t s in t he Arc are pri s tine. There is no significant deformaton invol ved. Hyd rotherma l brecciation and other mine raliz ation features are un- deformed. Three discr ete time periods show IOCG miner alizat ion in close temporal spatial association with sedimentary- hosted copp er de posits. The first took place aro u nd Witvlei (Namibia) fro m 1108 to 1059 Ma. The second and thir d ocurr ed in the baseme n t to the Zam bian Cop per belt from 882 to 725 Ma and from 607 to 500 Ma. This idea may gener ate a new concept for the origin of sedimentary-hosted cop per and cobalt deposits. ABBREVIATED TABLE OF CONTENTS Abstr ac t Short Table of Contents Detailed Table of Contents Aknow l e dg em e n t s 1. Introduction, 1 2. Methodology, 4 3. Generaliz e d Geolog y of the Greater Lufilian Arc, 21 4. Description of Rocks from the Different Domains, 23 Zambian domains , 24 Hook Granite Batholith, Zambia, 24 West Lusaka/Kafue Flats domain, 46 Kalengwa-Kas empa Area, Zambia, 53 Northwes tern Zambia domain, 60 Kalene Hill area, 61 Introduction to the geolog y of the Domes Region, NW Zambia , 72 Kabompo Dome, 73 Mwombez h i Dome, 80 Solwezi Dome, 91 Conc lus i o ns on entire NW Zambia region , 94 Zambian Copperbe l t , 96 Nchanga Granite, 102 Nchanga mine area, 112 Muliashi Porphyry, 115 Deep borehole, Konkola mine, 120 Chambishi granite, 124 Mufulira granite, 129 Samba deposit, 132 Conc l us i o ns , 136 Namibian Domains, 142 Kamanjab Batholith, 142 Khorixas Inlier, 182 Oas farm, 184 Lofdal farm, 207 Other Small Outcrops in Namibia and Bostwana, 223 Mesopot a m ie, 223 Summas Mountains, 228 Ugab River outcrop s , 230 Okwa River Outcrops , Botswana, 232 Grootfontein Inlier, 234 Review of observations, 235 Environs of Otjiwarongo, Namibia, 237 Witvlei, Namibia, 245 5. Thorium Content of Granitoids in the Greater Lufilian Arc, 253 6. Geoc hronolog y, 257 New radio m etr i c ages, 257 Geoc hronolog ical database and interpretation, 257 New Re-Os ages from copper mineral iz a t i o n , Zambian Copperb e l t , 262 7. Some Aspects of Anorog en i c Intrus i v e Rocks, 265 Comparis on of batholit h i c granitoid bodies with anorogen ic ring complex clus ters , 266 Comparis on of Lufilian small basic intrus ions with examples from the literatur e, 279 8. Iron Oxide- Copper-Gold Mineraliz at ion in the Greater Lufilian Arc, 281 Some notes on iron oxide-co pp e r - go l d deposits , 281 Iron oxide- copper-gold systems in the Greater Lufilian Arc, 289 Some known IOCG-l i k e deposi ts and prospe c ts , 305 Relation ship between IOCG and sedimentary-hosted Cu mineralization, 334 Sedimentar y-hosted Au mineraliz ation in the Greater Lufilian Arc, 334 Peculiar i t i es of Zambian and Namibia n IOCG systems , 335 Conc l us i o ns , 335 9. Conc lus i o ns , 337 10. Referenc es , 347 Appendices 3 9 5 9 CONCLUSIONS 9.1 Main Granitoid Terranes in the Greater Lufilian Arc The nature of the granitoid terran es in the study area of the Greater Lufilian Arc can be summariz ed as follows : 1. Foliated alkali granite, quartzmo nz on ite and grani te were emplac ed at 1900?100 Ma. They are pres ent beneath the Katanga Supergr o up in the Copperb e l t, the Mkus hi- S e r en j e area, NW Zambia, and the Domes region (Zambia ) ; Kaokola n d , central Namibia , the Kamanjab Batholith and Grootfontein Inlier (Namibia). The environment of emplac ement for these rocks has not been well identified, but tends to be anorogen i c . This period may be broken in to at least four discrete events. 2. Generally poorly outcropping pre-Katanga gr anito id and felsic to mafic volcan ic s were emplac e d at 1100?50 Ma. They are pres ent south of the Copperb el t , and west of Lus ak a (Zambia) ; around Omitiomi r e , Kaokolan d and the Witvlei area (Namib ia ) . These roc ks surro u nd the Kapva al Cr aton continuously from Namaqualand in South Africa, to the Irumide Belt in Zambia . They were emplaced in anorogenic continen t a l rift?rel a t e d environme n t s . 3. Sporadic, but widely distributed, small igne ous intrus i on s were emplace d at 750?50 Ma. They comprise granite, alkali granite, syenite and gabbro with felsic and mafic volcan i c s , as observe d in the Copperbe l t , Kalengwa- K as e m pa and NW Zambia (Zambia) ; Khorixas Inlier and Summas Mountains (Namib i a) . These bodies intrud e Roan and Nguba Fo rmat i on lithol o g ie s but are genera l l y overla in by (Upper ) Kunde l u n gu sedime n t s and their Namib i an equi val e n ts . They were emplace d in anoroge n ic rift- related and continental epe irogenic uplift environments. 4. Widespr ea d and volumin o us granit o id magmat is m (Pan African ) was emplac ed at 550?50 Ma. It is well pres er ved in the environs of Otjiw ar o n g o , central Namibia , Kaokola nd , and in west-cen t r a l Zambia (includi ng the Hook Granite Batholit h ) , but also sporadically detec ted in NW Zambia. The Otjiwarongo batholith, a covered pluton in Namibia, may be similar to the Hook Granite batholi t h in size, rock type and age. Thes e rocks were emplaced in continental epei roge n ic uplift and rift-re la t e d environme n t s . This period may be brok en into at least three discrete events. 5. Several, more restricte d magmatic events occur du ring the las t 2000 Ma in the Greater Lufilia n Arc . Examples of this are the Nchanga Granite in Zambia (880 Ma); magmatis m at 1700 Ma in the Khorixa s Inlier, Namibia; and at 1600 in the Kamanjab Batholith. The Zambian Lufilian Arc and Damara region of Namibia behaved in a different way from 2200 to 2000 Ma; they were indepen d e n t entitie s . They also behaved sign ificantly different from 1400 to 850 Ma. Geological history of the two main portions of t he Greater Lufilia n Arc is cons iste n t from circa 800 Ma to the presen t, and especially during the last 600 Ma. 9.2 Polycyclic Geological History Most areas studied in the Greater Lufilia n Arc show polycycl ic geolog ic a l histories . Repea ted anorogen i c intrusiv e events are a common denomina t o r . Source rocks for the various melts come from previously-formed intrusive rocks and siliciclas tics. Prolonged crustal histories have resulted in superimposition of events. Two Namibian examples illustrate this. In the Otjiwar ongo environ s, Neoproterozoic granites intruded anor ogenic Paleoproterozoic granites, and both were intruded almost in the same location by two large Mesozoic alkaline comple x e s . At the Oas farm, a Mesozoic mafic feeder pipe cuts through 750 Ma alkaline intrusion s that had intrud ed Paleop r o t er oz o ic anorog en i c granit o i ds . Melts and sedime n t a r y rocks have been re-work e d in each of the areas; a lot of magma mixing and crus tal contami nation processes were involved in the formation of the granito id s . 9.3 Rock Types The majority of the rocks from the Greater Lufilian Arc t hat were analysed had midal kaline character. Table 9.1 compiles statist ic s on sample composi t i on and alkali n i t y that were carried out in all samplin g domains . Any rock that plotted outside of the fields of the m odified TAS diagram was not included in the statistics. 3 9 6 Table 9.1 Rock type statistics of all sa mples analysed from the Greater Lufilian Arc Group Rock type number % Granitoids Groups A l k a l i grani t e 102 22.1 3 Q u a r t z m o n z o n i t e 83 18.00 S ye n i t e 32 6.94 M o n z o n i t e 17 3.69 6 3 . 9 3 Monzo d i o r i t e 10 2.1 7 M o n z o g a b b r o 12 2.60 Midalkaline Rocks A l k a l i gabbr o 20 4.3 4 59.87 Granite 99 21.48 G r a n o d i o r i t e 33 7.16 3 6 . 0 7 Diorit e 6 1.30 Gabb ro-di o ri te 3 0.65 Q u a r t z o l i t e 4 0.87 Subalkaline Rocks Gabb ro 6 1.30 32.75 foid sye ni t e 11 2.3 9 f o i d monzo s ye n i t e 4 0 . 8 7 f o i d monzo - d i o r i t e 2 0 . 4 3 f o i d gabbro 12 2.60 Fo i d o l i t e 3 0.65 Alkaline Rocks P e r i d o t gabbr o 2 0.43 7.38 Total 4 6 1 9 9 . 5 7 1 0 0 . 0 0 100.00 C a r b o n a t i t e 10 Total including carbonatites 4 7 1 The database of 471 sample s was brok en into domain s as indicat e d on Table 9.2 . R oc k type perce n ta g es for each domain is listed on Table 9.3. Table 9.2 Number of samples from each rock type for domains of the Greater Lufilian Arc. 3 9 7 Table 9.3 Percentages of each rock type for domains of the Greater Lufilian Arc. 60%, 33%, 7% is the percentage relationship of midalka l i n e to subalkal i n e to alkaline rock groups for the entire project (Fig 9.1) . 64%, 36% is the percentag e relatio ns hi p of midalkal i n e to subalka l i ne granito i d s . Carbonatites make 2.1% of the total sample s. If the suite of mafic rocks collec t e d are cons ide r ed repr es entative of reality, then mi dalka l in e gabbroi ds make 66%; alkalin e gabbroi ds , 18%; and subalka l in e gabbroids, 17%. Fig 9.1 Distribution of rock types and comparat ive composition of rock alkalinity in the Greater Lufilian Arc granitoid project. Based on the names of the modified TAS diagram of Middlemost, 1994a. Note the absolute domination of alkali granite, granite and quartzmonzonite. Toge ther thes e rock types account for almost 62 % o f all samples st udied. That is also clear on Fig. 9.2. 0.00 5.00 10.00 15.00 20.00 25.00 alkali granite granite quartzmonzonite granodiorite syenite alkali gabbro monzonite monzogabbro foid gabbro foid syenite monzodiorite diorite gabbro quartzolite foid monzosyenite gabbro-diorite foidolite foid monzo-diorite peridot gabbro 3 9 8 Fig 9.2 Composition of the samples collected in the Greater Lufilian Arc. T h e u p per pie diagram groups rocks according to t h eir alkalinity, sens u Middlemost , 1 99 4 . T h e l o w er diagram breaks the samples into their respective rock types . Midalkaline rocks predominate, whatever the point of vi ew. That corres ponds with the continental extension, anorogenic environment that has ruled formation of plutonic rocks in the Greater Lufilian Arc. The average rock type distribution for the entire Great er Lufilian Arc closely rese mble s that of the Hook Granite Batholith, as indicated on Table 9.3. 9.3.1 Mafic, Ultramafic and Alkaline Rocks Mafic, ultrama f i c , carbona ti t i c and alkalin e intrus i on s ar e well repr es ented , albeit volumetric ally minor, in most domains of the Greater Lufilian Arc that were studied. In certa i n cases , these rocks might be implicat e d in mineral i z i ng proc es s e s (Kalengw a deposit , Lofdal rare earth mineral iz a t i on and Lof dal carbonatites ). These rocks occur in anoroge n ic epeiroge n ic uplift and rift-re l a t e d envir on m e n t s . Mafic ro cks are under- r e pr es en t e d in the geochemical datab as e, becaus e they were not the primar y sampling target. The widesp r e a d small gabbro ic bodies in the Greate r Luf ili a n Arc were emplac ed as mafic plugs in large, within-p l a t e areas that were being subjec t to incipien t rifting. The mafic plugs could intersec t the sedimenta r y cover of the plate, includ in g marine and contine n t a l deposits . A modern day analogue of the same proc es s takes place in the envir ons of Filiya, Nigeria. 9.3.2 Rock Associations in Anorogenic Environments A frequent field observation is the per sist en t cluster i n g of small bodies of red- al t e r e d granito i d s , gabbro id s , massive magnetite-hematite and quar tz pods that are linked to ages around 550 and 750 Ma. The four -rock associa t i o n seems to be a char ac t e ristic of continental extension ano rogen i c environme n ts . It is spatia ll y related to iron oxide-c opper-gold mineraliz ation. A recurren t feature observe d in most outcrops of the study area is the pr esence of two or more contrast i ng types of pluto n i c rocks . In some ca ses gabbro i ds and granit o i ds ; in othe rs, syenitoids and granitoids; even three or four types of granites and alkali granites. Many of the small areas also contain mafic, ultrama f i c and alkalin e plugs and dikes of varying composi t i on , such as lamprop h y r es , carbon a t i t e and nephel in e syenit e . alkali gr anite gr anite quar tz monz onite gr anodior ite s y enite alkali gabbr o monz onite monz ogabbr o f oid gabbr o f oid s y enite monz odior ite dior ite gabbr o quar tz olite f oid monz os y enite gabbr o- dior ite f oidolite f oid monz o- dior ite per idot gabbr o 3 9 9 T h e multi p l ic it y of rock types in a small area seems to be another char ac teristic of continental extens ion anorog en i c enviro n me n t s . 9.3.3 Quartz Pods Quartz pods have been identified throughout most of t he Greater Lufilian Arc region. They differ from veins, boudina g ed veins and pegmati t i c quartz units, particu l a r l y in geometry: outcrop s of undeformed bodies are typically round to elliptical, and vary from a few to several- hundred meters in diameter . Dimensio ns of some quartz pods exceed four kilometers in diameter and ther e is geophysical eviden ce of even larger ones. They seem to be a special type of silicific ation. Hyper-alk ali ne, hydrothermal solutions seem to be involved in the transpor t a t i o n of silica and emplac e me n t of the quartz pods . Quartz pods are emerging as a type of alterat i on that is associated to IOCG systems in the Greater Luf ilian Arc. Improved identification in the field and an increase d understa n d in g of their physico -chemic al features may aid in the explor ation of mineral deposits. 9.3.4 Iron Oxide Bodies Masive bodies of magnetite and/or hematite at macros c o p ic , mesosc o p ic and micros c op i c scales emplac e d themselves by gradual replacement of the host rock. The proces s seems to involv e silica te dissolu t i o n by hyper-alk aline hydrothermally-driven solutions. 9.3.5 Round-Pebble Hydrothermal Breccias Round-pebble hydrot hermal breccias occur often in and around IOCG systems th roughout the Greater Lufilian Arc. They seem to have been produced by hyper-alk aline solutions that corroded previous l y angular hydroth er m a l breccia s . In some cases, they act as good hosts for sulfide mineraliz a t i o n . 9.4 Ring Complex Clusters Clus ters of anorogen ic granitoi d ring complexes have been produced all along from Archean times to the pres ent. Clusteri n g of multip le anorogen ic ring complex intrusio ns can form batho lit h i c size bodies. At least ten clusters of ring complexes were identified in the Greater Lufilian Arc. Ri ng complex cl usters have the followin g char ac t e r is t i c s : 1) Mult iple ring complexe s of varying chemical composit i on and size that might interse c t each other. 2) Volcanic and plutoni c rocks of roughly the same compos ition occur togethe r. 3) Successive magmatic events of vary ing compos ition allowed for abundant oppo rtunities of magma mixing and recycli n g of crustal materials . 4) The plan view geomet ry of un-tectonized ring complex clusters is roughly that of an isos cele s triangle . 5) Less volumino us prec urso r and waning events of magmatis m may occur. 6) The princip a l chemica l compos i t i o n of the magmas is midalkaline, but may ocassionally vary to alkaline and subalkaline. In extreme cases, it may be peralk alin e and can even produc e carbon a t i t i c rocks. 7) Isolate d bodies of mafic and ultramafic rocks often come in the la tter stages of the process . 8) Total duratio n of ring comple x clus ter cycles aver ages 110 Ma. Several cycles of ring complex clus ter s have repeated l y oc curre d in roughly the same location in at least three differen t localiti e s . Thes e repeated cycles were sepa rated 1095 Ma in NW Zambia; 933 Ma at the Khorixas area, Namibia; and 50 Ma in West Lusak a, Zambia . 9.5 Tectonic Environment of Emplacement The tectonic environment of emplacement for part of t he rocks collected is not yet well constrain e d ; active resear ch is curren tly being carried out to address th is issue. Nevertheless, several clear patterns are emerging : 1) The largest portion of granitoi ds collec t e d are midalk a l in e rocks that formed in an anorog e n ic contine n t a l epeirog e n ic uplift environm e n t . 2) Next co me thos e formed in rift environments. 3) Another signif ic a n t group of rocks formed in a post orogen i c gr anitization environment. 4) Continen t-continent collision environments were not positively identified. 5) Sub duc t i o n a l magmat i s m seems to have been very restric te d both in terms of time and areal extens ion. Ther e is ev idence of minor such magmatis m in Paleop roterozoic rocks of Kalene Hill and in portions of the Kamanjab Ba tholith. In any given area, two or more of these settings may be superimp os e d . Anor ogen i c continen t a l ex tension is the main geologi cal process of the Arc. Comple te Wils on cycles were not identifi e d in the doma ins of the Greater Lufilian Arc that were studied . The dominan t magmatic proc ess, as eviden ced by the volume of extrude d rock, is anoroge n i c continen t a l epeirogenic uplift, closely-fo llowed in time by a rift-re lated granitoid emplacement. Coalescing and overprinting aulac ogens seem to be the main type of geolog ical event in the arc. 4 0 0 The environment of emplacement of Pa leoproterozoic rocks that occur thro ughout the Arc cannot be identified using the established methods for granitoid envir onment of emplacemen t. Intense sodic alteration and hematit i z a t i on were observe d in part of these rocks. Another alteration proc ess is a net enric hment in potassium that is evident by the abundant biotite and alkali feldspar over growth. Part of th e rocks showed diffus e crys tal margin s and abunda n t blue quartz phenoc r y s tals. Incipient migmatitization of these rocks may have modified their chemistry to a point wher e they don?t fit tr aditional proc edures to evaluate granitoid environment of emplac ement. The alteration processes just mention e d seem to have taken place before ~880 Ma, becau se the environment of emplacem ent of younger rocks can be identified. 9.6 High Thorium High values of thorium were found in part of the granito ids of NW Zambia, Kafue Flats, Hook Granite Batholith (Zambia ) , Oas farm and Otjiwar o n go environ s (Namib i a ) . They are high-heat pr oducing rocks. The anomalous thorium content in some granitoids of the Greater Lufilian Arc indu ced and maintained long-lived, large convec tive cells of hydrothe rmal fluid flow . High-th or i u m granito id s in all five domains have a parti cul ar trac e element chemica l signatu r e that is not common, and probabl y were subject ed to analogo us geolog i c a l process es at differe n t points in time. 9.7 Correlation of Granitoids Granitoid rock suites with clos ely matching chemis tr y and macros copic features have been found to form in the same region, two or three times with up to a thous and million years of age diffe renc e . Source rocks and environm e n t of emplac e me n t for the anoroge n ic intr usi v e events were the same: for that reason, magmatic products turned out equivalent. These features preclu de lithological or detailed geochemic al correlation. Rocks from the suites of Muliash i Porphyr y and Mufulir a , Zambia are an example of this. They both have pink and gray granitoids with similar compositions, but the ages of the rocks are completely different. Several lithological correlations have been developed for granitoid s in variou s domains of the Greater Lufilian Arc. The rocks cannot be properly correlated until mo re geochronological information is available. 9.8 Main Findings in Specific Domains 9.8.1 Hook Granite Batholith, Zambia Information currently available on geophysics, geochr onology, rock distribution an d geoche mistry from the Hook Granite Batholith fit quite well with an intrac on tinental, anorogenic, ring complex cluster origin. The batholith is mainly composed by midalkaline granitoid s. Alkali granites , quartzmo n z o n i t es and granites make up 70% of all rocks. 9.8.2 Nchanga Granite, Zambia The Nchanga Granite has all the char acteristics of an anorogenic granite ri ng complex. Chemistry of its rocks crosses the midalk a l i n e to subalk a l i ne fields . Parts of t he pluton are made of high heat produci n g granit e s that maintain ed a long-lived circulat i on of hydrother m a l fl uids. The Nchanga Granite might have contribu t e d to the origin of copper in its environs. 9.8.3 Kamanjab Batholith, Namibia Sixteen suites with more than two contrast i ng rock types were identified in the Kamanjab Batholith. No two suites are identica l , and they are made by a large variet y of rock types. This multip licity of rock types at a given site is one of the charact e r is t i c s of anorogen i c environme n t s in the Greater Lufilian Arc. There is no direct proof of the pres enc e of ring comp lexes at the Kamanjab Batholith. Nevertheless, several sources of evidence point to the batholith as a cluster of ring comple xe s . Among other s, thes e are: 1) the lack of continui t y in the rock types along traverses; 2) the pres ence of mult iple rocks types in at least fifteen discret e sites; 3) General anoroge n ic charac t e r of most of the rocks; 4) three quarters of the rocks in the suite are midalka l in e ; 4) the size and shape of the batholith, as well as its event diagra m has simila r i t i e s with other ring complex clus ters . 4 0 1 9.8.5 New Temporal Constrain to Katangan Sedimentation G r a n i t ic dikes emplac e d at the Nchang a mine area in anorogen i c extens i on a l environ m e n ts were dated at ~765 Ma. They provide the youngest age of deposition for that portion of the Katanga sediment a r y sequen ce at Nchanga (Roan sedimen t s ) , and might provi de a significant brac ket age for mineralization. 9.8.6 Khorixas Inlier-Kamanjab Batholith Geolog ical history for the Khorixas Inlier and the Kamanj ab Batholith are significantly different. They probably were not in the same geograph i c positio n all the time. Older basemen t is known in the Khor ixa s Inlier than at the Kamajab. The two regions seem to have had a common geolog ic a l history for the past 550 Ma. 9.8.7 Long-Lived Fractures E-W-tre nd i n g region a l fractu r e systems that run paralle l to the elongation of the Greater Lufilian Arc play an important role in the emplac emen t of magmatism and IOCG mineraliz a t i o n . They acted as routes for intr us ion , channe ls for fluids and contro l for ore deposi t i o n . Those structures are generally paralle l to the main Lufilian Arc trend , and could have been norma l syn-rift faults that have been reac ti v a t e d through o u t geologic a l history . Some N-S-tre n d i ng structu r es are also mineral iz ed and t hey are sub- per p en dic u l ar to the main trend of the Lufilian Arc. 9.9 Metallogeny Various types of mineral iz ati o n were seen to be asso ciated with intrusive rocks along the Greater Lufilian Arc (Table 9.4) . These include rare earth minerali z a t i o n as socia t e d to alkali ne dikes and carbona t i t e s in the Khorixas Inlier, sedimentary-ho sted gold (so-called ?Car lin?-style deposits), several low-sulfidation hydrot h er m a l gold occurr e n c e s , low su lfida t i on hydroth er m a l copper deposti s , epigen eti c copper vein deposits, alkaline porphyry molybdenum (-copper?) styl e mineral i z a t i o n , sedimen t a r y - h os t e d copper- c ob a l t deposits , and a wide variety of iron oxide-cop pe r - g o l d and relate d deposi t s and prospe c ts . Severa l Paleoproterozoic rocks throughout the Greater Lufili an Arc are enriched in copper. Some Mesoproterozoic syenites and alkali granites are enriched in zinc . The si gnific a nce of the latter observa t i on remains unclear . Paleopr o t e r oz o ic copper - r ic h rocks could be the source of metal for later events. Incipient migmatitization of those rocks could have remobilized t he copper. Copper is probably bei ng recycled. Very little skarn mineralization was observed in Ka tanga n carbona te s , even though they ar e intruded by multiple pluton ic episo d es . Possib l e excep t i o n s occur around the Hook batholit h . The Samba deposi t is not conside r ed to be a copper porphyr y ; it is a low sulfida t i o n epither m a l copper mineral iz a t i o n host ed in pyroclas tic rocks that were sheared during regiona l metamor ph i s m . 9.9.1 Metallogenic Epochs At least eight discret e periods of mineral iz a t i o n can be interpr e t e d from Table 9.4 (The same are simplif i e d on Table 9.5) . Wher e possib l e , radiome tr i c ages have bee n used to place the various events. Most have been assigned to specific ages by correl ation or association. Six deposits could not be placed chrono lo g ic a l l y and are included at the bottom of the list. There is a wi de-sp r e a d series of mid- alk a l i n e intrusi on s emplac ed around 750 Ma that produces a variety of mineral deposi t s . Another such event (separ a te d in at leas t three different phases: 500- 513, 550 and 583 Ma) took place around 540?40 Ma. Five less well defined events took place as indicated on Table 9.5. From old to young, they occurred at ~1970, ~1930, ~1866 , 1097-105 9 and ~460 Ma (See Tables 9.4 and 9.5). The dominant depos it type is iron oxide-cop per-gold mineralization. The age of sedimentary-ho sted copper mineralization in the Copperbe lt is currently being re-evaluated using Re-Os dating at the University of Arizona. Three tentative ages for them are 796-756, ~583 and ~550 Ma. The main events of sedimen t a r y - h os t e d gold mineral i z a t i o n in Namibia are ~750 Ma in the environ s of Sesfontein, ~550 Ma in Eastern Na mibia. The age of the Zambian de posits and prospects could not be estimated. At least two distinct events of diss emi na t e d copper mineral iz a t i on associa t ed to midakaline granitoid intrusives were identified in the Kamanjab Batholith. The first took place around 1975 Ma and the second around 1928 Ma. 4 0 2 4 0 3 Table 9.5 Simplified Classification of Metallogenic Events in the Greater Lufilian Arc By Alberto Lobo-Gu errero, M.Sc., Min.Ex., December, 2004 Economic Geology Research Institute, Univer sity of the Witwatersrand, Johannesburg Commodities Location Deposit Type Age * Environment A u Sasare , Zm IOCG 460 ACR Cu,Co,Ni, Au,U,Fe Kansanshi, Zm + some southe r n Congo l es e Fe + Cu- Co deposi t s IOCG + Kansanshi veins 500-513 Eo Extension Mo Marink as Kwela Mo porphyry 520-560 E ACR Cu,Au,Fe, REE,Ag,Zn,Pb Hook Granite batholith satellite bodies , Zm IOCG ~533 E1 ACR Cu,Au Otjiwarongo, Otavi Mts., Nm; Kafue Flats, Zm IOCG + Sedimentary- h o s t ed Au + Navachab , Nm ~550 E2 ACR Cu,Co (U) Copper b e l t and Congol ese Cu- Co minera l iz at i o n hosted in sediments; remobilization and mineralization Sed- ho s ted Cu (epigene t ic overprin t ) ~ 5 83 E3 Event related to Verang i a n Glacia t i o n ? Cu,Co,Ni,Au Kabompo Dome, Zm IOCG, sed-ho sted Co- Ni -C u ~730 I CEUG Cu,Au,REE, Ag,Mn Kalengwa-Kas empa area,Zm Oas, Lofda l, Mesopotamie, Nm IOC G ~745- 75 6 I ACR Cu,Co Initial copper mineralization in the Zambian Copperbe l t (and Katang a ?) Sed-ho s t ed Cu 756-79 6 I-J ACR Cu,Au Witvlei, Nm; Mkus hi,Zm; Omitiomire,Zm IOCG + Intrus ive related mineralization 1 0 5 9- 1 0 9 7 L ACR Au,As ,Bi,Sb Karibar e mb i and Kililamirombwe, Zm Sed- ho s ted Au L or younger L ACR Cu,Au? Kamanjab Batholith, Nm IOCG, hydrotherma l Cu dissemi n ati o n 1866 U enviro nm e n t cannot be identif i e d - probab l y CEUG Cu,Au? Kabompo Dome, Mwinilunga, Lumwana, Zm Schis t- h os te d Cu 1928 U ? Cu, Au,Fe,F,REE Kamanjab Batholith, Nm; Mwinilun g a , Zm (?) IOCG 1930 U ACR Cu,Mo Samba, Zm Schist- h os t e d Cu 1965 V ? Cu,Au,Ag? Kamanjab Batholith, Nm Hydrot he r ma l Cu dissemination 1975 V CEUG NOTE: ACR = Anorogenic continental rift. CEUG = continental epeirogenic uplift granitization. * Letters in the fifth column refer to labels for magmatic events in geochronolog ic al correlation diagrams (Figs A79 to A83). White and gray colorati o n serves to separate major metalloge n i c times. 4 0 4 9.9.2 Iron Oxide-Copper-Gold Mineralization The iron oxide copper- g o ld (IOCG) styl e of minera l iz a t i o n is far broader in terms of both spatial distribut i o n and age of emplacemen t than previous ly thought. IOCG deposit s have been identif i e d in both Namibia and Zambia. In Namibia, for example, the IOCG deposit Tevrede is curren tly being explor ed by junior mining corpor ations in the northwes tern portion of the Kamanjab batholith; in addition, the Kombat copper mine in the Otavi Mountains and Otjikoto, a gold deposit in the environs of Otjiwarongo, s eem to be IOCG depos i t s . Several IOCG-li k e mineral i z e d areas were identif i e d at the Oas, Lofdal, Mesopo t a m i e and Gelbinge n farms as outliers to the Kamanjab Batholith. Zambia also has se veral known IOCG depos it s like the Kalengw a copper- silver mine, the Kitumba and Kantonga copper depo sit s and others around the Kasempa area. The Nampundwe pyrite mine as well as Dunr obin gold mine also have IOCG char ac teristics. Quartz ites are good hosts for mineralization. This wa s observ e d in severa l Namibi a n areas, includ i n g the southe r n part of the Oas farm, the Gelbing e n farm and the western portion of the Kamdes cha farm, bordering the Kamanjab Batholith. Quartz ites fracture in a bri ttle manner that is ideal for hydrothe rmal brecciation. Equivalent rocks might host mineraliz ation in Zambia . The main IOCG events that have been identified in t he Greater Lufilia n Arc took place during eight time periods . Thes e are listed on Table 9.6. The possible IOCG events that took plac e in the basement to the Zambian Copperbelt (at Chambishi, Mufulira, the main Copper be l t , Konkol a and Nchanga ) are not very well define d or constr a in e d geoc hr o n o lo g ic a l ly . Table 9.6 Periods of iron oxide-copper-g old mineralization in the Greater Lufilian Arc. Period Main representative mineralization ~ 4 60 Ma Sas are, Zambia ~533 Ma Hook Granite Ba tholith satellites, Zambia ~550 Ma Otjiwarongo, Namibia; Kafue Flats, Zambia ~746 Ma Kalengwa-Kas empa , Zambia; Khorixas, Namibia ~825 Ma Copperb e l t , Zambia (possib l e , see section 6.4) ~1078 Ma Witvlei, Omitiomire, Namibia ~1937 Ma Kamanjab Batholith, Namibia The rocks of many IOCG deposit s and prospec t s in the Greater Lufilia n Arc are pristin e . There is no signifi c an t deforma ton involved. Hydr othermal bre ccia t i o n and other mineraliz a t i o n f eatures are un-defor m ed . This may be very useful to study mineralization and alteration processes. 9 . 9 . 3 Association of Sedimentary Hosted C opper Mineralization with IOCG Mineralization A significant finding is the juxtaposit ion of iron-oxide-copper-gold minera lization undernea th the sedimentary- h o s t ed copper deposit at Witvlei , Namibia . This metall ogenic event occurred at 1110 Ma. Secondary copper in the sedimentary-ho sted deposit might have come from the IOCG deposit that lies undernea t h . This idea may generat e a new conc ep t for the origin of the Copper b e l t - K a t an g a copper and cobalt deposits . The concep t also opens an entir e new age gap for the explor a t i on of base metal mineralization in the Greater Lufilian Arc and the surrounding environment, includ in g South Africa. There is additiona l evidence of IOCG mineraliz a tio n related to sediment - h os t ed copper in other parts of Namibia and Zambia, includ in g the Chambish i area and parts of the basement to the Copperbelt. At least three discrete time periods show IOCG miner alization in close temporal spatial associa t i on with sedimen t ar y - h o s t ed copper deposits . The first took pl ace around Witvlei from 1108 to 1059 Ma. The second and third oc urred in the basement to the Zambian C opperbe lt from 882 to 725 Ma and from 607 to 500 Ma. i APPENDICES VOLUME Abbreviated Table of Contents A Sample Maps, 127 B TAS Diag ra m for Suite s of the Kaman j a b Batho l i t h , Namib i a , 165 C Geochem i s t r y Data ba s e , 1 D Geogr a p h i c Coord i na t e s of Sampl e s Colle c te d and Geolo g i c a l Stati on s , 25 E Geochr o n o l o g y Datab a s e , 41 F Geochr o n o l o g i c a l Event Diagr a m s , 67 G Tecton i c Envir o n e n t of Empla c e m e n t for Sa mpl e s , 95 H Parti a l Trans c r i p t i o n of Field Notes , 183 I Other Infor m a t i o n , 222 J Raw Data for New Ge ochr o n o l o g y , 237 K Geochr o n o l o g i c a l Corre l a t i o n Diagr a m s , 257 ii APPENDICES VOLUME Complete Table of Contents APPENDIX A SAMPLE MAPS , 127 M1 Key for Zambian Sample Maps, 128 M2 Sample map, Hook Granite Batholith, Zambia over 1:1'000,000 geological map, 129 M3 Sample map, Hook Granite Batholith, Zambia over 1:100,000 geologic a l sheets, 130 M4 Enlarged sample map, Hook Granite Batho lith, Zambia over 1:100,000 geological sheets, (See Fig 4.15) M5 Enlargement of sample, Hook Granite Batholith, northern portion, 131 M6 Enlargement of sample, Hook Granite Batholith, southern portion, 132 M7 Sample map of the Kafue Flats area, Zambia, 133 M8 Sample map, Kalengwa mine environ s, Zambia, 134 M9 Sample map, Kasempa environs, Zambia , 135 M10 Sample map, Kalene Hill and Kabompo Dome, NW Zambia, 136 M11 Sample map of Kalene Hill and environ s, NW Zambia , 137 M12 Sample map, Domes Area, Zambia, 138 M13 Sample map, Kabompo and Mwombezhi Domes, Zambia, 139 M14 Sample map SE of Mwinilunga, 140 M15 Sample map, Solwesi Dome environs, Zambia, 141 M16 Sample map of the Nchanga Granite, Zambia, 142 M17 Sample map of the Chambishi-Mufulira Area, Zambia, 143 M18 Sample map of the Serenje area, Zambia, 144 M19 Key for Namibian Sample Maps, 145 M20 Sample map of the Khorixas inlier and the Mesopotamie farm, Namibia, 146 M21 Sample map of the Oas and Lofdal fa rms, Khorixas Inlier, Namibia, 147 M22 Sample map of the Summas Mountains and Ugab River, Namibia, 148 M23 Sample map, Otjiwaron g o environs , Namibia, 149 M24 Clos e-up of sample map, Otjiw aro n go environs , Namibia, 150 M25 Sample map, Otavi Mountains, Namibia, 151 M26 Sample map, Witvlei environs, Namibia, 152 M27 Key for Kamanjab Batholith sample maps , Namibia, 153 M28 K-14 portion of sample map, Kamanjab Batholith, Namibia, 154 M29 K-15 portion of sample map, Kamanjab Batholith, Namibia, 155 M30 K-16 portion of sample map, Kamanjab Batholith, Namibia, 156 M31 K-17 portion of sample map, Kamanjab Batholith, Namibia, 157 M32 K-18 portion of sample map, Kamanjab Batholith, Namibia, 158 M33 K-19 portion of sample map, Kamanjab Batholith, Namibia, 159 M34 K-20 portion of sample map, Kamanjab Batholith, Namibia, 160 M35 K-21 portion of sample map, Kamanjab Batholith, Namibia, 161 M36 K-22 portion of sample map, Kamanjab Batholith, Namibia, 162 M37 K-23 portion of sample map, Kamanjab Batholith, Namibia, 163 M38 K-24 portion of sample map, Kamanjab Batholith, Namibia, 164 M39 K-25 portion of sample map, Kamanjab Batholith, Namibia, 165 APPENDIX B TAS DIAGRAM FOR SUITES OF THE KAMANJAB BATHOLITH, NAMIBIA, 165 F 1 Suite A, 166 F2 Suite B, 167 F3 Suite C, 168 F4 Suite D, 169 F5 Suite E, 170 F6 Suite F, 171 F7 Suite G, 172 iii F 8 Suite H, 173 F9 Suite I, 174 F10 Suite J, 175 F11 Suite K, 176 F12 Suite L, 177 F13 Suite M, 178 F14 Suite N, 179 F15 Suite P, 180 F16 Suite Q, 181 APPENDIX C GEOCHEMISTRY DATABASE , 1 A1 Chemic al analysis of sample s from t he Greater Lufilian Arc sorted by region, 2 A2 West Lusaka-Kafue Flats, Zambia, 2 A3 Hook Granite Batholith, Zambia, 3 A4 Serenje, Zambia, 4 A5 Kalengwa-Kas empa Area, Zambia, 5 A6 Northw es tern Zambia Region Zambia , 6 A7 Kalene Hill, Archean rocks, Paleopr o t e r oz o ic Group 2, Paleopr o t e r oz o ic Group 3, Paleoproterozoic Group 4, Other sample s, 6 A7.1 Kabompo Dome, 6 A7.2 Solwesi Dome, 7 A7.3 Mwombez h i Dome, 7 A7.4 Sodalite Syenite Quarry, 7 A7.5 Shilenda, 7 A8 Basement to the Copperbelt, Zambia, 7 A8.1 Muliashi Porphyry, 7 A8.2 Chambish i mine area, 8 A8.3 Samba copper prospect, 8 A8.4 Nchanga Granite, 8 A8.5 Nchanga mine, 8 A8.6 Mufulira Granite, 8 A8.7 Other, 8 A9 Kamanjab Batholith, 9 A10 Felsic volcan ics, Namibia; Ugab River, Namibia; Okwa River, Botswana; Summas Mountains , Namibia, 11 A11 Oas farm, Namibia, 12 A12 Lofdal farm, Namibia; Mesopotamie farm, Namibia; other alkaline and gabbroic rocks, Khorixas , Namibia, 13 A13 Otjiwarongo environs, Namibia; Grootfontein In lier, Otavi Mountains, Namibia; Okatjepuiko, Witvlei, Namibia, 14 A14 Spitskop p e complexes , Namibia; Erongo comple x, Namibia; Brandberg complex, Namibia; Nigeri a n ring comple x e s , 15 A15 Chemical analysis from the Greater Lufilian Arc sorted by number, 16 APPENDIX D GEOGRAPHIC COO RDINATES OF SAMPLES COLLECTED, 25 A16 Zambian sample s located on UTM zone 35, 26 A17 Zambian samples located using latitude and longitude (WGS84), 31 Zambian samples that are located in UTM zone 36, 31 A18 Namibian samples that are located in UTM zone 33 (Schwartzeck), 32 A19 Namibian samples that are located in UTM zone 34, (Schwartzeck), 36 A20 Namibian samples that are located using latit ud e and longit u de coordin a t es (Schwa r tz ec k ) , 37 iv APPENDIX E GEOCHRONOLOGY , 41 A21 Compila t i o n of radiom e t r ic ages, Great er Lufilia n Arc ? sorted by chronol og i c a l order, 42 A22 Compila t i o n of radiom e t r ic ages, Greater Lufili a n Arc ? sorted by region and sites , 50 ZAMBIA , 50 A22.1 Hook Granite Batholith, Zambia, 50 A22.2 Northwes tern Zambia, Domes Area, 50 A22.3 Solwesi Dome Area, Zambia, 50 A22.4 Western Lusaka-Kafue Flats Area, Zambia, 50 A22.5 Kalengwa-Kas empa Area, Zambia, 51 A22.6 Mkus hi-Seren je Area, Zambia, 51 A22.7 Copperbelt region, Zambia , 51 A22.8 Mufulira Area, Zambia, 52 A22.9 Nchanga Area, Zambia, 52 A22.10 All Basement to the Copperbelt, Zambia (Compilation of Groups), 52 A22.11 Choma-Kalomo Batholith, Zambia, 52 A22.12 Irumide Belt, Zambia, 53 A22.13 Luangwa Valley, Zambia, 53 A22.14 Other Zambia, 54 NAMIBIA, 54 A22.15 True Kamanjab Batholith, Namibia, 54 A22.16 Khorixas Inlier, Namibia, 54 A22.17 All Kamanjab Area, Namibia, 55 A22.18 Witvlei Area and possible correlatives in the region, 55 A22.19 Central Namibia, 57 A22.20 Northe rnmost Namibia, 57 A22.21 Southernmost Namibia, 57 A22.22 Kaokoveld, Namibia, 57 A22.23 Rehoboth Inlier, Namibia, 58 A22.24 Namibr an d - Sa s r ie m Area, Namibia , 58 A22.25 Namaqua Metamor ph i c Complex , Namibia , 58 A22.26 ?Kibara n? rocks of Namibia, 59 A22.27 Other Namibia , 59 OTHER, 59 A22.28 Other countrie s relevant to Lufilian Arc projec t, 59 A22.29 All Zambia (compilation of all Zambian ages), 60 A22.30 All Namibia (compilation of all ages from the country), 64 APPENDIX F EVENT DIAGRAMS , 67 ZAMBIA , 68 A23 Hook Granite Batholith, Zambia, 68 A24 NW Zambia, 69 A25 West Lusaka-Kafue Flats Area, Zambia, 70 A26 Environs of the Nchanga Mine, Zambia, 71 A27 Basement to the main Copperbe lt, Zambia, 72 A28 Environs of the Mufulira Area, Zambia, 73 A29 All basement to the Copperbelt, Zambia, 74 A30 Luangwa Valley, Zambia, 75 A31 Mkus hi-Seren je Area, Zambia, 76 A32 Choma-Kalomo Batholith, Zambia, 77 A33 Irumide Belt, Zambia, 78 A34 Other Zambian reporte d ages, 79 A35 All Zambian radiome tr i c ages, 80 v APPENDIX F (cont.) NAMIBIA, 81 A36 Kaokoland Area, Namibia, 81 A37 Entire Kamanjab region, Namibia, 82 A38 Khorixas Inlier, Namibia, 83 A39 True Kamanjab Batholith, Namibia, 84 A40 Comparative event diagram for Khorixas In lier and Kamanjab Batholith, Namibia, 85 A41 Central Namibian Area, 86 A42 Namaqua Metamor ph i c Complex , Namibia , 87 A43 Witvlei Area and correlatives in the Greater Lufilian Arc, 88 A44 So-called ?Kibaran -Age ? rocks, Namibia, 89 A45 Southernmost portion of Namibia, 90 A46 Namibr an d - Sa s r ie m Area, Namibia , 91 A47 Rehoboth Inlier, Namibia, 92 A48 All Namibi a n radiome t r ic ages, 93 A49 Radiom e t r ic ages of other countr i es that are related to the Greater Lufilian Arc, 94 APPENDIX G TECTONIC ENVIRONMENT OF EMPLACEMENT , 95 A50 Tectonic envir onme n t of emplacem en t for sa mples from the Greater Lufilian Arc, 96 A51 Results of determination for environment of emplace me n t of granito id s based on methodology of Maniar & Piccoli, 1989, 102 A52 Result s of determ i na t i o n for anorog e n ic charac t er of granito i ds based on the Whalen et al, 1987 plots, 108 A53 Results of determination for environment of emplace me n t of granito id s based on methodology of Pearce et al, 1984, 113 A54 Discrim i n a t i on of granito i ds followin g procedure of Harris et al, 1986, 118 A55 Results of determination for environment of emplace me n t of granito id s based on methodology of Batchelor & Bowden, 1985, 122 A56 Tectonic envir on me n t of mafic roc ks, Greater Lufilian Arc projec t, 123 APPENDIX H PARTIAL TRANSCRIPTION OF FIELD NOTES , 183 ZAMBIA , 184 A57 Field notes taken along E-W transec t of the Hook Granite Batholith, 184 A58 Abbrevia t ed descrip t i o n of samples collecte d in the Hook Granite Batholith by Pepper, 2001, 186 A59 Comment s from publis h ed Zambian geologi c a l su rvey reports and maps on iron oxide bodies , quartz pods, associa t e d granito id s and round- p e bb l e hydr oth e r m a l brec cia s , 188 A60 Sample description and field relationships in the West Lusaka-Kafue Flats Area, Zambia, 189 A60.1 Quartz pods, 189 A60.2 Granito id s , 189 A60.3 Gabbroi ds , 190 A60.4 Iron oxide bodies, 191 A60.5 Contac t metamorphic rocks, 191 A61 Descriptions of samples from the Kale ng wa Area, Zambia by Pepper, 2001, 192 A62 Descriptions of samples collected in the field, Kalene Hill Area, NW Zambia , 193 A63 Field descriptions of sample s L-032 to L-034, Kabompo dome, NW Zambia, 194 A64 Petrography of the Chitungulu sodalite sy enites, Mwombezhi Dome, NW Zambia, 195 vi APPENDIX H (cont.) NAMIBIA, 196 A65 Field notes for a few suites of Cu-mineralized rocks in the Kamanjab Batholith, Namibia, 196 A65.1 Suite G, 196 A65.2 Suite H, 196 A65.3 Suite M, 197 A65.4 Suite N, 198 A66 Field notes on the N-S transect through the Oas Farm, Namibia, 199 A67 Field notes from the Lofdal farm, Namibia, 207 A67.1 Cross section through series of ultramaf ic dikes, Lofda l farm, Namibia, 210 A67.2 Magnetite- cemented, polymictic hydr otherma l breccia that makes a diatre me , 211 A68 Partial field notes collected at the Mesopo tamie farm, Namibia, 213 A69 Field notes , Ugab River, Namibia, 214 A70 Field notes , Okwa River, Botswana, 217 A71 Field notes Grootfontein Inlier, Namibia, 218 A72 Field notes from Okatjepuiko, Witvlei, Namibia, 219 APPENDIX I OTHER INFORMATION , 223 A73 Persons interviewed for preparation of fiel dwork, during fieldwor k , and when proc es s in g information, 223 A74 Rock names of samples from the Greater Lufilian Arc Granitoi d project, 224 A75 Experiment to test quality of chemic al laborator y, 229 A76 Heat production capa city of intrusive rocks from the Greater Lufilian Arc at the time of their emplac eme n t, 231 APPENDIX J RAW DATA FOR NEW GEOCHRONOLOGY , 237 A77.1 Raw data obtained for SHRIMP II U-Pb dating at the Australian National University, Canberra, 238 L-030, 238 L-075, 238 L-158, 238 L-160, 239 L-207, 239 L-213, 240 L-638, 240 L-688, 241 A77.2 Raw data and proc es s in g for zircon dating using U-Pb laser- a b l a t io n ICP-MS techniq u e , 242 L-855, 242 L-868, 242 L-943, 242 L-969, 242 L-993, 243 L-1013, 243 L-1043, 243 A78 CONCORDIA DIAGRAMS, 244 A78.1 Sample L-030, 244 A78.2 Sample L-047, 244 A78.3 Sample L-075, 245 A78.4 Sample L-158, 245 A78.5 Sample L-160, 246 A78.6 Sample L-207, 246 A78.7 Sample L-213 Conc or d i a diagra m for high U zircons + rims , 247 A78.8 Sample L-213 Conc or di a diagram for cores and rims, 247 A78.9 Sample L-638 Conc or d i a diagram for all zircons includ i n g xenocrys t s , 248 vii APPENDIX J (cont.) A78.10 Sample L-638 Conc or dia diagram for main clus ter of zircons, 248 A78.11 Sample L-688 Conc or di a diagram for all zircons, 249 A78.12 Sample L-688 Histog ram of all 12 ages in main clus ter, 249 A78.13 Sample L-693, 250 A78.14 Sample L-868, 250 A78.15 Sample L-855 Conc or di a diagram for all zircons, 251 A78.16 Sample L-855 Conc or dia diagram for main clus ter of ages, 251 A78.17 Sample L-943 Conc or di a diagram for all zircons, 252 A78.18 Sample L-943 Conc or dia diagram for main clus ter of zircons, 252 A78.19 Sample L-969, 253 A78.20 Sample L-993, 253 A78.21 Sample L-1013 first, 254 A78.22 Sample L-1013 second, 254 A78.23 Sample L-1043 concord ia diagram for older group of zircons , 255 A78.24 Sample L-1043 concordia diagram fo r younger group of zircons , 255 A78.25 Sample L-1043 concord ia diagram for all zircons 2, 256 A78.26 Sample L-1043 concord ia diagram for all zircons 1, 256 APPENDIX K GEOCHRONOLOGI CAL CORRELATION DIAGRAMS, 257 A79 Correlation of dated events, Zambian locations, 258 A80 Correlation of dated events, Namibian locations, 259 A81 Correlation of dated events, Greater Lufilian Arc, 260 A82 Correlation of dated events, Greater Lufili an Arc, first portion (3000 to 1400 Ma), 261 A83 Correlation of dated events, Greater Lufili an Arc, second portion (1400 to 0 Ma), 262 APPENDIX C GEOCHEMISTRY A1 Chemic al analysis of sample s from t he Greater Lufilian Arc sorted by region, 2 A2 West Lusaka-Kafue Flats, Zambia, 2 A3 Hook Granite Batholith, Zambia, 3 A4 Serenje, Zambia, 4 A5 Kalengwa-Kas empa Area, Zambia, 5 A6 Northw es tern Zambia Region Zambia , 6 A7 Kalene Hill, Archean rocks, Paleopr o t e r oz o ic Group 2, Paleopr o t e r oz o ic Group 3, Paleoproterozoic Group 4, Other sample s, 6 A7.1 Kabompo Dome, 6 A7.2 Solwesi Dome, 7 A7.3 Mwombez h i Dome, 7 A7.4 Sodalite Syenite Quarry, 7 A7.5 Shilenda, 7 A8 Basement to the Copperbelt, Zambia, 7 A8.1 Muliashi Porphyry, 7 A8.2 Chambish i mine area, 8 A8.3 Samba copper prospect, 8 A8.4 Nchanga Granite, 8 A8.5 Nchanga mine, 8 A8.6 Mufulira Granite, 8 A8.7 Other, 8 A9 Kamanjab Batholith, 9 A10 Felsic volcan ics, Namibia; Ugab River, Namibia; Okwa River, Botswana; Summas Mountains , Namibia, 11 A11 Oas farm, Namibia, 12 A12 Lofdal farm, Namibia; Mesopotamie farm, Namibia; other alkaline and gabbroic rocks, Khorixas , Namibia, 13 A13 Otjiwarongo environs, Namibia; Grootfontein In lier, Otavi Mountains, Namibia; Okatjepuiko, Witvlei, Namibia, 14 A14 Spitskop p e complexes , Namibia; Erongo comple x, Namibia; Brandberg complex, Namibia; Nigeri a n ring comple x e s , 15 A15 Chemical analysis from the Greater Lufilian Arc sorted by number, 16 Table No. A1 A2 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGION PAGE 1/14 West Lusaka-Kafue Flats, Zambi a Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20.0 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-175 74.72 0.41 12.60 2.96 0.00 0.00 0.41 1.08 2.71 4.60 0.09 0.32 99.90 221 63 45 229 29.0 9 7 31 31 15 28 17 541 <6 25.0 <10 5.913 30.08 47.8 153 19 41.58 0.263 1.300 0.838 7.31 L-181 49.82 1.08 15.86 11.33 0.00 0.16 6.30 11.28 2.94 0.24 0.06 0.86 99.94 7 157 29 62 8.0 34 30 57 94 16 293 35 <22 <6 <15 35 <12 <12 3.18 L-195 61.25 0.38 15.84 8.67 0.00 0.09 0.04 2.35 5.66 5.03 0.09 0.51 99.91 89 130 ## 1054 80.0 <6 <6 10 71 40 13 <12 2151 8.0 <15 <10 15.84 44.14 74.3 118 25 145.1 3.888 1.463 7.500 2.200 10.69 L-199 10 787 42 534 46.6 399 8.8 38.7 5.6 20.0 137 35.6 288 95 0.67 10.8 2.65 5.38 12.6 1.58 9.10 1.61 4.24 0.59 3.76 0.53 0.00 L-207 75.03 0.07 13.63 0.68 0.00 0.00 0.00 0.11 4.32 6.27 0.01 0.26 100.39 123 182 12 432 6.0 8 6 10 13 0 <12 13 557 0.0 0.0 0 4.58 0 2 19.10 0.225 0.63 0.438 10.59 L-208 74.23 0.05 13.85 0.87 0.00 0.03 0.00 0.12 4.36 6.13 0.05 0.24 99.93 137 178 12 431 33.0 <6 <6 14 10 25 <12 238 517 9.0 132.0 <10 35 20 10.49 L-209 46.78 1.81 16.06 9.69 0.00 0.05 7.51 11.46 2.34 1.91 0.57 0.60 98.79 53 1592 27 111 17.0 36 42 29 52 19 243 50 1437 <6 <15 27 113 61 4.25 L-210 66.74 0.43 17.99 3.52 0.00 0.00 0.29 0.69 9.58 0.09 0.14 0.39 99.87 4 275 30 474 36.0 6 7 143 13 22 28 <12 83 7.0 74.0 <10 372 223 9.67 L-212 67.27 0.40 15.94 2.89 0.00 0.00 0.15 0.81 4.44 7.04 0.03 0.71 99.69 149 117 51 336 49.0 8 <6 32 17 22 <12 <12 503 8.0 79.0 <10 250 130 11.48 L-213 66.68 0.36 17.40 3.03 0.00 0.00 0.08 0.23 6.87 4.87 0.03 0.60 100.17 73 193 27 596 39.0 8 6 18 22 25 22 <12 762 12.0 163.0 <10 4.43 42.11 69.13 137 20 16.48 39.14 0.663 0.738 0.813 11.74 L-214 66.63 0.39 17.62 1.54 0.00 0.03 0.00 0.24 7.68 3.92 0.06 0.63 98.74 65 167 24 662 77.0 <6 12 20 15 25 19 81 657 7.0 104.0 <10 181 89 11.60 L-215 70.53 0.23 16.82 0.65 0.00 0.00 0.00 0.15 10.32 0.19 0.03 0.36 99.30 7 72 15 443 23.0 6 7 6 9 27 <12 <12 71 <6 193.0 <10 18 <12 10.51 L-217 73.54 0.39 10.80 3.98 0.00 0.09 3.40 1.35 0.64 2.97 0.15 2.41 99.72 124 48 10 128 10.0 86 17 8 43 13 67 502 805 <6 <15 11 6.750 28.16 53.20 89 30 58.60 0.763 3.61 L-218 66.30 0.52 15.92 4.64 0.00 0.00 0.49 2.01 4.79 5.43 0.11 0.21 100.42 202 344 46 601 53.0 8 <6 6 30 22 15 16 793 8.0 99.0 <10 16.74 74.63 265 342 135 7.513 65 .38 1.450 2.063 1.063 10.22 L-222 64.17 0.57 13.11 13.72 0.00 0.00 0.80 0.08 0.15 4.74 0.12 2.46 99.94 304 122 69 275 30.0 <6 7 <6 22 29 79 18 499 7.0 20.0 11 220 121 4.89 L-223 66.79 0.57 14.12 10.16 0.00 0.00 0.79 0.08 0.17 5.20 0.10 2.49 100.48 312 122 77 270 28.0 <6 <6 <6 27 28 68 18 468 8.0 21.0 <10 2.188 0.575 20.21 250 2 166. 0 0.988 5.37 L-224 62.03 0.58 13.42 15.02 0.00 0.00 0.62 0.07 0.24 5.69 0.11 2.33 100.13 261 103 35 301 28.0 9 8 <6 21 24 76 16 1065 8.0 19.0 <10 120 65 5.93 L-416 52.44 0.65 15.34 8.63 0.00 0.15 7.28 12.42 2.55 0.73 0.07 0.20 100.46 6 126 17 41 5.0 34 72 94 84 17 195 217 43 6.0 <15 42 <12 <12 3.28 L-458 72.83 0.09 13.43 1.35 0.00 0.02 0.00 0.20 3.52 6.94 0.03 0.37 98.78 277 30 72 45 13.0 <6 <6 9 11 18 <12 13 129 8.0 <15 <10 38 42 10.46 L-459 61.30 0.79 13.54 9.09 0.00 0.13 3.38 5.88 3.02 1.16 0.10 0.63 99.02 87 204 22 81 8.0 26 40 111 ## 19 181 57 287 <6 <15 23 54 30 4.18 L-460 74.38 0.43 11.58 4.11 0.00 0.03 0.62 1.86 3.67 2.33 0.12 0.34 99.47 68 482 13 632 7.0 8 9 19 63 18 22 14 596 <6 20.0 <10 197 102 6.00 L-461 71.85 0.20 14.11 1.77 0.00 0.02 0.26 1.01 3.45 5.34 0.06 0.70 98.77 178 241 14 65 10.0 <6 <6 30 36 18 <12 13 1222 <6 15.0 <10 43 21 8.79 L-462 72.04 0.34 13.78 2.58 0.00 0.02 0.38 1.21 3.18 5.19 0.04 0.37 99.13 114 630 5 95 11.0 <6 <6 11 32 17 25 <12 3607 <6 16.0 <10 61 25 8.37 L-463 48.36 2.43 14.19 14.79 0.00 0.19 7.26 7.68 2.85 1.01 0.40 -0.53 98.63 25 255 38 193 15.0 39 11 16 ## 21 133 94 285 <6 <15 30 30 18 3.86 L-464 5.46 0.07 0.00 77.49 0.00 0.08 0.50 6.09 0.10 0.52 0.06 3.16 93.53 14 13 16 17 3.0 25 185 184 ## <9 34 <12 142 29.0 <15 37 <12 <12 0.62 L-465 14.01 0.58 2.56 64.74 0.00 0.03 0.70 0.17 0.06 0.43 0.12 12.85 96.25 25 76 9 129 17.0 13 85 143 ## 11 127 <12 694 24.0 <15 36 <12 <12 0.49 L-466 73.93 0.13 12.78 1.65 0.00 0.03 0.08 0.98 4.27 4.50 0.03 0.30 98.68 351 83 31 75 39.0 <6 <6 15 21 24 <12 14 225 <6 23.0 <10 57 27 8.77 L-467 70.78 0.25 13.75 2.33 0.00 0.02 0.18 0.87 4.53 5.45 0.08 0.50 98.74 145 1046 29 208 18.0 7 10 12 30 22 16 <12 2676 <6 67.0 <10 224 130 9.98 X-90 73.62 0.31 12.90 0.54 1.67 0.05 0.42 1.13 3.37 5.90 0.10 0.44 100.45 370 9.27 Table No. A3 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGIO N PAGE 2/14 Hook Granite, Zambia Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-012 64.19 0.66 17.47 3.45 0.00 0.03 1.12 2.55 4.34 6.14 0.18 0.30 100.43 131 516 33 189 29.2 7 9 7 42 20 46 36 1042 4.3 50.4 <10 3.8 15.4 112 31.5 293 163 1.08 4. 73 1.57 293 2.69 9.76 1.21 6.81 1.22 3.22 0.47 3.14 0.48 10.48 L-012A 64.38 0.61 17.86 3.18 0.00 0.03 1.13 2.40 4.10 6.24 0.15 0.32 100.40 143 536 36 360 32.0 9 10 9 28 21 33 36 940 <6 49.0 <10 312 216 10.34 L-079 67.09 0.80 14.65 4.99 0.00 0.07 1.21 2.40 3.35 4.98 0.19 0.83 100.56 165 216 40 332 24.0 14 12 41 45 0 68 40 1291 0.0 0.0 0 0 0 8.33 L-237 70.85 0.37 13.24 4.02 0.00 0.00 0.52 1.36 2.51 5.44 0.11 0.40 98.83 151 276 74 194 24.0 8 6 25 16 18 28 <12 815 <6 26.0 <10 273 148 7.95 L-238 70.02 0.51 13.56 3.71 0.00 0.00 0.67 1.50 2.89 6.16 0.15 0.74 99.92 156 260 58 240 27.0 7 <6 9 18 18 33 15 747 6.0 24.0 <10 130 67 9.05 L-239 70.02 0.51 13.56 3.71 0.00 0.00 0.67 1.50 2.89 6.16 0.15 0.74 99.92 156 260 58 240 27.0 7 <6 9 18 18 33 15 747 6.0 24.0 <10 130 67 9.05 L-241 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 156 229 55 174 24.1 0 0 0 0 0 0 594 0.0 0.0 0 2.4 9.21 45.22 10.98 0 0 1.91 5.17 1.86 0 0 1.64 9. 31 1.44 9.41 1.92 5.84 0.87 5.96 0.89 0.00 L-242 76.03 0.29 10.81 5.91 0.00 0.01 2.03 0.21 0.57 1.96 0.11 1.21 99.14 42 228 33 256 11.0 14 18 8 12 38 87 309 617 7.0 <15 29 148 112 2.53 L-248 64.40 0.91 15.35 6.34 0.00 0.00 2.74 3.49 2.97 2.10 0.26 0.53 99.08 126 300 54 205 42.0 15 15 13 28 25 109 39 271 6.0 <15 21 77 42 5.07 L-248-L 76.71 0.14 13.26 0.92 0.00 0.00 0.04 0.66 3.71 4.49 0.04 0.32 100.29 121 314 48 206 20.0 9 7 8 16 19 35 25 745 <6 27.0 <10 139 68 8.20 L-249 70.32 0.42 14.04 3.50 0.00 0.00 0.75 1.96 3.00 4.50 0.14 0.29 98.93 123 309 49 211 23.0 8 7 8 16 19 45 21 716 <6 20.0 <10 0.700 0.725 4.800 124 0 46.24 1.313 0.350 0.688 7.50 L-257 73.62 0.26 13.30 1.97 0.00 0.00 0.15 1.23 3.67 5.29 0.05 0.55 100.10 214 117 53 208 25.0 6 <6 <6 13 22 <12 14 321 16.0 74.0 <10 113.8 42.95 114.8 192 66 5.3 6 26.34 0.663 4.013 1.18 8.96 L-259 69.45 0.42 15.44 2.77 0.00 0.00 0.29 1.80 3.10 6.11 0.07 0.59 100.05 174 199 72 402 47.0 7 <6 <6 21 20 13 26 911 7.0 21.0 11 113 58 9.21 L-259- B 73.83 0.30 12.91 2.80 0.00 0.00 0.17 1.01 3.55 5.35 0.04 0.44 100.42 204 118 ## 292 39.0 <6 <6 12 28 20 <12 15 617 10.0 29.0 <10 277 209 8.90 L-263 67.90 0.54 13.93 2.49 0.00 0.00 0.71 3.88 3.29 5.55 0.27 0.54 99.13 83 640 51 244 26.0 7 <6 23 15 20 34 16 920 <6 19.0 10 118.9 46.66 91.5 118 32 29.10 1.813 2.863 1.063 8.84 L-341 63.54 0.75 13.15 4.88 0.00 0.03 1.09 5.99 6.86 0.95 0.32 1.14 98.70 19 703 76 329 29.0 11 9 31 21 21 45 20 72 <6 20.0 11 174 89 7.81 L-343 65.60 0.61 13.71 4.43 0.00 0.05 0.83 6.46 5.59 1.11 0.20 0.17 98.76 20 616 ## 408 40.0 11 7 12 24 19 44 16 187 <6 35.0 12 162 103 6.70 L-344 61.49 1.13 15.69 3.77 0.00 0.07 1.27 6.94 5.64 1.83 0.40 0.98 99.21 47 555 ## 485 41.0 10 <6 13 25 27 44 22 577 6.0 24.0 15 209 107 7.47 L-345 62.53 0.76 14.29 8.20 0.00 0.05 0.77 1.46 2.52 7.65 0.20 0.40 98.83 210 366 61 494 18.0 7 11 19 27 23 67 24 1440 6.0 <15 <10 174 94 10.17 L-346 70.01 0.49 13.71 5.02 0.00 0.05 0.31 0.96 3.40 5.99 0.10 0.64 100.68 195 168 69 469 27.0 12 <6 80 77 20 14 <12 774 11.0 24.0 <10 190 98 9.39 L-347 45.32 1.57 12.74 9.07 0.00 0.11 6.14 18.97 3.89 0.45 0.08 0.42 98.76 11 497 14 77 6.0 26 21 197 ## 22 127 131 48 9.0 29.0 <10 111 57 4.34 L-348 68.82 0.46 13.11 3.52 0.00 0.14 0.29 3.80 4.97 3.37 0.13 0.31 98.92 38 762 56 329 19.0 7 <6 13 20 19 43 17 439 <6 40.0 <10 130 61 8.34 L-349 67.98 0.35 13.65 3.38 0.00 0.07 0.35 2.69 4.47 4.97 0.13 0.82 98.86 108 423 55 230 32.0 7 11 24 16 19 21 16 590 <6 23.0 <10 106 50 9.44 L-352 70.34 0.51 13.27 4.15 0.00 0.05 0.53 1.63 3.37 4.96 0.10 0.26 99.17 178 166 35 357 20.0 10 11 17 30 19 16 21 861 <6 19.0 <10 212 123 8.33 L-353 64.23 0.92 13.89 5.97 0.00 0.04 1.34 3.73 3.62 5.05 0.24 0.49 99.52 120 400 ## 404 20.0 10 <6 67 24 21 36 19 606 6.0 20.0 12 141 73 8.67 L-354 64.83 0.81 14.83 6.19 0.00 0.07 1.46 2.45 3.15 4.06 0.20 0.95 99.00 138 207 77 435 25.0 11 17 115 78 20 71 22 977 <6 22.0 12 156 82 7.21 L-355 72.83 0.18 13.16 2.91 0.00 0.04 0.11 0.78 3.18 5.57 0.11 0.53 99.40 263 46 46 126 19.0 <6 7 20 21 18 79 38 135 8.0 21.0 <10 80 37 8.75 L-402 68.46 0.60 13.71 5.64 0.00 0.04 0.43 2.96 4.94 1.14 0.11 0.82 98.85 70 286 ## 602 44.0 7 10 12 29 22 25 20 272 6.0 21.0 12 178 107 6.08 L-403 64.07 0.68 14.61 7.86 0.00 0.06 1.14 3.13 3.50 4.38 0.16 0.71 100.30 119 277 83 762 25.0 9 9 196 89 25 19 19 1054 8.0 17.0 15 141 80 7.88 L-405 52.10 1.22 16.06 10.02 0.00 0.11 5.30 8.98 3.30 1.08 0.15 0.71 99.03 23 882 24 121 14.0 37 72 30 53 17 220 35 226 <6 <15 26 78 37 4.38 L-406 46.64 2.48 13.15 14.14 0.00 0.23 6.55 10.17 3.29 0.80 0.26 1.09 98.80 11 282 38 180 17.0 43 73 80 ## 18 374 106 118 <6 <15 37 29 18 4.09 L-407 60.09 1.12 13.19 6.31 0.00 0.07 1.49 8.27 4.03 3.86 0.30 0.61 99.34 92 396 79 532 28.0 13 8 43 40 19 71 29 689 7.0 26.0 14 188 96 7.89 L-408 70.26 0.33 13.59 3.87 0.00 0.05 0.26 1.23 3.49 5.24 0.07 0.43 98.82 241 95 ## 348 33.0 7 6 15 34 23 <12 13 483 12.0 32.0 <10 241 121 8.73 L-409 69.36 0.41 14.76 3.25 0.00 0.02 0.49 1.13 4.47 5.43 0.10 0.44 99.86 206 151 43 313 32.0 6 <6 10 16 19 25 12 677 13.0 53.0 <10 120 60 9.90 L-410 67.74 0.44 12.99 8.55 0.00 0.02 0.88 0.29 0.17 4.34 0.09 3.18 98.69 233 16 25 177 33.0 9 9 489 ## 17 51 14 187 7.0 32.0 <10 147 80 4.51 L-411 8.09 0.09 0.85 0.57 0.00 0.02 4.72 43.80 0.04 0.35 0.16 41.87 100.56 6 87 4 17 3.0 <6 <6 <6 16 <9 <12 <12 23 <6 <15 45 12 <12 0.39 L-433 51.23 2.42 14.76 11.92 0.00 0.16 4.74 8.16 3.82 2.33 0.42 0.59 100.55 71 396 44 261 22.0 28 11 45 99 20 275 62 384 7.0 <15 27 96 52 6.15 L-434 69.24 0.53 13.96 4.52 0.00 0.06 0.74 1.98 1.92 4.77 0.13 1.32 99.17 149 247 8 411 7.0 8 9 25 35 16 19 18 869 <6 <15 30 18 <12 6.69 L-435 67.58 0.43 15.29 3.91 0.00 0.05 0.36 1.59 3.89 6.45 0.10 0.32 99.97 142 271 34 389 11.0 8 <6 29 34 21 15 13 1227 <6 <15 <10 86 43 10.34 L-436 73.93 0.27 12.03 2.68 0.00 0.04 0.17 1.02 4.15 4.81 0.06 0.39 99.55 235 74 45 303 31.0 <6 <6 10 21 21 <12 <12 195 26.0 99.0 <10 223 114 8.96 L-437 55.61 1.95 14.33 9.89 0.00 0.14 2.79 5.09 3.77 4.40 0.52 0.58 99.07 113 395 52 404 32.0 21 8 121 ## 22 144 21 736 <6 <15 18 111 56 8.17 L-438 53.44 1.57 14.02 8.54 0.00 0.13 5.89 7.86 3.34 3.75 0.49 0.76 99.79 171 402 43 390 31.0 27 77 43 71 19 163 250 592 7.0 22.0 22 99 55 7.09 L-439 70.07 0.33 12.99 4.06 0.00 0.02 0.22 0.77 4.27 5.46 0.05 0.62 98.86 243 66 90 572 46.0 <6 3 21 16 25 <12 <12 163 19.0 90.0 <10 237 124 9.73 L-440 51.34 2.12 14.48 11.82 0.00 0.15 4.77 7.19 3.18 2.19 0.48 0.89 98.61 74 395 39 348 19.0 32 29 27 99 21 244 101 373 <6 <15 29 56 29 5.37 L-441 62.98 1.11 14.13 7.49 0.00 0.12 0.99 2.75 3.71 5.30 0.35 0.46 99.39 180 226 74 414 46.0 10 <6 13 88 24 28 <12 893 6.0 19.0 12 187 98 9.01 L-442 78.22 0.33 8.81 3.27 0.00 0.03 0.00 0.10 0.23 7.61 0.06 0.34 99.00 227 44 99 349 18.0 <6 <6 16 16 12 27 <12 618 <6 44.0 <10 288 149 7.84 L-443 76.23 0.44 9.57 5.13 0.00 0.03 0.10 0.43 0.20 6.79 0.05 0.40 99.37 201 24 64 391 48.0 8 7 12 14 14 28 <12 499 <6 100.0 <10 49 25 6.99 L-444 52.77 2.43 15.66 11.98 0.00 0.17 3.98 7.06 3.24 1.98 0.56 0.22 100.05 43 404 41 170 21.0 33 14 27 ## 21 245 54 396 6.0 <15 33 67 36 5.22 X-43 72.65 0.27 14.34 0.34 1.10 0.04 0.73 1.21 3.07 5.46 0.12 0.55 99.88 8.53 X-44 76.59 0.32 12.60 0.28 2.08 0.04 0.82 0.78 0.87 5.77 0.04 0.49 100.68 6.64 X-45 68.41 0.69 14.46 0.29 4.31 0.08 1.29 2.07 3.47 4.63 0.25 0.92 100.87 8.10 X-46 72.98 0.13 14.41 0.10 1.05 0.04 0.42 1.03 4.45 4.57 0.07 0.79 100.04 9.02 X-47 78.16 0.15 11.55 0.00 0.86 0.02 0.70 0.41 2.45 6.08 0.40 0.18 100.96 8.53 X-48 73.41 0.14 13.97 0.16 1.08 0.05 0.37 1.05 4.41 4.44 0.35 0.59 100.02 8.85 Table No. A3 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGIO N PAGE 3/14 Hook Granite, Zambia (cont.) Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 X-49 64.17 0.89 20.28 0.26 1.06 0.05 0.19 2.30 6.14 4.57 0.14 0.49 100.54 10.71 X-50 62.31 0.11 18.36 1.53 3.07 0.10 0.90 1.00 5.67 6.04 0.07 0.98 100.14 11.71 X-51 60.19 0.49 18.14 0.84 3.86 0.14 0.33 2.35 5.31 7.00 0.07 1.55 100.27 12.31 X-52 67.17 0.72 14.55 0.48 4.33 0.07 1.20 2.05 3.59 5.30 0.20 0.85 100.51 8.89 X-53 71.79 0.23 14.21 0.31 2.26 0.05 0.37 1.06 3.40 5.64 0.12 0.98 100.42 9.04 X-54 71.06 0.45 14.42 0.03 1.25 0.05 0.65 4.21 2.70 5.49 0.11 0.57 100.99 8.19 X-55 75.50 0.31 12.40 1.50 0.60 0.03 0.40 0.60 3.10 5.60 0.04 0.94 101.02 8.70 X-56 67.80 0.71 14.50 0.90 3.60 0.05 1.18 2.90 3.10 4.60 0.21 0.87 100.42 7.70 X-57 67.00 0.75 14.20 1.10 4.00 0.07 1.30 2.40 2.80 5.10 0.22 1.34 100.28 7.90 X-58 71.10 0.28 14.50 1.20 1.10 0.03 0.29 1.10 3.40 6.30 0.07 0.93 100.30 9.70 X-59 69.70 0.52 14.20 1.00 2.40 0.07 0.60 1.70 4.80 5.50 0.14 0.77 101.40 10.30 X-60 71.10 0.38 13.60 1.10 2.50 0.06 0.42 1.50 3.50 5.50 0.08 1.27 101.01 9.00 X-61 71.74 0.27 14.47 0.32 1.73 0.05 0.42 1.62 3.44 4.65 0.24 0.55 99.50 8.09 X-62 61.07 0.80 16.53 1.03 5.61 0.16 0.56 2.97 3.75 6.03 0.14 0.84 99.49 9.78 X-63 64.77 0.89 15.33 0.73 4.82 0.08 1.45 2.54 3.83 4.30 0.27 0.87 99.88 8.13 X-64 61.68 1.20 14.96 0.77 7.01 0.12 2.29 3.15 3.60 3.30 0.35 1.28 99.71 6.90 X-65 74.82 0.11 13.65 0.38 0.65 0.01 0.50 0.98 3.57 5.35 0.03 0.58 100.63 8.92 X-66 72.86 0.30 14.37 0.79 2.66 0.04 0.54 0.93 3.98 5.25 0.09 0.72 102.53 9.23 X-67 70.30 0.38 13.88 0.60 3.27 0.07 0.45 1.17 2.29 5.90 0.14 0.84 99.29 8.19 X-68 70.96 0.28 13.75 1.02 1.58 0.05 0.24 0.91 1.65 7.44 0.07 1.31 99.26 9.09 X-69 68.83 0.48 14.51 4.05 0.79 0.03 0.33 0.10 2.79 7.36 0.05 0.00 99.32 10.15 X-70 74.17 0.21 12.86 0.00 1.80 0.04 0.33 0.49 1.94 5.91 0.10 0.50 98.35 7.85 X-71 70.61 0.33 14.72 1.41 0.86 0.02 0.55 0.54 2.17 7.33 0.18 0.73 99.45 9.50 X-72 69.88 0.40 13.71 1.80 2.37 0.07 0.27 0.62 2.92 6.03 0.04 0.55 98.66 8.95 X-73 67.24 0.73 14.52 2.90 2.30 0.03 0.95 2.17 4.44 3.53 0.26 0.00 99.07 7.97 X-74 58.87 0.46 14.09 2.03 2.44 0.07 2.10 7.49 6.09 3.07 0.17 0.00 96.88 9.16 X-75 71.21 0.42 21.42 2.00 1.44 0.03 0.45 0.89 4.10 4.92 0.11 0.81 107.80 9.02 P-39 72.16 0.28 12.57 3.40 0.00 0.08 0.12 1.17 4.67 5.57 0.11 0.17 100.13 404 43 ## 309 59.0 56 4 <3 12 29 <4 5 182 19.0 71.0 4 11.0 21.40 ##### 33.00 290 145 2.00 10.00 2.50 <1 12 0.80 19.40 3.10 18.30 3.60 9.20 34.4 7.30 1.10 10.24 P-46 71.17 0.38 12.62 4.35 0.00 0.12 0.20 0.81 3.59 6.89 0.07 0.16 100.20 398 65 89 257 53.0 48 4 <3 45 27 <4 9 387 10.0 46.0 1 11.0 16.90 93.10 25.70 217 110 3.00 11.00 2.80 26 28 1.40 15.50 2.40 14.00 2.80 7.90 4.90 7.40 1.10 10.48 P-50 71.53 0.25 12.60 3.26 0.00 0.10 0.30 1.66 4.55 4.88 0.21 0.14 99.34 376 66 ## 312 107.0 40 16 <3 30 27 <4 4 314 62.0 256.0 3 23.0 54.30 334.8 100.2 899 505 4. 00 9.00 3.20 1 8 1.20 39.6 6.00 32.2 6.20 16.30 5.70 11.40 1.60 9.43 P-53 73.18 0.24 13.04 2.62 0.00 0.07 0.22 0.95 3.78 5.92 0.12 0.09 100.14 421 59 54 179 48.0 71 19 <3 <1 24 <4 24 209 21.0 43.0 2 11.0 5.60 25.70 8.00 78 44 6.00 6. 00 2.50 6 6 0.80 6.00 1.10 6.70 1.50 4.70 31.80 4.80 0.80 9.70 P-57 62.19 0.36 13.11 2.44 0.00 0.05 0.26 0.86 15.42 5.52 0.06 0.21 100.27 225 45 ## 404 48.0 63 21 <3 1 24 <4 <4 286 10.0 51.0 6 5.0 79.00 499.4 133.6 735 579 2.0 0 11.00 2.60 <1 5 7.60 80.5 10.00 55.6 11.10 28.9 35.9 21.40 3.30 20.94 P-58 67.76 0.79 13.46 6.83 0.00 0.17 1.40 2.21 3.78 4.27 0.18 0.25 100.85 210 189 66 223 30.0 77 4 21 72 26 45 12 680 4.0 24.0 8 12.0 10.30 50.50 13.10 107 53 5.00 6.00 2.10 1 30 2.10 9.90 1.50 8.50 1.70 4.70 33.4 3.90 0.60 8.05 P-40i 76.05 0.26 11.74 2.15 0.00 0.08 0.13 1.54 4.06 4.05 0.07 0.07 100.13 150 92 48 335 27.0 61 12 <3 26 26 <4 9 309 6.0 20.0 2 8.0 9.30 45.60 11.90 98 51 1.00 11. 00 1.30 2 8 1.50 8.80 1.40 8.30 1.70 5.00 35.3 5.00 0.80 8.11 P-40ii 68.86 0.55 13.67 4.56 0.00 0.12 0.33 1.82 4.52 5.77 0.12 0.19 100.32 195 110 77 391 52.0 53 14 <3 53 27 11 19 503 <2 15.0 5 10.0 15.90 78.80 20.00 157 71 1. 00 11.00 3.30 <1 22 2.00 14.40 2.40 14.20 2.80 7.50 34.9 6.40 1.00 10.29 Table No. A4 Serenje, Zambia Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 P-32 73.45 0.26 12.59 1.67 0.00 0.06 0.10 0.94 4.34 6.61 0.08 0.14 100.10 334 72 23 57 12.0 58 10 <3 14 17 <4 20 862 <2 7.0 3 48.0 3.60 15.80 4.30 36 18 3.00 4.00 0. 90 <1 4 1.30 3.80 0.60 3.50 0.60 1.40 36.4 1.00 0.10 10.95 P-33 68.30 0.54 14.41 3.20 0.00 0.10 0.73 1.53 5.65 6.09 0.19 0.20 100.74 230 222 81 157 19.0 52 6 <3 45 21 31 13 2028 <2 16.0 7 21.0 16.60 78.50 19.40 121 57 2.00 4.00 2.40 <1 13 2.90 16.70 2.30 12.80 2.60 7.00 33.10 5.60 0.80 11.74 P-35 74.32 0.25 13.99 1.48 0.00 0.07 0.33 1.12 6.19 2.54 0.07 0.18 100.36 83 188 2 99 6.0 41 2 <3 35 19 11 21 558 2.00 8.0 1 20.0 1.60 9.40 2.70 26 15 1.00 3.00 0.40 <1 5 0.50 1.20 0.10 0.60 0.10 0.20 33.4 0.20 0.00 8.73 X-15 67.63 0.59 14.37 2.02 1.66 0.07 1.15 1.90 4.59 5.21 0.26 0.86 100.31 592 9.80 Table No. A5 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGION PAGE 4/14 Kalengwa-Kasempa Area, Zambi a Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-139 75.60 0.09 11.88 1.50 0.00 0.03 0.62 0.14 1.61 7.87 0.01 0.79 100.14 399 17 40 75 41.0 10 7 55 34 23 14 47 769 <6 26.0 <10 42 12 9.48 L-313 54.29 1.67 13.47 10.37 0.00 0.06 5.07 4.92 4.55 0.80 0.67 4.40 100.27 21 164 89 445 40.0 14 12 42 39 23 102 21 104 7.0 <15 36 139 75 5.35 L-314 43.72 7.81 12.73 11.28 0.00 0.08 6.68 7.01 3.38 0.36 0.64 6.73 100.42 14 77 56 25 36.0 20 19 28 49 18 438 50 60 <6 <15 55 27 16 3.74 L-318 47.28 3.04 15.31 7.93 0.00 0.04 6.86 13.85 4.18 0.56 0.38 0.96 100.39 9 154 37 163 27.0 23 53 9 22 19 258 99 20 <6 <15 30 68 33 4.74 L-321 71.94 0.71 9.67 11.04 0.00 0.03 3.43 0.30 0.68 0.05 0.12 2.40 100.37 6 81 59 242 18.0 96 18 16 30 15 157 95 65 <6 <15 12 102 61 0.73 L-322 70.45 0.74 13.65 5.38 0.00 0.02 0.48 0.08 0.13 7.57 0.08 1.74 100.32 168 30 37 264 30.0 12 7 13 35 21 49 33 498 <6 27.0 <10 171 74 7.70 L-323 67.04 0.81 14.15 7.57 0.00 0.02 0.52 0.19 0.17 8.21 0.17 1.61 100.46 173 29 37 302 35.0 26 9 17 28 20 58 32 525 <6 30.0 <10 153 71 8.38 L-324 62.05 0.97 14.50 7.90 0.00 0.06 1.43 1.71 3.85 6.29 0.29 1.25 100.30 112 230 57 362 35.0 20 16 62 ## 21 96 27 1004 13.0 48.0 11 190 74 10.14 L-325 60.42 1.15 16.98 11.07 0.00 0.02 0.91 0.06 0.08 6.75 0.29 2.82 100.55 227 37 ## 372 31.0 28 13 55 48 26 114 <12 508 6.0 27.0 <10 1460 819 6.83 P-13 65.76 0.82 14.67 5.87 0.00 0.10 1.00 2.40 5.77 3.89 0.24 0.21 100.52 90 301 45 157 30.0 70 11 <3 4 23 55 22 787 10.0 56.0 7 4.0 9.90 58.80 16.50 153 80 <1 9.00 2.70 1 35 2.10 9.50 1.30 8.00 1.70 4.50 34.9 4.60 0.80 9.66 P-17 64.11 0.97 14.29 7.35 0.00 0.08 0.80 2.43 3.95 5.62 0.26 0.18 99.86 107 372 54 327 32.0 84 16 63 23 24 103 11 782 11.0 48.0 10 5.0 11.90 64.10 17.30 136 47 1. 00 8.00 2.40 3 88 2.40 11.70 1.50 9.00 1.80 5.10 35.7 5.00 0.80 9.57 P-25 51.44 2.40 20.38 8.73 0.00 0.71 3.91 5.28 6.42 1.71 0.38 0.12 100.72 55 348 24 107 14.0 33 6 40 13 24 98 90 120 <2 2.0 20 4.0 4.00 15.10 3.20 22 9 1.00 2.00 1.3 0 12 107 1.70 4.50 0.70 4.20 0.90 2.30 33.6 2.10 0.30 8.13 P-26 76.20 0.13 11.58 0.93 0.00 0.05 <.1 0.25 10.51 0.03 0.03 0.08 99.71 7 15 ## 705 243.0 39 4 <3 <1 68 <4 24 22 6.0 76.0 1 5.0 6.90 15.00 3.20 24 8 <1 31.00 4.80 1 7 0.70 11.80 3.30 27.5 6.70 21.30 35.7 23.00 3.40 10.54 X-76 55.35 1.48 14.63 10.86 0.00 0.10 4.43 2.43 0.91 7.34 0.50 1.65 99.69 209 199 56 591 28.0 13 11 295 50 139 <9 1379 8.25 X-77 61.50 1.10 15.15 7.30 0.00 0.11 1.58 2.81 4.39 5.07 0.34 1.21 100.59 182 313 48 339 34.0 15 <9 7 47 92 11 1189 9.46 X-78 51.81 3.13 15.06 11.46 0.00 0.06 7.53 1.00 3.02 4.48 0.33 2.67 100.54 137 109 32 290 46.0 25 102 20 ## 415 117 118 7.50 X-79 48.31 4.07 11.38 9.92 0.00 0.21 9.92 5.90 2.58 1.14 0.57 6.34 100.34 18 234 32 358 44.0 47 70 35 ## 458 74 75 3.72 X-80 45.03 3.27 13.53 16.29 0.00 0.09 6.04 5.05 5.14 3.32 0.53 2.13 100.41 97 112 48 325 55.0 24 81 12 23 327 142 141 8.46 X-81 46.37 3.96 13.46 15.27 0.00 0.05 6.20 4.88 4.91 2.96 0.54 1.92 100.52 103 94 55 302 48.0 17 88 7 22 324 135 148 7.87 X-82 48.60 1.56 13.71 18.47 0.00 0.08 2.02 5.07 7.38 1.05 0.81 1.52 100.26 32 122 61 567 84.0 <9 10 777 47 58 <9 233 8.43 X-83 46.07 2.56 14.20 17.60 0.00 0.15 5.97 5.84 3.60 3.20 0.32 0.85 100.37 88 105 27 177 32.0 17 44 102 44 325 79 384 6.80 X-84 46.07 3.95 12.30 12.67 0.00 0.06 3.44 8.56 5.49 0.87 0.91 6.14 100.47 27 106 59 444 89.0 11 11 26 59 138 <9 152 6.36 X-85 47.35 2.56 14.08 13.25 0.00 0.14 7.29 8.22 4.21 0.61 0.32 2.54 100.58 21 287 26 173 37.0 36 69 11 ## 318 36 127 4.82 X-86 45.88 3.96 12.72 16.75 0.00 0.25 5.61 7.19 3.78 1.46 0.31 2.23 100.14 37 319 33 201 40.0 14 36 124 ## 522 <9 303 5.24 X-87 46.09 2.86 13.80 14.33 0.00 0.23 6.98 7.07 4.90 0.32 0.41 3.05 100.06 13 344 31 208 42.0 18 50 9 ## 315 23 119 5.22 X-88 45.24 2.00 14.37 11.55 0.00 0.11 10.97 4.11 2.72 5.24 0.20 3.85 100.37 147 69 25 131 21.0 35 201 <2 ## 326 515 112 7.96 X-89 46.20 3.57 8.68 14.36 0.00 0.18 11.42 6.07 4.30 2.70 0.67 1.85 100.01 56 337 36 223 53.0 37 30 7 ## 474 9 155 7.00 Table No. A6 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGIO N PAGE 5/14 Northwestern Zambia Region, Zambi a Table No. A7 Kalene Hill Archean rocks Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-372 54.14 0.84 17.15 9.33 0.00 0.12 3.24 7.00 4.31 2.25 0.28 1.85 100.51 86 764 11 193 8.0 20 9 57 ## 21 23 18 423 <6 <15 24 135 71 6.56 L-373 72.41 0.25 14.10 2.22 0.00 0.03 0.41 1.36 3.49 4.20 0.05 0.93 99.45 114 353 31 147 8.0 6 7 17 28 14 198 12 1215 <6 17.0 <10 105.3 14.70 34.69 90 10 3.05 21.3 1 0.200 0.600 7.69 L-374 70.46 0.20 14.58 2.28 0.00 0.04 0.31 1.75 5.02 3.92 0.05 0.77 99.38 97 473 10 105 6.0 <6 <6 9 33 17 17 14 1054 <6 <15 <10 49 23 8.94 L-375 69.92 0.45 12.64 4.64 0.00 0.07 0.33 1.04 3.27 5.81 0.13 0.77 99.07 140 197 47 365 30.0 7 11 26 55 18 22 19 1228 <6 21.0 <10 296 145 9.08 L-376 59.71 0.51 17.93 5.54 0.00 0.09 1.10 2.05 6.07 4.94 0.12 0.83 98.89 74 419 29 280 27.0 11 <6 18 58 20 67 <12 1036 <6 <15 <10 174 95 11.01 L-380 70.37 0.39 13.41 3.59 0.00 0.05 0.27 0.92 3.65 5.94 0.09 0.69 99.37 177 135 57 365 28.0 7 10 116 83 18 17 13 1129 <6 18.0 <10 14.90 65.63 187.9 241 95 0.69 4 4.41 1.500 2.85 2.488 1.13 9.59 Paleoproterozoic Group 2 Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-020 74.44 0.22 12.70 2.48 0.00 0.05 0.28 0.58 3.03 5.85 0.02 0.75 100.40 226 91 53 228 19.0 <6 <6 9 64 18 <12 47 553 10.0 62.0 <10 11.13 88.15 144.8 286 75 73.2 3.33 2.68 1.28 8.88 L-025 70.60 0.40 13.80 3.70 0.00 0.05 0.73 1.82 3.19 4.80 0.08 0.96 100.13 91 370 11 108 10.0 6 8 9 71 17 38 42 1390 <6 <15 <10 4.163 31.91 47.41 85 20 24.6 0.750 0 .900 0.563 0.83 7.99 L-026 71.92 0.37 13.46 3.29 0.00 0.04 0.67 1.98 3.23 4.51 0.08 0.82 100.37 85 384 12 392 14.0 6 7 8 55 16 38 42 1367 <6 <15 <10 97 41 7.74 L-360 68.89 0.31 14.44 3.71 0.00 0.04 0.60 1.23 3.18 6.02 0.07 0.91 99.40 100 369 67 134 15.0 7 6 9 46 16 40 20 2144 <6 <15 <10 114 57 9.20 L-364 74.42 0.19 11.94 2.26 0.00 0.02 0.40 0.26 3.54 5.07 0.04 0.68 98.82 236 34 42 207 10.0 <6 9 9 23 20 59 23 198 8.0 44.0 <10 179 88 8.61 L-365 72.12 0.48 12.08 4.21 0.00 0.04 1.25 0.45 2.64 4.87 0.12 1.33 99.59 146 81 75 353 24.0 8 7 24 38 19 <12 15 881 <6 26.0 <10 212 114 7.51 L-366 67.02 0.66 13.23 5.79 0.00 0.09 0.90 1.76 4.05 4.28 0.18 0.92 98.88 142 188 54 448 19.0 7 <6 13 86 20 21 12 1082 <6 <15 11 10.44 139.3 247.0 347 139 88.13 6. 08 42.5 13.2 2.600 8.33 L-368 67.04 0.71 14.00 4.96 0.00 0.05 1.32 0.98 3.41 4.64 0.17 1.39 98.67 112 156 18 565 10.0 10 8 13 61 18 38 15 1652 <6 <15 <10 189 101 8.05 L-369 71.39 0.21 13.38 1.89 0.00 0.03 0.49 1.80 4.10 3.83 0.04 1.74 98.90 78 254 51 135 25.0 <6 6 119 ## 16 53 20 789 <6 <15 <10 114.3 19.38 57.14 86 27 23.1 0.600 1.363 0.688 7.93 L-370 74.09 0.20 12.02 2.58 0.00 0.03 0.26 0.95 4.32 4.07 0.04 0.88 99.44 279 61 7 195 6.0 <6 10 10 32 21 16 <12 264 9.0 52.0 <10 145 73 8.39 L-371 70.77 0.25 14.56 1.78 0.00 0.03 0.40 1.37 4.85 4.06 0.08 1.04 99.19 104 650 59 127 23.0 <6 10 10 38 18 <12 15 1474 <6 <15 <10 110 52 8.91 L-377 69.88 0.26 12.62 3.07 0.00 0.04 0.28 1.27 5.06 5.45 0.05 1.01 98.99 255 69 91 174 17.0 <6 9 167 ## 19 12 19 365 8.0 45.0 <10 135 71 10.51 L-378 73.20 0.22 12.15 3.08 0.00 0.04 0.23 0.84 3.95 4.18 0.05 0.84 98.78 216 69 79 255 19.0 <6 10 163 98 19 <12 15 371 6.0 33.0 <10 267 135 8.13 L-379 72.89 0.21 12.77 2.54 0.00 0.03 0.45 0.72 6.12 2.92 0.07 0.62 99.34 139 54 59 84 27.0 <6 14 17 15 25 <12 20 133 10.0 <15 <10 39 18 9.04 Paleoproterozoic Group 3 Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-023 67.01 0.56 14.95 5.02 0.00 0.07 1.83 2.74 3.71 3.60 0.19 0.80 100.48 78 376 24 133 13.0 10 6 <6 44 16 80 219 1283 <6 <15 12 6.93 49.95 76.63 127 44 61.23 0.7 38 1.43 1.300 1.13 7.31 L-027 67.24 0.53 15.50 4.74 0.00 0.09 1.38 4.31 3.75 1.72 0.19 1.02 100.47 49 619 21 123 13.0 7 <6 <6 49 18 68 161 573 <6 <15 12 107 58 5.47 L-363 65.30 0.64 15.16 5.30 0.00 0.09 1.23 3.11 3.95 3.37 0.16 1.49 99.80 119 398 31 202 9.0 11 6 18 69 20 73 20 1054 <6 <15 <10 82 40 7.32 Paleoproterozoic Group 4 Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-357 61.26 0.49 17.43 5.33 0.00 0.07 1.08 2.85 4.92 3.59 0.22 1.77 99.01 69 568 67 298 29.0 10 9 36 70 21 <12 12 1645 <6 <15 <10 111 55 8.51 L-358 63.11 0.65 15.74 6.29 0.00 0.07 1.04 3.80 4.03 2.31 0.17 1.51 98.72 80 492 29 233 13.0 12 10 479 ## 22 58 16 950 <6 <15 14 9.988 28.21 68.8 106 32 98.13 0.18 8 0.563 1.063 6.34 L-359 66.92 0.41 14.63 4.21 0.00 0.06 0.79 2.31 3.91 4.84 0.12 1.07 99.27 120 359 28 192 13.0 8 8 11 54 22 64 26 1134 <6 <15 10 149 76 8.75 L-361 63.38 0.74 15.35 6.08 0.00 0.06 1.57 3.80 4.38 2.06 0.22 1.49 99.13 118 544 17 246 8.0 12 15 20 78 21 36 <12 844 <6 <15 12 162 84 6.44 L-362 64.93 0.66 14.31 5.80 0.00 0.07 1.39 3.79 3.72 2.15 0.17 1.66 98.65 77 452 35 221 9.0 9 8 17 93 19 79 22 1523 <6 <15 10 113 61 5.87 L-367 72.13 0.48 11.76 4.45 0.00 0.06 1.30 3.17 1.69 2.41 0.13 1.70 99.28 59 232 ## 162 22.0 10 <6 7 61 15 29 14 1518 <6 <15 <10 80 42 4.10 Other Samples L-024 48.01 2.10 12.37 18.91 0.00 0.28 4.93 8.74 1.70 0.43 0.17 1.16 98.80 16 78 51 140 11.0 57 66 236 ## 22 470 79 108 6.00 <15 43 13.59 38.8 39.5 25 19 391.4 3.1 00 2.250 2.088 2.13 Table No. A7.1 Kabompo Dome Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-028 60.53 0.60 14.99 6.80 0.00 0.09 4.08 3.69 3.88 3.07 0.26 1.58 99.57 124 581 20 155 16.0 26 52 79 45 16 79 89 532 <6 17.0 17 5.88 43.06 63.88 109 32 95.3 2.93 0.650 1.03 6.95 L-029 63.66 0.66 17.38 5.28 0.00 0.05 2.34 3.70 3.95 2.50 0.26 0.70 100.48 88 542 12 147 11.0 20 23 26 49 18 87 51 574 <6 <15 11 89 45 6.45 L-030 74.74 0.10 13.50 1.47 0.00 0.04 0.09 0.45 2.16 5.91 0.00 1.92 100.38 262 67 15 128 16.2 <6 7 22 34 16 13 15 391 16.0 40.0 <10 35.7 2.87 14.89 4.15 76 26 2.70 4.00 1.24 0 0 0.39 2.41 0.41 2.81 0.59 1.87 0.30 2.17 0.34 8.07 L-047 66.09 0.46 14.68 5.40 0.00 0.08 0.20 2.42 4.99 4.75 0.08 0.54 99.70 110 83 ## 634 105.0 <6 <6 <6 47 22 12 <12 1015 6.0 <15 10 127.3 186.3 308 164 68.50 6.43 8 29.4 7.750 19.71 3.538 9.74 Table No. CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGION PAGE 6/14 Northwestern Z ambia Region, Z ambia ( cont.) Table No. A7.2 Solwesi Dome Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-049 47.30 2.03 15.47 13.49 0.00 0.25 5.41 10.51 3.04 0.93 0.22 0.92 99.58 13 346 30 109 17.0 34 46 143 ## 19 296 85 127 <6 <15 31 23 <12 3.97 L-050 46.86 2.06 15.40 13.35 0.00 0.21 5.20 10.46 3.73 0.89 0.27 0.52 98.95 11 321 31 114 16.0 46 49 91 70 18 321 171 93 <6 <15 34 30 <12 4.62 L-060a 45.83 4.36 11.86 17.84 0.00 0.26 6.24 9.49 2.29 1.12 0.43 0.38 100.11 149 64 19 128 9.5 31 39 20 ## 396 38 477 4.9 46.5 0 20.4 3.67 27.0 9.06 113 61 0.87 4. 08 1.16 0.57 2.65 0.44 3.02 0.66 2.15 0.36 2.73 0.42 3.41 L-060b 76.30 0.15 11.89 1.79 0.00 0.04 0.14 0.53 3.65 5.74 0.04 0.28 100.55 154 64 23 141 13.0 <6 <6 14 25 22 <12 54 481 <6 <15 35 37 20 9.39 L-060c 45.43 4.31 11.83 17.86 0.00 0.28 6.23 9.37 2.11 1.09 0.45 0.42 99.57 24 330 38 165 27.0 37 39 29 ## 387 33 118 3.20 L-420 71.91 0.31 13.61 2.62 0.00 0.02 0.48 0.67 4.95 2.98 0.06 1.08 98.69 187 93 38 178 28.0 8 10 31 26 18 20 20 532 13.0 37.0 <10 165 103 7.93 L-421 69.53 0.52 14.84 3.30 0.00 0.03 0.79 1.40 2.52 6.69 0.24 0.74 100.60 278 240 17 303 18.0 7 <6 34 24 18 42 19 1428 <6 57.0 <10 229 101 9.21 East of Solwesi Dome L-063 46.39 0.84 12.95 3.10 0.00 0.09 5.95 9.71 6.97 0.15 0.12 14.12 100.39 4 51 19 192 7.0 <6 18 7 22 21 86 36 <20 <6 <15 23 25 16 7.12 L-064 47.31 0.82 12.99 3.23 0.00 0.10 5.76 9.38 6.85 0.05 0.12 13.87 100.48 4 51 19 175 7.0 <6 18 8 28 20 92 36 <20 <6 <15 24 16 <12 6.90 L-065 39.63 0.57 9.98 4.16 0.00 0.11 7.62 13.40 4.80 0.12 0.07 19.80 100.26 4 125 24 108 8.0 <6 20 8 29 12 102 45 <20 <6 <15 30 5.65 1.725 18.83 15 10 71.00 0.988 0 .763 4.92 Table No. A7.3 Mwombezhi Dome Sodalite Syenite Quarry Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.0 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-032 59.58 1.09 15.52 7.08 0.00 0.07 3.07 5.01 2.80 3.13 0.54 0.82 98.71 110 566 26 284 23.0 25 34 17 58 19 151 78 703 <6 <15 16 7.98 54.33 82.8 109 37 96.13 0.71 3 1.050 1.063 5.93 L-034 60.10 0.04 23.01 3.98 0.00 0.07 0.11 0.14 6.82 4.47 0.07 1.68 100.49 79 342 27 708 92.0 <6 12 8 18 17 74 87 705 <6 20.0 11 311 134 11.29 L-034A 60.10 0.04 23.01 3.98 0.00 0.07 0.11 0.14 6.82 4.47 0.07 1.68 100.49 79 342 27 708 92.0 <6 12 8 18 17 74 87 705 <6 20.0 11 311 134 11.29 L-036 73.57 1.10 15.97 1.46 0.00 0.02 0.12 0.10 4.47 6.82 0.09 7.83 100.54 34 51 30 635 38.0 <6 26 36 37 28 52 30 196 <6 36.0 <10 282 240 11.29 L-037 56.10 0.04 21.65 3.00 0.00 0.12 0.04 1.20 10.22 5.51 0.05 2.53 100.46 92 465 33 792 101.0 <6 7 10 ## 25 <12 117 423 9.0 17.0 <10 108.3 38.65 70.88 139 63 50 .70 0.413 0.688 0.68 15.73 L-038 56.45 0.12 21.07 3.77 0.00 0.08 0.00 0.32 12.27 4.32 0.07 2.01 100.48 72 244 29 859 114.0 <6 7 12 ## 26 <12 65 318 8.0 32.0 <10 261 146 16.59 L-039 57.37 0.05 21.32 3.71 0.00 0.20 0.08 0.75 9.68 4.63 0.06 2.64 100.49 87 355 37 808 120.0 <6 <6 12 ## 27 <12 68 349 9.0 30.0 <10 231 166 14.31 L-040 55.44 0.04 20.98 5.81 0.00 0.34 0.02 1.29 9.89 6.14 0.06 0.44 100.45 75 283 38 922 135.0 2 8 8 ## 25 4 139 261 8.0 30.0 <10 278 186 16.03 L-041 57.71 0.05 20.81 4.02 0.00 0.07 0.00 0.60 8.89 5.41 0.02 2.85 100.45 85 283 33 950 134.0 <6 <6 6 98 27 <12 <12 347 11.0 22.0 <10 183 109 14.30 L-044 57.32 0.03 21.02 3.15 0.00 0.14 0.00 0.65 12.04 4.28 0.05 1.70 100.38 109 616 ## 1758 178.0 4 8 10 ## 26 11 120 1441 10.0 31.0 <10 0.263 4.488 196 0 37.10 1 .48 1.150 0.288 0.713 16.32 L - 045 57 . 75 0 . 10 20 . 94 6 . 96 0 . 00 0 . 03 0 . 00 0 . 14 7 . 96 4 . 16 0 . 06 1 . 17 99 . 27 58 367 20 186 97 . 6 < 6 11 32 34 27 < 12 45 764 7 . 2 17 . 8 < 10 1 . 9 7 . 13 57 . 9 20 . 0 214 158 0 . 29 2 . 38 9 . 70 214 1 . 22 4 . 71 0 . 77 4 . 50 0 . 77 2 . 09 0 . 31 2 . 01 0 . 27 12 . 12 L-046 55.67 0.05 20.92 3.40 0.00 0.19 0.09 1.07 8.51 5.27 0.06 5.21 100.44 82 311 30 670 82.0 <6 6 115 ## 24 <12 51 526 <6 29.0 <10 0.53 0.550 6.700 204 1 44.38 0. 64 1.400 0.250 0.688 13.78 ZGSI 58.04 Tr 20.76 4.45 0.20 0.09 0.95 9.22 4.81 Tr 1.99 100.51 ZGSII 56.31 Tr 19.89 4.28 0.30 0.16 0.26 0.74 8.33 5.75 n.d. 3.56 99.58 Shilenda L-311 50.33 3.00 14.97 10.04 0.00 0.00 5.02 4.99 3.78 0.84 1.25 5.18 99.40 26 76 59 326 36.0 15 <6 19 39 19 121 16 88 8.00 <15 40 76 44 4.62 Table No. A8 Granitoids in the Copperbelt, Zambi a Table No. A8.1 Muliashi Porphyry Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-075 65.53 0.91 13.91 5.81 0.00 0.07 1.46 2.59 3.43 5.10 0.23 1.14 100.18 162 217 33 50 16.8 0 0 0 0 16 0 0 1339 <6 16.0 <10 21.1 9.40 53.11 13.45 160 61 2.48 1.38 0.81 0 0 1.89 7.80 1.11 6.66 1.26 3.52 0.49 3.17 0.45 8.53 L-076 65.53 0.91 13.91 5.81 0.00 0.07 1.46 2.59 3.43 5.10 0.23 1.14 100.18 182 212 48 361 26.0 22 16 105 35 17 82 56 1344 <6 17.0 10 137 61 8.53 L-077 66.70 0.79 14.45 4.66 0.00 0.06 1.36 2.66 3.78 5.06 0.21 0.77 100.50 174 216 39 290 22.0 14 11 28 46 18 59 41 1391 <6 14.0 <10 11.11 35.10 86.3 119 41 75.13 1.088 1.213 1.088 8.84 L-078 67.56 0.89 13.59 5.37 0.00 0.07 1.27 3.08 3.93 3.78 0.23 0.81 100.58 143 235 47 343 25.0 19 13 31 48 17 74 51 964 <6 18.0 10 131 61 7.71 L-157 75.81 0.19 12.48 1.25 0.00 0.00 1.16 0.18 0.19 6.95 0.03 1.39 99.63 225 12 12 107 17.0 26 8 7 14 14 20 15 618 <6 18.0 <10 43 17 7.14 L-158 73.58 0.20 12.85 1.36 0.00 0.00 1.46 0.93 0.33 7.11 0.04 2.00 99.87 233 19 13 109 16.0 32 7 <6 13 14 20 14 628 6.00 26.0 <10 107.9 26.04 63.13 76 31 2.100 8. 23 0.450 0.588 7.44 L-159 68.02 0.64 14.23 2.82 0.00 0.00 1.74 1.42 0.95 6.80 0.16 2.10 98.87 303 47 34 209 28.0 38 7 <6 19 17 57 18 919 11.00 24.0 10 118 60 7.75 L-160 67.96 0.55 14.78 2.29 0.00 0.00 1.47 1.67 2.46 5.69 0.16 2.10 99.14 264 40 49 223 32.0 39 9 <6 18 16 47 16 805 <6 15.0 13 117.8 42.35 102.1 156 49 27.91 1.13 2.788 0.988 8.15 L-163 43.65 1.23 15.61 14.61 0.00 0.30 11.50 4.45 1.80 3.69 0.14 2.97 99.95 149 179 25 85 9.0 172 410 <6 ## 15 228 292 478 <6 <15 22 16 <12 5.49 L-161 51.48 1.05 20.52 6.92 0.00 0.10 7.54 1.15 2.18 6.26 0.37 1.89 99.47 225 54 40 319 29.0 93 26 <6 ## 24 102 18 1829 <6 30.0 17 128 64 8.44 X-01 73.81 0.08 12.29 0.37 1.52 0.04 0.70 2.24 4.21 4.83 0.04 0.66 100.79 9.04 X-02 72.56 0.23 14.28 0.94 0.68 0.02 0.83 0.76 2.88 6.12 0.05 1.96 101.31 9.00 X-03 70.95 0.42 15.07 1.13 1.29 0.03 1.32 0.83 4.23 3.03 0.11 2.60 101.01 7.26 X-04 75.20 0.33 10.10 1.55 1.69 0.04 2.81 2.08 2.02 2.13 0.34 2.36 100.65 4.15 X-05 65.27 0.84 15.18 3.20 1.94 0.08 1.01 2.90 3.00 4.70 0.31 1.39 99.82 7.70 Table No. CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGION PAGE 7/14 Basement to the Copperbelt, Zambia (cont.) Table No. A8.2 Chambishi Mine Area Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-155 72.00 0.28 12.99 2.57 0.00 0.00 1.51 0.95 1.03 6.03 0.09 1.71 99.17 219 62 20 99 13.0 61 12 <6 26 15 44 21 848 <6 <15 <10 109.6 25.34 56.81 69 23 36.41 0.53 0 .23 0.713 7.06 X-42 68.6 0.3 14 1.14 1.25 0.06 2.29 2.25 2.13 4.04 0.11 3.54 99.7 6.17 X-06 46.85 15.87 3.33 7.40 0.11 8.61 7.29 3.65 2.50 0.15 3.06 98.82 6.15 X-07 58.63 13.08 6.07 6.68 0.15 1.87 4.70 5.50 0.66 0.32 1.66 99.32 6.16 X-08 67.94 12.08 7.23 1.01 0.04 0.60 1.65 6.70 0.20 0.07 1.70 99.22 6.90 X-09 59.26 16.65 1.26 0.43 0.06 2.04 4.59 9.80 0.20 0.65 4.48 99.42 10.00 X-10 47.87 14.53 4.50 9.05 0.15 6.13 6.12 2.95 1.55 0.37 7.22 100.44 4.50 X-11 48.19 14.53 4.13 7.18 0.12 6.66 9.00 4.25 1.40 0.17 3.60 99.23 5.65 Table No. A8.3 Samba copper prospect Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-268 69.51 0.69 16.52 4.32 0.00 0.01 0.35 0.13 0.54 4.53 0.17 3.62 100.39 178 37 48 275 22.00 10 10 942 14 19 72 187 1116 <6 19.00 13.00 151 81 5.07 L-269 75.84 0.31 13.87 3.02 0.00 0.00 0.00 0.20 0.31 3.67 0.21 3.03 100.46 94 20 16 179 19.00 <6 8 6 11 15 27 185 291 <6 <15 <10 83 41 3.98 L-273 65.92 0.52 14.92 4.14 0.00 0.12 1.78 3.54 2.94 3.12 0.18 2.98 100.16 128 110 31 173 14.00 18 9 49 38 16 77 206 966 <6 <15 15.00 101 56 6.06 L-279 67.94 0.63 14.39 4.41 0.00 0.08 1.31 3.25 3.31 3.08 0.22 1.29 99.91 123 204 39 285 19.00 7 13 6 51 16 64 302 810 6.00 20 <10 10.43 33.43 80.8 140 39 69.3 0.9 00 1.60 1.08 6.39 Table No. A8.4 Nchanga Granite Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 X-34 76.8 0.09 11.8 0.82 0.58 0.03 0.16 0.72 3.08 5.01 0.1 0.84 99.96 8.09 X-34a 76.8 0.09 11.8 0.82 0.58 0.03 0.16 0.72 5.01 3.08 0.1 0.84 99.96 8.09 X-35 76.8 0.08 10.7 1.3 0.04 0.1 0.8 2.3 4.9 0.02 0.69 97.77 7.20 X-36 76.9 0.01 12.3 0.6 0.01 0.1 0.5 3.6 4.4 0.04 0.35 98.81 8.00 X-37 78.2 0.04 10.3 1.1 0.04 0.1 0.7 2.2 4.9 0.01 0.44 98.03 7.10 X-38 59.8 1.1 10.4 12.6 0.3 0.6 4.3 1.7 2.9 0.08 0.99 94.77 4.60 X-39 66.6 0.01 18 0.2 0.02 0.03 0.2 2.4 11.9 0.01 0.95 100.3 14.30 X-40 64.8 0.01 16.7 0.4 0.01 0.03 0.1 0.7 15.5 0 0 98.25 16.20 P-28 68.49 0.34 12.40 3.43 0.00 0.12 0.26 1.06 8.74 5.32 0.11 0.13 100.27 345 58 ## 261 64.0 34 19 <3 97 24 <4 8 689 13.0 98.0 5 61.0 75.30 ##### 89.80 600 383 5.0 0 11.00 2.90 4 7 6.40 97.8 16.20 98.2 20.3 53.3 40.9 38.70 5.90 14.06 P-29 72.84 0.31 13.07 2.71 0.00 0.11 0.19 1.28 4.04 5.56 0.08 0.17 100.19 278 79 89 183 46.0 38 3 6 58 22 <4 8 724 9.0 65.0 6 53.0 16.20 82.60 23.20 204 101 3.00 6. 00 2.20 2 7 1.70 14.80 2.40 14.40 2.90 8.10 36.9 8.20 1.40 9.60 L-151 77.00 0.10 11.82 1.67 0.00 0.03 0.17 0.11 3.47 5.54 0.02 0.51 100.44 351 32 ## 197 91.0 10 8 42 39 24 <12 42 441 11.0 65.0 <10 113.8 48.59 96.88 167 49 6.94 13.56 0.538 10.61 2.200 9.01 L-153 77.40 0.07 11.91 1.65 0.00 0.03 0.12 0.27 3.51 4.89 0.01 0.51 100.37 438 25 ## 106 70.0 <6 8 58 33 24 <12 60 236 11.0 44.0 <10 87 38 8.40 L-154 77.07 0.07 12.06 1.22 0.00 0.00 0.00 0.25 3.07 5.78 0.01 0.50 100.05 478 27 68 122 58.0 7 <6 17 22 23 <12 <12 255 <6 44.0 <10 105.1 2.513 22.06 90 4 3.59 9.9 8 2.363 0.888 8.85 L-162 76.11 0.19 12.33 1.25 0.00 0.00 0.28 0.70 3.48 4.92 0.03 0.59 99.88 119 155 14 96 10.0 6 <6 7 22 13 17 15 793 <6 <15 <10 82 37 8.40 Table No. A8.5 Nchanga Mine Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-150 51.05 2.91 15.47 10.19 0.00 0.00 10.09 0.68 1.69 6.12 0.36 1.16 99.72 361 24 45 150 28.0 851 191 623 66 24 424 94 349 6.0 <15 29 12.9 13.43 54.96 18 7 220.8 0.263 1.250 7.81 L-167a 47.14 0.78 19.71 6.10 0.00 0.08 12.98 0.00 0.00 8.70 0.08 4.00 99.57 255 64 ## 781 147.0 266 57 1896 65 28 95 74 615 12.0 37.0 12 43 13 8.70 L-168 79.68 0.15 10.06 0.72 0.00 0.02 0.10 0.02 0.19 7.61 0.08 0.59 99.22 132 125 19 258 11.0 32 <6 261 10 <9 16 59 1190 <6 <15 <10 9.900 61 1 0.175 0.48 7.80 L-170 70.45 0.86 15.35 3.22 0.00 0.03 1.50 0.01 0.02 5.02 0.13 3.05 99.64 110 46 42 320 79.0 131 14 1954 25 29 92 335 766 10.0 <15 11 6.038 25.63 30.29 44 21 46.4 9 0.188 1.963 1.413 0.888 5.04 L-172 74.42 0.06 13.07 1.32 0.00 0.04 0.21 0.14 1.85 7.48 0.06 0.71 99.36 316 32 49 113 85.0 9 8 242 23 21 <12 618 668 5.3 48.5 <10 27.3 8.66 41.2 11.3 79 50 1.13 4 .97 3.20 0.41 7.22 1.32 9.90 2.23 7.30 1.12 7.27 1.00 9.33 L-173 74.69 0.09 12.55 1.37 0.00 0.03 0.28 0.14 1.87 7.51 0.05 0.78 99.36 314 29 78 172 128.0 11 6 232 20 22 <12 453 598 7.0 58.0 <10 85 49 9.38 Table No. A8.6 Mufulira Granite X-41 64.2 1.05 14.8 2.89 2.68 0.05 1.68 3.11 3.7 4.65 0.31 0.97 100.1 8.35 L-166 70.84 0.39 13.91 2.93 0.00 0.00 0.61 1.97 4.13 4.54 0.13 0.44 99.89 209 89 31 89 18.0 6 <6 22 18 15 <12 17 741 <6 15.0 <10 109.0 34.36 63.50 105 35 3.06 3.31 3 0.713 0.863 0.68 8.67 Other Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 X-12 30.05 0.37 8.60 39.65 4.48 0.05 0.27 6.82 5.78 0.35 96.42 0.00 X-13 49.41 2.67 12.71 2.18 10.07 0.14 6.93 10.46 2.46 0.80 0.46 2.38 100.67 3.26 X-14 46.76 3.30 10.31 5.81 9.10 0.14 7.25 10.24 4.26 0.86 0.38 4.05 102.46 5.12 Table No. A9 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGION PAGE 8/14 Kamanjab Inlier, Namibi a Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-832 73.67 0.32 12.24 1.83 0.00 0.04 0.14 0.46 4.39 5.23 0.11 0.63 99.06 154 297 38 307 15.0 8 10 19 70 17 46 <12 1468 <6 19.0 <10 121 58 9.62 L-834 59.92 0.47 16.55 4.88 0.00 0.05 0.10 1.72 0.29 14.06 0.12 1.28 99.44 283 70 49 274 20.0 7 <6 14 19 9 26 <12 1842 7.0 25.0 <10 12.06 41.53 111.4 192 54 2.88 7 7.3 0.700 2.450 1.28 14.35 L-835 65.67 0.65 15.35 3.98 0.00 0.08 0.87 2.29 4.41 4.48 0.19 1.44 99.41 135 203 38 342 15.0 <6 <6 7 68 17 40 <12 1318 <6 15.0 10 127 60 8.89 L-836 67.42 0.74 14.82 4.07 0.00 0.10 0.86 2.21 4.08 4.77 0.20 0.79 100.06 159 266 40 343 17.0 6 <6 19 69 0 45 <12 1272 0.0 0.0 0 0 0 8.85 L-838 67.61 0.61 14.50 3.84 0.00 0.09 0.82 2.37 3.62 4.48 0.18 0.50 98.62 208 69 22 93 15.6 <6 8 10 30 15 12 <12 552 4.0 21.2 <10 130 55 8.10 L-839 76.62 0.29 11.26 1.41 0.00 0.04 0.23 0.35 3.05 5.28 0.07 0.47 99.07 218 67 27 163 17.0 <6 9 19 35 13 12 <12 565 <6 16.0 <10 102 44 8.33 L-840 70.88 0.42 13.61 2.64 0.00 0.07 0.48 1.29 3.97 4.93 0.13 0.75 99.17 176 247 37 237 15.0 <6 8 20 47 16 20 <12 1054 <6 18.0 <10 127 62 8.90 L-842 65.32 0.68 14.27 4.45 0.00 0.10 1.13 2.64 4.17 3.50 0.19 2.76 99.21 141 316 38 361 16.0 10 11 37 83 16 49 13 1668 <6 16.0 12 11.19 33.40 82.63 135 41 1.48 62 .88 1.013 1.638 1.08 7.67 L-843 75.42 0.33 12.58 1.52 0.00 0.03 0.25 0.31 3.01 4.39 0.10 1.13 99.07 163 61 41 199 20.0 <6 <6 6 25 14 16 177 907 <6 21.0 <10 113.0 35.20 74.00 126 32 3.95 9.9 50 0.650 2.038 0.88 7.40 L-844 68.18 0.63 14.42 3.75 0.00 0.08 0.82 2.22 3.87 4.35 0.20 1.02 99.54 137 259 39 345 16.0 6 7 20 62 17 42 <12 1378 6.0 16.0 <10 129 63 8.22 L-846 67.61 0.60 14.35 3.72 0.00 0.08 0.89 1.97 4.09 4.59 0.18 0.78 98.86 134 246 44 306 16.0 6 10 18 56 15 39 <12 1240 <6 19.0 <10 11.76 41.76 86.50 133 45 50.38 1.000 1.913 1.088 8.68 L-849 73.54 0.33 12.99 1.74 0.00 0.02 0.20 0.14 3.78 5.57 0.04 0.55 98.90 189 43 24 243 27.0 <6 7 <6 22 18 17 217 451 <6 16.0 <10 107.3 30.33 47.9 152 20 1.013 33. 66 0.263 0.238 0.38 9.35 L-855 76.63 0.15 11.87 1.14 0.00 0.02 0.05 0.25 4.70 4.06 0.02 0.25 99.14 88 39 10 71 10.0 <6 10 9 11 15 <12 <12 328 <6 <15 <10 39 16 8.76 L-857 73.33 0.32 13.00 1.84 0.00 0.04 0.43 1.21 4.01 4.21 0.11 1.00 99.50 155 211 17 141 14.0 <6 9 26 28 15 22 <12 1081 <6 <15 <10 80 38 8.22 L-863 64.77 0.71 14.71 5.42 0.00 0.08 1.57 3.06 3.37 3.86 0.24 1.14 98.93 155 288 33 228 19.0 14 15 23 72 18 100 122 1004 <6 17.0 11 89 44 7.23 L-864 66.28 0.74 14.57 5.01 0.00 0.09 1.56 2.96 3.05 4.14 0.33 1.62 100.35 97 249 23 39 11.9 10 16 28 58 16 91 273 1039 3.1 13.4 10 17.4 6.19 37.8 9.86 78 45 0.83 1 .38 0.83 1.27 5.35 0.73 4.38 0.86 2.38 0.34 2.22 0.32 7.19 L-864 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0 0 0 0 0.0 0 0 0 0 <9 <6 <15 <10 23 <12 0.00 L-865 66.29 0.76 14.63 4.88 0.00 0.08 1.51 2.53 3.09 4.38 0.27 1.26 99.68 179 240 34 241 19.0 10 20 21 68 17 84 226 1100 <6 16.0 10 129 67 7.47 L-868 66.57 0.77 14.29 4.73 0.00 0.10 1.11 2.09 3.56 4.38 0.29 1.15 99.04 112 186 32 22 15.3 10 13 14 . 19 68 114 1100 <6 <15 10 14.6 8.72 52.03 13.28 154 79 1.07 0 .84 0.55 0 0 1.83 7.21 0.99 6.12 1.18 3.36 0.47 3.09 0.45 7.94 L-874 96.83 0.09 0.64 0.69 0.00 0.01 0.00 0.02 0.02 0.31 0.03 0.08 98.72 11 8 5 29 4.0 <6 13 8 6 17 <12 538 30 6.0 17.0 11 144 73 0.33 L-874a 67.47 0.89 13.68 4.67 0.00 0.10 1.05 1.71 3.48 4.99 0.27 1.09 99.40 155 181 57 348 24.0 12 14 19 69 63 17 1380 8.47 L-875 66.20 0.78 14.38 5.11 0.00 0.12 1.18 2.90 3.74 4.25 0.30 1.32 100.28 138 222 46 329 23.0 7 13 14 68 18 71 181 1294 <6 <15 10 12.16 42.90 111.4 157 54 76.63 1 .588 1.963 1.23 7.99 L-877 66.24 0.93 13.94 5.04 0.00 0.09 1.14 2.08 3.48 4.74 0.41 1.24 99.33 140 224 54 377 23.0 9 16 22 75 19 62 17 1371 <6 17.0 10 169 87 8.22 L-878 67.83 0.67 13.61 4.34 0.00 0.09 0.95 1.67 3.73 4.58 0.23 1.08 98.78 152 176 57 329 19.0 9 12 34 71 19 46 16 1143 <6 17.0 <10 12.29 39.36 92.38 150 41 56.10 1 .150 2.563 1.213 8.31 L-895 55.24 0.90 18.42 6.32 0.00 0.11 3.12 4.54 4.23 4.61 0.50 1.93 99.92 164 840 22 172 7.0 18 43 164 69 18 134 91 1382 <6 <15 14 8.250 23.24 53.84 74 22 98.63 0. 33 0.363 0.913 8.84 L-898 69.20 0.58 12.94 5.11 0.00 0.08 0.60 1.62 4.21 5.14 0.15 0.09 99.72 112 193 33 215 15.0 <6 7 17 46 27 189 1049 9.35 L-899 71.98 0.41 12.65 2.41 0.00 0.06 0.72 1.79 4.23 3.72 0.11 0.69 98.77 112 193 33 210 18.0 <6 7 17 46 17 26 182 1049 <6 16.0 <10 119 56 7.95 L-900 67.40 0.67 14.52 4.30 0.00 0.08 1.12 2.21 4.83 4.01 0.21 0.90 100.25 101 244 40 361 16.0 8 8 17 43 17 48 <12 1239 <6 16.0 11 127 61 8.84 L-902 77.60 0.17 12.00 0.96 0.00 0.02 0.08 0.11 4.16 4.81 0.10 0.34 100.35 160 35 18 95 22.0 <6 7 33 15 15 13 <12 131 <6 25.0 <10 85 39 8.97 L-903 79.24 0.19 10.48 1.02 0.00 0.02 0.12 0.14 2.98 4.99 0.04 0.32 99.54 262 21 23 103 16.0 <6 8 10 15 13 <12 <12 132 <6 25.0 <10 80 38 7.97 L-904 76.77 0.24 11.40 1.61 0.00 0.05 0.16 0.10 3.59 4.81 0.05 0.45 99.23 242 44 30 149 18.0 <6 8 15 37 15 <12 14 233 <6 21.0 <10 107.0 29.65 49.94 99 23 7.188 0.2 8 1.300 0.900 8.40 L-905 77.13 0.29 11.44 1.46 0.00 0.03 0.23 0.54 5.65 1.54 0.06 0.51 98.88 75 80 40 160 19.0 <6 9 17 23 13 13 <12 672 <6 22.0 <10 116 55 7.19 L-906 76.57 0.27 12.23 1.45 0.00 0.03 0.07 0.32 3.00 5.97 0.03 0.42 100.36 254 43 51 164 21.0 <6 7 37 14 13 <12 269 219 <6 19.0 <10 122 62 8.97 L-907 71.26 0.43 13.59 2.43 0.00 0.06 0.51 1.34 3.85 5.07 0.11 0.52 99.17 175 181 41 248 16.0 <6 8 11 44 15 24 <12 1136 <6 16.0 <10 135 69 8.92 L-908 66.78 0.41 16.95 1.82 0.00 0.08 0.28 0.22 9.57 2.63 0.03 0.34 99.11 96 28 10 66 15.5 <6 8 12 53 26 <12 <12 125 <6 15.0 <10 9.7 2.50 17.12 5.04 82 40 1.49 2.03 1.06 0 0 0.29 1.92 0.28 1.78 0.37 1.19 0.20 1.64 0.29 12.20 L-909 71.39 0.41 13.73 1.94 0.00 0.07 0.35 0.72 4.37 4.96 0.08 0.91 98.93 153 134 46 285 18.0 <6 8 25 56 17 15 <12 1346 <6 18.0 <10 163 82 9.33 L-910 70.84 0.59 13.17 3.28 0.00 0.04 0.51 0.53 4.21 4.24 0.20 1.11 98.72 129 126 44 360 17.0 <6 8 12 47 16 26 <12 1115 <6 <15 <10 152 76 8.45 L-911 72.60 0.37 14.49 2.24 0.00 0.03 0.81 0.22 0.16 5.19 0.11 2.40 98.62 170 16 45 344 27.0 <6 10 33 48 19 17 139 398 <6 19.0 <10 145 75 5.35 L-912 73.33 0.37 13.50 1.75 0.00 0.02 0.70 0.22 2.05 5.30 0.08 1.55 98.87 139 29 38 273 20.0 <6 7 9 34 17 15 <12 787 <6 16.0 <10 148 47 7.35 L-917 71.65 0.73 12.99 3.87 0.00 0.08 1.25 0.71 3.95 4.48 0.20 0.63 100.54 113 116 16 39 15.2 6 12 17 50 15 46 15 967 <6 <15 <10 13.4 5.26 30.24 7.86 85 42 1.40 1.3 6 0.92 0 0 1.04 4.56 0.63 3.72 0.68 1.87 0.27 1.86 0.27 8.43 L-919 87.60 0.31 4.60 3.09 0.00 0.03 0.08 0.09 0.12 2.09 0.04 0.79 98.84 79 9 11 99 8.0 6 15 13 14 <9 27 32 297 <6 <15 <10 55 26 2.21 L-920 36.93 0.23 6.77 1.19 0.00 0.03 0.22 0.29 2.90 2.72 0.06 49.01 100.35 124 81 20 208 15.0 <6 <6 16 29 14 17 134 1088 <6 <15 <10 113.1 35.71 61.91 99 29 18.89 0 .663 0.200 0.700 5.62 L-922 68.49 0.77 14.39 4.18 0.00 0.07 0.89 1.69 3.76 4.88 0.23 0.98 100.33 143 206 56 426 27.0 8 9 15 58 18 56 244 1598 <6 16.0 10 22.13 52.85 122.3 159 56 61.63 1 .73 4.29 2.488 1.13 8.64 L-923 70.32 0.62 13.18 3.95 0.00 0.06 0.59 0.92 4.03 4.67 0.17 1.02 99.53 162 156 56 425 21.0 6 12 11 55 18 37 <12 1168 <6 21.0 <10 159 89 8.70 L-924 71.99 0.63 12.33 2.83 0.00 0.05 0.57 1.46 3.58 3.97 0.13 1.69 99.23 82 63 46 359 22.0 8 9 14 26 15 38 <12 1811 <6 19.0 <10 158 79 7.55 L-938 70.06 0.58 13.36 3.13 0.00 0.05 0.58 1.70 4.16 4.11 0.19 0.90 98.82 76 244 38 294 19.0 6 7 11 44 16 40 266 1785 <6 <15 <10 23.8 117.0 49.23 83.50 96 37 1.37 3 .22 38.46 1.43 3.22 0.53 3.70 0.77 2.40 0.39 1.213 0.888 8.27 L-939 68.27 0.56 15.25 3.83 0.00 0.08 0.63 1.89 3.55 5.28 0.14 0.74 100.22 132 422 22 166 11.0 15 16 29 68 16 89 23 1059 <6 <15 11 8.33 30.34 57.99 77 28 77.50 0.5 8 0.93 8.83 L-940 62.87 0.57 14.38 5.03 0.00 0.09 1.98 6.05 4.02 3.40 0.20 0.69 99.28 133 422 23 173 12.0 14 13 22 64 18 94 17 1043 <6 <15 11 9.050 25.39 64.13 90 31 79.8 0.43 0.638 0.98 7.42 L-943 74.31 0.15 13.23 1.77 0.00 0.04 0.03 0.75 3.70 5.72 0.11 0.29 100.10 137 123 4 65 7.2 <6 9 19 17 14 13 15 350 <6 28.0 <10 18.5 0.91 6.77 2.16 42 20 2.27 3.29 0 .51 0 0 0.15 0.72 0.10 0.64 0.14 0.46 0.09 0.83 0.17 9.42 L-945 67.85 0.52 15.01 3.25 0.00 0.07 0.55 1.40 4.19 5.08 0.11 0.92 98.95 169 235 45 386 18.0 9 8 20 64 18 2 13 1409 <6 19.0 <10 12.43 41.88 115.1 178 53 61.16 0.8 50 1.663 2.463 1.13 9.27 L-946 67.96 0.48 14.78 2.89 0.00 0.06 0.59 1.58 4.39 5.01 0.12 0.73 98.59 165 232 38 250 19.0 6 8 8 45 16 30 185 1451 <6 <15 <10 175 88 9.40 L-948 70.39 0.65 13.17 3.48 0.00 0.11 0.62 1.58 4.48 4.47 0.13 0.41 99.49 160 174 63 368 21.0 7 8 10 73 17 22 <12 1424 <6 15.0 <10 175 92 8.95 L-951 66.61 0.52 15.75 3.69 0.00 0.02 0.04 0.50 11.34 0.33 0.12 0.19 99.11 4 30 50 261 24.0 <6 10 6 9 16 39 137 <20 <6 22.0 <10 10.83 28.36 109.6 166 14 48.54 0.71 3 3.138 1.888 1.088 11.67 L-952 67.68 0.59 15.55 4.09 0.00 0.02 0.15 0.73 10.86 0.35 0.15 0.22 100.39 6 38 36 308 23.0 <6 9 6 10 16 31 173 52 <6 <15 <10 38 27 11.21 Table No. A9 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGIO N PAGE 9/14 Kamanjab Inlier, Namibia (cont. ) Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-955 67.86 0.41 16.46 3.50 0.00 0.05 0.11 0.33 10.16 0.19 0.23 0.82 100.12 4 37 40 340 17.0 <6 13 333 ## 21 36 <12 30 <6 <15 16 13.3 62.33 671.3 965 405 42.79 0.4 00 1.788 1.03 10.35 L-956 61.48 2.00 9.60 15.05 0.00 0.04 0.23 2.72 7.38 0.01 0.92 0.23 99.66 5 36 63 321 14.0 9 11 7 17 17 91 <12 51 <6 <15 24 41.30 97.50 116 63 297.1 3.050 2.13 7.39 L-957 75.71 0.31 11.71 1.52 0.00 0.04 0.21 1.09 2.90 4.90 0.05 0.66 99.10 126 135 32 207 20.0 <6 7 <6 36 14 <12 228 571 <6 26.0 <10 112.1 34.19 59.59 156 79 3.20 7 .188 0.28 0.338 0.68 7.80 L-958 47.73 1.22 15.13 13.06 0.00 0.23 7.23 8.03 3.57 0.36 0.22 2.21 98.99 5 188 34 105 5.0 63 122 59 ## 19 296 107 297 <6 <15 37 15 <12 3.93 L-963 88.82 0.21 4.22 2.07 0.00 0.03 0.19 0.14 1.00 1.77 0.06 0.66 99.17 63 17 18 133 8.0 8 11 20 15 <9 25 12 308 <6 <15 <10 64 31 2.77 L-965 67.45 0.59 13.65 6.24 0.00 0.03 0.32 0.69 4.10 5.73 0.19 0.42 99.41 156 43 88 358 29.0 <6 11 8 24 17 33 12 741 7.00 30.0 <10 125 56 9.83 L-966 68.15 0.60 12.90 6.30 0.00 0.02 0.16 0.43 4.46 5.68 0.19 0.27 99.16 144 39 74 108 17.1 <6 9 6 19 16 42 193 708 5.82 27.2 <10 17.8 6.29 34.8 9.84 103 45 0.41 3 .12 1.20 0.89 7.00 1.36 10.3 2.34 7.51 1.13 7.93 1.21 10.14 L-967 70.72 0.48 12.92 3.64 0.00 0.07 0.46 1.11 3.78 5.05 0.12 0.63 98.98 269 119 83 395 22.0 8 9 13 60 17 31 <12 883 8.00 36.0 <10 259 130 8.83 L-967a 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0 0 0 0 0.0 0 0 0 0 15 0 0 0 <6 20.0 <10 153 119 0.00 L-968 72.13 0.34 13.69 2.21 0.00 0.03 0.17 0.89 3.99 4.79 0.05 0.51 98.80 136 145 37 225 15.0 7 9 20 86 15 16 <12 1370 <6 23.0 <10 110.0 16.73 28.51 110 11 2.86 26 .16 0.488 0.763 8.78 L-969 59.46 0.49 19.16 4.28 0.00 0.05 0.68 0.38 0.55 14.31 0.08 0.84 100.28 393 66 59 293 24.0 6 <6 47 53 22 61 <12 2451 6.00 29.0 <10 10.51 36.03 92.38 159 37 7. 20 60.24 0.663 3.050 1.288 14.86 L-971 64.34 0.54 17.73 1.51 0.00 0.09 0.14 0.68 4.58 8.51 0.11 0.69 98.92 148 66 47 358 22.0 <6 9 10 14 13 34 <12 2236 <6 <15 <10 137 81 13.09 L-973 71.06 0.42 12.34 2.89 0.00 0.04 0.12 1.90 0.51 9.97 0.09 0.97 100.31 266 42 47 249 19.0 6 <6 141 70 9 28 12 1800 <6 18.0 <10 9.588 33.88 96.50 128 42 5.85 36 .50 0.500 3.23 1.138 10.48 L-975 72.48 0.35 13.19 2.05 0.00 0.06 0.27 0.82 3.81 5.40 0.10 0.56 99.09 164 149 34 215 16.0 7 9 45 47 14 19 <12 1327 <6 21.0 <10 137 68 9.21 L-976 72.48 0.37 13.10 1.84 0.00 0.04 0.29 0.71 4.00 5.29 0.06 0.50 98.68 195 113 55 203 21.0 <6 10 8 29 18 209 1114 115.8 48.35 91.8 71 3.23 13.38 1.03 2.213 2. 93 1.08 9.29 L-977 74.68 0.27 11.99 1.72 0.00 0.04 0.24 0.55 3.86 5.21 0.04 0.45 99.05 121 81 27 197 13.0 <6 8 <6 39 15 12 <12 766 <6 16.0 <10 110 57 9.07 L-978 76.43 0.22 11.10 2.76 0.00 0.10 0.04 0.28 4.16 5.19 0.05 0.18 100.51 139 58 15 133 16.9 <6 10 37 73 20 14 20 264 3.59 19.1 <10 21.3 2.08 13.4 4.14 50 25 0.75 5.11 1.02 0.29 1.79 0.29 2.06 0.48 1.79 0.33 2.76 0.49 9.35 L-979 66.06 0.48 15.03 3.97 0.00 0.09 1.33 3.18 4.23 3.67 0.14 0.79 98.97 108 435 35 143 15.0 10 10 76 88 16 68 242 1077 <6 <15 11 92 44 7.90 L-980 67.03 0.53 15.05 4.32 0.00 0.09 1.37 3.20 4.47 3.48 0.18 0.77 100.49 115 424 32 157 17.0 10 15 28 62 17 72 200 1140 <6 <15 <10 104 52 7.95 L-982 66.31 0.56 15.11 3.80 0.00 0.09 1.18 3.09 4.72 3.57 0.19 0.80 99.42 99 495 25 176 12.0 11 10 11 56 17 54 <12 1245 <6 <15 <10 8.588 26.96 66.38 74 30 53.76 0. 363 0.550 0.83 8.29 L-983 72.59 0.29 13.57 1.83 0.00 0.04 0.07 0.90 4.08 4.95 0.04 0.51 98.87 197 156 28 181 17.0 <6 6 7 32 15 13 <12 963 <6 19.0 <10 90 39 9.03 L-985 72.90 0.46 12.76 2.61 0.00 0.05 0.29 1.39 3.72 4.25 0.06 0.63 99.12 123 219 5 51 6.1 <6 7 9 46 14 25 173 1580 1.49 17.1 <10 25.6 3.41 33.2 9.78 103 61 2.13 1. 48 0.19 1.09 2.00 0.20 0.97 0.17 0.46 0.07 0.54 0.10 7.97 L-987a 45.74 2.33 16.73 14.31 0.00 0.17 4.10 10.53 2.62 1.59 0.46 1.99 100.57 22 598 11 18 1.9 41 8 75 ## 17 429 <12 397 <6 <15 36 7.7 2.50 10.86 2.08 <12 <12 0.29 0.51 0.03 0 0 1.03 2.95 0.39 2.37 0.46 1.20 0.15 0.92 0.13 4.21 L-987b 40.92 2.62 19.28 13.71 0.00 0.19 4.13 12.81 2.45 0.79 1.19 2.06 100.15 35 646 19 31 4.0 28 <6 37 72 17 307 <12 284 <6 <15 32 7.100 29.40 16 5 284.3 1.338 3. 24 L-990 53.79 0.31 13.92 7.16 0.00 0.15 8.22 7.59 5.52 0.32 0.10 2.29 99.37 10 267 12 84 10.0 38 178 73 69 13 75 584 187 <6 <15 20 39 22 5.84 L-991 48.45 0.96 11.97 11.52 0.00 0.19 11.57 9.20 3.07 0.46 0.12 1.70 99.21 7 217 20 53 9.0 64 251 83 93 12 255 870 188 <6 <15 35 19 12 3.53 L-992 50.94 0.49 19.38 7.11 0.00 0.15 5.16 9.79 3.16 1.87 0.09 2.25 100.39 67 659 10 28 3.4 27 53 35 53 16 144 100 460 0.24 0.9 26 4.4 1.92 9.78 2.25 19 9 0.49 0.75 0.13 0.79 2.03 0.30 1.93 0.39 1.11 0.16 1.04 0.15 5.03 L-993 71.34 0.39 13.57 2.03 0.00 0.05 0.39 1.42 3.97 5.33 0.07 0.81 99.37 115 224 27 75 11.5 <6 6 8 34 15 24 160 1595 <6 17.0 <10 22.5 7.25 47.18 12.68 139 69 0.45 2.38 0.59 0 0 1.21 5.76 0.82 5.12 1.00 2.86 0.42 2.84 0.41 9.30 L-994 70.70 0.40 13.83 2.09 0.00 0.05 0.43 1.46 3.95 5.07 0.09 0.73 98.80 110 226 37 208 19.0 6 7 10 33 15 32 195 1763 <6 <15 <10 142 70 9.02 L-995 39.21 3.69 11.13 22.15 0.00 0.26 7.20 10.83 1.60 0.53 1.13 1.13 98.86 14 449 21 27 4.0 59 <6 54 ## 19 491 <12 457 <6 <15 45 <12 <12 2.13 L-996 69.95 0.44 14.71 2.86 0.00 0.06 0.50 1.75 4.30 4.78 0.11 0.95 100.41 121 274 24 78 13.9 6 9 67 71 16 30 <12 1498 2.82 14.9 <10 23.0 6.17 39.6 10.8 113 49 0.6 9 2.30 0.83 1.22 4.96 0.74 4.69 0.93 2.78 0.42 2.93 0.42 9.08 L-997 69.62 0.34 15.29 1.59 0.00 0.04 0.27 0.51 5.88 5.33 0.05 0.73 99.65 135 65 57 241 22.0 8 9 8 24 16 19 <12 542 <6 33.0 <10 111.4 28.71 57.06 156 21 4.188 11.0 6 2.450 0.950 11.21 L-998 64.78 0.73 15.67 4.59 0.00 0.11 1.41 2.78 4.52 4.03 0.24 1.33 100.19 103 300 34 347 15.0 6 9 29 96 18 53 13 2134 <6 <15 10 10.00 32.01 78.50 106 38 63.00 0.9 38 1.038 1.03 8.55 L-999 67.68 0.49 14.73 3.02 0.00 0.07 0.74 1.83 4.31 4.65 0.13 1.19 98.84 140 252 37 288 20.0 <6 9 10 58 17 33 205 1537 <6 16.0 <10 9.700 36.04 91.88 144 44 1.53 3 9.16 0.83 1.488 0.888 8.96 L-1000 67.91 0.47 15.37 2.32 0.00 0.06 0.52 1.06 4.28 5.11 0.10 1.68 98.88 192 112 37 251 18.0 <6 10 62 58 17 35 <12 1206 <6 20.0 <10 11.6 90.10 152.3 134 80 82 3. 48 2.58 1.200 9.39 L-1002 77.59 0.26 11.61 1.64 0.00 0.05 0.10 0.32 3.59 4.97 0.03 0.33 100.49 180 40 25 134 22.0 <6 8 6 14 14 10 <12 180 <6 28.0 <10 104.0 18.61 52.50 87 26 3.35 5.3 88 1.600 0.93 8.56 L-1003 68.00 0.50 15.07 2.73 0.00 0.05 0.58 1.60 4.64 5.26 0.12 0.69 99.24 145 242 40 289 16.0 <6 8 12 47 17 32 <12 1796 <6 15.0 <10 8.450 28.94 79.13 133 26 2.58 31.71 0.78 1.713 0.950 9.90 L-1005 71.20 0.48 12.46 3.35 0.00 0.06 0.56 1.47 3.93 4.47 0.18 0.76 98.92 171 218 46 298 18.0 7 9 15 50 17 26 16 1194 <6 18.0 <10 132 64 8.40 L-1007 64.26 0.56 15.15 5.20 0.00 0.10 1.92 3.56 4.03 3.92 0.20 0.55 99.45 169 234 45 318 16.0 7 10 22 61 17 38 <12 1413 <6 22.0 <10 160 78 7.95 L-1009 66.67 0.69 15.06 4.31 0.00 0.09 1.05 2.81 4.12 4.42 0.26 0.88 100.36 129 347 38 354 15.0 7 7 18 71 17 53 <12 1757 <6 16.0 10 115 55 8.54 L-1010 63.36 0.80 15.40 5.08 0.00 0.11 1.26 3.27 4.15 4.24 0.34 1.17 99.18 138 385 37 372 15.0 9 10 21 74 18 53 <12 1944 <6 <15 12 110 55 8.39 L-1011 66.33 0.64 14.74 3.94 0.00 0.09 0.94 2.72 4.53 4.43 0.19 0.82 99.37 152 302 38 308 20.0 7 9 21 73 17 50 126 1322 <6 17.0 10 129 66 8.96 L-1012 64.77 0.68 15.28 4.30 0.00 0.20 0.95 3.01 5.41 3.94 0.20 0.97 99.71 132 337 42 332 22.0 8 10 9 ## 17 53 105 1550 <6 17.0 <10 139 74 9.35 L-1013 67.41 0.61 14.33 4.04 0.00 0.08 0.94 2.09 4.00 4.72 0.21 0.95 99.38 171 240 39 331 16.0 6 10 26 67 17 47 <12 1290 <6 19.0 <10 108.4 40.58 79.3 131 35 48.23 0.638 1.738 0.98 8.72 C-1 74.03 0.27 12.73 1.15 1.51 0.05 0.31 0.48 3.67 5.09 0.05 0.71 100.05 100 50 70 500 30.0 <10 <10 n.d 25 <3 10 1200 25.0 95 <100 <3 <3 <3 0 <3 8.76 C-2 69.71 0.68 14.17 1.69 1.57 0.04 0.84 0.82 4.10 5.30 0.27 0.67 99.86 70 110 45 550 30.0 25 35 25 2100 8.0 90 35 9.40 C-3 68.63 0.67 15.43 1.74 1.03 0.10 0.51 1.99 4.50 4.42 0.18 0.50 99.70 90 350 ## 700 40.0 25 35 11 2500 25.0 130 30 8.92 C-4 73.63 0.33 14.16 1.13 0.24 0.02 0.00 0.50 3.14 6.35 0.07 0.44 100.01 200 80 20 380 20.0 20 9 13 1200 40.0 95 11 9.49 C-5 75.35 0.27 13.18 1.08 0.22 0.02 0.00 0.62 3.15 5.50 0.05 0.36 99.80 110 100 35 280 10.0 20 5 15 1400 30.0 65 12 8.65 C-6 66.09 0.69 14.60 3.06 1.72 0.08 1.81 2.54 3.25 4.71 0.28 1.11 99.94 150 480 25 280 <10 20 85 18 1900 14.0 75 25 7.96 C-7 69.29 0.47 14.55 1.81 1.48 0.06 1.19 2.83 3.33 4.40 0.17 0.46 100.04 230 650 25 320 10.0 19 70 35 1700 16.0 70 13 7.73 C-8 73.88 0.33 13.85 0.87 0.24 0.03 0.18 0.26 4.05 5.93 0.09 0.39 100.10 130 40 55 450 15.0 20 7 11 400 20.0 65 4 9.98 C-9 73.30 0.32 13.20 2.93 0.48 0.01 0.00 0.24 3.46 5.67 0.07 0.34 100.02 130 50 80 650 30.0 30 <3 14 1200 12.0 85 9 9.13 C-10 68.63 0.49 15.01 1.62 1.44 0.07 1.22 2.74 4.41 3.60 0.20 0.57 100.00 65 720 25 230 <10 20 55 30 1900 18.0 70 20 8.01 C-11 78.84 0.29 10.79 0.95 0.27 0.03 0.09 0.60 2.94 5.20 0.06 0.22 100.28 120 65 55 180 18.0 15 5 25 560 20.0 100 <3 8.14 C-13 ( w 75.89 0.41 12.46 1.07 0.13 n.d. 0.05 0.25 3.60 5.71 0.04 0.50 100.11 100 40 65 650 40.0 <10 <10 n.d. 25 <3 10 1000 30.0 90 <100 <3 <3 <3 0 <3 9.31 C-14 48.69 1.26 13.27 4.86 8.71 0.18 6.15 10.49 2.41 1.05 0.22 0.50 97.79 3.46 Table No. A10 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGION PAGE 10/14 Felsic volcanics, Namibia Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 X-16 75.93 0.26 12.08 2.96 0.32 0.01 0.36 0.48 7.93 0.13 0.07 0.42 100.95 8.06 X-17 72.07 0.33 13.36 3.76 0.25 0.02 1.33 1.01 7.95 0.30 0.04 0.49 100.91 8.25 X-18 69.24 12.00 0.55 3.83 5.36 0.00 90.98 9.19 X-19 72.02 0.32 13.78 2.24 1.02 0.02 0.20 0.39 4.07 5.18 0.03 0.65 99.92 9.25 X-20 76.01 0.23 12.05 0.80 0.91 0.03 0.20 1.02 3.09 5.02 0.01 1.14 100.51 8.11 Ugab River, Namibia Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-793 74.92 0.33 12.39 2.15 0.00 0.08 0.24 1.00 3.28 5.24 0.14 0.37 100.14 251 140 81 213 78.0 <6 7 7 34 19 22 390 435 12.00 61.0 <10 119.3 50.99 175.4 234 98 1.8 00 28.5 0.938 6.63 1.700 8.52 L-797 75.11 0.21 13.05 1.92 0.00 0.04 0.08 0.51 3.62 4.63 0.08 0.61 99.86 225 107 23 199 38.0 <6 6 <6 33 21 17 372 658 6.00 37.0 <10 132 76 8.25 L-798 72.64 0.26 14.07 2.13 0.00 0.08 0.26 1.09 3.42 5.17 0.12 0.91 100.15 222 204 26 229 48.0 <6 <6 <6 40 20 16 285 1117 7.00 27.0 <10 211 102 8.59 L-799 73.13 0.08 13.93 1.96 0.00 0.06 0.04 0.95 3.84 4.84 0.13 0.63 99.59 153 168 53 183 14.0 <6 7 11 19 18 29 326 727 7.00 <15 <10 102 36 8.68 L-802 73.34 0.23 14.56 1.83 0.00 0.05 0.29 1.08 3.46 4.55 0.13 0.84 100.36 234 141 32 142 41.0 <6 6 <6 51 19 22 260 745 <6 15.0 <10 77 38 8.01 Owka River, Botswana Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-600A 76.09 0.13 11.83 1.93 0.00 0.04 0.07 0.45 3.85 5.55 0.06 0.40 100.40 160 59 23 137 14.0 <6 6 14 29 15 <12 68 508 <6 43.0 <10 141 77 9.40 L-602 70.15 0.49 13.13 3.63 0.00 0.06 0.83 1.80 3.43 4.54 0.16 0.98 99.20 214 137 64 305 26.0 8 7 9 60 18 13 189 716 <6 36.0 <10 14.31 62.39 169.4 213 86 53.19 0.8 13 4.213 1.338 7.97 L-605 76.55 0.12 12.03 1.16 0.00 0.01 0.02 0.81 3.42 5.47 0.07 0.41 100.07 198 99 7 89 7.0 <6 <6 9 19 13 <12 227 772 <6 42.0 <10 148 102 8.89 L-606 72.56 0.36 12.83 3.51 0.00 0.06 0.48 1.32 3.22 5.19 0.07 0.73 100.33 185 105 38 202 17.0 <6 6 7 61 18 20 57 781 <6 38.0 <10 227 149 8.41 Summas Mountains, Namibia, (Volcanic Rocks ) Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-789 63.91 1.38 14.35 7.45 0.00 0.07 1.13 1.09 4.87 5.21 0.41 0.55 100.42 125 29 66 715 149.0 <6 6 10 80 21 32 135 1019 8.00 15.0 <10 15.46 50.01 136.3 196 67 12 7.6 2.03 3.88 1.58 10.08 L-791a 72.44 0.40 13.01 3.67 0.00 0.06 0.32 0.54 3.80 5.16 0.10 0.61 100.11 141 25 97 685 130.0 <6 7 <6 35 17 <12 220 637 6.00 32.0 <10 109 22.50 36.51 63 18 2.04 7.288 0.438 5.688 1.400 8.96 L-791b 76.38 0.14 12.55 1.25 0.00 0.02 0.00 0.51 3.09 5.85 0.03 0.29 100.11 270 74 83 70 65.0 <6 10 <6 15 22 16 234 332 8.00 17.0 <10 224 108 8.94 Table No. A11 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGION PAGE 11/14 Oas Farm, Namibia Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-668 62.61 0.89 17.32 4.83 0.00 0.14 0.72 1.80 6.42 4.79 0.36 0.59 100.47 121 474 69 710 193.0 7 7 6 ## 26 14 139 2037 7.0 22.0 <10 13.58 101.4 182.0 235 110 4.4 5 23.33 0.850 3.85 2.38 1.03 11.21 L-669 64.34 0.61 16.76 4.66 0.00 0.12 0.36 1.46 6.43 4.80 0.23 0.74 100.51 115 350 73 378 204.4 <6 9 7 ## 28 <12 124 1647 9.0 31.0 <10 21.7 17.80 102.1 28.00 267 137 0.70 8.24 12.29 0 0 3.96 14.64 2.26 14.05 2.62 7.39 1.00 5.97 0.73 11.23 L-670 57.01 1.45 15.14 11.08 0.00 0.21 1.42 2.33 6.69 3.35 0.53 1.32 100.53 173 1219 73 1843 458.0 <6 9 9 85 42 <12 18 767 17.0 46.0 <10 3.13 27.46 72.13 219 42 7 4.00 0.288 2.088 0.988 10.04 L-675 60.71 0.10 21.99 3.59 0.00 0.09 0.13 0.94 4.92 6.41 0.03 1.61 100.52 125 384 ## 1520 345.0 7 9 23 ## 30 20 17 1321 10.0 78.0 11 140.0 591.5 844 440 238.0 3. 438 4.23 6.513 1.98 11.33 L-676 59.35 0.87 18.13 5.92 0.00 0.17 1.24 2.05 5.20 5.55 0.24 1.84 100.56 226 634 58 553 139.0 7 7 11 ## 26 19 31 1591 <6 19.0 <10 180 85 10.75 L-691 50.24 3.31 12.95 14.15 0.00 0.21 4.13 6.53 2.95 2.82 0.55 1.51 99.35 151 589 52 368 62.0 39 32 190 ## 19 357 66 617 <6 <15 33 110 61 5.77 L-693 71.37 0.48 11.65 6.47 0.00 0.14 0.19 0.77 4.62 4.46 0.09 0.31 100.55 86 98 31 132 105.3 6 7 14 ## 33 <12 60 241 2.3 8.6 <10 4.8 13.2 114 35.3 357 216 0.23 2.8 1 4.94 0.94 7.69 0.92 5.26 0.97 2.65 0.43 3.26 0.54 9.08 L-694 59.18 1.09 17.07 5.91 0.00 0.17 1.01 2.48 6.84 4.89 0.36 0.54 99.54 106 633 39 333 93.0 7 <6 10 ## 23 27 <12 1995 <6 <15 <10 166 87 11.73 L-695 46.29 3.29 13.34 13.54 0.00 0.48 3.19 4.92 4.10 3.51 0.68 6.78 100.12 197 399 53 329 54.0 27 22 89 ## 19 353 28 639 <6 <15 26 64 30 7.61 L-697 59.94 0.86 16.90 5.28 0.00 0.17 0.99 2.06 6.58 4.59 0.32 1.54 99.23 169 491 ## 1363 432.0 8 9 5 ## 26 <12 117 1444 15.0 51.0 <10 127.3 480.3 582 291 1.713 1 07.9 4.550 15.49 10.2 2.08 11.17 L-698 71.68 0.46 11.40 5.84 0.00 0.10 0.10 0.85 4.91 4.10 0.10 0.40 99.94 77 45 50 329 124.0 <6 7 7 ## 35 <12 207 157 <6 <15 <10 16.00 66.88 227.6 372 143 92.13 0. 250 2.03 1.338 9.01 L-699 63.41 0.28 17.28 5.27 0.00 0.20 0.34 0.93 7.40 4.73 0.12 0.56 100.52 98 114 75 1246 307.0 <6 10 7 ## 34 <12 126 458 15.0 50.0 <10 470 310 12.13 L-708 47.15 0.47 8.72 11.27 0.00 0.53 13.12 14.15 1.46 1.77 0.04 1.79 100.47 86 578 ## 469 126.0 16 26 13 ## 17 68 14 2096 <6 <15 23 258 97 3.23 L-712 79.11 0.04 12.04 0.83 0.00 0.04 0.11 0.40 5.47 1.95 0.01 0.54 100.54 33 159 12 17 7.0 <6 10 8 35 18 <12 47 662 <6 <15 <10 107 13.44 41 7 1.700 0.213 0.638 7.4 2 L-713 71.32 0.16 14.36 2.37 0.00 0.05 0.08 0.32 5.76 5.66 0.02 0.41 100.51 117 94 30 277 71.0 <6 8 9 53 25 19 49 909 <6 <15 <10 120.8 80.38 294.6 436 188 0.96 24.5 4 0.763 1.200 0.88 11.42 L-714 77.55 0.05 13.19 0.73 0.00 0.03 0.17 0.85 6.33 0.76 0.02 0.67 100.35 16 338 9 250 9.0 <6 9 8 40 23 <12 50 538 <6 16.0 <10 106.0 2.950 83 3.213 0.188 0.488 7. 09 L-714a 74.47 0.12 14.63 0.94 0.00 0.04 0.12 0.59 8.15 0.94 0.05 0.41 100.46 16 152 25 237 50.0 <6 8 <6 17 0 12 160 606 0.0 0.0 0 0 0 9.09 L-715 72.13 0.48 13.02 3.49 0.00 0.09 0.48 1.12 3.88 4.88 0.12 0.50 100.19 118 147 58 348 25.0 8 11 12 67 18 28 47 1230 <6 19.0 <10 75.8 38.91 87.88 154 44 38.90 1 .13 3.588 1.363 8.76 L-716 73.88 0.30 12.54 2.79 0.00 0.04 0.41 0.98 4.49 3.98 0.04 0.68 100.13 69 164 38 332 15.9 8 11 12 51 16 19 57 1389 7.0 24.0 <10 9.2 7.00 41.87 11.18 134 66 0.8 3 6.58 0.73 0 0 1.48 5.96 0.90 6.07 1.28 4.03 0.63 4.55 0.70 8.47 L-1016 77.33 0.10 1.04 2.18 0.00 0.47 2.02 6.71 0.50 0.09 0.13 8.00 98.57 6 124 8 15 4.0 <6 <6 56 14 <9 <12 351 33 <6 <15 12 24 <12 0.59 L-1016 a 79.38 0.10 0.80 2.49 0.00 0.45 1.96 5.74 0.55 0.13 0.04 7.50 99.14 5 140 6 37 4.0 <6 7 28 27 <9 13 15 57 <6 <15 10 23 <12 0.68 L-1019 72.23 0.41 13.17 3.00 0.00 0.11 0.24 0.79 6.18 3.79 0.08 0.41 100.41 50 101 31 290 46.9 <6 10 9 62 17 <12 253 1351 1.8 17.0 <10 29.0 7.79 47.2 12.5 110 60 0 .15 7.31 2.12 2.05 6.81 0.95 5.85 1.15 3.36 0.49 3.38 0.50 9.97 L-1020 70.82 0.58 12.68 4.01 0.00 0.10 0.76 1.57 5.17 3.14 0.09 0.31 99.23 70 173 52 445 22.0 <6 8 64 85 17 19 <12 1364 <6 19.0 <10 180 95 8.31 X-21 60.78 0.87 16.97 1.13 4.10 0.16 0.99 1.94 5.65 5.27 0.22 1.78 99.86 10.92 X-22 64.42 1.12 14.69 4.34 1.80 0.07 1.37 1.17 3.71 5.64 0.25 1.78 100.36 9.35 X-23 63.81 0.59 14.21 3.67 1.10 0.15 1.48 2.27 4.37 6.00 0.09 3.13 100.87 10.37 X-24 51.29 0.40 19.06 5.95 1.05 0.42 0.82 4.79 6.75 5.19 0.30 3.38 99.40 11.94 X-25 47.49 2.22 14.47 3.74 8.09 0.05 6.73 11.57 1.24 0.77 0.30 2.80 99.47 2.01 X-26 48.82 1.03 12.21 3.62 6.54 0.15 13.68 9.63 1.77 1.10 0.59 1.16 100.30 2.87 Table No. A12 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGION PAGE 12/14 Lofdal Farm, Namibia Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-722 7.50 0.04 0.13 9.55 0.00 0.68 2.58 43.77 0.00 0.00 0.03 36.2 100.52 7 210 ## 119 13.0 23 <6 5 37 <9 194 12 145 6.00 27.0 54 17.16 15.61 10 <12 229.3 0.263 0. 863 0.00 L-728 75.06 0.16 10.35 2.83 0.00 0.14 0.22 2.20 6.61 0.86 0.06 2.04 100.53 23 140 58 212 33.0 <6 10 15 45 18 14 67 581 4.64 20.9 15 24.2 17.2 82.2 20.2 171 73 0.33 6.35 2.52 3.25 14.4 2.01 12.1 2.23 6.18 0.99 6.52 1.07 7.47 L-729 73.58 0.31 12.64 2.31 0.00 0.05 0.34 0.84 3.69 4.96 0.03 1.70 100.45 113 82 46 281 24.0 <6 6 6 60 <12 58 957 8.65 L-740 56.74 0.26 18.91 5.92 0.00 0.18 0.21 1.03 6.29 4.68 0.03 6.26 100.51 170 442 26 1803 563.0 <6 11 8 ## 42 <12 27 617 27.0 18.0 <10 8.750 22.20 71.88 112 36 1 14.8 0.500 0.138 0.838 10.97 L-741 56.63 0.47 19.54 7.23 0.00 0.44 0.80 3.09 4.14 7.21 0.11 0.91 100.57 169 548 49 640 337.0 <6 <6 14 ## 34 14 18 1955 19.00 <15 <10 14.68 51.69 210.8 248 131 127.0 1.813 1.863 1.100 11.35 L-742 68.41 0.18 10.00 3.45 0.00 0.20 2.09 0.90 5.40 1.17 0.03 8.44 100.27 59 181 41 310 26.0 11 13 32 ## 19 18 44 802 <6 21.0 <10 2.538 32.53 52.30 79 44 71.88 0. 588 1.350 0.600 6.57 L-754 53.02 1.59 13.32 16.18 0.00 0.28 6.53 7.50 0.32 1.02 0.30 0.15 100.21 318 84 40 94 8.0 50 53 94 ## 17 393 178 235 <6 <15 49 25 12 1.34 L-1021 72.02 0.43 12.86 3.47 0.00 0.05 0.24 1.10 4.37 4.02 0.07 0.53 99.16 83 92 84 464 33.0 <6 8 5 29 17 <12 250 1355 <6 18.0 <10 143 61 8.39 L-1022 54.76 0.44 20.41 5.90 0.00 0.20 0.33 1.95 4.97 7.25 0.13 2.78 99.12 189 616 24 767 249.0 7 <6 11 ## 36 14 <12 629 8.00 <15 <10 2.638 27.54 47.69 61 19 94.3 8 0.38 0.763 12.22 L-1023 47.51 0.82 15.70 11.39 0.00 0.21 7.63 10.97 2.78 0.87 0.09 2.31 100.28 19 177 23 45 5.0 51 86 11 ## 19 246 354 223 <6 <15 42 33 20 3.65 L-1024 a 7.58 0.07 0.57 9.33 0.00 0.79 5.76 37.24 0.03 0.15 0.23 38.8 100.50 6 335 62 9 44.1 28 21 177 59 <9 23 <12 115 19.00 20.0 49 2.4 50.29 543.3 178.9 2058 1583 0.06 0 .11 n.d. 0 0 7.27 28.4 3.20 14.82 2.54 6.75 1.02 7.22 1.10 0.18 L-1024 c 5.56 0.06 0.20 9.37 0.00 0.84 6.08 39.51 0.01 0.04 0.23 38.7 100.56 10 325 92 18 31.0 29 11 116 29 <9 24 <12 99 20.0 18.0 49 1786 1383 0.05 L-1025 42.06 1.06 1.26 21.42 0.00 0.77 2.76 17.44 1.61 0.56 3.85 7.40 100.19 30 1546 50 1312 1425 42 10 29 ## 12 334 106 214 86.4 19.5 33 4.8 27.7 183 47.1 396 17 6 0.39 10.1 33.6 8.30 21.9 2.59 13.0 2.12 5.37 0.85 7.25 1.48 2.17 L-1027 55.06 0.81 15.77 5.91 0.00 0.27 2.32 3.60 4.38 6.88 0.23 3.58 98.81 177 429 37 621 220.0 14 42 25 ## 24 45 174 1043 <6 <15 <10 58.35 136.1 239 72 94.3 1.66 3 1.063 0.838 11.26 L-1032 46.04 1.99 15.47 14.07 0.00 0.33 6.80 9.26 3.22 0.75 0.42 1.94 100.29 10 322 48 132 9.0 47 45 26 ## 15 345 218 299 <6 <15 40 109.3 42.20 61.28 <12 40 3.53 2 2.53 0.600 3.588 1.138 3.97 LR25 4.673 0.29 0.34 5.85 1.89 0.76 70.8 1.58 0.01 5.82 1 6765 12358 65 128 167 58 166 ## 0 191 50 469 24 7730 7 0 673 1335 0 3341 2342 0 8 35 0 0 75 1.59 27 LR23 6.138 0.06 1.84 14.0 0.45 30.5 40.6 2.47 0.10 0.18 6 941 2633 327 152 71 53 41 53 0 62 86 25 15 130 19 71 0 0 88 0 32 0 13 449 24 0 5 2.57 0 LR20 2.875 0.02 0.60 12.9 0.38 33.1 45.0 1.67 0.04 0.15 0 1166 ## 97 22 16 44 31 79 0 115 85 32 0 36 0 10 0 0 0 0 37 25 0 42 6 0 2 1.71 0 LR5 7.666 0.30 1.32 16.1 2.24 3.89 48.8 1.51 0.53 8.09 19 1669 4033 130 181 90 46 89 45 0 36 114 393 26 2347 0 91 655 1734 486 4909 3846 18 7 75 49 0 21 2.05 0 LR4 2.133 0.10 0.12 33.4 3.12 1.61 48.6 1.71 0.04 0.66 0 1054 2761 44 598 44 21 0 99 -5 0 0 0 28 1593 0 438 0 2003 0 6950 5436 3 7 2199 93 0 74 1.75 12 AM-1 1839 8630 114 11 1019 330 748 1726 1061 78 0.00 Mesopotamie Farm, Copper Vallei Mine, Namibia Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-759 74.06 0.03 14.47 0.47 0.00 0.04 0.02 0.70 3.55 5.54 0.06 0.94 99.88 109 124 20 16 7.0 <6 <6 <6 12 13 <12 185 649 <6 <15 <10 12 <12 9.09 L-772 72.55 0.03 14.29 0.43 0.00 0.03 0.03 0.05 2.34 10.07 0.02 0.67 100.51 201 100 7 <8 4.0 <6 <6 8 28 13 <12 44 579 <6 <15 <10 21 <12 12.41 L-773 74.83 0.06 14.98 0.87 0.00 0.02 0.11 0.80 5.35 3.07 0.04 0.41 100.54 76 71 ## 64 14.0 <6 10 8 43 20 <12 47 176 <6 <15 <10 25 <12 8.42 L-783 71.86 0.45 13.96 3.32 0.00 0.08 0.50 0.78 3.49 5.15 0.18 0.71 100.48 223 85 54 273 22.0 <6 6 9 49 17 25 239 859 <6 27.0 <10 161 75 8.64 L-784 71.83 0.39 13.23 3.59 0.00 0.06 0.56 1.31 3.67 5.07 0.09 0.70 100.50 193 105 58 312 23.0 <6 7 7 59 17 23 63 1049 7.00 26.0 <10 11.3 37.06 98.50 155 51 1.513 41.66 0.78 3.938 1.400 8.74 Other alkaline and gabbroic rocks to compare with (used by Frets) Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 X-27 47.85 1.47 16.84 2.70 8.50 0.19 6.66 11.79 2.54 0.75 0.27 0.46 100.02 3.29 X-28 60.59 0.58 14.99 2.44 2.30 1.13 0.91 2.55 8.98 3.81 tr 1.00 99.28 12.79 X-29 61.03 18.63 3.66 1.04 1.56 7.68 5.57 0.41 99.58 13.25 X-30 63.34 0.57 16.00 4.17 1.69 0.11 0.35 2.29 3.93 5.86 0.17 2.04 100.52 9.79 X-31 61.56 0.82 15.25 4.29 3.89 0.25 1.28 1.68 4.10 4.40 0.16 1.24 98.92 8.50 X-32 65.80 0.60 15.40 3.84 0.28 0.06 0.11 1.12 5.60 5.10 0.38 1.05 99.34 10.70 X-33 51.80 0.32 18.20 2.24 2.09 0.17 2.56 4.93 8.22 5.36 0.50 3.69 100.08 13.58 Table No. A13 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGIO N PAGE 13/14 Otjiwarongo Environs, Namibi a Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-808 70.53 0.14 15.35 1.50 0.00 0.05 0.42 1.71 4.80 3.67 0.07 2.04 100.28 140 89 12 29 13.9 <6 7 10 71 16 13 39 154 <6 <15 <10 32.4 2.03 9.16 2.46 26 <12 5.99 1.17 1.22 0 0 0.50 1.81 0.31 2.11 0.42 1.29 0.21 1.48 0.22 8.47 L-809 71.56 0.07 14.95 1.24 0.00 0.03 0.23 0.87 3.46 7.52 0.06 0.50 100.49 253 92 19 <8 9.0 <6 7 11 56 16 <12 27 301 <6 <15 <10 29 <12 10.98 L-810 73.89 0.06 14.05 1.11 0.00 0.04 0.16 1.04 4.00 5.44 0.04 0.50 100.33 173 85 7 <8 7.0 9 10 13 50 14 <12 56 249 <6 <15 <10 24 <12 9.44 L-812 75.60 0.08 12.89 1.27 0.00 0.03 0.25 1.29 4.03 4.17 0.09 0.71 100.41 141 104 86 215 10.0 <6 8 9 67 13 <12 34 439 17.00 30.0 <10 93 55 8.20 L-813 71.80 0.04 15.51 0.86 0.00 0.03 0.12 1.40 4.26 5.59 0.08 0.78 100.47 173 115 65 77 6.0 <6 9 13 23 14 <12 42 625 13.00 21.0 <10 63 22 9.85 L-814 89.59 0.02 5.33 0.65 0.00 0.02 0.02 0.84 2.94 0.31 0.04 0.63 100.39 23 38 5 <8 4.0 <6 7 10 54 <9 <12 77 50 <6 <15 <10 26 <12 3.25 L-815 69.73 0.30 14.51 3.35 0.00 0.08 0.84 1.34 3.85 5.59 0.16 0.65 100.40 214 122 43 268 25.0 <6 8 10 75 17 12 68 584 42.0 16.0 <10 68 29 9.44 L-850 71.15 0.38 13.69 2.97 0.00 0.05 0.47 1.56 3.09 4.96 0.10 0.48 98.90 264 153 22 241 15.0 7 7 23 57 17 27 13 919 <6 46.0 <10 116.9 48.33 131.0 171 67 4.76 34.1 3 0.588 0.18 0.73 8.05 L-1037 67.15 0.44 16.05 2.51 0.00 0.02 0.77 1.33 2.99 7.49 0.15 0.46 99.36 204 190 22 149 16.0 <6 6 8 41 17 15 156 1143 <6 105.0 <10 288 157 10.48 L-1038 68.09 0.44 15.77 2.42 0.00 0.02 0.69 1.39 3.03 6.45 0.17 0.40 98.87 185 178 26 247 18.0 <6 8 13 39 16 14 162 975 <6 112.0 <10 316 175 9.48 L-1039 70.93 0.25 13.72 2.43 0.00 0.01 0.03 0.57 3.62 5.51 0.10 1.71 98.88 160 562 19 156 20.0 <6 7 21 11 18 <12 230 793 <6 26.0 <10 88 46 9.13 L-1039 a 73.60 0.10 13.76 0.98 0.00 0.02 0.06 0.47 3.67 6.14 0.03 0.53 99.36 168 205 12 38 2.1 <6 8 6 11 13 12 250 1060 <6 <15 <10 24.9 3.17 17.63 4.60 55 23 2.53 1.29 0.08 0 0 1.07 2.98 0.39 2.17 0.40 1.09 0.15 0.98 0.15 9.81 L-1039 c 70.50 0.34 13.95 3.40 0.00 0.02 0.00 0.71 3.38 5.94 0.11 2.16 100.51 172 547 24 162 24.0 <6 7 29 12 18 <12 309 776 <6 32.0 <10 103 55 9.32 LJ1 68.16 0.46 16.02 2.81 0.00 0.02 0.89 1.54 2.85 7.17 0.16 0.55 100.07 196 191 24 259 17.0 4 30 42 15 0 954 1.00 95.0 4 10.02 LL1 73.41 0.09 14.65 0.80 0.00 0.01 0.27 1.00 3.34 6.24 0.20 1.26 100.02 150 176 17 42 6.0 3 3 13 11 6 1 1468 0.00 5.0 2 9.58 LL10 56.48 1.24 17.84 6.85 0.00 0.19 1.96 3.78 5.74 4.86 0.74 0.74 99.67 135 965 36 340 99.0 11 3 0 78 44 0 1366 9.00 25.0 1 10.60 LL11 73.00 0.00 14.00 2.00 0.00 0.00 0.00 1.00 3.00 6.00 0.00 1.00 99.86 287 134 34 210 16.0 2 1 0 30 20 3 880 3.00 55.0 5 9.00 LL13 62.00 1.00 11.00 4.00 0.00 0.00 3.00 18.00 1.00 0.00 0.00 7.00 100.02 12 701 42 128 6.0 9 26 3 58 101 66 448 4.00 5.0 10 1.00 LL14 57.00 1.00 17.00 9.00 0.00 0.00 1.00 3.00 6.00 5.00 0.00 1.00 99.52 280 355 ## 2052 364.0 4 5 ## 4 0 1161 22.0 83.0 5 11.00 LL15 62.00 1.00 16.00 6.00 0.00 0.00 1.00 4.00 6.00 5.00 0.00 4.00 99.73 118 328 31 305 47.0 10 9 0 73 125 22 1308 3.00 26.0 15 11.00 LL16 70.00 1.00 14.00 3.00 0.00 0.00 1.00 2.00 3.00 5.00 0.00 0.00 99.49 230 152 24 320 30.0 4 2 0 33 39 9 790 3.00 33.0 4 8.00 LL17a 73.00 0.00 14.00 1.00 0.00 0.00 0.00 1.00 3.00 7.00 0.00 1.00 99.75 202 57 12 29 9.0 2 5 8 4 6 220 5.00 3.0 1 10.00 LL17b 66.00 1.00 16.00 5.00 0.00 0.00 1.00 3.00 3.00 5.00 0.00 0.00 99.77 140 208 22 311 16.0 13 2 2 60 50 7 1167 4.00 18.0 9 8.00 LL18 76.00 0.00 13.00 1.00 0.00 0.00 0.00 1.00 3.00 7.00 0.00 1.00 100.07 178 84 8 55 3.0 0 8 5 4 316 5.00 4.0 1 10.00 LL2a 75.73 0.02 14.98 0.67 0.00 0.01 0.06 0.12 3.62 4.86 0.04 1.36 100.11 181 35 10 19 19.0 2 1 14 8 11 0 104 2.00 4.0 2 8.48 LL2b 69.71 0.00 16.92 0.31 0.00 0.01 0.00 0.04 2.54 10.40 0.13 0.60 100.06 356 67 7 4 1.0 2 1 0 2 0 1 205 0.00 2.0 0 12.94 LL3a 75.92 0.03 13.87 0.68 0.00 0.01 0.05 0.39 2.87 5.93 0.01 1.19 99.77 156 182 13 29 0.0 2 1 14 4 5 3 659 0.00 7.0 1 8.80 LL3b 70.31 0.04 16.91 0.47 0.00 0.01 0.24 0.37 2.44 9.09 0.09 1.20 99.96 348 252 9 5 4.0 2 1 0 7 7 1 495 1.00 0.0 5 11.53 LL4 74.72 0.10 13.50 1.59 0.00 0.03 0.10 0.80 3.49 5.74 0.02 0.41 100.08 365 50 32 138 29.0 1 0 27 1 0 235 4.00 52.0 5 9.23 LL5 75.94 0.03 14.40 0.33 0.00 0.00 0.00 1.44 4.03 3.46 0.03 0.64 99.67 180 89 47 48 11.0 1 6 4 0 0 151 5.00 11.0 1 7.49 LL9 79.03 0.02 14.86 0.39 0.00 0.00 0.01 0.02 0.30 5.63 0.00 3.19 100.25 256 26 9 33 9.0 2 2 1 3 12 3 285 2.00 3.0 2 5.93 Grootfontein Inlier, Otavi Mountains, Namibia Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-1014 68.99 0.41 14.20 3.21 0.00 0.05 1.35 2.61 3.04 3.64 0.11 1.80 99.41 58.9 321 5 43.2 2.55 9.0 20.0 13.00 43 13 60 173 1632 <6 <15 <10 14.1 2.27 18.16 4.86 64 34.0 0.24 1.00 n.d. 0.0 0.0 1.27 1.76 0.20 1.08 0.20 0.51 0.07 0.44 0.07 6.68 L-1042 70.57 0.26 14.13 2.58 0.00 0.06 0.45 0.67 2.79 6.14 0.10 1.35 99.10 317 68 65 161 17.0 7 12 20 29 14 16 <12 471 <6 35.0 <10 109.9 44.76 78.50 106 34 3.63 26 .99 0.413 0.78 3.88 1.213 8.93 L-1043 72.42 0.34 13.62 2.40 0.00 0.04 0.57 0.57 2.76 5.77 0.10 1.27 99.86 276 85 71 207 17.0 7 9 51 30 14 28 <12 525 <6 44.0 <10 109.1 41.74 89.3 140 35 1.713 36. 96 0.750 8.700 1.850 8.53 L-1044 73.43 0.25 12.72 2.04 0.00 0.04 0.39 0.49 2.79 5.94 0.11 1.10 99.30 293 67 47 166 16.0 6 9 115 70 12 20 12 415 <6 36.0 <10 109 44 8.73 L-1045 65.28 0.40 17.54 2.82 0.00 0.08 0.36 3.60 6.67 1.70 0.11 1.41 99.97 90 471 ## 246 24.0 5 7 48 18 20 24 <12 116 <6 57.0 12 12.20 14.56 48.3 154 16 297.8 0.18 8 2.238 1.68 8.37 L-1046 72.78 0.33 12.73 2.40 0.00 0.03 0.55 0.76 2.61 5.45 0.12 1.39 99.15 283 61 69 193 16.0 6 9 30 27 13 25 16 473 <6 42.0 <10 126 53 8.06 Okatjepuiko, Witvlei, Namibi a Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 L-625 74.31 0.32 12.49 2.19 0.00 0.04 0.42 0.94 5.72 2.00 0.10 0.70 99.23 43 78 49 280 30.0 <6 15 753 26 15 21 123 493 <6 <15 <10 125 54 7.72 L-626 75.44 0.32 12.53 3.15 0.00 0.05 0.57 0.71 5.99 1.04 0.06 0.63 100.49 18 64 50 263 30.0 <6 13 1078 41 17 21 53 609 <6 <15 <10 10.56 33.25 65.50 112 31 38.58 1 .038 3.050 1.238 7.03 L-633 51.27 1.55 16.00 10.81 0.00 0.18 6.69 7.17 3.71 1.69 0.26 1.07 100.40 56 239 26 123 13.0 52 115 499 ## 17 279 202 550 <6 <15 31 12.91 15.65 35.9 43 11 224.0 5.638 0.563 1.23 5.40 L-635 62.14 0.98 15.43 6.05 0.00 0.12 3.29 3.28 7.37 0.22 0.15 1.00 100.03 9 33 31 241 19.0 20 64 64 46 20 134 101 58 <6 <15 19 9.03 23.53 48.81 67 21 90.3 0.650 2. 688 0.900 1.08 7.59 L-637 69.84 0.53 13.33 5.85 0.00 0.06 0.58 2.19 5.95 0.76 0.10 1.00 100.19 17 165 56 727 29.0 8 18 128 34 20 26 49 359 <6 <15 10 123 60.93 134.1 180 93 3.313 34.34 0.588 4.300 1.53 6.71 L-638 77.05 0.18 11.68 2.36 0.00 0.04 0.14 0.62 4.27 3.73 0.02 0.42 100.51 59 91 35 148 17.5 <6 9 95 29 15 14 66 751 <6 <15 <10 10.8 7.71 40.96 10.40 116 53 0.41 4. 36 0.51 0 0 1.02 7.02 1.09 6.94 1.36 3.85 0.54 3.56 0.51 8.00 L-641 50.76 2.24 13.78 12.16 0.00 0.24 6.49 7.32 4.30 0.62 0.40 1.90 100.21 27 195 33 131 15.0 48 90 704 ## 17 262 196 247 <6 <15 34 12.08 46.00 28 <12 4.92 L-645 56.67 1.27 14.07 9.26 0.00 0.09 0.42 5.87 8.40 0.16 0.33 3.96 100.50 5 67 38 214 17.0 9 21 6 21 19 113 185 87 <6 <15 26 49 22 8.56 L-648 72.50 0.35 12.81 4.25 0.00 0.05 0.69 0.64 7.27 1.32 0.06 0.59 100.53 25 69 21 248 12.0 6 17 1546 44 13 47 67 1144 <6 <15 <10 89 30 8.59 L-649 73.86 0.30 12.07 4.77 0.00 0.06 0.53 0.64 5.74 1.86 0.05 0.56 100.44 37 63 16 193 11.0 9 19 2238 37 11 50 78 1330 <6 <15 <10 74 19 7.60 L-816 74.57 0.30 12.43 3.00 0.00 0.06 0.39 1.37 6.02 1.96 0.04 0.44 100.58 43 91 52 284 32.0 <6 13 104 62 17 18 81 386 <6 <15 <10 115.9 35.64 72.13 122 33 1.200 32 .86 1.13 2.68 1.18 7.98 Table No. A14 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY REGIO N PAGE 14/14 Spitzkoppe Complexes, Namibia Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 X-92 77 0.1 11.7 2.06 0.02 0.08 0.74 3.03 5.23 0.02 0.52 473 14 ## 196 141 3 3 44 2 7 75 2 148 84 8.26 X-93 76 0.04 12.8 1.57 0.02 0.04 0.62 3.89 4.93 0.01 0.46 604 2 ## 112 88 2 3 58 6 2 9 1 63 26 8.82 X-94 75.7 0.04 12.9 1.71 0.02 0.05 0.65 4.05 4.84 0.02 0.45 620 1 ## 128 83 4 4 45 2 7 2 - 54 21 8.89 X-95 69.8 0.51 12.6 5.77 0.08 0.11 2.3 2.55 6.29 0.09 1.38 243 81 68 474 24 - - - - - 1051 10 162 77 8.84 Erongo Complex, Namibia X-96 76.3 0.07 13.3 1.43 0.03 0.06 0.43 3.08 5.07 0.26 - 637 25 ## 60 26 10 2 38 76 6 8.15 Brandberg Complex, Namibia Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 X-97 75 0.16 10.4 5.06 0.07 0.06 0.16 4.43 4.69 0 0.66 1241 18 ## 537 95 14 459 207 9.12 X-98 71.3 0.48 13.1 4.71 0.11 0.23 0.91 3.45 5.53 0.11 0.98 211 111 66 483 56 856 134 64 8.98 X-99 71.1 0.45 13.1 4.38 0.11 0.3 1.46 3.46 5.6 0.1 0.49 210 112 ## 455 53 807 163 85 9.06 X-100 70.3 0.5 13.5 4.37 0.11 0.38 1.52 3.58 5.66 0.11 0.28 209 111 78 505 61 808 144 66 9.24 X-101 70 0.55 13.7 4.65 0.11 0.3 1.88 3.59 5.15 0.11 0.56 188 132 73 472 51 112 54 8.74 Nigerian Ring Complexes Sample SiO2 TiO2 A l2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 ## 4 30 5 20 3 9 35.5 7.5 1.6 AMN24 72.60 0.29 14.07 0.90 1.73 0.07 0.43 1.01 3.36 5.74 0.07 0.47 100.74 185 100 63 246 57 61 9 362 27 22 144 59 6 34 5 9.10 8 RN75 75.90 0.11 12.85 0.33 1.05 0.05 0.02 0.24 3.91 4.31 0.01 0.88 99.66 979 15 ## 399 214 120 ## 0 109 111 56 296 234 28 391 7 8.22 40 PAN11 2 73.90 0.15 14.88 0.43 0.80 0.02 0.67 0.43 3.98 5.17 0.02 0.61 101.06 192 28 ## 234 88 0 80 25 22 195 189 7 25 8 9.15 19 JON14 7 73.20 0.18 14.18 0.67 1.19 0.02 0.08 0.73 3.45 5.32 0.03 0.98 100.03 296 38 ## 330 118 ## 0 264 41 38 251 218 8 32 14 8.77 39 B34 76.00 0.10 11.74 0.37 0.89 0.02 0.09 0.83 3.78 5.77 0.04 0.24 99.87 574 4 ## 141 158 60 12 39 40 74 114 64 5 205 9 9.55 ## MD333 75.40 0.10 13.33 0.01 0.96 0.02 0.04 0.34 4.26 4.53 0.01 0.20 99.20 620 0 ## 129 78 9 68 0 0 66 70 79 28 9 158 8 8.79 0 NG208 75.70 0.20 13.18 1.48 0.01 0.03 0.09 0.44 3.41 5.10 0.01 0.66 100.31 318 29 75 186 80 70 2 151 63 57 156 83 7 13 16 8.51 34 T15A 74.30 0.08 11.74 0.33 0.89 0.02 0.01 0.26 3.88 4.59 0.01 0.64 96.75 502 1 86 166 132 7 61 3 0 69 37 153 166 7 122 12 8.47 DR11 76.70 0.14 13.36 0.00 1.16 0.03 0.05 0.33 4.41 3.58 0.02 0.34 100.12 966 0 87 81 119 ## 4 0 61 47 149 88 9 558 15 7.99 76 DW1 78.03 0.06 12.14 0.33 0.89 0.01 0.09 0.52 4.59 3.56 0.01 0.42 100.65 389 22 ## 207 205 77 0 71 42 16 275 169 10 138 10 8.15 10 FG5 77.44 0.08 11.99 0.37 0.87 0.02 0.07 0.49 3.89 4.45 0.01 0.34 100.02 347 3 ## 161 148 42 0 43 39 27 117 64 8 67 13 8.34 10 KD12 76.50 0.10 12.83 0.35 0.84 0.02 0.07 0.46 4.17 4.39 0.01 0.34 100.08 283 4 ## 147 96 48 0 4 36 41 62 27 6 56 9 8.56 Table No. A15 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY NUMBER PAGE 1/10 Sample SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 100 4 30 5 20 3 9 35.5 7. 5 1.6 AM-1 1839 8630 114 11 1019 330 748 1726 1061 78 0.00 C-1 74.03 0.27 12.73 1.15 1.51 0.05 0.31 0.48 3.67 5.09 0.05 0.71 100.05 100 50 70 500 30.0 <10 <10 n.d 25 <3 10 1200 25.0 95 <100 <3 <3 <3 0 <3 8.76 C-10 68.63 0.49 15.01 1.62 1.44 0.07 1.22 2.74 4.41 3.60 0.20 0.57 100.00 65 720 25 230 <10 20 55 30 1900 18.0 70 20 8.01 C-11 78.84 0.29 10.79 0.95 0.27 0.03 0.09 0.60 2.94 5.20 0.06 0.22 100.28 120 65 55 180 18.0 15 5 25 560 20.0 100 <3 8.14 C-13 (w e 75.89 0.41 12.46 1.07 0.13 n.d. 0.05 0.25 3.60 5.71 0.04 0.50 100.11 100 40 65 650 40.0 <10 <10 n.d. 25 <3 10 1000 30.0 90 <100 <3 <3 <3 0 <3 9.31 C-14 48.69 1.26 13.27 4.86 8.71 0.18 6.15 10.49 2.41 1.05 0.22 0.50 97.79 3.46 C-2 69.71 0.68 14.17 1.69 1.57 0.04 0.84 0.82 4.10 5.30 0.27 0.67 99.86 70 110 45 550 30.0 25 35 25 2100 8.0 90 35 9.40 C-3 68.63 0.67 15.43 1.74 1.03 0.10 0.51 1.99 4.50 4.42 0.18 0.50 99.70 90 350 140 700 40.0 25 35 11 2500 25.0 130 30 8.92 C-4 73.63 0.33 14.16 1.13 0.24 0.02 0.00 0.50 3.14 6.35 0.07 0.44 100.01 200 80 20 380 20.0 20 9 13 1200 40.0 95 11 9.49 C-5 75.35 0.27 13.18 1.08 0.22 0.02 0.00 0.62 3.15 5.50 0.05 0.36 99.80 110 100 35 280 10.0 20 5 15 1400 30.0 65 12 8.65 C-6 66.09 0.69 14.60 3.06 1.72 0.08 1.81 2.54 3.25 4.71 0.28 1.11 99.94 150 480 25 280 <10 20 85 18 1900 14.0 75 25 7.96 C-7 69.29 0.47 14.55 1.81 1.48 0.06 1.19 2.83 3.33 4.40 0.17 0.46 100.04 230 650 25 320 10.0 19 70 35 1700 16.0 70 13 7.73 C-8 73.88 0.33 13.85 0.87 0.24 0.03 0.18 0.26 4.05 5.93 0.09 0.39 100.10 130 40 55 450 15.0 20 7 11 400 20.0 65 4 9.98 C-9 73.30 0.32 13.20 2.93 0.48 0.01 0.00 0.24 3.46 5.67 0.07 0.34 100.02 130 50 80 650 30.0 30 <3 14 1200 12.0 85 9 9.13 L-012 64.19 0.66 17.47 3.45 0.00 0.03 1.12 2.55 4.34 6.14 0.18 0.30 100.43 131 516 33 189 29.2 7 9 7 42 20 46 36 1042 4.27 50.4 <10 3.8 15.4 112 31.5 293 163 1.08 4 .73 1.57 293 2.69 9.76 1.21 6.81 1.22 3.22 0.47 3.14 0.48 10.48 L-012A 64.38 0.61 17.86 3.18 0.00 0.03 1.13 2.40 4.10 6.24 0.15 0.32 100.40 143 536 36 360 32.0 9 10 9 28 21 33 36 940 <6 49.0 <10 312 216 10.34 L-020 74.44 0.22 12.70 2.48 0.00 0.05 0.28 0.58 3.03 5.85 0.02 0.75 100.40 226 91 53 228 19.0 <6 <6 9 64 18 <12 47 553 10.00 62.0 <10 11.13 88.15 144.8 286 75 73. 15 3.33 2.68 1.275 8.88 L-023 67.01 0.56 14.95 5.02 0.00 0.07 1.83 2.74 3.71 3.60 0.19 0.80 100.48 78 376 24 133 13.0 10 6 <6 44 16 80 219 1283 <6 <15 12 6.925 49.95 76.63 127 44 61.23 0. 738 1.43 1.300 1.125 7.31 L-024 48.01 2.10 12.37 18.91 0.00 0.28 4.93 8.74 1.70 0.43 0.17 1.16 98.80 16 78 51 140 11.0 57 66 236 149 22 470 79 108 6.00 <15 43 13.59 38.8 39.45 25 19 391.38 3.100 2.250 2.088 2.13 L-025 70.60 0.40 13.80 3.70 0.00 0.05 0.73 1.82 3.19 4.80 0.08 0.96 100.13 91 370 11 108 10.0 6 8 9 71 17 38 42 1390 <6 <15 <10 4.163 31.91 47.41 85 20 24.55 0.750 0.900 0.563 0.825 7.99 L-026 71.92 0.37 13.46 3.29 0.00 0.04 0.67 1.98 3.23 4.51 0.08 0.82 100.37 85 384 12 392 14.0 6 7 8 55 16 38 42 1367 <6 <15 <10 97 41 7.74 L-027 67.24 0.53 15.50 4.74 0.00 0.09 1.38 4.31 3.75 1.72 0.19 1.02 100.47 49 619 21 123 13.0 7 <6 <6 49 18 68 161 573 <6 <15 12 107 58 5.47 L-028 60.53 0.60 14.99 6.80 0.00 0.09 4.08 3.69 3.88 3.07 0.26 1.58 99.57 124 581 20 155 16.0 26 52 79 45 16 79 89 532 <6 17.0 17 5.875 43.06 63.88 109 32 95.25 2. 93 0.650 1.025 6.95 L-029 63.66 0.66 17.38 5.28 0.00 0.05 2.34 3.70 3.95 2.50 0.26 0.70 100.48 88 542 12 147 11.0 20 23 26 49 18 87 51 574 <6 <15 11 89 45 6.45 L-030 74.74 0.10 13.50 1.47 0.00 0.04 0.09 0.45 2.16 5.91 0.00 1.92 100.38 262 67 15 128 16.2 <6 7 22 34 16 13 15 391 16.00 40.0 <10 35.7 2.87 14.89 4.15 76 26 2.7 0 4.00 1.24 0 0 0.39 2.41 0.41 2.81 0.59 1.87 0.30 2.17 0.34 8.07 L-032 59.58 1.09 15.52 7.08 0.00 0.07 3.07 5.01 2.80 3.13 0.54 0.82 98.71 110 566 26 284 23.0 25 34 17 58 19 151 78 703 <6 <15 16 7.975 54.33 82.75 109 37 96.13 0. 713 1.050 1.063 5.93 L-034 60.10 0.04 23.01 3.98 0.00 0.07 0.11 0.14 6.82 4.47 0.07 1.68 100.49 79 342 27 708 92.0 <6 12 8 18 17 74 87 705 <6 20.0 11 311 134 11.29 L-036 73.57 1.10 15.97 1.46 0.00 0.02 0.12 0.10 0.03 0.25 0.09 7.83 100.54 34 51 30 635 38.0 <6 26 36 37 28 52 30 196 <6 36.0 <10 282 240 0.28 L-037 56.10 0.04 21.65 3.00 0.00 0.12 0.04 1.20 10.22 5.51 0.05 2.53 100.46 92 465 33 792 101.0 <6 7 10 171 25 <12 117 423 9.00 17.0 <10 108.3 38.65 70.88 139 63 50.70 0.413 0.688 0.675 15.73 L-038 56.45 0.12 21.07 3.77 0.00 0.08 0.00 0.32 12.27 4.32 0.07 2.01 100.48 72 244 29 859 114.0 <6 7 12 108 26 <12 65 318 8.00 32.0 <10 261 146 16.59 L-039 57.37 0.05 21.32 3.71 0.00 0.20 0.08 0.75 9.68 4.63 0.06 2.64 100.49 87 355 37 808 120.0 <6 <6 12 127 27 <12 68 349 9.00 30.0 <10 231 166 14.31 L-040 55.44 0.04 20.98 5.81 0.00 0.34 0.02 1.29 9.89 6.14 0.06 0.44 100.45 75 283 38 922 135.0 2 8 8 106 25 4 139 261 8.00 30.0 <10 278 186 16.03 L-041 57.71 0.05 20.81 4.02 0.00 0.07 0.00 0.60 8.89 5.41 0.02 2.85 100.45 85 283 33 950 134.0 <6 <6 6 98 27 <12 <12 347 11.00 22.0 <10 183 109 14.30 L-044 57.32 0.03 21.02 3.15 0.00 0.14 0.00 0.65 12.04 4.28 0.05 1.70 100.38 109 616 107 1758 178.0 4 8 10 227 26 11 120 1441 10.00 31.0 <10 0.263 4.488 196 0 37. 10 1.48 1.150 0.288 0.713 16.32 L-045 57.75 0.10 20.94 6.96 0.00 0.03 0.00 0.14 7.96 4.16 0.06 1.17 99.27 58 367 20 186 97.6 <6 11 32 34 27 <12 45 764 7.24 17.8 <10 1.9 7.13 57.9 20.0 214 158 0.2 9 2.38 9.70 214 1.22 4.71 0.77 4.50 0.77 2.09 0.31 2.01 0.27 12.12 L-046 55.67 0.05 20.92 3.40 0.00 0.19 0.09 1.07 8.51 5.27 0.06 5.21 100.44 82 311 30 670 82.0 <6 6 115 168 24 <12 51 526 <6 29.0 <10 0.525 0.550 6.700 204 1 44.38 0.638 1.400 0.250 0.688 13.78 L-047 66.09 0.46 14.68 5.40 0.00 0.08 0.20 2.42 4.99 4.75 0.08 0.54 99.70 110 83 458 634 105.0 <6 <6 <6 47 22 12 <12 1015 6.00 <15 10 127.3 186.3 308 164 68.50 6. 438 29.43 7.750 19.71 3.538 9.74 L-049 47.30 2.03 15.47 13.49 0.00 0.25 5.41 10.51 3.04 0.93 0.22 0.92 99.58 13 346 30 109 17.0 34 46 143 119 19 296 85 127 <6 <15 31 23 <12 3.97 L-050 46.86 2.06 15.40 13.35 0.00 0.21 5.20 10.46 3.73 0.89 0.27 0.52 98.95 11 321 31 114 16.0 46 49 91 70 18 321 171 93 <6 <15 34 30 <12 4.62 L-060a 45.83 4.36 11.86 17.84 0.00 0.26 6.24 9.49 2.29 1.12 0.43 0.38 100.11 149 64 19 128 9.5 31 39 20 105 396 38 477 4.91 46.5 0 20.4 3.67 27.0 9.06 113 61 0.87 4.08 1.16 0.57 2.65 0.44 3.02 0.66 2.15 0.36 2.73 0.42 3.41 L-060b 76.30 0.15 11.89 1.79 0.00 0.04 0.14 0.53 3.65 5.74 0.04 0.28 100.55 154 64 23 141 13.0 <6 <6 14 25 22 <12 54 481 <6 <15 35 37 20 9.39 L-060c 45.43 4.31 11.83 17.86 0.00 0.28 6.23 9.37 2.11 1.09 0.45 0.42 99.57 24 330 38 165 27.0 37 39 29 101 387 33 118 3.20 L-063 46.39 0.84 12.95 3.10 0.00 0.09 5.95 9.71 6.97 0.15 0.12 14.12 100.39 4 51 19 192 7.0 <6 18 7 22 21 86 36 <20 <6 <15 23 25 16 7.12 L-064 47.31 0.82 12.99 3.23 0.00 0.10 5.76 9.38 6.85 0.05 0.12 13.87 100.48 4 51 19 175 7.0 <6 18 8 28 20 92 36 <20 <6 <15 24 16 <12 6.90 L-065 39.63 0.57 9.98 4.16 0.00 0.11 7.62 13.40 4.80 0.12 0.07 19.80 100.26 4 125 24 108 8.0 <6 20 8 29 12 102 45 <20 <6 <15 30 5.65 1.725 18.83 15 10 71.00 0.988 0 .763 4.92 L-075 65.53 0.91 13.91 5.81 0.00 0.07 1.46 2.59 3.43 5.10 0.23 1.14 100.18 162 217 33 50 16.8 0 0 0 0 16 0 0 1339 <6 16.0 <10 21.1 9.40 53.11 13.45 160 61 2.48 1.38 0.81 0 0 1.89 7.80 1.11 6.66 1.26 3.52 0.49 3.17 0.45 8.53 L-076 65.53 0.91 13.91 5.81 0.00 0.07 1.46 2.59 3.43 5.10 0.23 1.14 100.18 182 212 48 361 26.0 22 16 105 35 17 82 56 1344 <6 17.0 10 137 61 8.53 L-077 66.70 0.79 14.45 4.66 0.00 0.06 1.36 2.66 3.78 5.06 0.21 0.77 100.50 174 216 39 290 22.0 14 11 28 46 18 59 41 1391 <6 14.0 <10 11.11 35.10 86.25 119 41 75.1 3 1.088 1.213 1.088 8.84 L-078 67.56 0.89 13.59 5.37 0.00 0.07 1.27 3.08 3.93 3.78 0.23 0.81 100.58 143 235 47 343 25.0 19 13 31 48 17 74 51 964 <6 18.0 10 131 61 7.71 L-079 67.09 0.80 14.65 4.99 0.00 0.07 1.21 2.40 3.35 4.98 0.19 0.83 100.56 165 216 40 332 24.0 14 12 41 45 0 68 40 1291 0.00 0.0 0 0 0 8.33 L-139 75.60 0.09 11.88 1.50 0.00 0.03 0.62 0.14 1.61 7.87 0.01 0.79 100.14 399 17 40 75 41.0 10 7 55 34 23 14 47 769 <6 26.0 <10 42 12 9.48 L-150 51.05 2.91 15.47 10.19 0.00 0.00 10.09 0.68 1.69 6.12 0.36 1.16 99.72 361 24 45 150 28.0 851 191 623 66 24 424 94 349 6.00 <15 29 12.85 13.43 54.96 18 7 220 .8 0.263 1.250 7.81 L-151 77.00 0.10 11.82 1.67 0.00 0.03 0.17 0.11 3.47 5.54 0.02 0.51 100.44 351 32 158 197 91.0 10 8 42 39 24 <12 42 441 11.00 65.0 <10 113.8 48.59 96.88 167 49 6. 938 13.56 0.538 10.61 2.200 9.01 L-153 77.40 0.07 11.91 1.65 0.00 0.03 0.12 0.27 3.51 4.89 0.01 0.51 100.37 438 25 117 106 70.0 <6 8 58 33 24 <12 60 236 11.00 44.0 <10 87 38 8.40 L-154 77.07 0.07 12.06 1.22 0.00 0.00 0.00 0.25 3.07 5.78 0.01 0.50 100.05 478 27 68 122 58.0 7 <6 17 22 23 <12 <12 255 <6 44.0 <10 105.1 2.513 22.06 90 4 3.588 9. 975 2.363 0.888 8.85 Table No. A15 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY NUMBER PAGE 2/10 Sample SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 100 4 30 5 20 3 9 35.5 7. 5 1.6 L-155 72.00 0.28 12.99 2.57 0.00 0.00 1.51 0.95 1.03 6.03 0.09 1.71 99.17 219 62 20 99 13.0 61 12 <6 26 15 44 21 848 <6 <15 <10 109.6 25.34 56.81 69 23 36.41 0.53 0 .23 0.713 7.06 L-157 75.81 0.19 12.48 1.25 0.00 0.00 1.16 0.18 0.19 6.95 0.03 1.39 99.63 225 12 12 107 17.0 26 8 7 14 14 20 15 618 <6 18.0 <10 43 17 7.14 L-158 73.58 0.20 12.85 1.36 0.00 0.00 1.46 0.93 0.33 7.11 0.04 2.00 99.87 233 19 13 109 16.0 32 7 <6 13 14 20 14 628 6.00 26.0 <10 107.9 26.04 63.13 76 31 2.100 8. 225 0.450 0.588 7.44 L-159 68.02 0.64 14.23 2.82 0.00 0.00 1.74 1.42 0.95 6.80 0.16 2.10 98.87 303 47 34 209 28.0 38 7 <6 19 17 57 18 919 11.00 24.0 10 118 60 7.75 L-160 67.96 0.55 14.78 2.29 0.00 0.00 1.47 1.67 2.46 5.69 0.16 2.10 99.14 264 40 49 223 32.0 39 9 <6 18 16 47 16 805 <6 15.0 13 117.8 42.35 102.1 156 49 27.91 1.13 2.788 0.988 8.15 L-161 51.48 1.05 20.52 6.92 0.00 0.10 7.54 1.15 2.18 6.26 0.37 1.89 99.47 225 54 40 319 29.0 93 26 <6 160 24 102 18 1829 <6 30.0 17 128 64 8.44 L-162 76.11 0.19 12.33 1.25 0.00 0.00 0.28 0.70 3.48 4.92 0.03 0.59 99.88 119 155 14 96 10.0 6 <6 7 22 13 17 15 793 <6 <15 <10 82 37 8.40 L-163 43.65 1.23 15.61 14.61 0.00 0.30 11.50 4.45 1.80 3.69 0.14 2.97 99.95 149 179 25 85 9.0 172 410 <6 240 15 228 292 478 <6 <15 22 16 <12 5.49 L-166 70.84 0.39 13.91 2.93 0.00 0.00 0.61 1.97 4.13 4.54 0.13 0.44 99.89 209 89 31 89 18.0 6 <6 22 18 15 <12 17 741 <6 15.0 <10 109.0 34.36 63.50 105 35 3.063 3.3 13 0.713 0.863 0.675 8.67 L-167 47.14 0.78 19.71 6.10 0.00 0.08 12.98 0.00 0.00 8.70 0.08 4.00 99.57 255 64 101 781 147.0 266 57 1896 65 28 95 74 615 12.00 37.0 12 43 13 8.70 L-167a 47.14 0.78 19.71 6.10 0.00 0.08 12.98 0.00 0.00 8.70 0.08 4.00 99.57 255 64 101 781 147.0 266 57 1896 65 28 95 74 615 12.0 37.0 12 43 13 8.70 L-168 79.68 0.15 10.06 0.72 0.00 0.02 0.10 0.02 0.19 7.61 0.08 0.59 99.22 132 125 19 258 11.0 32 <6 261 10 <9 16 59 1190 <6 <15 <10 9.900 61 1 0.175 0.475 7.80 L-170 70.45 0.86 15.35 3.22 0.00 0.03 1.50 0.01 0.02 5.02 0.13 3.05 99.64 110 46 42 320 79.0 131 14 1954 25 29 92 335 766 10.00 <15 11 6.038 25.63 30.29 44 21 46. 49 0.188 1.963 1.413 0.888 5.04 L-172 74.42 0.06 13.07 1.32 0.00 0.04 0.21 0.14 1.85 7.48 0.06 0.71 99.36 316 32 49 113 85.0 9 8 242 23 21 <12 618 668 5.31 48.5 <10 27.3 8.66 41.2 11.3 79 50 1.13 4.97 3.20 0.41 7.22 1.32 9.90 2.23 7.30 1.12 7.27 1.00 9.33 L-173 74.69 0.09 12.55 1.37 0.00 0.03 0.28 0.14 1.87 7.51 0.05 0.78 99.36 314 29 78 172 128.0 11 6 232 20 22 <12 453 598 7.00 58.0 <10 85 49 9.38 L-175 74.72 0.41 12.60 2.96 0.00 0.00 0.41 1.08 2.71 4.60 0.09 0.32 99.90 221 63 45 229 29.0 9 7 31 31 15 28 17 541 <6 25.0 <10 5.913 30.08 47.8 153 19 41.58 0.263 1.300 0.838 7.31 L-181 49.82 1.08 15.86 11.33 0.00 0.16 6.30 11.28 2.94 0.24 0.06 0.86 99.94 7 157 29 62 8.0 34 30 57 94 16 293 35 <22 <6 <15 35 <12 <12 3.18 L-195 61.25 0.38 15.84 8.67 0.00 0.09 0.04 2.35 5.66 5.03 0.09 0.51 99.91 89 130 115 1054 80.0 <6 <6 10 71 40 13 <12 2151 8.00 <15 <10 15.84 44.14 74.25 118 25 14 5.1 3.888 1.463 7.500 2.200 10.69 L-199 10 787 42 534 46.6 399 8.85 38.7 5.6 20.0 137 35.6 288 95 0.67 10.8 2.65 5.38 12.6 1.58 9.10 1.61 4.24 0.59 3.76 0.53 0.00 L-207 75.03 0.07 13.63 0.68 0.00 0.00 0.00 0.11 4.32 6.27 0.01 0.26 100.39 123 182 12 432 6.0 8 6 10 13 0 <12 13 557 0.00 0.0 0 4.575 0 2 19.10 0.225 0.63 0.438 10. 59 L-208 74.23 0.05 13.85 0.87 0.00 0.03 0.00 0.12 4.36 6.13 0.05 0.24 99.93 137 178 12 431 33.0 <6 <6 14 10 25 <12 238 517 9.00 132.0 <10 35 20 10.49 L-209 46.78 1.81 16.06 9.69 0.00 0.05 7.51 11.46 2.34 1.91 0.57 0.60 98.79 53 1592 27 111 17.0 36 42 29 52 19 243 50 1437 <6 <15 27 113 61 4.25 L-210 66.74 0.43 17.99 3.52 0.00 0.00 0.29 0.69 9.58 0.09 0.14 0.39 99.87 4 275 30 474 36.0 6 7 143 13 22 28 <12 83 7.00 74.0 <10 372 223 9.67 L-212 67.27 0.40 15.94 2.89 0.00 0.00 0.15 0.81 4.44 7.04 0.03 0.71 99.69 149 117 51 336 49.0 8 <6 32 17 22 <12 <12 503 8.00 79.0 <10 250 130 11.48 L-213 66.68 0.36 17.40 3.03 0.00 0.00 0.08 0.23 6.87 4.87 0.03 0.60 100.17 73 193 27 596 39.0 8 6 18 22 25 22 <12 762 12.00 163.0 <10 4.425 42.11 69.13 137 20 16. 48 39.14 0.663 0.738 0.813 11.74 L-214 66.63 0.39 17.62 1.54 0.00 0.03 0.00 0.24 7.68 3.92 0.06 0.63 98.74 65 167 24 662 77.0 <6 12 20 15 25 19 81 657 7.00 104.0 <10 181 89 11.60 L-215 70.53 0.23 16.82 0.65 0.00 0.00 0.00 0.15 10.32 0.19 0.03 0.36 99.30 7 72 15 443 23.0 6 7 6 9 27 <12 <12 71 <6 193.0 <10 18 <12 10.51 L-217 73.54 0.39 10.80 3.98 0.00 0.09 3.40 1.35 0.64 2.97 0.15 2.41 99.72 124 48 10 128 10.0 86 17 8 43 13 67 502 805 <6 <15 11 6.750 28.16 53.20 89 30 58.60 0.763 3.61 L-218 66.30 0.52 15.92 4.64 0.00 0.00 0.49 2.01 4.79 5.43 0.11 0.21 100.42 202 344 46 601 53.0 8 <6 6 30 22 15 16 793 8.00 99.0 <10 16.74 74.63 264.5 342 135 7.51 3 65.38 1.450 2.063 1.063 10.22 L-222 64.17 0.57 13.11 13.72 0.00 0.00 0.80 0.08 0.15 4.74 0.12 2.46 99.94 304 122 69 275 30.0 <6 7 <6 22 29 79 18 499 7.00 20.0 11 220 121 4.89 L-223 66.79 0.57 14.12 10.16 0.00 0.00 0.79 0.08 0.17 5.20 0.10 2.49 100.48 312 122 77 270 28.0 <6 <6 <6 27 28 68 18 468 8.00 21.0 <10 2.188 0.575 20.21 250 2 166 .0 0.988 5.37 L-224 62.03 0.58 13.42 15.02 0.00 0.00 0.62 0.07 0.24 5.69 0.11 2.33 100.13 261 103 35 301 28.0 9 8 <6 21 24 76 16 1065 8.00 19.0 <10 120 65 5.93 L-237 70.85 0.37 13.24 4.02 0.00 0.00 0.52 1.36 2.51 5.44 0.11 0.40 98.83 151 276 74 194 24.0 8 6 25 16 18 28 <12 815 <6 26.0 <10 273 148 7.95 L-238 70.02 0.51 13.56 3.71 0.00 0.00 0.67 1.50 2.89 6.16 0.15 0.74 99.92 156 260 58 240 27.0 7 <6 9 18 18 33 15 747 6.00 24.0 <10 130 67 9.05 L-239 70.02 0.51 13.56 3.71 0.00 0.00 0.67 1.50 2.89 6.16 0.15 0.74 99.92 156 260 58 240 27.0 7 <6 9 18 18 33 15 747 6.00 24.0 <10 130 67 9.05 L-241 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 156 229 55 174 24.1 0 0 0 0 0 0 594 0.00 0.0 0 2.4 9.21 45.22 10.98 0 0 1.91 5.17 1.86 0 0 1.64 9 .31 1.44 9.41 1.92 5.84 0.87 5.96 0.89 0.00 L-242 76.03 0.29 10.81 5.91 0.00 0.01 2.03 0.21 0.57 1.96 0.11 1.21 99.14 42 228 33 256 11.0 14 18 8 12 38 87 309 617 7.00 <15 29 148 112 2.53 L-248 64.40 0.91 15.35 6.34 0.00 0.00 2.74 3.49 2.97 2.10 0.26 0.53 99.08 126 300 54 205 42.0 15 15 13 28 25 109 39 271 6.00 <15 21 77 42 5.07 L-248-L G 76.71 0.14 13.26 0.92 0.00 0.00 0.04 0.66 3.71 4.49 0.04 0.32 100.29 121 314 48 206 20.0 9 7 8 16 19 35 25 745 <6 27.0 <10 139 68 8.20 L-249 70.32 0.42 14.04 3.50 0.00 0.00 0.75 1.96 3.00 4.50 0.14 0.29 98.93 123 309 49 211 23.0 8 7 8 16 19 45 21 716 <6 20.0 <10 0.700 0.725 4.800 124 0 46.24 1.313 0.350 0.688 7.50 L-257 73.62 0.26 13.30 1.97 0.00 0.00 0.15 1.23 3.67 5.29 0.05 0.55 100.10 214 117 53 208 25.0 6 <6 <6 13 22 <12 14 321 16.00 74.0 <10 113.8 42.95 114.8 192 66 5. 363 26.34 0.663 4.013 1.175 8.96 L-259 69.45 0.42 15.44 2.77 0.00 0.00 0.29 1.80 3.10 6.11 0.07 0.59 100.05 174 199 72 402 47.0 7 <6 <6 21 20 13 26 911 7.00 21.0 11 113 58 9.21 L-259-B 73.83 0.30 12.91 2.80 0.00 0.00 0.17 1.01 3.55 5.35 0.04 0.44 100.42 204 118 214 292 39.0 <6 <6 12 28 20 <12 15 617 10.00 29.0 <10 277 209 8.90 L-263 67.90 0.54 13.93 2.49 0.00 0.00 0.71 3.88 3.29 5.55 0.27 0.54 99.13 83 640 51 244 26.0 7 <6 23 15 20 34 16 920 <6 19.0 10 118.9 46.66 91.5 118 32 29.10 1.813 2.863 1.063 8.84 L-268 69.51 0.69 16.52 4.32 0.00 0.01 0.35 0.13 0.54 4.53 0.17 3.62 100.39 178 37 48 275 22.00 10 10 942 14 19 72 187 1116 <6 19.00 13.00 151 81 5.07 L-269 75.84 0.31 13.87 3.02 0.00 0.00 0.00 0.20 0.31 3.67 0.21 3.03 100.46 94 20 16 179 19.00 <6 8 6 11 15 27 185 291 <6 <15 <10 83 41 3.98 L-273 65.92 0.52 14.92 4.14 0.00 0.12 1.78 3.54 2.94 3.12 0.18 2.98 100.16 128 110 31 173 14.00 18 9 49 38 16 77 206 966 <6 <15 15.00 101 56 6.06 L-279 67.94 0.63 14.39 4.41 0.00 0.08 1.31 3.25 3.31 3.08 0.22 1.29 99.91 123 204 39 285 19.00 7 13 6 51 16 64 302 810 6.00 20 <10 10.43 33.43 80.75 140 39 69.25 0 .900 1.60 1.075 6.39 L-311 50.33 3.00 14.97 10.04 0.00 0.00 5.02 4.99 3.78 0.84 1.25 5.18 99.40 26 76 59 326 36.0 15 <6 19 39 19 121 16 88 8.00 <15 40 76 44 4.62 L-313 54.29 1.67 13.47 10.37 0.00 0.06 5.07 4.92 4.55 0.80 0.67 4.40 100.27 21 164 89 445 40.0 14 12 42 39 23 102 21 104 7.00 <15 36 139 75 5.35 L-314 43.72 7.81 12.73 11.28 0.00 0.08 6.68 7.01 3.38 0.36 0.64 6.73 100.42 14 77 56 25 36.0 20 19 28 49 18 438 50 60 <6 <15 55 27 16 3.74 L-318 47.28 3.04 15.31 7.93 0.00 0.04 6.86 13.85 4.18 0.56 0.38 0.96 100.39 9 154 37 163 27.0 23 53 9 22 19 258 99 20 <6 <15 30 68 33 4.74 L-321 71.94 0.71 9.67 11.04 0.00 0.03 3.43 0.30 0.68 0.05 0.12 2.40 100.37 6 81 59 242 18.0 96 18 16 30 15 157 95 65 <6 <15 12 102 61 0.73 L-322 70.45 0.74 13.65 5.38 0.00 0.02 0.48 0.08 0.13 7.57 0.08 1.74 100.32 168 30 37 264 30.0 12 7 13 35 21 49 33 498 <6 27.0 <10 171 74 7.70 L-323 67.04 0.81 14.15 7.57 0.00 0.02 0.52 0.19 0.17 8.21 0.17 1.61 100.46 173 29 37 302 35.0 26 9 17 28 20 58 32 525 <6 30.0 <10 153 71 8.38 L-324 62.05 0.97 14.50 7.90 0.00 0.06 1.43 1.71 3.85 6.29 0.29 1.25 100.30 112 230 57 362 35.0 20 16 62 121 21 96 27 1004 13.00 48.0 11 190 74 10.14 Table No. A15 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY NUMBER PAGE 3/10 Sample SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 100 4 30 5 20 3 9 35.5 7. 5 1.6 L-325 60.42 1.15 16.98 11.07 0.00 0.02 0.91 0.06 0.08 6.75 0.29 2.82 100.55 227 37 346 372 31.0 28 13 55 48 26 114 <12 508 6.00 27.0 <10 1460 819 6.83 L-341 63.54 0.75 13.15 4.88 0.00 0.03 1.09 5.99 6.86 0.95 0.32 1.14 98.70 19 703 76 329 29.0 11 9 31 21 21 45 20 72 <6 20.0 11 174 89 7.81 L-343 65.60 0.61 13.71 4.43 0.00 0.05 0.83 6.46 5.59 1.11 0.20 0.17 98.76 20 616 180 408 40.0 11 7 12 24 19 44 16 187 <6 35.0 12 162 103 6.70 L-344 61.49 1.13 15.69 3.77 0.00 0.07 1.27 6.94 5.64 1.83 0.40 0.98 99.21 47 555 126 485 41.0 10 <6 13 25 27 44 22 577 6.00 24.0 15 209 107 7.47 L-345 62.53 0.76 14.29 8.20 0.00 0.05 0.77 1.46 2.52 7.65 0.20 0.40 98.83 210 366 61 494 18.0 7 11 19 27 23 67 24 1440 6.00 <15 <10 174 94 10.17 L-346 70.01 0.49 13.71 5.02 0.00 0.05 0.31 0.96 3.40 5.99 0.10 0.64 100.68 195 168 69 469 27.0 12 <6 80 77 20 14 <12 774 11.00 24.0 <10 190 98 9.39 L-347 45.32 1.57 12.74 9.07 0.00 0.11 6.14 18.97 3.89 0.45 0.08 0.42 98.76 11 497 14 77 6.0 26 21 197 147 22 127 131 48 9.00 29.0 <10 111 57 4.34 L-348 68.82 0.46 13.11 3.52 0.00 0.14 0.29 3.80 4.97 3.37 0.13 0.31 98.92 38 762 56 329 19.0 7 <6 13 20 19 43 17 439 <6 40.0 <10 130 61 8.34 L-349 67.98 0.35 13.65 3.38 0.00 0.07 0.35 2.69 4.47 4.97 0.13 0.82 98.86 108 423 55 230 32.0 7 11 24 16 19 21 16 590 <6 23.0 <10 106 50 9.44 L-352 70.34 0.51 13.27 4.15 0.00 0.05 0.53 1.63 3.37 4.96 0.10 0.26 99.17 178 166 35 357 20.0 10 11 17 30 19 16 21 861 <6 19.0 <10 212 123 8.33 L-353 64.23 0.92 13.89 5.97 0.00 0.04 1.34 3.73 3.62 5.05 0.24 0.49 99.52 120 400 152 404 20.0 10 <6 67 24 21 36 19 606 6.00 20.0 12 141 73 8.67 L-354 64.83 0.81 14.83 6.19 0.00 0.07 1.46 2.45 3.15 4.06 0.20 0.95 99.00 138 207 77 435 25.0 11 17 115 78 20 71 22 977 <6 22.0 12 156 82 7.21 L-355 72.83 0.18 13.16 2.91 0.00 0.04 0.11 0.78 3.18 5.57 0.11 0.53 99.40 263 46 46 126 19.0 <6 7 20 21 18 79 38 135 8.00 21.0 <10 80 37 8.75 L-357 61.26 0.49 17.43 5.33 0.00 0.07 1.08 2.85 4.92 3.59 0.22 1.77 99.01 69 568 67 298 29.0 10 9 36 70 21 <12 12 1645 <6 <15 <10 111 55 8.51 L-358 63.11 0.65 15.74 6.29 0.00 0.07 1.04 3.80 4.03 2.31 0.17 1.51 98.72 80 492 29 233 13.0 12 10 479 261 22 58 16 950 <6 <15 14 9.988 28.21 68.75 106 32 98.13 0. 188 0.563 1.063 6.34 L-359 66.92 0.41 14.63 4.21 0.00 0.06 0.79 2.31 3.91 4.84 0.12 1.07 99.27 120 359 28 192 13.0 8 8 11 54 22 64 26 1134 <6 <15 10 149 76 8.75 L-360 68.89 0.31 14.44 3.71 0.00 0.04 0.60 1.23 3.18 6.02 0.07 0.91 99.40 100 369 67 134 15.0 7 6 9 46 16 40 20 2144 <6 <15 <10 114 57 9.20 L-361 63.38 0.74 15.35 6.08 0.00 0.06 1.57 3.80 4.38 2.06 0.22 1.49 99.13 118 544 17 246 8.0 12 15 20 78 21 36 <12 844 <6 <15 12 162 84 6.44 L-362 64.93 0.66 14.31 5.80 0.00 0.07 1.39 3.79 3.72 2.15 0.17 1.66 98.65 77 452 35 221 9.0 9 8 17 93 19 79 22 1523 <6 <15 10 113 61 5.87 L-363 65.30 0.64 15.16 5.30 0.00 0.09 1.23 3.11 3.95 3.37 0.16 1.49 99.80 119 398 31 202 9.0 11 6 18 69 20 73 20 1054 <6 <15 <10 82 40 7.32 L-364 74.42 0.19 11.94 2.26 0.00 0.02 0.40 0.26 3.54 5.07 0.04 0.68 98.82 236 34 42 207 10.0 <6 9 9 23 20 59 23 198 8.00 44.0 <10 179 88 8.61 L-365 72.12 0.48 12.08 4.21 0.00 0.04 1.25 0.45 2.64 4.87 0.12 1.33 99.59 146 81 75 353 24.0 8 7 24 38 19 <12 15 881 <6 26.0 <10 212 114 7.51 L-366 67.02 0.66 13.23 5.79 0.00 0.09 0.90 1.76 4.05 4.28 0.18 0.92 98.88 142 188 54 448 19.0 7 <6 13 86 20 21 12 1082 <6 <15 11 10.44 139.3 247.0 347 139 88.13 6. 08 42.50 13.2 2.600 8.33 L-367 72.13 0.48 11.76 4.45 0.00 0.06 1.30 3.17 1.69 2.41 0.13 1.70 99.28 59 232 237 162 22.0 10 <6 7 61 15 29 14 1518 <6 <15 <10 80 42 4.10 L-368 67.04 0.71 14.00 4.96 0.00 0.05 1.32 0.98 3.41 4.64 0.17 1.39 98.67 112 156 18 565 10.0 10 8 13 61 18 38 15 1652 <6 <15 <10 189 101 8.05 L-369 71.39 0.21 13.38 1.89 0.00 0.03 0.49 1.80 4.10 3.83 0.04 1.74 98.90 78 254 51 135 25.0 <6 6 119 118 16 53 20 789 <6 <15 <10 114.3 19.38 57.14 86 27 23.1 0.60 0 1.363 0.688 7.93 L-370 74.09 0.20 12.02 2.58 0.00 0.03 0.26 0.95 4.32 4.07 0.04 0.88 99.44 279 61 7 195 6.0 <6 10 10 32 21 16 <12 264 9.00 52.0 <10 145 73 8.39 L-371 70.77 0.25 14.56 1.78 0.00 0.03 0.40 1.37 4.85 4.06 0.08 1.04 99.19 104 650 59 127 23.0 <6 10 10 38 18 <12 15 1474 <6 <15 <10 110 52 8.91 L-372 54.14 0.84 17.15 9.33 0.00 0.12 3.24 7.00 4.31 2.25 0.28 1.85 100.51 86 764 11 193 8.0 20 9 57 116 21 23 18 423 <6 <15 24 135 71 6.56 L-373 72.41 0.25 14.10 2.22 0.00 0.03 0.41 1.36 3.49 4.20 0.05 0.93 99.45 114 353 31 147 8.0 6 7 17 28 14 198 12 1215 <6 17.0 <10 105.3 14.70 34.69 90 10 3.050 21. 31 0.200 0.600 7.69 L-374 70.46 0.20 14.58 2.28 0.00 0.04 0.31 1.75 5.02 3.92 0.05 0.77 99.38 97 473 10 105 6.0 <6 <6 9 33 17 17 14 1054 <6 <15 <10 49 23 8.94 L-375 69.92 0.45 12.64 4.64 0.00 0.07 0.33 1.04 3.27 5.81 0.13 0.77 99.07 140 197 47 365 30.0 7 11 26 55 18 22 19 1228 <6 21.0 <10 296 145 9.08 L-376 59.71 0.51 17.93 5.54 0.00 0.09 1.10 2.05 6.07 4.94 0.12 0.83 98.89 74 419 29 280 27.0 11 <6 18 58 20 67 <12 1036 <6 <15 <10 174 95 11.01 L-377 69.88 0.26 12.62 3.07 0.00 0.04 0.28 1.27 5.06 5.45 0.05 1.01 98.99 255 69 91 174 17.0 <6 9 167 109 19 12 19 365 8.00 45.0 <10 135 71 10.51 L-378 73.20 0.22 12.15 3.08 0.00 0.04 0.23 0.84 3.95 4.18 0.05 0.84 98.78 216 69 79 255 19.0 <6 10 163 98 19 <12 15 371 6.00 33.0 <10 267 135 8.13 L-379 72.89 0.21 12.77 2.54 0.00 0.03 0.45 0.72 6.12 2.92 0.07 0.62 99.34 139 54 59 84 27.0 <6 14 17 15 25 <12 20 133 10.00 <15 <10 39 18 9.04 L-380 70.37 0.39 13.41 3.59 0.00 0.05 0.27 0.92 3.65 5.94 0.09 0.69 99.37 177 135 57 365 28.0 7 10 116 83 18 17 13 1129 <6 18.0 <10 14.90 65.63 187.9 241 95 0.688 44.41 1.500 2.850 2.488 1.125 9.59 L-402 68.46 0.60 13.71 5.64 0.00 0.04 0.43 2.96 4.94 1.14 0.11 0.82 98.85 70 286 178 602 44.0 7 10 12 29 22 25 20 272 6.00 21.0 12 178 107 6.08 L-403 64.07 0.68 14.61 7.86 0.00 0.06 1.14 3.13 3.50 4.38 0.16 0.71 100.30 119 277 83 762 25.0 9 9 196 89 25 19 19 1054 8.00 17.0 15 141 80 7.88 L-405 52.10 1.22 16.06 10.02 0.00 0.11 5.30 8.98 3.30 1.08 0.15 0.71 99.03 23 882 24 121 14.0 37 72 30 53 17 220 35 226 <6 <15 26 78 37 4.38 L-406 46.64 2.48 13.15 14.14 0.00 0.23 6.55 10.17 3.29 0.80 0.26 1.09 98.80 11 282 38 180 17.0 43 73 80 104 18 374 106 118 <6 <15 37 29 18 4.09 L-407 60.09 1.12 13.19 6.31 0.00 0.07 1.49 8.27 4.03 3.86 0.30 0.61 99.34 92 396 79 532 28.0 13 8 43 40 19 71 29 689 7.00 26.0 14 188 96 7.89 L-408 70.26 0.33 13.59 3.87 0.00 0.05 0.26 1.23 3.49 5.24 0.07 0.43 98.82 241 95 104 348 33.0 7 6 15 34 23 <12 13 483 12.00 32.0 <10 241 121 8.73 L-409 69.36 0.41 14.76 3.25 0.00 0.02 0.49 1.13 4.47 5.43 0.10 0.44 99.86 206 151 43 313 32.0 6 <6 10 16 19 25 12 677 13.00 53.0 <10 120 60 9.90 L-410 67.74 0.44 12.99 8.55 0.00 0.02 0.88 0.29 0.17 4.34 0.09 3.18 98.69 233 16 25 177 33.0 9 9 489 218 17 51 14 187 7.00 32.0 <10 147 80 4.51 L-411 8.09 0.09 0.85 0.57 0.00 0.02 4.72 43.80 0.04 0.35 0.16 41.87 100.56 6 87 4 17 3.0 <6 <6 <6 16 <9 <12 <12 23 <6 <15 45 12 <12 0.39 L-416 52.44 0.65 15.34 8.63 0.00 0.15 7.28 12.42 2.55 0.73 0.07 0.20 100.46 6 126 17 41 5.0 34 72 94 84 17 195 217 43 6.00 <15 42 <12 <12 3.28 L-420 71.91 0.31 13.61 2.62 0.00 0.02 0.48 0.67 4.95 2.98 0.06 1.08 98.69 187 93 38 178 28.0 8 10 31 26 18 20 20 532 13.00 37.0 <10 165 103 7.93 L-421 69.53 0.52 14.84 3.30 0.00 0.03 0.79 1.40 2.52 6.69 0.24 0.74 100.60 278 240 17 303 18.0 7 <6 34 24 18 42 19 1428 <6 57.0 <10 229 101 9.21 L-433 51.23 2.42 14.76 11.92 0.00 0.16 4.74 8.16 3.82 2.33 0.42 0.59 100.55 71 396 44 261 22.0 28 11 45 99 20 275 62 384 7.00 <15 27 96 52 6.15 L-434 69.24 0.53 13.96 4.52 0.00 0.06 0.74 1.98 1.92 4.77 0.13 1.32 99.17 149 247 8 411 7.0 8 9 25 35 16 19 18 869 <6 <15 30 18 <12 6.69 L-435 67.58 0.43 15.29 3.91 0.00 0.05 0.36 1.59 3.89 6.45 0.10 0.32 99.97 142 271 34 389 11.0 8 <6 29 34 21 15 13 1227 <6 <15 <10 86 43 10.34 L-436 73.93 0.27 12.03 2.68 0.00 0.04 0.17 1.02 4.15 4.81 0.06 0.39 99.55 235 74 45 303 31.0 <6 <6 10 21 21 <12 <12 195 26.00 99.0 <10 223 114 8.96 L-437 55.61 1.95 14.33 9.89 0.00 0.14 2.79 5.09 3.77 4.40 0.52 0.58 99.07 113 395 52 404 32.0 21 8 121 132 22 144 21 736 <6 <15 18 111 56 8.17 L-438 53.44 1.57 14.02 8.54 0.00 0.13 5.89 7.86 3.34 3.75 0.49 0.76 99.79 171 402 43 390 31.0 27 77 43 71 19 163 250 592 7.00 22.0 22 99 55 7.09 Table No. A15 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY NUMBER PAGE 4/10 Sample SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 100 4 30 5 20 3 9 35.5 7. 5 1.6 L-439 70.07 0.33 12.99 4.06 0.00 0.02 0.22 0.77 4.27 5.46 0.05 0.62 98.86 243 66 90 572 46.0 <6 3 21 16 25 <12 <12 163 19.00 90.0 <10 237 124 9.73 L-440 51.34 2.12 14.48 11.82 0.00 0.15 4.77 7.19 3.18 2.19 0.48 0.89 98.61 74 395 39 348 19.0 32 29 27 99 21 244 101 373 <6 <15 29 56 29 5.37 L-441 62.98 1.11 14.13 7.49 0.00 0.12 0.99 2.75 3.71 5.30 0.35 0.46 99.39 180 226 74 414 46.0 10 <6 13 88 24 28 <12 893 6.00 19.0 12 187 98 9.01 L-442 78.22 0.33 8.81 3.27 0.00 0.03 0.00 0.10 0.23 7.61 0.06 0.34 99.00 227 44 99 349 18.0 <6 <6 16 16 12 27 <12 618 <6 44.0 <10 288 149 7.84 L-443 76.23 0.44 9.57 5.13 0.00 0.03 0.10 0.43 0.20 6.79 0.05 0.40 99.37 201 24 64 391 48.0 8 7 12 14 14 28 <12 499 <6 100.0 <10 49 25 6.99 L-444 52.77 2.43 15.66 11.98 0.00 0.17 3.98 7.06 3.24 1.98 0.56 0.22 100.05 43 404 41 170 21.0 33 14 27 108 21 245 54 396 6.00 <15 33 67 36 5.22 L-458 72.83 0.09 13.43 1.35 0.00 0.02 0.00 0.20 3.52 6.94 0.03 0.37 98.78 277 30 72 45 13.0 <6 <6 9 11 18 <12 13 129 8.00 <15 <10 38 42 10.46 L-459 61.30 0.79 13.54 9.09 0.00 0.13 3.38 5.88 3.02 1.16 0.10 0.63 99.02 87 204 22 81 8.0 26 40 111 107 19 181 57 287 <6 <15 23 54 30 4.18 L-460 74.38 0.43 11.58 4.11 0.00 0.03 0.62 1.86 3.67 2.33 0.12 0.34 99.47 68 482 13 632 7.0 8 9 19 63 18 22 14 596 <6 20.0 <10 197 102 6.00 L-461 71.85 0.20 14.11 1.77 0.00 0.02 0.26 1.01 3.45 5.34 0.06 0.70 98.77 178 241 14 65 10.0 <6 <6 30 36 18 <12 13 1222 <6 15.0 <10 43 21 8.79 L-462 72.04 0.34 13.78 2.58 0.00 0.02 0.38 1.21 3.18 5.19 0.04 0.37 99.13 114 630 5 95 11.0 <6 <6 11 32 17 25 <12 3607 <6 16.0 <10 61 25 8.37 L-463 48.36 2.43 14.19 14.79 0.00 0.19 7.26 7.68 2.85 1.01 0.40 -0.53 98.63 25 255 38 193 15.0 39 11 16 153 21 133 94 285 <6 <15 30 30 18 3.86 L-464 5.46 0.07 0.00 77.49 0.00 0.08 0.50 6.09 0.10 0.52 0.06 3.16 93.53 14 13 16 17 3.0 25 185 184 122 <9 34 <12 142 29.00 <15 37 <12 <12 0.62 L-465 14.01 0.58 2.56 64.74 0.00 0.03 0.70 0.17 0.06 0.43 0.12 12.85 96.25 25 76 9 129 17.0 13 85 143 102 11 127 <12 694 24.00 <15 36 <12 <12 0.49 L-466 73.93 0.13 12.78 1.65 0.00 0.03 0.08 0.98 4.27 4.50 0.03 0.30 98.68 351 83 31 75 39.0 <6 <6 15 21 24 <12 14 225 <6 23.0 <10 57 27 8.77 L-467 70.78 0.25 13.75 2.33 0.00 0.02 0.18 0.87 4.53 5.45 0.08 0.50 98.74 145 1046 29 208 18.0 7 10 12 30 22 16 <12 2676 <6 67.0 <10 224 130 9.98 L-600A 76.09 0.13 11.83 1.93 0.00 0.04 0.07 0.45 3.85 5.55 0.06 0.40 100.40 160 59 23 137 14.0 <6 6 14 29 15 <12 68 508 <6 43.0 <10 141 77 9.40 L-602 70.15 0.49 13.13 3.63 0.00 0.06 0.83 1.80 3.43 4.54 0.16 0.98 99.20 214 137 64 305 26.0 8 7 9 60 18 13 189 716 <6 36.0 <10 14.31 62.39 169.4 213 86 53.19 0.8 13 4.213 1.338 7.97 L-605 76.55 0.12 12.03 1.16 0.00 0.01 0.02 0.81 3.42 5.47 0.07 0.41 100.07 198 99 7 89 7.0 <6 <6 9 19 13 <12 227 772 <6 42.0 <10 148 102 8.89 L-606 72.56 0.36 12.83 3.51 0.00 0.06 0.48 1.32 3.22 5.19 0.07 0.73 100.33 185 105 38 202 17.0 <6 6 7 61 18 20 57 781 <6 38.0 <10 227 149 8.41 L-625 74.31 0.32 12.49 2.19 0.00 0.04 0.42 0.94 5.72 2.00 0.10 0.70 99.23 43 78 49 280 30.0 <6 15 753 26 15 21 123 493 <6 <15 <10 125 54 7.72 L-626 75.44 0.32 12.53 3.15 0.00 0.05 0.57 0.71 5.99 1.04 0.06 0.63 100.49 18 64 50 263 30.0 <6 13 1078 41 17 21 53 609 <6 <15 <10 10.56 33.25 65.50 112 31 38.58 1 .038 3.050 1.238 7.03 L-633 51.27 1.55 16.00 10.81 0.00 0.18 6.69 7.17 3.71 1.69 0.26 1.07 100.40 56 239 26 123 13.0 52 115 499 110 17 279 202 550 <6 <15 31 12.91 15.65 35.85 43 11 224 .0 5.638 0.563 1.225 5.40 L-635 62.14 0.98 15.43 6.05 0.00 0.12 3.29 3.28 7.37 0.22 0.15 1.00 100.03 9 33 31 241 19.0 20 64 64 46 20 134 101 58 <6 <15 19 9.025 23.53 48.81 67 21 90.25 0.650 2.688 0.900 1.075 7.59 L-637 69.84 0.53 13.33 5.85 0.00 0.06 0.58 2.19 5.95 0.76 0.10 1.00 100.19 17 165 56 727 29.0 8 18 128 34 20 26 49 359 <6 <15 10 122.5 60.93 134.1 180 93 3.313 34. 34 0.588 4.300 1.525 6.71 L-638 77.05 0.18 11.68 2.36 0.00 0.04 0.14 0.62 4.27 3.73 0.02 0.42 100.51 59 91 35 148 17.5 <6 9 95 29 15 14 66 751 <6 <15 <10 10.8 7.71 40.96 10.40 116 53 0.41 4. 36 0.51 0 0 1.02 7.02 1.09 6.94 1.36 3.85 0.54 3.56 0.51 8.00 L-641 50.76 2.24 13.78 12.16 0.00 0.24 6.49 7.32 4.30 0.62 0.40 1.90 100.21 27 195 33 131 15.0 48 90 704 133 17 262 196 247 <6 <15 34 12.08 46.00 28 <12 4.92 L-645 56.67 1.27 14.07 9.26 0.00 0.09 0.42 5.87 8.40 0.16 0.33 3.96 100.50 5 67 38 214 17.0 9 21 6 21 19 113 185 87 <6 <15 26 49 22 8.56 L-648 72.50 0.35 12.81 4.25 0.00 0.05 0.69 0.64 7.27 1.32 0.06 0.59 100.53 25 69 21 248 12.0 6 17 1546 44 13 47 67 1144 <6 <15 <10 89 30 8.59 L-649 73.86 0.30 12.07 4.77 0.00 0.06 0.53 0.64 5.74 1.86 0.05 0.56 100.44 37 63 16 193 11.0 9 19 2238 37 11 50 78 1330 <6 <15 <10 74 19 7.60 L-668 62.61 0.89 17.32 4.83 0.00 0.14 0.72 1.80 6.42 4.79 0.36 0.59 100.47 121 474 69 710 193.0 7 7 6 127 26 14 139 2037 7.00 22.0 <10 13.58 101.4 182.0 235 110 4 .450 23.33 0.850 3.850 2.38 1.025 11.21 L-669 64.34 0.61 16.76 4.66 0.00 0.12 0.36 1.46 6.43 4.80 0.23 0.74 100.51 115 350 73 378 204.4 <6 9 7 146 28 <12 124 1647 9.00 31.0 <10 21.7 17.80 102.06 28.00 267 137 0.70 8.24 12.29 0 0 3.96 14.64 2.26 14.05 2.62 7.39 1.00 5.97 0.73 11.23 L-670 57.01 1.45 15.14 11.08 0.00 0.21 1.42 2.33 6.69 3.35 0.53 1.32 100.53 173 1219 73 1843 458.0 <6 9 9 85 42 <12 18 767 17.00 46.0 <10 3.125 27.46 72.13 219 4 2 74.00 0.288 2.088 0.988 10.04 L-675 60.71 0.10 21.99 3.59 0.00 0.09 0.13 0.94 4.92 6.41 0.03 1.61 100.52 125 384 123 1520 345.0 7 9 23 167 30 20 17 1321 10.00 78.0 11 140.0 591.5 844 440 238. 0 3.438 4.23 6.513 1.975 11.33 L-676 59.35 0.87 18.13 5.92 0.00 0.17 1.24 2.05 5.20 5.55 0.24 1.84 100.56 226 634 58 553 139.0 7 7 11 177 26 19 31 1591 <6 19.0 <10 180 85 10.75 L-691 50.24 3.31 12.95 14.15 0.00 0.21 4.13 6.53 2.95 2.82 0.55 1.51 99.35 151 589 52 368 62.0 39 32 190 166 19 357 66 617 <6 <15 33 110 61 5.77 L-693 71.37 0.48 11.65 6.47 0.00 0.14 0.19 0.77 4.62 4.46 0.09 0.31 100.55 86 98 31 132 105.3 6 7 14 128 33 <12 60 241 2.29 8.6 <10 4.8 13.2 114 35.3 357 216 0.23 2 .81 4.94 0.94 7.69 0.92 5.26 0.97 2.65 0.43 3.26 0.54 9.08 L-694 59.18 1.09 17.07 5.91 0.00 0.17 1.01 2.48 6.84 4.89 0.36 0.54 99.54 106 633 39 333 93.0 7 <6 10 107 23 27 <12 1995 <6 <15 <10 166 87 11.73 L-695 46.29 3.29 13.34 13.54 0.00 0.48 3.19 4.92 4.10 3.51 0.68 6.78 100.12 197 399 53 329 54.0 27 22 89 120 19 353 28 639 <6 <15 26 64 30 7.61 L-697 59.94 0.86 16.90 5.28 0.00 0.17 0.99 2.06 6.58 4.59 0.32 1.54 99.23 169 491 151 1363 432.0 8 9 5 129 26 <12 117 1444 15.00 51.0 <10 127.3 480.3 582 291 1.7 13 107.9 4.550 15.49 10.2 2.075 11.17 L-698 71.68 0.46 11.40 5.84 0.00 0.10 0.10 0.85 4.91 4.10 0.10 0.40 99.94 77 45 50 329 124.0 <6 7 7 104 35 <12 207 157 <6 <15 <10 16.00 66.88 227.6 372 143 92.13 0 .250 2.03 1.338 9.01 L-699 63.41 0.28 17.28 5.27 0.00 0.20 0.34 0.93 7.40 4.73 0.12 0.56 100.52 98 114 75 1246 307.0 <6 10 7 147 34 <12 126 458 15.00 50.0 <10 470 310 12.13 L-708 47.15 0.47 8.72 11.27 0.00 0.53 13.12 14.15 1.46 1.77 0.04 1.79 100.47 86 578 146 469 126.0 16 26 13 279 17 68 14 2096 <6 <15 23 258 97 3.23 L-712 79.11 0.04 12.04 0.83 0.00 0.04 0.11 0.40 5.47 1.95 0.01 0.54 100.54 33 159 12 17 7.0 <6 10 8 35 18 <12 47 662 <6 <15 <10 106.5 13.44 41 7 1.700 0.213 0.638 7 .42 L-713 71.32 0.16 14.36 2.37 0.00 0.05 0.08 0.32 5.76 5.66 0.02 0.41 100.51 117 94 30 277 71.0 <6 8 9 53 25 19 49 909 <6 <15 <10 120.8 80.38 294.6 436 188 0.963 24. 54 0.763 1.200 0.875 11.42 L-714 77.55 0.05 13.19 0.73 0.00 0.03 0.17 0.85 6.33 0.76 0.02 0.67 100.35 16 338 9 250 9.0 <6 9 8 40 23 <12 50 538 <6 16.0 <10 106.0 2.950 83 3.213 0.188 0.488 7. 09 L-714a 74.47 0.12 14.63 0.94 0.00 0.04 0.12 0.59 8.15 0.94 0.05 0.41 100.46 16 152 25 237 50.0 <6 8 <6 17 0 12 160 606 0.00 0.0 0 0 0 9.09 L-715 72.13 0.48 13.02 3.49 0.00 0.09 0.48 1.12 3.88 4.88 0.12 0.50 100.19 118 147 58 348 25.0 8 11 12 67 18 28 47 1230 <6 19.0 <10 75.75 38.91 87.88 154 44 38.90 1.13 3.588 1.363 8.76 L-716 73.88 0.30 12.54 2.79 0.00 0.04 0.41 0.98 4.49 3.98 0.04 0.68 100.13 69 164 38 332 15.9 8 11 12 51 16 19 57 1389 7.00 24.0 <10 9.2 7.00 41.87 11.18 134 66 0. 83 6.58 0.73 0 0 1.48 5.96 0.90 6.07 1.28 4.03 0.63 4.55 0.70 8.47 L-722 7.50 0.04 0.13 9.55 0.00 0.68 2.58 43.77 0.00 0.00 0.03 36.24 100.52 7 210 260 119 13.0 23 <6 5 37 <9 194 12 145 6.00 27.0 54 17.16 15.61 10 <12 229.3 0.263 0.863 0.00 L-728 75.06 0.16 10.35 2.83 0.00 0.14 0.22 2.20 6.61 0.86 0.06 2.04 100.53 23 140 58 212 33.0 <6 10 15 45 18 14 67 581 4.64 20.9 15 24.2 17.2 82.2 20.2 171 73 0.33 6.35 2.52 3.25 14.4 2.01 12.1 2.23 6.18 0.99 6.52 1.07 7.47 L-729 73.58 0.31 12.64 2.31 0.00 0.05 0.34 0.84 3.69 4.96 0.03 1.70 100.45 113 82 46 281 24.0 <6 6 6 60 <12 58 957 8.65 L-740 56.74 0.26 18.91 5.92 0.00 0.18 0.21 1.03 6.29 4.68 0.03 6.26 100.51 170 442 26 1803 563.0 <6 11 8 189 42 <12 27 617 27.00 18.0 <10 8.750 22.20 71.88 112 3 6 114.8 0.500 0.138 0.838 10.97 L-741 56.63 0.47 19.54 7.23 0.00 0.44 0.80 3.09 4.14 7.21 0.11 0.91 100.57 169 548 49 640 337.0 <6 <6 14 164 34 14 18 1955 19.00 <15 <10 14.68 51.69 210.8 248 13 1 127.0 1.813 1.863 1.100 11.35 L-742 68.41 0.18 10.00 3.45 0.00 0.20 2.09 0.90 5.40 1.17 0.03 8.44 100.27 59 181 41 310 26.0 11 13 32 227 19 18 44 802 <6 21.0 <10 2.538 32.53 52.30 79 44 71.88 0 .588 1.350 0.600 6.57 Table No. A15 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY NUMBER PAGE 5/10 Sample SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 100 4 30 5 20 3 9 35.5 7. 5 1.6 L-754 53.02 1.59 13.32 16.18 0.00 0.28 6.53 7.50 0.32 1.02 0.30 0.15 100.21 318 84 40 94 8.0 50 53 94 252 17 393 178 235 <6 <15 49 25 12 1.34 L-759 74.06 0.03 14.47 0.47 0.00 0.04 0.02 0.70 3.55 5.54 0.06 0.94 99.88 109 124 20 16 7.0 <6 <6 <6 12 13 <12 185 649 <6 <15 <10 12 <12 9.09 L-772 72.55 0.03 14.29 0.43 0.00 0.03 0.03 0.05 2.34 10.07 0.02 0.67 100.51 201 100 7 <8 4.0 <6 <6 8 28 13 <12 44 579 <6 <15 <10 21 <12 12.41 L-773 74.83 0.06 14.98 0.87 0.00 0.02 0.11 0.80 5.35 3.07 0.04 0.41 100.54 76 71 103 64 14.0 <6 10 8 43 20 <12 47 176 <6 <15 <10 25 <12 8.42 L-783 71.86 0.45 13.96 3.32 0.00 0.08 0.50 0.78 3.49 5.15 0.18 0.71 100.48 223 85 54 273 22.0 <6 6 9 49 17 25 239 859 <6 27.0 <10 161 75 8.64 L-784 71.83 0.39 13.23 3.59 0.00 0.06 0.56 1.31 3.67 5.07 0.09 0.70 100.50 193 105 58 312 23.0 <6 7 7 59 17 23 63 1049 7.00 26.0 <10 11.25 37.06 98.50 155 51 1.51 3 41.66 0.78 3.938 1.400 8.74 L-789 63.91 1.38 14.35 7.45 0.00 0.07 1.13 1.09 4.87 5.21 0.41 0.55 100.42 125 29 66 715 149.0 <6 6 10 80 21 32 135 1019 8.00 15.0 <10 15.46 50.01 136.3 196 67 12 7.6 2.03 3.88 1.575 10.08 L-791a 72.44 0.40 13.01 3.67 0.00 0.06 0.32 0.54 3.80 5.16 0.10 0.61 100.11 141 25 97 685 130.0 <6 7 <6 35 17 <12 220 637 6.00 32.0 <10 108.5 22.50 36.51 63 18 2. 038 7.288 0.438 5.688 1.400 8.96 L-791b 76.38 0.14 12.55 1.25 0.00 0.02 0.00 0.51 3.09 5.85 0.03 0.29 100.11 270 74 83 70 65.0 <6 10 <6 15 22 16 234 332 8.00 17.0 <10 224 108 8.94 L-793 74.92 0.33 12.39 2.15 0.00 0.08 0.24 1.00 3.28 5.24 0.14 0.37 100.14 251 140 81 213 78.0 <6 7 7 34 19 22 390 435 12.00 61.0 <10 119.3 50.99 175.4 234 98 1.8 00 28.45 0.938 6.63 1.700 8.52 L-797 75.11 0.21 13.05 1.92 0.00 0.04 0.08 0.51 3.62 4.63 0.08 0.61 99.86 225 107 23 199 38.0 <6 6 <6 33 21 17 372 658 6.00 37.0 <10 132 76 8.25 L-798 72.64 0.26 14.07 2.13 0.00 0.08 0.26 1.09 3.42 5.17 0.12 0.91 100.15 222 204 26 229 48.0 <6 <6 <6 40 20 16 285 1117 7.00 27.0 <10 211 102 8.59 L-799 73.13 0.08 13.93 1.96 0.00 0.06 0.04 0.95 3.84 4.84 0.13 0.63 99.59 153 168 53 183 14.0 <6 7 11 19 18 29 326 727 7.00 <15 <10 102 36 8.68 L-802 73.34 0.23 14.56 1.83 0.00 0.05 0.29 1.08 3.46 4.55 0.13 0.84 100.36 234 141 32 142 41.0 <6 6 <6 51 19 22 260 745 <6 15.0 <10 77 38 8.01 L-808 70.53 0.14 15.35 1.50 0.00 0.05 0.42 1.71 4.80 3.67 0.07 2.04 100.28 140 89 12 29 13.9 <6 7 10 71 16 13 39 154 <6 <15 <10 32.4 2.03 9.16 2.46 26 <12 5.99 1.17 1.22 0 0 0.50 1.81 0.31 2.11 0.42 1.29 0.21 1.48 0.22 8.47 L-809 71.56 0.07 14.95 1.24 0.00 0.03 0.23 0.87 3.46 7.52 0.06 0.50 100.49 253 92 19 <8 9.0 <6 7 11 56 16 <12 27 301 <6 <15 <10 29 <12 10.98 L-810 73.89 0.06 14.05 1.11 0.00 0.04 0.16 1.04 4.00 5.44 0.04 0.50 100.33 173 85 7 <8 7.0 9 10 13 50 14 <12 56 249 <6 <15 <10 24 <12 9.44 L-812 75.60 0.08 12.89 1.27 0.00 0.03 0.25 1.29 4.03 4.17 0.09 0.71 100.41 141 104 86 215 10.0 <6 8 9 67 13 <12 34 439 17.00 30.0 <10 93 55 8.20 L-813 71.80 0.04 15.51 0.86 0.00 0.03 0.12 1.40 4.26 5.59 0.08 0.78 100.47 173 115 65 77 6.0 <6 9 13 23 14 <12 42 625 13.00 21.0 <10 63 22 9.85 L-814 89.59 0.02 5.33 0.65 0.00 0.02 0.02 0.84 2.94 0.31 0.04 0.63 100.39 23 38 5 <8 4.0 <6 7 10 54 <9 <12 77 50 <6 <15 <10 26 <12 3.25 L-815 69.73 0.30 14.51 3.35 0.00 0.08 0.84 1.34 3.85 5.59 0.16 0.65 100.40 214 122 43 268 25.0 <6 8 10 75 17 12 68 584 42.00 16.0 <10 68 29 9.44 L-816 74.57 0.30 12.43 3.00 0.00 0.06 0.39 1.37 6.02 1.96 0.04 0.44 100.58 43 91 52 284 32.0 <6 13 104 62 17 18 81 386 <6 <15 <10 115.9 35.64 72.13 122 33 1.200 32 .86 1.13 2.68 1.175 7.98 L-832 73.67 0.32 12.24 1.83 0.00 0.04 0.14 0.46 4.39 5.23 0.11 0.63 99.06 154 297 38 307 15.0 8 10 19 70 17 46 <12 1468 <6 19.0 <10 121 58 9.62 L-834 59.92 0.47 16.55 4.88 0.00 0.05 0.10 1.72 0.29 14.06 0.12 1.28 99.44 283 70 49 274 20.0 7 <6 14 19 9 26 <12 1842 7.00 25.0 <10 12.06 41.53 111.4 192 54 2.87 5 77.25 0.700 2.450 1.275 14.35 L-835 65.67 0.65 15.35 3.98 0.00 0.08 0.87 2.29 4.41 4.48 0.19 1.44 99.41 135 203 38 342 15.0 <6 <6 7 68 17 40 <12 1318 <6 15.0 10 127 60 8.89 L-836 67.42 0.74 14.82 4.07 0.00 0.10 0.86 2.21 4.08 4.77 0.20 0.79 100.06 159 266 40 343 17.0 6 <6 19 69 0 45 <12 1272 0.00 0.0 0 0 0 8.85 L-838 67.61 0.61 14.50 3.84 0.00 0.09 0.82 2.37 3.62 4.48 0.18 0.50 98.62 208 69 22 93 15.6 <6 8 10 30 15 12 <12 552 3.98 21.2 <10 130 55 8.10 L-839 76.62 0.29 11.26 1.41 0.00 0.04 0.23 0.35 3.05 5.28 0.07 0.47 99.07 218 67 27 163 17.0 <6 9 19 35 13 12 <12 565 <6 16.0 <10 102 44 8.33 L-840 70.88 0.42 13.61 2.64 0.00 0.07 0.48 1.29 3.97 4.93 0.13 0.75 99.17 176 247 37 237 15.0 <6 8 20 47 16 20 <12 1054 <6 18.0 <10 127 62 8.90 L-842 65.32 0.68 14.27 4.45 0.00 0.10 1.13 2.64 4.17 3.50 0.19 2.76 99.21 141 316 38 361 16.0 10 11 37 83 16 49 13 1668 <6 16.0 12 11.19 33.40 82.63 135 41 1.475 6 2.88 1.013 1.638 1.075 7.67 L-843 75.42 0.33 12.58 1.52 0.00 0.03 0.25 0.31 3.01 4.39 0.10 1.13 99.07 163 61 41 199 20.0 <6 <6 6 25 14 16 177 907 <6 21.0 <10 113.0 35.20 74.00 126 32 3.950 9. 950 0.650 2.038 0.875 7.40 L-844 68.18 0.63 14.42 3.75 0.00 0.08 0.82 2.22 3.87 4.35 0.20 1.02 99.54 137 259 39 345 16.0 6 7 20 62 17 42 <12 1378 6.00 16.0 <10 129 63 8.22 L-846 67.61 0.60 14.35 3.72 0.00 0.08 0.89 1.97 4.09 4.59 0.18 0.78 98.86 134 246 44 306 16.0 6 10 18 56 15 39 <12 1240 <6 19.0 <10 11.76 41.76 86.50 133 45 50.38 1.000 1.913 1.088 8.68 L-849 73.54 0.33 12.99 1.74 0.00 0.02 0.20 0.14 3.78 5.57 0.04 0.55 98.90 189 43 24 243 27.0 <6 7 <6 22 18 17 217 451 <6 16.0 <10 107.3 30.33 47.85 152 20 1.013 33 .66 0.263 0.238 0.375 9.35 L-850 71.15 0.38 13.69 2.97 0.00 0.05 0.47 1.56 3.09 4.96 0.10 0.48 98.90 264 153 22 241 15.0 7 7 23 57 17 27 13 919 <6 46.0 <10 116.9 48.33 131.0 171 67 4.763 34. 13 0.588 0.18 0.725 8.05 L-855 76.63 0.15 11.87 1.14 0.00 0.02 0.05 0.25 4.70 4.06 0.02 0.25 99.14 88 39 10 71 10.0 <6 10 9 11 15 <12 <12 328 <6 <15 <10 39 16 8.76 L-857 73.33 0.32 13.00 1.84 0.00 0.04 0.43 1.21 4.01 4.21 0.11 1.00 99.50 155 211 17 141 14.0 <6 9 26 28 15 22 <12 1081 <6 <15 <10 80 38 8.22 L-863 64.77 0.71 14.71 5.42 0.00 0.08 1.57 3.06 3.37 3.86 0.24 1.14 98.93 155 288 33 228 19.0 14 15 23 72 18 100 122 1004 <6 17.0 11 89 44 7.23 L-864 66.28 0.74 14.57 5.01 0.00 0.09 1.56 2.96 3.05 4.14 0.33 1.62 100.35 97 249 23 39 11.9 10 16 28 58 16 91 273 1039 3.14 13.4 10 17.4 6.19 37.8 9.86 78 45 0.83 1.38 0.83 1.27 5.35 0.73 4.38 0.86 2.38 0.34 2.22 0.32 7.19 L-864 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0 0 0 0 0.0 0 0 0 0 <9 <6 <15 <10 23 <12 0.00 L-865 66.29 0.76 14.63 4.88 0.00 0.08 1.51 2.53 3.09 4.38 0.27 1.26 99.68 179 240 34 241 19.0 10 20 21 68 17 84 226 1100 <6 16.0 10 129 67 7.47 L-868 66.57 0.77 14.29 4.73 0.00 0.10 1.11 2.09 3.56 4.38 0.29 1.15 99.04 112 186 32 22 15.3 10 13 14 . 19 68 114 1100 <6 <15 10 14.6 8.72 52.03 13.28 154 79 1.07 0 .84 0.55 0 0 1.83 7.21 0.99 6.12 1.18 3.36 0.47 3.09 0.45 7.94 L-874 96.83 0.09 0.64 0.69 0.00 0.01 0.00 0.02 0.02 0.31 0.03 0.08 98.72 11 8 5 29 4.0 <6 13 8 6 17 <12 538 30 6.00 17.0 11 144 73 0.33 L-874a 67.47 0.89 13.68 4.67 0.00 0.10 1.05 1.71 3.48 4.99 0.27 1.09 99.40 155 181 57 348 24.0 12 14 19 69 63 17 1380 8.47 L-875 66.20 0.78 14.38 5.11 0.00 0.12 1.18 2.90 3.74 4.25 0.30 1.32 100.28 138 222 46 329 23.0 7 13 14 68 18 71 181 1294 <6 <15 10 12.16 42.90 111.4 157 54 76.63 1 .588 1.963 1.225 7.99 L-877 66.24 0.93 13.94 5.04 0.00 0.09 1.14 2.08 3.48 4.74 0.41 1.24 99.33 140 224 54 377 23.0 9 16 22 75 19 62 17 1371 <6 17.0 10 169 87 8.22 L-878 67.83 0.67 13.61 4.34 0.00 0.09 0.95 1.67 3.73 4.58 0.23 1.08 98.78 152 176 57 329 19.0 9 12 34 71 19 46 16 1143 <6 17.0 <10 12.29 39.36 92.38 150 41 56.10 1 .150 2.563 1.213 8.31 L-895 55.24 0.90 18.42 6.32 0.00 0.11 3.12 4.54 4.23 4.61 0.50 1.93 99.92 164 840 22 172 7.0 18 43 164 69 18 134 91 1382 <6 <15 14 8.250 23.24 53.84 74 22 98.63 0. 33 0.363 0.913 8.84 L-898 69.20 0.58 12.94 5.11 0.00 0.08 0.60 1.62 4.21 5.14 0.15 0.09 99.72 112 193 33 215 15.0 <6 7 17 46 27 189 1049 9.35 L-899 71.98 0.41 12.65 2.41 0.00 0.06 0.72 1.79 4.23 3.72 0.11 0.69 98.77 112 193 33 210 18.0 <6 7 17 46 17 26 182 1049 <6 16.0 <10 119 56 7.95 L-900 67.40 0.67 14.52 4.30 0.00 0.08 1.12 2.21 4.83 4.01 0.21 0.90 100.25 101 244 40 361 16.0 8 8 17 43 17 48 <12 1239 <6 16.0 11 127 61 8.84 L-902 77.60 0.17 12.00 0.96 0.00 0.02 0.08 0.11 4.16 4.81 0.10 0.34 100.35 160 35 18 95 22.0 <6 7 33 15 15 13 <12 131 <6 25.0 <10 85 39 8.97 L-903 79.24 0.19 10.48 1.02 0.00 0.02 0.12 0.14 2.98 4.99 0.04 0.32 99.54 262 21 23 103 16.0 <6 8 10 15 13 <12 <12 132 <6 25.0 <10 80 38 7.97 L-904 76.77 0.24 11.40 1.61 0.00 0.05 0.16 0.10 3.59 4.81 0.05 0.45 99.23 242 44 30 149 18.0 <6 8 15 37 15 <12 14 233 <6 21.0 <10 107.0 29.65 49.94 99 23 7.188 0.2 8 1.300 0.900 8.40 L-905 77.13 0.29 11.44 1.46 0.00 0.03 0.23 0.54 5.65 1.54 0.06 0.51 98.88 75 80 40 160 19.0 <6 9 17 23 13 13 <12 672 <6 22.0 <10 116 55 7.19 Table No. A15 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY NUMBER PAGE 6/10 Sample SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 100 4 30 5 20 3 9 35.5 7. 5 1.6 L-906 76.57 0.27 12.23 1.45 0.00 0.03 0.07 0.32 3.00 5.97 0.03 0.42 100.36 254 43 51 164 21.0 <6 7 37 14 13 <12 269 219 <6 19.0 <10 122 62 8.97 L-907 71.26 0.43 13.59 2.43 0.00 0.06 0.51 1.34 3.85 5.07 0.11 0.52 99.17 175 181 41 248 16.0 <6 8 11 44 15 24 <12 1136 <6 16.0 <10 135 69 8.92 L-908 66.78 0.41 16.95 1.82 0.00 0.08 0.28 0.22 9.57 2.63 0.03 0.34 99.11 96 28 10 66 15.5 <6 8 12 53 26 <12 <12 125 <6 15.0 <10 9.7 2.50 17.12 5.04 82 40 1.49 2.03 1.06 0 0 0.29 1.92 0.28 1.78 0.37 1.19 0.20 1.64 0.29 12.20 L-909 71.39 0.41 13.73 1.94 0.00 0.07 0.35 0.72 4.37 4.96 0.08 0.91 98.93 153 134 46 285 18.0 <6 8 25 56 17 15 <12 1346 <6 18.0 <10 163 82 9.33 L-910 70.84 0.59 13.17 3.28 0.00 0.04 0.51 0.53 4.21 4.24 0.20 1.11 98.72 129 126 44 360 17.0 <6 8 12 47 16 26 <12 1115 <6 <15 <10 152 76 8.45 L-911 72.60 0.37 14.49 2.24 0.00 0.03 0.81 0.22 0.16 5.19 0.11 2.40 98.62 170 16 45 344 27.0 <6 10 33 48 19 17 139 398 <6 19.0 <10 145 75 5.35 L-912 73.33 0.37 13.50 1.75 0.00 0.02 0.70 0.22 2.05 5.30 0.08 1.55 98.87 139 29 38 273 20.0 <6 7 9 34 17 15 <12 787 <6 16.0 <10 148 47 7.35 L-917 71.65 0.73 12.99 3.87 0.00 0.08 1.25 0.71 3.95 4.48 0.20 0.63 100.54 113 116 16 39 15.2 6 12 17 50 15 46 15 967 <6 <15 <10 13.4 5.26 30.24 7.86 85 42 1.40 1.3 6 0.92 0 0 1.04 4.56 0.63 3.72 0.68 1.87 0.27 1.86 0.27 8.43 L-919 87.60 0.31 4.60 3.09 0.00 0.03 0.08 0.09 0.12 2.09 0.04 0.79 98.84 79 9 11 99 8.0 6 15 13 14 <9 27 32 297 <6 <15 <10 55 26 2.21 L-920 36.93 0.23 6.77 1.19 0.00 0.03 0.22 0.29 2.90 2.72 0.06 49.01 100.35 124 81 20 208 15.0 <6 <6 16 29 14 17 134 1088 <6 <15 <10 113.1 35.71 61.91 99 29 18.89 0 .663 0.200 0.700 5.62 L-922 68.49 0.77 14.39 4.18 0.00 0.07 0.89 1.69 3.76 4.88 0.23 0.98 100.33 143 206 56 426 27.0 8 9 15 58 18 56 244 1598 <6 16.0 10 22.13 52.85 122.3 159 56 61.63 1 .73 4.288 2.488 1.125 8.64 L-923 70.32 0.62 13.18 3.95 0.00 0.06 0.59 0.92 4.03 4.67 0.17 1.02 99.53 162 156 56 425 21.0 6 12 11 55 18 37 <12 1168 <6 21.0 <10 159 89 8.70 L-924 71.99 0.63 12.33 2.83 0.00 0.05 0.57 1.46 3.58 3.97 0.13 1.69 99.23 82 63 46 359 22.0 8 9 14 26 15 38 <12 1811 <6 19.0 <10 158 79 7.55 L-938 70.06 0.58 13.36 3.13 0.00 0.05 0.58 1.70 4.16 4.11 0.19 0.90 98.82 76 244 38 294 19.0 6 7 11 44 16 40 266 1785 <6 <15 <10 23.8 117.0 49.23 83.50 96 37 1.37 3 .22 38.46 1.43 3.22 0.53 3.70 0.77 2.40 0.39 1.213 0.888 8.27 L-939 68.27 0.56 15.25 3.83 0.00 0.08 0.63 1.89 3.55 5.28 0.14 0.74 100.22 132 422 22 166 11.0 15 16 29 68 16 89 23 1059 <6 <15 11 8.325 30.34 57.99 77 28 77.50 0. 58 0.925 8.83 L-940 62.87 0.57 14.38 5.03 0.00 0.09 1.98 6.05 4.02 3.40 0.20 0.69 99.28 133 422 23 173 12.0 14 13 22 64 18 94 17 1043 <6 <15 11 9.050 25.39 64.13 90 31 79.75 0.4 3 0.638 0.975 7.42 L-943 74.31 0.15 13.23 1.77 0.00 0.04 0.03 0.75 3.70 5.72 0.11 0.29 100.10 137 123 4 65 7.2 <6 9 19 17 14 13 15 350 <6 28.0 <10 18.5 0.91 6.77 2.16 42 20 2.27 3.29 0 .51 0 0 0.15 0.72 0.10 0.64 0.14 0.46 0.09 0.83 0.17 9.42 L-945 67.85 0.52 15.01 3.25 0.00 0.07 0.55 1.40 4.19 5.08 0.11 0.92 98.95 169 235 45 386 18.0 9 8 20 64 18 2 13 1409 <6 19.0 <10 12.43 41.88 115.1 178 53 61.16 0.8 50 1.663 2.463 1.125 9.27 L-946 67.96 0.48 14.78 2.89 0.00 0.06 0.59 1.58 4.39 5.01 0.12 0.73 98.59 165 232 38 250 19.0 6 8 8 45 16 30 185 1451 <6 <15 <10 175 88 9.40 L-948 70.39 0.65 13.17 3.48 0.00 0.11 0.62 1.58 4.48 4.47 0.13 0.41 99.49 160 174 63 368 21.0 7 8 10 73 17 22 <12 1424 <6 15.0 <10 175 92 8.95 L-951 66.61 0.52 15.75 3.69 0.00 0.02 0.04 0.50 11.34 0.33 0.12 0.19 99.11 4 30 50 261 24.0 <6 10 6 9 16 39 137 <20 <6 22.0 <10 10.83 28.36 109.6 166 14 48.54 0.71 3 3.138 1.888 1.088 11.67 L-952 67.68 0.59 15.55 4.09 0.00 0.02 0.15 0.73 10.86 0.35 0.15 0.22 100.39 6 38 36 308 23.0 <6 9 6 10 16 31 173 52 <6 <15 <10 38 27 11.21 L-955 67.86 0.41 16.46 3.50 0.00 0.05 0.11 0.33 10.16 0.19 0.23 0.82 100.12 4 37 40 340 17.0 <6 13 333 142 21 36 <12 30 <6 <15 16 13.25 62.33 671.3 965 405 42.79 0 .400 1.788 1.025 10.35 L-956 61.48 2.00 9.60 15.05 0.00 0.04 0.23 2.72 7.38 0.01 0.92 0.23 99.66 5 36 63 321 14.0 9 11 7 17 17 91 <12 51 <6 <15 24 41.30 97.50 116 63 297.1 3.050 2.125 7.3 9 L-957 75.71 0.31 11.71 1.52 0.00 0.04 0.21 1.09 2.90 4.90 0.05 0.66 99.10 126 135 32 207 20.0 <6 7 <6 36 14 <12 228 571 <6 26.0 <10 112.1 34.19 59.59 156 79 3.200 7.188 0.28 0.338 0.675 7.80 L-958 47.73 1.22 15.13 13.06 0.00 0.23 7.23 8.03 3.57 0.36 0.22 2.21 98.99 5 188 34 105 5.0 63 122 59 119 19 296 107 297 <6 <15 37 15 <12 3.93 L-963 88.82 0.21 4.22 2.07 0.00 0.03 0.19 0.14 1.00 1.77 0.06 0.66 99.17 63 17 18 133 8.0 8 11 20 15 <9 25 12 308 <6 <15 <10 64 31 2.77 L-965 67.45 0.59 13.65 6.24 0.00 0.03 0.32 0.69 4.10 5.73 0.19 0.42 99.41 156 43 88 358 29.0 <6 11 8 24 17 33 12 741 7.00 30.0 <10 125 56 9.83 L-966 68.15 0.60 12.90 6.30 0.00 0.02 0.16 0.43 4.46 5.68 0.19 0.27 99.16 144 39 74 108 17.1 <6 9 6 19 16 42 193 708 5.82 27.2 <10 17.8 6.29 34.8 9.84 103 45 0.41 3 .12 1.20 0.89 7.00 1.36 10.3 2.34 7.51 1.13 7.93 1.21 10.14 L-967 70.72 0.48 12.92 3.64 0.00 0.07 0.46 1.11 3.78 5.05 0.12 0.63 98.98 269 119 83 395 22.0 8 9 13 60 17 31 <12 883 8.00 36.0 <10 259 130 8.83 L-967a 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0 0 0 0 0.0 0 0 0 0 15 0 0 0 <6 20.0 <10 153 119 0.00 L-968 72.13 0.34 13.69 2.21 0.00 0.03 0.17 0.89 3.99 4.79 0.05 0.51 98.80 136 145 37 225 15.0 7 9 20 86 15 16 <12 1370 <6 23.0 <10 110.0 16.73 28.51 110 11 2.863 2 6.16 0.488 0.763 8.78 L-969 59.46 0.49 19.16 4.28 0.00 0.05 0.68 0.38 0.55 14.31 0.08 0.84 100.28 393 66 59 293 24.0 6 <6 47 53 22 61 <12 2451 6.00 29.0 <10 10.51 36.03 92.38 159 37 7. 200 60.24 0.663 3.050 1.288 14.86 L-971 64.34 0.54 17.73 1.51 0.00 0.09 0.14 0.68 4.58 8.51 0.11 0.69 98.92 148 66 47 358 22.0 <6 9 10 14 13 34 <12 2236 <6 <15 <10 137 81 13.09 L-973 71.06 0.42 12.34 2.89 0.00 0.04 0.12 1.90 0.51 9.97 0.09 0.97 100.31 266 42 47 249 19.0 6 <6 141 70 9 28 12 1800 <6 18.0 <10 9.588 33.88 96.50 128 42 5.850 3 6.50 0.500 3.23 1.138 10.48 L-975 72.48 0.35 13.19 2.05 0.00 0.06 0.27 0.82 3.81 5.40 0.10 0.56 99.09 164 149 34 215 16.0 7 9 45 47 14 19 <12 1327 <6 21.0 <10 137 68 9.21 L-976 72.48 0.37 13.10 1.84 0.00 0.04 0.29 0.71 4.00 5.29 0.06 0.50 98.68 195 113 55 203 21.0 <6 10 8 29 18 209 1114 115.8 48.35 91.75 71 3.225 13.38 1.03 2.213 2.93 1.075 9.29 L-977 74.68 0.27 11.99 1.72 0.00 0.04 0.24 0.55 3.86 5.21 0.04 0.45 99.05 121 81 27 197 13.0 <6 8 <6 39 15 12 <12 766 <6 16.0 <10 110 57 9.07 L-978 76.43 0.22 11.10 2.76 0.00 0.10 0.04 0.28 4.16 5.19 0.05 0.18 100.51 139 58 15 133 16.9 <6 10 37 73 20 14 20 264 3.59 19.1 <10 21.3 2.08 13.4 4.14 50 25 0.75 5.11 1.02 0.29 1.79 0.29 2.06 0.48 1.79 0.33 2.76 0.49 9.35 L-979 66.06 0.48 15.03 3.97 0.00 0.09 1.33 3.18 4.23 3.67 0.14 0.79 98.97 108 435 35 143 15.0 10 10 76 88 16 68 242 1077 <6 <15 11 92 44 7.90 L-980 67.03 0.53 15.05 4.32 0.00 0.09 1.37 3.20 4.47 3.48 0.18 0.77 100.49 115 424 32 157 17.0 10 15 28 62 17 72 200 1140 <6 <15 <10 104 52 7.95 L-982 66.31 0.56 15.11 3.80 0.00 0.09 1.18 3.09 4.72 3.57 0.19 0.80 99.42 99 495 25 176 12.0 11 10 11 56 17 54 <12 1245 <6 <15 <10 8.588 26.96 66.38 74 30 53.76 0. 363 0.550 0.825 8.29 L-983 72.59 0.29 13.57 1.83 0.00 0.04 0.07 0.90 4.08 4.95 0.04 0.51 98.87 197 156 28 181 17.0 <6 6 7 32 15 13 <12 963 <6 19.0 <10 90 39 9.03 L-985 72.90 0.46 12.76 2.61 0.00 0.05 0.29 1.39 3.72 4.25 0.06 0.63 99.12 123 219 5 51 6.1 <6 7 9 46 14 25 173 1580 1.49 17.1 <10 25.6 3.41 33.2 9.78 103 61 2.13 1. 48 0.19 1.09 2.00 0.20 0.97 0.17 0.46 0.07 0.54 0.10 7.97 L-987a 45.74 2.33 16.73 14.31 0.00 0.17 4.10 10.53 2.62 1.59 0.46 1.99 100.57 22 598 11 18 1.9 41 8 75 109 17 429 <12 397 <6 <15 36 7.7 2.50 10.86 2.08 <12 <12 0.2 9 0.51 0.03 0 0 1.03 2.95 0.39 2.37 0.46 1.20 0.15 0.92 0.13 4.21 L-987b 40.92 2.62 19.28 13.71 0.00 0.19 4.13 12.81 2.45 0.79 1.19 2.06 100.15 35 646 19 31 4.0 28 <6 37 72 17 307 <12 284 <6 <15 32 7.100 29.40 16 5 284.3 1.338 3. 24 L-990 53.79 0.31 13.92 7.16 0.00 0.15 8.22 7.59 5.52 0.32 0.10 2.29 99.37 10 267 12 84 10.0 38 178 73 69 13 75 584 187 <6 <15 20 39 22 5.84 L-991 48.45 0.96 11.97 11.52 0.00 0.19 11.57 9.20 3.07 0.46 0.12 1.70 99.21 7 217 20 53 9.0 64 251 83 93 12 255 870 188 <6 <15 35 19 12 3.53 L-992 50.94 0.49 19.38 7.11 0.00 0.15 5.16 9.79 3.16 1.87 0.09 2.25 100.39 67 659 10 28 3.4 27 53 35 53 16 144 100 460 0.24 0.9 26 4.4 1.92 9.78 2.25 19 9 0.49 0.75 0.13 0.79 2.03 0.30 1.93 0.39 1.11 0.16 1.04 0.15 5.03 L-993 71.34 0.39 13.57 2.03 0.00 0.05 0.39 1.42 3.97 5.33 0.07 0.81 99.37 115 224 27 75 11.5 <6 6 8 34 15 24 160 1595 <6 17.0 <10 22.5 7.25 47.18 12.68 139 69 0.45 2.38 0.59 0 0 1.21 5.76 0.82 5.12 1.00 2.86 0.42 2.84 0.41 9.30 L-994 70.70 0.40 13.83 2.09 0.00 0.05 0.43 1.46 3.95 5.07 0.09 0.73 98.80 110 226 37 208 19.0 6 7 10 33 15 32 195 1763 <6 <15 <10 142 70 9.02 L-995 39.21 3.69 11.13 22.15 0.00 0.26 7.20 10.83 1.60 0.53 1.13 1.13 98.86 14 449 21 27 4.0 59 <6 54 128 19 491 <12 457 <6 <15 45 <12 <12 2.13 L-996 69.95 0.44 14.71 2.86 0.00 0.06 0.50 1.75 4.30 4.78 0.11 0.95 100.41 121 274 24 78 13.9 6 9 67 71 16 30 <12 1498 2.82 14.9 <10 23.0 6.17 39.6 10.8 113 49 0.6 9 2.30 0.83 1.22 4.96 0.74 4.69 0.93 2.78 0.42 2.93 0.42 9.08 L-997 69.62 0.34 15.29 1.59 0.00 0.04 0.27 0.51 5.88 5.33 0.05 0.73 99.65 135 65 57 241 22.0 8 9 8 24 16 19 <12 542 <6 33.0 <10 111.4 28.71 57.06 156 21 4.188 11.0 6 2.450 0.950 11.21 L-998 64.78 0.73 15.67 4.59 0.00 0.11 1.41 2.78 4.52 4.03 0.24 1.33 100.19 103 300 34 347 15.0 6 9 29 96 18 53 13 2134 <6 <15 10 10.00 32.01 78.50 106 38 63.00 0.9 38 1.038 1.025 8.55 Table No. A15 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY NUMBER PAGE 7/10 Sample SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 100 4 30 5 20 3 9 35.5 7. 5 1.6 L-999 67.68 0.49 14.73 3.02 0.00 0.07 0.74 1.83 4.31 4.65 0.13 1.19 98.84 140 252 37 288 20.0 <6 9 10 58 17 33 205 1537 <6 16.0 <10 9.700 36.04 91.88 144 44 1.525 39.16 0.83 1.488 0.888 8.96 L-1000 67.91 0.47 15.37 2.32 0.00 0.06 0.52 1.06 4.28 5.11 0.10 1.68 98.88 192 112 37 251 18.0 <6 10 62 58 17 35 <12 1206 <6 20.0 <10 11.55 90.10 152.3 134 80 81. 95 3.48 2.58 1.200 9.39 L-1002 77.59 0.26 11.61 1.64 0.00 0.05 0.10 0.32 3.59 4.97 0.03 0.33 100.49 180 40 25 134 22.0 <6 8 6 14 14 10 <12 180 <6 28.0 <10 104.0 18.61 52.50 87 26 3.350 5. 388 1.600 0.925 8.56 L-1003 68.00 0.50 15.07 2.73 0.00 0.05 0.58 1.60 4.64 5.26 0.12 0.69 99.24 145 242 40 289 16.0 <6 8 12 47 17 32 <12 1796 <6 15.0 <10 8.450 28.94 79.13 133 26 2.57 5 31.71 0.78 1.713 0.950 9.90 L-1005 71.20 0.48 12.46 3.35 0.00 0.06 0.56 1.47 3.93 4.47 0.18 0.76 98.92 171 218 46 298 18.0 7 9 15 50 17 26 16 1194 <6 18.0 <10 132 64 8.40 L-1007 64.26 0.56 15.15 5.20 0.00 0.10 1.92 3.56 4.03 3.92 0.20 0.55 99.45 169 234 45 318 16.0 7 10 22 61 17 38 <12 1413 <6 22.0 <10 160 78 7.95 L-1009 66.67 0.69 15.06 4.31 0.00 0.09 1.05 2.81 4.12 4.42 0.26 0.88 100.36 129 347 38 354 15.0 7 7 18 71 17 53 <12 1757 <6 16.0 10 115 55 8.54 L-1010 63.36 0.80 15.40 5.08 0.00 0.11 1.26 3.27 4.15 4.24 0.34 1.17 99.18 138 385 37 372 15.0 9 10 21 74 18 53 <12 1944 <6 <15 12 110 55 8.39 L-1011 66.33 0.64 14.74 3.94 0.00 0.09 0.94 2.72 4.53 4.43 0.19 0.82 99.37 152 302 38 308 20.0 7 9 21 73 17 50 126 1322 <6 17.0 10 129 66 8.96 L-1012 64.77 0.68 15.28 4.30 0.00 0.20 0.95 3.01 5.41 3.94 0.20 0.97 99.71 132 337 42 332 22.0 8 10 9 331 17 53 105 1550 <6 17.0 <10 139 74 9.35 L-1013 67.41 0.61 14.33 4.04 0.00 0.08 0.94 2.09 4.00 4.72 0.21 0.95 99.38 171 240 39 331 16.0 6 10 26 67 17 47 <12 1290 <6 19.0 <10 108.4 40.58 79.25 131 35 48.2 3 0.638 1.738 0.975 8.72 L-1014 68.99 0.41 14.20 3.21 0.00 0.05 1.35 2.61 3.04 3.64 0.11 1.80 99.41 59 321 5 43 2.55 9.0 20.0 13.0 43 13 60.0 173 1632 <6 <15 <10 14.1 2.27 18.16 4.86 64. 0 34.0 0.24 1.00 n.d. 0.0 0.0 1.27 1.76 0.20 1.08 0.20 0.51 0.07 0.44 0.07 6.68 L-1016 77.33 0.10 1.04 2.18 0.00 0.47 2.02 6.71 0.50 0.09 0.13 8.00 98.57 6 124 8 15 4.0 <6 <6 56 14 <9 <12 351 33 <6 <15 12 24 <12 0.59 L-1016a 79.38 0.10 0.80 2.49 0.00 0.45 1.96 5.74 0.55 0.13 0.04 7.50 99.14 5 140 6 37 4.0 <6 7 28 27 <9 13 15 57 <6 <15 10 23 <12 0.68 L-1019 72.23 0.41 13.17 3.00 0.00 0.11 0.24 0.79 6.18 3.79 0.08 0.41 100.41 50 101 31 290 46.9 <6 10 9 62 17 <12 253 1351 1.82 17.0 <10 29.0 7.79 47.2 12.5 110 60 0.15 7.31 2.12 2.05 6.81 0.95 5.85 1.15 3.36 0.49 3.38 0.50 9.97 L-1020 70.82 0.58 12.68 4.01 0.00 0.10 0.76 1.57 5.17 3.14 0.09 0.31 99.23 70 173 52 445 22.0 <6 8 64 85 17 19 <12 1364 <6 19.0 <10 180 95 8.31 L-1021 72.02 0.43 12.86 3.47 0.00 0.05 0.24 1.10 4.37 4.02 0.07 0.53 99.16 83 92 84 464 33.0 <6 8 5 29 17 <12 250 1355 <6 18.0 <10 143 61 8.39 L-1022 54.76 0.44 20.41 5.90 0.00 0.20 0.33 1.95 4.97 7.25 0.13 2.78 99.12 189 616 24 767 249.0 7 <6 11 171 36 14 <12 629 8.00 <15 <10 2.638 27.54 47.69 61 19 94. 38 0.38 0.763 12.22 L-1023 47.51 0.82 15.70 11.39 0.00 0.21 7.63 10.97 2.78 0.87 0.09 2.31 100.28 19 177 23 45 5.0 51 86 11 157 19 246 354 223 <6 <15 42 33 20 3.65 L-1024a 7.58 0.07 0.57 9.33 0.00 0.79 5.76 37.24 0.03 0.15 0.23 38.75 100.50 6 335 62 9 44.1 28 21 177 59 <9 23 <12 115 19.00 20.0 49 2.4 50.29 543.29 178.89 205 8 1583 0.06 0.11 n.d. 0 0 7.27 28.38 3.20 14.82 2.54 6.75 1.02 7.22 1.10 0.18 L-1024c 5.56 0.06 0.20 9.37 0.00 0.84 6.08 39.51 0.01 0.04 0.23 38.66 100.56 10 325 92 18 31.0 29 11 116 29 <9 24 <12 99 20.00 18.0 49 1786 1383 0.05 L-1025 42.06 1.06 1.26 21.42 0.00 0.77 2.76 17.44 1.61 0.56 3.85 7.40 100.19 30 1546 50 1312 1425.4 42 10 29 207 12 334 106 214 86.4 19.5 33 4.8 27.7 183 47.1 39 6 176 0.39 10.1 33.6 8.30 21.9 2.59 13.0 2.12 5.37 0.85 7.25 1.48 2.17 L-1027 55.06 0.81 15.77 5.91 0.00 0.27 2.32 3.60 4.38 6.88 0.23 3.58 98.81 177 429 37 621 220.0 14 42 25 134 24 45 174 1043 <6 <15 <10 58.35 136.1 239 72 94.25 1. 663 1.063 0.838 11.26 L-1032 46.04 1.99 15.47 14.07 0.00 0.33 6.80 9.26 3.22 0.75 0.42 1.94 100.29 10 322 48 132 9.0 47 45 26 163 15 345 218 299 <6 <15 40 109.3 42.20 61.28 <12 40 3.52 5 22.53 0.600 3.588 1.138 3.97 L-1037 67.15 0.44 16.05 2.51 0.00 0.02 0.77 1.33 2.99 7.49 0.15 0.46 99.36 204 190 22 149 16.0 <6 6 8 41 17 15 156 1143 <6 105.0 <10 288 157 10.48 L-1038 68.09 0.44 15.77 2.42 0.00 0.02 0.69 1.39 3.03 6.45 0.17 0.40 98.87 185 178 26 247 18.0 <6 8 13 39 16 14 162 975 <6 112.0 <10 316 175 9.48 L-1039 70.93 0.25 13.72 2.43 0.00 0.01 0.03 0.57 3.62 5.51 0.10 1.71 98.88 160 562 19 156 20.0 <6 7 21 11 18 <12 230 793 <6 26.0 <10 88 46 9.13 L-1039a 73.60 0.10 13.76 0.98 0.00 0.02 0.06 0.47 3.67 6.14 0.03 0.53 99.36 168 205 12 38 2.1 <6 8 6 11 13 12 250 1060 <6 <15 <10 24.9 3.17 17.63 4.60 55 23 2.53 1. 29 0.08 0 0 1.07 2.98 0.39 2.17 0.40 1.09 0.15 0.98 0.15 9.81 L-1039c 70.50 0.34 13.95 3.40 0.00 0.02 0.00 0.71 3.38 5.94 0.11 2.16 100.51 172 547 24 162 24.0 <6 7 29 12 18 <12 309 776 <6 32.0 <10 103 55 9.32 L-1042 70.57 0.26 14.13 2.58 0.00 0.06 0.45 0.67 2.79 6.14 0.10 1.35 99.10 317 68 65 161 17.0 7 12 20 29 14 16 <12 471 <6 35.0 <10 109.9 44.76 78.50 106 34 3.625 2 6.99 0.413 0.78 3.88 1.213 8.93 L-1043 72.42 0.34 13.62 2.40 0.00 0.04 0.57 0.57 2.76 5.77 0.10 1.27 99.86 276 85 71 207 17.0 7 9 51 30 14 28 <12 525 <6 44.0 <10 109.1 41.74 89.25 140 35 1.713 36 .96 0.750 8.700 1.850 8.53 L-1044 73.43 0.25 12.72 2.04 0.00 0.04 0.39 0.49 2.79 5.94 0.11 1.10 99.30 293 67 47 166 16.0 6 9 115 70 12 20 12 415 <6 36.0 <10 109 44 8.73 L-1045 65.28 0.40 17.54 2.82 0.00 0.08 0.36 3.60 6.67 1.70 0.11 1.41 99.97 90 471 107 246 24.0 5 7 48 18 20 24 <12 116 <6 57.0 12 12.20 14.56 48.25 154 16 297.8 0. 188 2.238 1.675 8.37 L-1046 72.78 0.33 12.73 2.40 0.00 0.03 0.55 0.76 2.61 5.45 0.12 1.39 99.15 283 61 69 193 16.0 6 9 30 27 13 25 16 473 <6 42.0 <10 126 53 8.06 LJ1 68.16 0.46 16.02 2.81 0.00 0.02 0.89 1.54 2.85 7.17 0.16 0.55 100.07 196 191 24 259 17.0 4 30 42 15 0 954 1.00 95.0 4 10.02 LL1 73.41 0.09 14.65 0.80 0.00 0.01 0.27 1.00 3.34 6.24 0.20 1.26 100.02 150 176 17 42 6.0 3 3 13 11 6 1 1468 0.00 5.0 2 9.58 LL10 56.48 1.24 17.84 6.85 0.00 0.19 1.96 3.78 5.74 4.86 0.74 0.74 99.67 135 965 36 340 99.0 11 3 0 78 44 0 1366 9.00 25.0 1 10.60 LL11 73.00 0.00 14.00 2.00 0.00 0.00 0.00 1.00 3.00 6.00 0.00 1.00 99.86 287 134 34 210 16.0 2 1 0 30 20 3 880 3.00 55.0 5 9.00 LL13 62.00 1.00 11.00 4.00 0.00 0.00 3.00 18.00 1.00 0.00 0.00 7.00 100.02 12 701 42 128 6.0 9 26 3 58 101 66 448 4.00 5.0 10 1.00 LL14 57.00 1.00 17.00 9.00 0.00 0.00 1.00 3.00 6.00 5.00 0.00 1.00 99.52 280 355 161 2052 364.0 4 5 133 4 0 1161 22.00 83.0 5 11.00 LL15 62.00 1.00 16.00 6.00 0.00 0.00 1.00 4.00 6.00 5.00 0.00 4.00 99.73 118 328 31 305 47.0 10 9 0 73 125 22 1308 3.00 26.0 15 11.00 LL16 70.00 1.00 14.00 3.00 0.00 0.00 1.00 2.00 3.00 5.00 0.00 0.00 99.49 230 152 24 320 30.0 4 2 0 33 39 9 790 3.00 33.0 4 8.00 LL17a 73.00 0.00 14.00 1.00 0.00 0.00 0.00 1.00 3.00 7.00 0.00 1.00 99.75 202 57 12 29 9.0 2 5 8 4 6 220 5.00 3.0 1 10.00 LL17b 66.00 1.00 16.00 5.00 0.00 0.00 1.00 3.00 3.00 5.00 0.00 0.00 99.77 140 208 22 311 16.0 13 2 2 60 50 7 1167 4.00 18.0 9 8.00 LL18 76.00 0.00 13.00 1.00 0.00 0.00 0.00 1.00 3.00 7.00 0.00 1.00 100.07 178 84 8 55 3.0 0 8 5 4 316 5.00 4.0 1 10.00 LL2a 75.73 0.02 14.98 0.67 0.00 0.01 0.06 0.12 3.62 4.86 0.04 1.36 100.11 181 35 10 19 19.0 2 1 14 8 11 0 104 2.00 4.0 2 8.48 LL2b 69.71 0.00 16.92 0.31 0.00 0.01 0.00 0.04 2.54 10.40 0.13 0.60 100.06 356 67 7 4 1.0 2 1 0 2 0 1 205 0.00 2.0 0 12.94 LL3a 75.92 0.03 13.87 0.68 0.00 0.01 0.05 0.39 2.87 5.93 0.01 1.19 99.77 156 182 13 29 0.0 2 1 14 4 5 3 659 0.00 7.0 1 8.80 LL3b 70.31 0.04 16.91 0.47 0.00 0.01 0.24 0.37 2.44 9.09 0.09 1.20 99.96 348 252 9 5 4.0 2 1 0 7 7 1 495 1.00 0.0 5 11.53 LL4 74.72 0.10 13.50 1.59 0.00 0.03 0.10 0.80 3.49 5.74 0.02 0.41 100.08 365 50 32 138 29.0 1 0 27 1 0 235 4.00 52.0 5 9.23 LL5 75.94 0.03 14.40 0.33 0.00 0.00 0.00 1.44 4.03 3.46 0.03 0.64 99.67 180 89 47 48 11.0 1 6 4 0 0 151 5.00 11.0 1 7.49 LL9 79.03 0.02 14.86 0.39 0.00 0.00 0.01 0.02 0.30 5.63 0.00 3.19 100.25 256 26 9 33 9.0 2 2 1 3 12 3 285 2.00 3.0 2 5.93 LR20 2.875 0.02 0.60 12.9 0.38 33.1 45.0 1.67 0.04 0.15 0 1166 152 97 22 16 44 31 79 0 115 85 32 0 36 0 10 0 0 0 0 37 25 0 42 6 0 2 1.71 0 LR23 6.138 0.06 1.84 14.0 0.45 30.5 40.6 2.47 0.10 0.18 6 941 2633 327 152 71 53 41 53 0 62 86 25 15 130 19 71 0 0 88 0 32 0 13 449 24 0 5 2.57 0 LR25 4.673 0.29 0.34 5.85 1.89 0.76 70.8 1.58 0.01 5.82 1 6765 12358 65 128 167 58 166 899 0 191 50 469 24 7730 7 0 673 1335 0 3341 2342 0 8 35 0 0 75 1.59 27 Table No. A15 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY NUMBER PAGE 8/10 Sample SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 100 4 30 5 20 3 9 35.5 7. 5 1.6 LR4 2.133 0.10 0.12 33.4 3.12 1.61 48.6 1.71 0.04 0.66 0 1054 2761 44 598 44 21 0 99 -5 0 0 0 28 1593 0 438 0 2003 0 6950 5436 3 7 2199 93 0 74 1.75 12 LR5 7.666 0.30 1.32 16.1 2.24 3.89 48.8 1.51 0.53 8.09 19 1669 4033 130 181 90 46 89 45 0 36 114 393 26 2347 0 91 655 1734 486 4909 3846 18 7 75 49 0 21 2.05 0 P-13 65.76 0.82 14.67 5.87 0.00 0.10 1.00 2.40 5.77 3.89 0.24 0.21 100.52 90 301 45 157 30.0 70 11 <3 4 23 55 22 787 10.00 56.0 7 4.0 9.90 58.80 16.50 153 80 <1 9.0 0 2.70 1 35 2.10 9.50 1.30 8.00 1.70 4.50 34.90 4.60 0.80 9.66 P-17 64.11 0.97 14.29 7.35 0.00 0.08 0.80 2.43 3.95 5.62 0.26 0.18 99.86 107 372 54 327 32.0 84 16 63 23 24 103 11 782 11.00 48.0 10 5.0 11.90 64.10 17.30 136 47 1 .00 8.00 2.40 3 88 2.40 11.70 1.50 9.00 1.80 5.10 35.70 5.00 0.80 9.57 P-25 51.44 2.40 20.38 8.73 0.00 0.71 3.91 5.28 6.42 1.71 0.38 0.12 100.72 55 348 24 107 14.0 33 6 40 13 24 98 90 120 <2 2.0 20 4.0 4.00 15.10 3.20 22 9 1.00 2.00 1.3 0 12 107 1.70 4.50 0.70 4.20 0.90 2.30 33.60 2.10 0.30 8.13 P-26 76.20 0.13 11.58 0.93 0.00 0.05 <.1 0.25 10.51 0.03 0.03 0.08 99.71 7 15 170 705 243.0 39 4 <3 <1 68 <4 24 22 6.00 76.0 1 5.0 6.90 15.00 3.20 24 8 <1 31.00 4.80 1 7 0.70 11.80 3.30 27.50 6.70 21.30 35.70 23.00 3.40 10.54 P-28 68.49 0.34 12.40 3.43 0.00 0.12 0.26 1.06 8.74 5.32 0.11 0.13 100.27 345 58 617 261 64.0 34 19 <3 97 24 <4 8 689 13.00 98.0 5 61.0 75.30 359.30 89.80 600 383 5.00 11.00 2.90 4 7 6.40 97.80 16.20 98.20 20.30 53.30 40.90 38.70 5.90 14.06 P-29 72.84 0.31 13.07 2.71 0.00 0.11 0.19 1.28 4.04 5.56 0.08 0.17 100.19 278 79 89 183 46.0 38 3 6 58 22 <4 8 724 9.00 65.0 6 53.0 16.20 82.60 23.20 204 101 3.00 6 .00 2.20 2 7 1.70 14.80 2.40 14.40 2.90 8.10 36.90 8.20 1.40 9.60 P-32 73.45 0.26 12.59 1.67 0.00 0.06 0.10 0.94 4.34 6.61 0.08 0.14 100.10 334 72 23 57 12.0 58 10 <3 14 17 <4 20 862 <2 7.0 3 48.0 3.60 15.80 4.30 36 18 3.00 4.00 0. 90 <1 4 1.30 3.80 0.60 3.50 0.60 1.40 36.40 1.00 0.10 10.95 P-33 68.30 0.54 14.41 3.20 0.00 0.10 0.73 1.53 5.65 6.09 0.19 0.20 100.74 230 222 81 157 19.0 52 6 <3 45 21 31 13 2028 <2 16.0 7 21.0 16.60 78.50 19.40 121 57 2.00 4.00 2.40 <1 13 2.90 16.70 2.30 12.80 2.60 7.00 33.10 5.60 0.80 11.74 P-35 74.32 0.25 13.99 1.48 0.00 0.07 0.33 1.12 6.19 2.54 0.07 0.18 100.36 83 188 2 99 6.0 41 2 <3 35 19 11 21 558 2.00 8.0 1 20.0 1.60 9.40 2.70 26 15 1.00 3.00 0.40 <1 5 0.50 1.20 0.10 0.60 0.10 0.20 33.40 0.20 0.00 8.73 P-39 72.16 0.28 12.57 3.40 0.00 0.08 0.12 1.17 4.67 5.57 0.11 0.17 100.13 404 43 109 309 59.0 56 4 <3 12 29 <4 5 182 19.00 71.0 4 11.0 21.40 114.10 33.00 290 145 2 .00 10.00 2.50 <1 12 0.80 19.40 3.10 18.30 3.60 9.20 34.40 7.30 1.10 10.24 P-40i 76.05 0.26 11.74 2.15 0.00 0.08 0.13 1.54 4.06 4.05 0.07 0.07 100.13 150 92 48 335 27.0 61 12 <3 26 26 <4 9 309 6.00 20.0 2 8.0 9.30 45.60 11.90 98 51 1.00 11 .00 1.30 2 8 1.50 8.80 1.40 8.30 1.70 5.00 35.30 5.00 0.80 8.11 P-40ii 68.86 0.55 13.67 4.56 0.00 0.12 0.33 1.82 4.52 5.77 0.12 0.19 100.32 195 110 77 391 52.0 53 14 <3 53 27 11 19 503 <2 15.0 5 10.0 15.90 78.80 20.00 157 71 1. 00 11.00 3.30 <1 22 2.00 14.40 2.40 14.20 2.80 7.50 34.90 6.40 1.00 10.29 P-46 71.17 0.38 12.62 4.35 0.00 0.12 0.20 0.81 3.59 6.89 0.07 0.16 100.20 398 65 89 257 53.0 48 4 <3 45 27 <4 9 387 10.00 46.0 1 11.0 16.90 93.10 25.70 217 110 3.0 0 11.00 2.80 26 28 1.40 15.50 2.40 14.00 2.80 7.90 4.90 7.40 1.10 10.48 P-50 71.53 0.25 12.60 3.26 0.00 0.10 0.30 1.66 4.55 4.88 0.21 0.14 99.34 376 66 163 312 107.0 40 16 <3 30 27 <4 4 314 62.00 256.0 3 23.0 54.30 334.80 100.20 899 5 05 4.00 9.00 3.20 1 8 1.20 39.60 6.00 32.20 6.20 16.30 5.70 11.40 1.60 9.43 P-53 73.18 0.24 13.04 2.62 0.00 0.07 0.22 0.95 3.78 5.92 0.12 0.09 100.14 421 59 54 179 48.0 71 19 <3 <1 24 <4 24 209 21.00 43.0 2 11.0 5.60 25.70 8.00 78 44 6.00 6 .00 2.50 6 6 0.80 6.00 1.10 6.70 1.50 4.70 31.80 4.80 0.80 9.70 P-57 62.19 0.36 13.11 2.44 0.00 0.05 0.26 0.86 15.42 5.52 0.06 0.21 100.27 225 45 375 404 48.0 63 21 <3 1 24 <4 <4 286 10.00 51.0 6 5.0 79.00 499.40 133.60 735 57 9 2.00 11.00 2.60 <1 5 7.60 80.50 10.00 55.60 11.10 28.90 35.90 21.40 3.30 20.94 P-58 67.76 0.79 13.46 6.83 0.00 0.17 1.40 2.21 3.78 4.27 0.18 0.25 100.85 210 189 66 223 30.0 77 4 21 72 26 45 12 680 4.00 24.0 8 12.0 10.30 50.50 13.10 107 53 5.0 0 6.00 2.10 1 30 2.10 9.90 1.50 8.50 1.70 4.70 33.40 3.90 0.60 8.05 X-01 73.81 0.08 12.29 0.37 1.52 0.04 0.70 2.24 4.21 4.83 0.04 0.66 100.79 9.04 X-02 72.56 0.23 14.28 0.94 0.68 0.02 0.83 0.76 2.88 6.12 0.05 1.96 101.31 9.00 X-03 70.95 0.42 15.07 1.13 1.29 0.03 1.32 0.83 4.23 3.03 0.11 2.60 101.01 7.26 X-04 75.20 0.33 10.10 1.55 1.69 0.04 2.81 2.08 2.02 2.13 0.34 2.36 100.65 4.15 X-05 65.27 0.84 15.18 3.20 1.94 0.08 1.01 2.90 3.00 4.70 0.31 1.39 99.82 7.70 X-06 46.85 15.87 3.33 7.40 0.11 8.61 7.29 3.65 2.50 0.15 3.06 98.82 6.15 X-07 58.63 13.08 6.07 6.68 0.15 1.87 4.70 5.50 0.66 0.32 1.66 99.32 6.16 X-08 67.94 12.08 7.23 1.01 0.04 0.60 1.65 6.70 0.20 0.07 1.70 99.22 6.90 X-09 59.26 16.65 1.26 0.43 0.06 2.04 4.59 9.80 0.20 0.65 4.48 99.42 10.00 X-10 47.87 14.53 4.50 9.05 0.15 6.13 6.12 2.95 1.55 0.37 7.22 100.44 4.50 X-11 48.19 14.53 4.13 7.18 0.12 6.66 9.00 4.25 1.40 0.17 3.60 99.23 5.65 X-12 30.05 0.37 8.60 39.65 4.48 0.05 0.27 6.82 5.78 0.35 96.42 0.00 X-13 49.41 2.67 12.71 2.18 10.07 0.14 6.93 10.46 2.46 0.80 0.46 2.38 100.67 3.26 X-14 46.76 3.30 10.31 5.81 9.10 0.14 7.25 10.24 4.26 0.86 0.38 4.05 102.46 5.12 X-15 67.63 0.59 14.37 2.02 1.66 0.07 1.15 1.90 4.59 5.21 0.26 0.86 100.31 592 9.80 X-16 75.93 0.26 12.08 2.96 0.32 0.01 0.36 0.48 7.93 0.13 0.07 0.42 100.95 8.06 X-17 72.07 0.33 13.36 3.76 0.25 0.02 1.33 1.01 7.95 0.30 0.04 0.49 100.91 8.25 X-18 69.24 12.00 0.55 3.83 5.36 0.00 90.98 9.19 X-19 72.02 0.32 13.78 2.24 1.02 0.02 0.20 0.39 4.07 5.18 0.03 0.65 99.92 9.25 X-20 76.01 0.23 12.05 0.80 0.91 0.03 0.20 1.02 3.09 5.02 0.01 1.14 100.51 8.11 X-21 60.78 0.87 16.97 1.13 4.10 0.16 0.99 1.94 5.65 5.27 0.22 1.78 99.86 10.92 X-22 64.42 1.12 14.69 4.34 1.80 0.07 1.37 1.17 3.71 5.64 0.25 1.78 100.36 9.35 X-23 63.81 0.59 14.21 3.67 1.10 0.15 1.48 2.27 4.37 6.00 0.09 3.13 100.87 10.37 X-24 51.29 0.40 19.06 5.95 1.05 0.42 0.82 4.79 6.75 5.19 0.30 3.38 99.40 11.94 X-25 47.49 2.22 14.47 3.74 8.09 0.05 6.73 11.57 1.24 0.77 0.30 2.80 99.47 2.01 X-26 48.82 1.03 12.21 3.62 6.54 0.15 13.68 9.63 1.77 1.10 0.59 1.16 100.30 2.87 X-27 47.85 1.47 16.84 2.70 8.50 0.19 6.66 11.79 2.54 0.75 0.27 0.46 100.02 3.29 X-28 60.59 0.58 14.99 2.44 2.30 1.13 0.91 2.55 8.98 3.81 tr 1.00 99.28 12.79 X-29 61.03 18.63 3.66 1.04 1.56 7.68 5.57 0.41 99.58 13.25 X-30 63.34 0.57 16.00 4.17 1.69 0.11 0.35 2.29 3.93 5.86 0.17 2.04 100.52 9.79 X-31 61.56 0.82 15.25 4.29 3.89 0.25 1.28 1.68 4.10 4.40 0.16 1.24 98.92 8.50 X-32 65.80 0.60 15.40 3.84 0.28 0.06 0.11 1.12 5.60 5.10 0.38 1.05 99.34 10.70 X-33 51.80 0.32 18.20 2.24 2.09 0.17 2.56 4.93 8.22 5.36 0.50 3.69 100.08 13.58 X-34 76.75 0.09 11.78 0.82 0.58 0.03 0.16 0.72 3.08 5.01 0.1 0.84 99.96 8.09 X-34a 76.75 0.09 11.78 0.82 0.58 0.03 0.16 0.72 5.01 3.08 0.1 0.84 99.96 8.09 X-35 76.84 0.08 10.7 1.3 0.04 0.1 0.8 2.3 4.9 0.02 0.69 97.77 7.20 Table No. A15 CHEMICAL ANALYSIS OF SAMPLES FROM THE GREATER LUFILIAN ARC SORTED BY NUMBER PAGE 9/10 Sample SiO2 TiO2 Al2O3 Fe2O 3 FeO MnO MgO CaO Na2O K2O P2O 5 LOI Total Rb Sr Y Zr Nb Co Ni Cu Zn Ga V Cr Ba U Th Sc Pb Sm Nd Pr Ce La Cs Hf Ta As Se Eu Gd Tb Dy Ho Er Tm Yb Lu Li Be Ge Mo Na+K Sn Notch 50.00 1.00 15.50 6.00 0.150 2.00 5.00 4.90 5.50 0.30 2.00 200 400 60 360 40 30 16 25 85 26 100 100 1300 20 37 20 20 50 50 15 175 95 3 10 120 100 4 30 5 20 3 9 35.5 7. 5 1.6 X-36 76.9 0.01 12.3 0.6 0.01 0.1 0.5 3.6 4.4 0.04 0.35 98.81 8.00 X-37 78.2 0.04 10.3 1.1 0.04 0.1 0.7 2.2 4.9 0.01 0.44 98.025 7.10 X-38 59.8 1.1 10.4 12.6 0.3 0.6 4.3 1.7 2.9 0.08 0.99 94.77 4.60 X-39 66.6 0.01 18 0.2 0.02 0.03 0.2 2.4 11.9 0.01 0.95 100.32 14.30 X-40 64.8 0.01 16.7 0.4 0.01 0.03 0.1 0.7 15.5 0 0 98.25 16.20 X-41 64.19 1.05 14.8 2.89 2.68 0.05 1.68 3.11 3.7 4.65 0.31 0.97 100.08 8.35 X-42 68.64 0.3 13.95 1.14 1.25 0.06 2.29 2.25 2.13 4.04 0.11 3.54 99.7 6.17 X-43 72.65 0.27 14.34 0.34 1.10 0.04 0.73 1.21 3.07 5.46 0.12 0.55 99.88 8.53 X-44 76.59 0.32 12.60 0.28 2.08 0.04 0.82 0.78 0.87 5.77 0.04 0.49 100.68 6.64 X-45 68.41 0.69 14.46 0.29 4.31 0.08 1.29 2.07 3.47 4.63 0.25 0.92 100.87 8.10 X-46 72.98 0.13 14.41 0.10 1.05 0.04 0.42 1.03 4.45 4.57 0.07 0.79 100.04 9.02 X-47 78.16 0.15 11.55 0.00 0.86 0.02 0.70 0.41 2.45 6.08 0.40 0.18 100.96 8.53 X-48 73.41 0.14 13.97 0.16 1.08 0.05 0.37 1.05 4.41 4.44 0.35 0.59 100.02 8.85 X-49 64.17 0.89 20.28 0.26 1.06 0.05 0.19 2.30 6.14 4.57 0.14 0.49 100.54 10.71 X-50 62.31 0.11 18.36 1.53 3.07 0.10 0.90 1.00 5.67 6.04 0.07 0.98 100.14 11.71 X-51 60.19 0.49 18.14 0.84 3.86 0.14 0.33 2.35 5.31 7.00 0.07 1.55 100.27 12.31 X-52 67.17 0.72 14.55 0.48 4.33 0.07 1.20 2.05 3.59 5.30 0.20 0.85 100.51 8.89 X-53 71.79 0.23 14.21 0.31 2.26 0.05 0.37 1.06 3.40 5.64 0.12 0.98 100.42 9.04 X-54 71.06 0.45 14.42 0.03 1.25 0.05 0.65 4.21 2.70 5.49 0.11 0.57 100.99 8.19 X-55 75.50 0.31 12.40 1.50 0.60 0.03 0.40 0.60 3.10 5.60 0.04 0.94 101.02 8.70 X-56 67.80 0.71 14.50 0.90 3.60 0.05 1.18 2.90 3.10 4.60 0.21 0.87 100.42 7.70 X-57 67.00 0.75 14.20 1.10 4.00 0.07 1.30 2.40 2.80 5.10 0.22 1.34 100.28 7.90 X-58 71.10 0.28 14.50 1.20 1.10 0.03 0.29 1.10 3.40 6.30 0.07 0.93 100.30 9.70 X-59 69.70 0.52 14.20 1.00 2.40 0.07 0.60 1.70 4.80 5.50 0.14 0.77 101.40 10.30 X-60 71.10 0.38 13.60 1.10 2.50 0.06 0.42 1.50 3.50 5.50 0.08 1.27 101.01 9.00 X-61 71.74 0.27 14.47 0.32 1.73 0.05 0.42 1.62 3.44 4.65 0.24 0.55 99.50 8.09 X-62 61.07 0.80 16.53 1.03 5.61 0.16 0.56 2.97 3.75 6.03 0.14 0.84 99.49 9.78 X-63 64.77 0.89 15.33 0.73 4.82 0.08 1.45 2.54 3.83 4.30 0.27 0.87 99.88 8.13 X-64 61.68 1.20 14.96 0.77 7.01 0.12 2.29 3.15 3.60 3.30 0.35 1.28 99.71 6.90 X-65 74.82 0.11 13.65 0.38 0.65 0.01 0.50 0.98 3.57 5.35 0.03 0.58 100.63 8.92 X-66 72.86 0.30 14.37 0.79 2.66 0.04 0.54 0.93 3.98 5.25 0.09 0.72 102.53 9.23 X-67 70.30 0.38 13.88 0.60 3.27 0.07 0.45 1.17 2.29 5.90 0.14 0.84 99.29 8.19 X-68 70.96 0.28 13.75 1.02 1.58 0.05 0.24 0.91 1.65 7.44 0.07 1.31 99.26 9.09 X-69 68.83 0.48 14.51 4.05 0.79 0.03 0.33 0.10 2.79 7.36 0.05 0.00 99.32 10.15 X-70 74.17 0.21 12.86 0.00 1.80 0.04 0.33 0.49 1.94 5.91 0.10 0.50 98.35 7.85 X-71 70.61 0.33 14.72 1.41 0.86 0.02 0.55 0.54 2.17 7.33 0.18 0.73 99.45 9.50 X-72 69.88 0.40 13.71 1.80 2.37 0.07 0.27 0.62 2.92 6.03 0.04 0.55 98.66 8.95 X-73 67.24 0.73 14.52 2.90 2.30 0.03 0.95 2.17 4.44 3.53 0.26 0.00 99.07 7.97 X-74 58.87 0.46 14.09 2.03 2.44 0.07 2.10 7.49 6.09 3.07 0.17 0.00 96.88 9.16 X-75 71.21 0.42 21.42 2.00 1.44 0.03 0.45 0.89 4.10 4.92 0.11 0.81 107.80 9.02 X-76 55.35 1.48 14.63 10.86 0.00 0.10 4.43 2.43 0.91 7.34 0.50 1.65 99.69 209 199 56 591 28.0 13 11 295 50 139 <9 1379 8.25 X-77 61.50 1.10 15.15 7.30 0.00 0.11 1.58 2.81 4.39 5.07 0.34 1.21 100.59 182 313 48 339 34.0 15 <9 7 47 92 11 1189 9.46 X-78 51.81 3.13 15.06 11.46 0.00 0.06 7.53 1.00 3.02 4.48 0.33 2.67 100.54 137 109 32 290 46.0 25 102 20 100 415 117 118 7.50 X-79 48.31 4.07 11.38 9.92 0.00 0.21 9.92 5.90 2.58 1.14 0.57 6.34 100.34 18 234 32 358 44.0 47 70 35 146 458 74 75 3.72 X-80 45.03 3.27 13.53 16.29 0.00 0.09 6.04 5.05 5.14 3.32 0.53 2.13 100.41 97 112 48 325 55.0 24 81 12 23 327 142 141 8.46 X-81 46.37 3.96 13.46 15.27 0.00 0.05 6.20 4.88 4.91 2.96 0.54 1.92 100.52 103 94 55 302 48.0 17 88 7 22 324 135 148 7.87 X-82 48.60 1.56 13.71 18.47 0.00 0.08 2.02 5.07 7.38 1.05 0.81 1.52 100.26 32 122 61 567 84.0 <9 10 777 47 58 <9 233 8.43 X-83 46.07 2.56 14.20 17.60 0.00 0.15 5.97 5.84 3.60 3.20 0.32 0.85 100.37 88 105 27 177 32.0 17 44 102 44 325 79 384 6.80 X-84 46.07 3.95 12.30 12.67 0.00 0.06 3.44 8.56 5.49 0.87 0.91 6.14 100.47 27 106 59 444 89.0 11 11 26 59 138 <9 152 6.36 X-85 47.35 2.56 14.08 13.25 0.00 0.14 7.29 8.22 4.21 0.61 0.32 2.54 100.58 21 287 26 173 37.0 36 69 11 182 318 36 127 4.82 X-86 45.88 3.96 12.72 16.75 0.00 0.25 5.61 7.19 3.78 1.46 0.31 2.23 100.14 37 319 33 201 40.0 14 36 124 167 522 <9 303 5.24 X-87 46.09 2.86 13.80 14.33 0.00 0.23 6.98 7.07 4.90 0.32 0.41 3.05 100.06 13 344 31 208 42.0 18 50 9 134 315 23 119 5.22 X-88 45.24 2.00 14.37 11.55 0.00 0.11 10.97 4.11 2.72 5.24 0.20 3.85 100.37 147 69 25 131 21.0 35 201 <2 168 326 515 112 7.96 X-89 46.20 3.57 8.68 14.36 0.00 0.18 11.42 6.07 4.30 2.70 0.67 1.85 100.01 56 337 36 223 53.0 37 30 7 228 474 9 155 7.00 X-90 73.62 0.31 12.90 0.54 1.67 0.05 0.42 1.13 3.37 5.90 0.10 0.44 100.45 370 9.27 ZGSI 58.04 Tr 20.76 4.45 0.20 0.09 0.95 9.22 4.81 Tr 1.99 100.51 ZGSII 56.31 Tr 19.89 4.28 0.30 0.16 0.26 0.74 8.33 5.75 n.d. 3.56 99.58 0.00 APPENDIX D GEOGRAPHIC COORDINATES OF SAMPLES COLLECTED A16 Zambian sample s located on UTM zone 35, 26 A17 Zambian samples located using latitude and longitude (WGS84), 31 Zambian samples that are located in UTM zone 36, 31 A18 Namibian samples that are located in UTM zone 33 (Schwartzeck), 32 A19 Namibian samples that are located in UTM zone 34, (Schwartzeck), 36 A20 Namibian samples that are located using latit ud e and longit u de coordin a t es (Schwa r tz ec k ) , 37 Table A16 Zambian samples that are located in UTM zone 35 ID UTMEAST UTMNORTH UTMZONE ROCK LOCATION SAMPLE PAGE ANALYSIS 5 731700 8457266 35L Mkushi Mine Granites Site of Patrick Mumba's work L-005 12 5a 6 731700 8457266 35L Mkushi Mine Granites Site of Patrick Mumba's work L-006 12 7 731700 8457266 35L Mkushi Mine Granites Site of Patrick Mumba's work L-007 12 8 731700 8457266 35L Mkushi Mine Granites Site of Patrick Mumba's work L-008 12 9 600660 8609383 35L Nchanga Granite na L-009 15 10 438010 8662976 35L Cu minzn, Kansanshi Mine na L-010 16 11 438010 8662976 35L Cu minzn, Kansanshi Mine na L-011 16 13 454177 8379381 35L Mineralized Quartz Veins na L-013 17 14 462917 8377465 35L Several Hydrothermal veins na L-014 18 20 185354 8761659 35L Granitoid Kalene Hill L-020 22 x 21 185354 8761659 35L Granitoid Kalene Hill L-021 22 22 188112 8765321 35L Granitoid Kalene Hill L-022 23 23 188112 8765321 35L Granitoid Kalene Hill L-023 23 24 191378 8764946 35L Gabbro Kalene Hill L-024 23 x 25 192873 8762357 35L Granitoid Kalene Hill L-025 23 x 26 192873 8762357 35L Granitoid Kalene Hill L-026 23 x 27 192873 8762357 35L Granitoid Kalene Hill L-027 23 x 28 282993 8698411 35L Non-foliated amphybolite Mwinilunga L-028 23 x 29 281721 8699392 35L Amphybolite Mwinilunga L-029 26 x 30 295813 8692365 35L Gneiss Mwinilunga L-030 26 x 31 295813 8692365 35L Gneiss Mwinilunga L-031 26 32 309413 8685473 35L Gneiss Mwembezhi L-032 27 x 33 318288 8680411 35L Soil (after granitoid) Mwembezhi L-033 27 34 318288 8680411 35L Termite Mound (after granitoid) Mwembezhi L-034 27 35 370413 8665100 35L Magnetite sand Solwesi, Nepheline syenite quarr L-035 31 36 370433 8665159 35L Red syenite Solwesi, Nepheline syenite quarr L-036 33 x 37 370435 8665166 35L Blue syenite Solwesi, Nepheline syenite quarr L-037 34 2 38 370437 8665173 35L Blue syenite Solwesi, Nepheline syenite quarr L-038 34 x 39 370462 8665115 35L Pink Granitoid that cuts the blue syenite Solwesi, Nepheline syenite quarr L-039 34 x 40 370443 8665082 35L Massive blue nepheline sodalite Solwesi, Nepheline syenite quarr L-040 34 x 41 370437 8665073 35L Massive non-foliated blue rock Solwesi, Nepheline syenite quarr L-041 35 x 42 370452 8665107 35L Black, crystalline, massive mineral that fills Solwesi, Nepheline syenite quarr L-042 35 43 370454 8665126 35L Fresh "blue" syenite Solwesi, Nepheline syenite quarr L-043 35 44 370454 8665126 35L Fresh "blue" syenite Solwesi, Nepheline syenite quarr L-044 35 x 45 370479 8665123 35L Finer-grained variety of pink syenite Solwesi, Nepheline syenite quarr L-045 35 x 46 370467 8665160 35L Fresh "brown", coarse-grained syenite Solwesi, Nepheline syenite quarr L-046 35 x 47 320870 8660393 35L Granitoid Site suggested by Peter Mann L-047 36 x 48 320900 8660423 35L Granitoid Site suggested by Peter Mann L-048 36 49 437651 8665739 35L Gabbro Solwesi L-049 37 x 50 437683 8665710 35L Gabbro Solwesi L-050 37 x 51 438010 8662976 35L Cu minzn Kansanshi Open Pit L-051 38 52 438010 8662976 35L Cu minzn, vein Kansanshi Open Pit L-052 38 53 438010 8662976 35L Cu minzn, vein Kansanshi Open Pit L-053 38 54 438010 8662976 35L Cu minzn, vein Kansanshi Open Pit L-054 38 55 438010 8662976 35L Secondary Cu minzn Kansanshi Open Pit L-055 38 56 438010 8662976 35L Secondary Cu minzn Kansanshi Open Pit L-056 38 57 438010 8662976 35L Secondary Cu minzn Kansanshi Open Pit L-057 38 58 438010 8662976 35L Secondary Cu minzn Kansanshi Open Pit L-058 38 59 438270 8664080 35L Granitoid, Diorite K-292 borehole, Kansanshi Mine L-059 38 x 60 438180 8664200 35L Granitoid, Diorite K-256 borehole, Kansanshi Mine L-060 38 2 61 438180 8664200 35L Granitoid, Diorite K-256 borehole, Kansanshi Mine L-061 38 62 482227 8643322 35L Massive Qtz Solwesi L-062 39 63 477452 8645003 35L Granitoid w/ FeOx altn? na L-063 39 x 64 477452 8645003 35L Granitoid, fresh na L-064 39 x 65 477452 8645003 35L Granitoid, pink, fresh na L-065 39 x 68 496214 8639513 35L f-g Granitoid na L-068 40 69 496887 8639716 35L Qtz blobs Solwesi L-069 40 70 496887 8639716 35L Qtz blobs Solwesi L-070 40 71 496887 8639716 35L Qtz blobs Solwesi L-071 40 72 496887 8639716 35L Qtz blobs Solwesi L-072 40 75 602900 8632253 35L Granitoid Muliashi Porphyry L-075 44 76 602900 8632253 35L Granitoid Muliashi Porphyry L-076 45 x 77 602900 8632253 35L Granitoid Muliashi Porphyry L-077 x 78 602900 8632253 35L Granitoid Muliashi Porphyry L-078 x 79 458795 8465379 35L Polymictic bx K-1 borehole, Kaungashi, Lunga A L-079 45 x 80 458795 8465379 35L Stkwk in syenite (magnetic?) K-1 borehole, Kaungashi, Lunga A L-080 45 81 458795 8465379 35L Granitoid K-1 borehole, Kaungashi, Lunga A L-081 45 82 458795 8465379 35L Stkwk in syenite w/ magnetite K-1 borehole, Kaungashi, Lunga A L-082 45 83 458795 8465379 35L Granitoid K-1 borehole, Kaungashi, Lunga A L-083 45 84 458795 8465379 35L Granitoid K-1 borehole, Kaungashi, Lunga A L-084 45 85 458795 8465379 35L Serpentinitized shear zone (?) K-1 borehole, Kaungashi, Lunga A L-085 45 86 458795 8465379 35L Stkwk w/ red calc matrix ~ jigsaw bx in granit o K-1 borehole, Kaungashi, Lunga A L-086 45 87 458795 8465379 35L Granitoid, f-g w/ foliation & red veins K-1 borehole, Kaungashi, Lunga A L-087 45 88 458795 8465379 35L Granitoid, f-g, dk green K-1 borehole, Kaungashi, Lunga A L-088 45 89 458795 8465379 35L Polymictic bx K-1 borehole, Kaungashi, Lunga A L-089 45 90 458795 8465379 35L Gray Syenite K-1 borehole, Kaungashi, Lunga A L-090 45 91 35L Granitoid KW-22 borehole, with Avmin L-091 45 95 35L Breccia MB-34 borehole L-095 66 147 593617 8616605 35L Basal Conglomerate Nchanga Mine L-147 68 148 594696 8617011 35L Massive Cu minzn along "lamprophyre" Nchanga Mine L-148 68 149 594696 8617011 35L Sheared sediments with Cu mnzn along "lam p Nchanga Mine L-149 68 150 594696 8617011 35L Gabbro from "Lamprophyre" Nchanga Mine L-150 68 x 151 591327 8609982 35L Granitoid Nchanga Granite L-151 69 x 152 591820 8609722 35L Granitoid Nchanga Granite L-152 70 153 591792 8609693 35L Granitoid Nchanga Granite L-153 70 x 154 591781 8609668 35L Granitoid Nchanga Granite L-154 70 x 155 613444 8600564 35L Granitoid Chambishi Open Pit L-155 71 x 163 35L Gabbro, very foliated? VS-3B borehole, Konkola Deep Sh L-163 72 x 164 636861 8611323 35L Granitoid Mufulira Granite L-164 72 ID UTMEAST UTMNORTH UTMZONE ROCK LOCATION SAMPLE PAGE ANALYSIS 165 636883 8611342 35L Granitoid Mufulira Granite L-165 72 166 636891 8611330 35L Granitoid Mufulira Granite L-166 72 x 167 626463 8602164 35L Schist Lufubu Schist under bridge L-167 72 x 168 35L Granitoid NOP-681 borehole, Nchanga Mine L-168 73 x 170 35L Granitoid NOP-681 borehole, Nchanga Mine L-170 73 x 171 35L Nchanga Bx NOP-836 borehole, Nchanga Mine L-171 73 173 35L Granitoid NOP-589 borehole, Nchanga Mine L-173 73 x 174 621165 8309439 35L Qtz blob West Lusaka L-174 73 175 622333 8310267 35L Foliated Granitoid West Lusaka L-175 73 x 176 622623 8310157 35L Qtz, massive, sugary West Lusaka L-176 74 177 622623 8310157 35L Qtz, massive, pink West Lusaka L-177 74 178 622623 8310157 35L Qtz w/ hem blog West Lusaka L-178 74 181 600818 8284839 35L Mafic Intrusive with garnet West Lusaka L-181 74 182 600750 8284708 35L Mafic Intrusive with garnet West Lusaka L-182 74 183 603222 8285377 35L Magnetite-hematite Bx West Lusaka L-183 75 184 603222 8285377 35L Magnetite Bx West Lusaka L-184 75 185 603222 8285377 35L Hematite jigsaw bx West Lusaka L-185 75 186 603222 8285377 35L Hematite jigsaw bx West Lusaka L-186 75 187 603222 8285377 35L Hematite angular bx West Lusaka L-187 75 195 602827 8285288 35L Syenite West Lusaka L-195 75 196 602834 8285513 35L Granitoid ? West Lusaka L-196 75 197 602834 8285513 35L Granitoid (contact metamorph.) West Lusaka L-197 75 198 536409 8292271 35L Gabbro West Lusaka L-198 76 199 536409 8292271 35L Syenite West Lusaka L-199 76 200 535941 8292080 35L Gabbro w/ epidote West Lusaka L-200 76 201 535941 8292080 35L Gabbro w/ epidote West Lusaka L-201 76 202 535941 8292080 35L Sandstone w/ hematite West Lusaka L-202 76 203 535941 8292080 35L Gabbro West Lusaka L-203 76 204 533464 8288234 35L Magnetite + hematite (skarn?) Mamba Coilliery Magnetite mine L-204 76 205 533464 8288234 35L Skarn tremolite-actinolite (sulfides?) Mamba Coilliery Magnetite mine L-205 76 206 533464 8288234 35L Skarn rocks Mamba Coilliery Magnetite mine L-206 76 207 520902 8295961 35L f-g Syenite w/ epidote? na L-207 77 208 520902 8295961 35L c-g Syenite w/ epidote? na L-208 77 209 520902 8295961 35L m-g Gabbro w/ epidote? na L-209 77 210 519179 8296368 35L f-g Syenite, pink na L-210 77 211 518327 8296538 35L porph. Syenite na L-211 77 212 517461 8296629 35L Syenite na L-212 77 213 511614 8297405 35L Syenite na L-213 77 214 511614 8297405 35L Syenite + hematite diss na L-214 77 215 511614 8297405 35L Syenite na L-215 77 216 510646 8297211 35L Bn Syenite na L-216 77 217 510646 8297211 35L f-g Syenite, red na L-217 77 218 509106 8296883 35L f-g Syenite, pink w/ bk needles na L-218 78 219 498596 8301830 35L 2 Gabbro samples na L-219 78 220 494828 8314088 35L Syenite + hematite + qtz na L-220 78 221 494828 8314088 35L Syenite + hematite + qtz na L-221 78 222 494828 8314088 35L Syenite + hematite + qtz na L-222 78 223 494828 8314088 35L Syenite + hematite + qtz na L-223 78 224 494875 8319257 35L Granitoid, coarse + hematite na L-224 78 225 494875 8319257 35L Granitoid, coarse + hematite na L-225 78 226 520190 8323570 35L Concentric banding Dun Robin Mine L-226 79 227 520190 8323570 35L Concentric banding Dun Robin Mine L-227 79 228 520190 8323570 35L Concentric banding Dun Robin Mine L-228 79 229 520190 8323570 35L Free Au in Gossan Dun Robin Mine L-229 79 230 520190 8323570 35L Free Au in Gossan Dun Robin Mine L-230 79 231 520190 8323570 35L Concentric banding Dun Robin Mine L-231 79 232 520190 8323570 35L Stkwk + Au Dun Robin Mine L-232 79 233 522000 8325777 35L Metaconglomerate Dun Robin Mine L-233 79 234 524120 8323852 35L Qtz blob Matala Mine ? L-234 80 235 405295 8345145 35L Granitoid Kafue Park L-235 81 236 407722 8344484 35L Granitoid Kafue Park L-236 81 237 408553 8344258 35L Granitoid Kafue Park L-237 81 238 409136 8344100 35L Granitoid, coarse, with sulfides Kafue Park L-238 81 239 409510 8343996 35L Granitoid, coarse Kafue Park L-239 81 240 409748 8343937 35L Granitoid, coarse Kafue Park L-240 81 241 410062 8343846 35L Granitoid w/ diss sulfides Kafue Park L-241 81 242 410387 8343757 35L Bx, angular, of bk & red material Kafue Park L-242 81 243 410387 8343757 35L Bx, angular, of bk & red material Kafue Park L-243 81 244 410337 8343780 35L Granitoid Kafue Park L-244 81 245 410436 8343754 35L Granitoid, pink, 2 samples Kafue Park L-245 81 246 410436 8343754 35L Granitoid, gray, c-g Kafue Park L-246 81 247 411817 8343369 35L Granitoid, m-g, foliated Kafue Park L-247 81 248 411300 8343517 35L Granitoid, m-g, foliated Kafue Park L-248 82 249 411300 8343517 35L Granitoid, m-g, foliated Kafue Park L-249 82 250 414509 8342637 35L Granitoid, m-g, foliated Kafue Park L-250 82 251 414509 8342637 35L Granitoid, m-g, foliated Kafue Park L-251 82 252 417308 8342625 35L Granitoid, m-g, foliated Kafue Park L-252 82 253 430325 8344423 35L Quartz blobs, pink-purple Kafue Park L-253 82 254 435923 8344774 35L Granitoid, f-m-g, gray Kafue Park L-254 82 255 437504 8344870 35L Granitoid, m-g, bn, w/ sulfides Kafue Park L-255 82 256 437300 8344864 35L Granitoid, good outcrop Kafue Park L-256 82 257 440501 8345047 35L Granitoid, pink, f-m-g, purple mnzn Kafue Park L-257 83 258 443166 8345205 35L Granitoid, lt gray m-f-g w/ sulfides Kafue Park L-258 83 259 443600 8345232 35L Granitoid, bn, m-g Kafue Park L-259 83 260 445480 8345341 35L Granitoid, lt bn w/ sulfides Kafue Park L-260 83 261 446235 8345377 35L Granitoid, gray-pink, mf-g, w/ diss cpy Kafue Park L-261 83 262 447650 8345462 35L Granitoid, foliated w/ sulfides ? Kafue Park L-262 83 263 455666 8344828 35L Granitoid, gray, foliated, w/ porphyroblasts Kafue Park L-263 83 264 458846 8344455 35L Granitoid, extremely foliated Kafue Park L-264 83 265 459827 8344327 35L Granitoid, bn, f-g Kafue Park L-265 83 266 658649 8591610 35L Qtz blob Eyes NE of Kitwe L-266 95 ID UTMEAST UTMNORTH UTMZONE ROCK LOCATION SAMPLE PAGE ANALYSIS 267 659696 8589920 35L Qtz pegmatite + muscovite Eyes NE of Kitwe L-267 95 268 35L Stkwk + hematite in schist CT-124 borehole, Samba L-268 96 278 306500 8507500 35L Schist after porphyritic igneous rock? W/ qtz v CT-116 borehole, Samba L-278 96 285 309650 8507300 35L Granitoid, coarse + hematite, cpy, py RKN-719 borehole L-285 97 294 309655 8507190 35L Bk hematite filling veins in stkwk RKN-801 borehole L-294 97 311 362655 8628407 35L Banded gabbro Shilenda, Jon Woodhead, Zamang L-311 312 362655 8628407 35L Gabbro w/ py mnzn Shilenda, Jon Woodhead, Zamang L-312 0 313 298404 8505075 35L Syenite w/ fine specularite diss Jikambo Old pits, Jon Woodhead, L-313 0 314 285600 8528650 35L F-g granitoid rock Kalengwa North, Jon Woodhead, Z L-314 0 315 287600 8528700 35L vitrophyre w/ patchy hematitization Kalengwa North, Jon Woodhead, Z L-315 0 316 297000 8521000 35L Granitoid Kalengwa Ndenda, Jon Woodhead L-316 0 317 297000 8521000 35L Granitoid Kalengwa Ndenda, Jon Woodhead L-317 0 318 297000 8521000 35L Granitoid Kalengwa Ndenda, Jon Woodhead L-318 0 319 297000 8521000 35L Granitoid Kalengwa Ndenda, Jon Woodhead L-319 0 320 297000 8521000 35L Granitoid Kalengwa Ndenda, Jon Woodhead L-320 0 321 283300 8511500 35L ferro-gabbro/diorite? Kalengwa Mine, Jon Woodhead, Z a L-321 0 322 283300 8511500 35L ferro-gabbro/diorite? Kalengwa Mine, Jon Woodhead, Z a L-322 0 323 283300 8511500 35L ferro-gabbro/diorite? Kalengwa Mine, Jon Woodhead, Z a L-323 0 324 283300 8511500 35L ferro-gabbro/diorite? Kalengwa Mine, Jon Woodhead, Z a L-324 0 325 299386 8507419 35L quartzmonzonite (altered) Jikambo RKN-719 samples, Jon W L-325 0 326 299386 8507419 35L quartzmonzonite (altered) Jikambo RKN-719 samples, Jon W L-326 0 327 35L 4DC-1 Granitoid porphyry (Rept. 111, Lumw a Geological Survey, Lusaka L-327 0 328 35L 4DC-1 Granitoid porphyry Geological Survey, Lusaka L-328 0 329 35L 4DC-1 Granitoid porphyry Geological Survey, Lusaka L-329 0 330 35L 4DC-8 Foliated granite. (dated 1940Ma) Geological Survey, Lusaka L-330 0 331 35L 4DC-9 Foliated granite Geological Survey, Lusaka L-331 0 35L 4DC-10 Schist (after altered granite) Geological Survey, Lusaka L-332 0 333 35L 4DC-11 Porphyroblastic schist Geological Survey, Lusaka L-333 0 334 35L 4DC-16 Granitoid (coarse gneiss) Geological Survey, Lusaka L-334 0 335 35L 4DC-55 Porphyritic gneiss Geological Survey, Lusaka L-335 0 336 35L 4DC-100 Gabbro Geological Survey, Lusaka L-336 0 337 35L 4DC-232 Gabbro, foliated, porphyroblastic Geological Survey, Lusaka L-337 0 338 35L 4DC-274 Porphyritic granitoid Geological Survey, Lusaka L-338 0 339 35L 4DC-29 Fine grained intrusive breccia Geological Survey, Lusaka L-339 0 340 35L 4DC-6 Granitoid Geological Survey, Lusaka L-340 0 341 405750 8350800 35L 5GC-164 Felsic granitoid. Aegirine augite gn e Geological Survey, Lusaka L-341 0 342 35L 5GC-180 Coarse gneiss after granitoid. Pyro x Geological Survey, Lusaka L-342 0 343 416000 8351000 35L 5GC-Granitoid, foliated. Pyroxene scapolite g Geological Survey, Lusaka L-343 0 344 434800 8351200 35L 5GC-236, Coarse granitoid. Aegirine augite g Geological Survey, Lusaka L-344 0 345 440750 8356400 35L 5GC-240 Pink syenite ? Geological Survey, Lusaka L-345 0 346 399750 8350000 35L 5GC-250 Coarse granitoid. Qtz felds porphy r Geological Survey, Lusaka L-346 0 347 427000 8345000 35L 5GC-251 Foliated granitoid. Qtz felds porph y Geological Survey, Lusaka L-347 0 348 399800 8350400 35L 5GC-258 Foliated granitoid. Pyroxene scapo Geological Survey, Lusaka L-348 0 349 401800 8351000 35L 5GC-259 Foliated granitoid. Pyroxene scapo Geological Survey, Lusaka L-349 0 350 35L 5GC-265 F-m g granitoid. Monzonite + qtz di Geological Survey, Lusaka L-350 0 351 35L 5GC-267 Pink-red granitoid Geological Survey, Lusaka L-351 0 352 405500 8355900 35L 5GC-283 Quartz feldespathic porphyry Geological Survey, Lusaka L-352 0 353 417000 8351000 35L 5GC-284 Granitoid w/ py Geological Survey, Lusaka L-353 0 354 442750 8344700 35L 5GC-330 Coarse granitoid (Quartz feldspathi c Geological Survey, Lusaka L-354 0 355 437000 8389000 35L 5GC-402 Coarse granitoid (Quartz feldspathi c Geological Survey, Lusaka L-355 0 356 35L 5GC-53 Medium grained granitoid Geological Survey, Lusaka L-356 0 357 202615 8771063 35L 3DA-34 Med. Granitoid (Rept 107, Kalene Hil Geological Survey, Lusaka L-357 0 358 202615 8771063 35L 3DA-35 Foliated granitoid Geological Survey, Lusaka L-358 0 359 202615 8771063 35L 3DA-36 Foliated granitoid Geological Survey, Lusaka L-359 0 360 198992 8767035 35L 3DA-45 Med granitoid Geological Survey, Lusaka L-360 0 361 202131 8775612 35L 3DA-56 Med granitoid. Massive med-grained Geological Survey, Lusaka L-361 0 362 203141 8776017 35L 3DA-58 med granitoid. Gray granite Geological Survey, Lusaka L-362 0 363 203846 8776213 35L 3DA-59 Med granitoid Geological Survey, Lusaka L-363 0 364 194000 8769500 35L 3DA-60 Med granitoid. Chloritized scales of b Geological Survey, Lusaka L-364 0 365 190353 8757416 35L 3DA-72 Med granitoid Geological Survey, Lusaka L-365 0 366 184965 8762141 35L 3DA-73 Med granitoid. Coarse biot leukogran Geological Survey, Lusaka L-366 0 367 191505 8761399 35L 3DA-82 Foliated granitoid Geological Survey, Lusaka L-367 0 368 182724 8766986 35L 3DA-83 Granitoid porphyry Geological Survey, Lusaka L-368 0 369 195407 8762331 35L 3DA-93 Granitoid. Massive granite Geological Survey, Lusaka L-369 0 370 179530 8790750 35L 3DA-97 Granitoid. Masive porph. Granite Geological Survey, Lusaka L-370 0 371 175705 8791238 35L 3DA-98 Granitoid Geological Survey, Lusaka L-371 0 372 180757 8787339 35L 3DA-100 Med grained gabbro Geological Survey, Lusaka L-372 0 373 180757 8787339 35L 3DA-101 Granitoid Geological Survey, Lusaka L-373 0 374 187816 8791635 35L 3DA-103 Granitoid Geological Survey, Lusaka L-374 0 375 182396 8783618 35L 3DA-106 Foliated Granitoid Geological Survey, Lusaka L-375 0 376 180961 8782807 35L 3DA-107 Foliated Granitoid Geological Survey, Lusaka L-376 0 377 191903 8770914 35L 3DA-109 Fine grained granitoid Geological Survey, Lusaka L-377 0 378 190430 8770699 35L 3DA-110 Coarse granitoid Geological Survey, Lusaka L-378 0 379 191290 8769017 35L 3DA-111 Fine grained gabbro. Massive porp h Geological Survey, Lusaka L-379 0 380 179813 8777986 35L 3DA-117 Foliated granitoid Geological Survey, Lusaka L-380 0 381 35L 5GB-42 Porphyritic granitoid (Rept 31) Geological Survey, Lusaka L-381 0 382 35L 5GB-Hematite stkwk in granitoid Geological Survey, Lusaka L-382 0 383 35L 5GB-44 Fine grained rock w/ Fe Ox Geological Survey, Lusaka L-383 0 384 35L 5GB-45 Massive hematite Geological Survey, Lusaka L-384 0 385 35L 5GB-46 Hematite-altered granitoid Geological Survey, Lusaka L-385 0 386 35L 5GB-48 Fine grained volcanic rock Geological Survey, Lusaka L-386 0 387 35L 5GB-49 Fine grained volcanic rock Geological Survey, Lusaka L-387 0 388 35L 5GB-50 Very fine-grained granitoid Geological Survey, Lusaka L-388 0 389 35L 5GB-51 Red rock-altered granitoid Geological Survey, Lusaka L-389 0 390 35L 5GB-52 Massive hematite Geological Survey, Lusaka L-390 0 391 35L 5GB-96 Red rock-altered granitoid. Syenite, p Geological Survey, Lusaka L-391 0 392 35L 5GB-97 Red rock-altered granitoid. Syenite, p Geological Survey, Lusaka L-392 0 393 35L 5GB-101 Red rock-altered granitoid Geological Survey, Lusaka L-393 0 394 35L 5GB-103 Volcanic porphyry w/ red rock altn. D Geological Survey, Lusaka L-394 0 395 35L 5GB-163 Hematitized wall rock. Tourmaline q Geological Survey, Lusaka L-395 0 396 35L 5GB-166 Granitoid Geological Survey, Lusaka L-396 0 ID UTMEAST UTMNORTH UTMZONE ROCK LOCATION SAMPLE PAGE ANALYSIS 397 35L N-90 Granitoid. Gneiss (rept 60) Geological Survey, Lusaka L-397 0 398 35L N-127 Gabbro Geological Survey, Lusaka L-398 0 399 35L N-235 Foliated granitoid Geological Survey, Lusaka L-399 0 400 35L N-265 Volcanic rock (pre-Karroo) Foliated gr a Geological Survey, Lusaka L-400 0 401 35L N-218 Foliated granitoid Geological Survey, Lusaka L-401 0 402 457000 8394000 35L 5GD-36 Foliated granitoid (rept 27) Geological Survey, Lusaka L-402 0 403 477000 8345000 35L 5GD-43 Porphyritic granitoid Geological Survey, Lusaka L-403 0 404 473500 8356000 35L 5GD-56 Granitoid Geological Survey, Lusaka L-404 0 405 467000 8345500 35L 5GD-77 Gabbro Geological Survey, Lusaka L-405 0 406 476200 8346600 35L 5GD-82 Gabbro Geological Survey, Lusaka L-406 0 407 457000 8380000 35L 5GD-153 Rapakivi granitoid Geological Survey, Lusaka L-407 0 408 463000 8344500 35L 5GD-147 Red granitoid Geological Survey, Lusaka L-408 0 409 453500 8351500 35L 5GD-167 Red granitoid Geological Survey, Lusaka L-409 0 410 450000 8379000 35L 5GD-184 Porphyritic granitoid (volc. Rk?) Geological Survey, Lusaka L-410 0 411 493000 8363000 35L 5GD-229 White coarse-g granitoid (marble?) Geological Survey, Lusaka L-411 0 412 35L 5GD-356 Granitoid Geological Survey, Lusaka L-412 0 413 35L 3DC-130 Vuggy hematite (rept 110 Mwinilun g Geological Survey, Lusaka L-413 0 414 35L 7ED-6 Coarse gneiss after granitoid (rept 20) Geological Survey, Lusaka L-414 0 415 35L 3DB-174 Massive hematite (rept 108) Geological Survey, Lusaka L-415 0 416 671000 8244000 35L 7HD-230 Gabbro (repy 21) Geological Survey, Lusaka L-416 0 417 671000 8244000 35L 7HD-250 Foliated granitoid Geological Survey, Lusaka L-417 0 418 35L 5EA-4 Gneiss (foliated granitoid) (repy 36) Geological Survey, Lusaka L-418 0 419 35L 5EA-6 Granitoid Geological Survey, Lusaka L-419 0 422 35L 5EA-162 Foliated granitoid Geological Survey, Lusaka L-422 0 423 755000 8458000 35L 8FC-16 Granitoid (rept 12) Geological Survey, Lusaka L-423 0 424 755000 8458000 35L 8FC-17 Granitoid Geological Survey, Lusaka L-424 0 425 755000 8458000 35L 8FC-18 White granitoid Geological Survey, Lusaka L-425 0 426 747000 8476500 35L 8FC-50 Massive quartz + hematite Geological Survey, Lusaka L-426 0 427 35L 8FC-59 Foliated granitoid Geological Survey, Lusaka L-427 0 428 35L 8FC-81 Foliated granitoid Geological Survey, Lusaka L-428 0 429 762000 8497000 35L 8FC-233 Mafic xenolith in granitoid (non-folia t Geological Survey, Lusaka L-429 0 430 35L 8FC-423 Fine grained foliated granitoid Geological Survey, Lusaka L-430 0 431 763200 8482500 35L 8FC-450 Foliated granitoid Geological Survey, Lusaka L-431 0 432 765200 8452200 35L 8FC-460 Foliated granitoid Geological Survey, Lusaka L-432 0 433 442000 8343000 35L 5HA-3 Gabbro (rept 33) Geological Survey, Lusaka L-433 0 434 456000 8340000 35L 5HA-4 Gabbro Geological Survey, Lusaka L-434 0 435 433700 8330500 35L 5HA-6 Undeformed (?) coarse granitoid Geological Survey, Lusaka L-435 0 436 417500 8349000 35L 5HA-13 Pink med-g granitoid Geological Survey, Lusaka L-436 0 437 426100 8299000 35L 5HA-17 Fine grained gabbro. Dike Geological Survey, Lusaka L-437 0 438 448000 8264000 35L 5HA-20 Gabbro. Dike Geological Survey, Lusaka L-438 0 439 422000 8318700 35L 5HA-21 Orange porphyritic granitoid. Dike Geological Survey, Lusaka L-439 0 440 432000 8298000 35L 5HA-24 Gabbro. Dike Geological Survey, Lusaka L-440 0 441 404500 8288300 35L 5HA-42 Med-g granitoid Geological Survey, Lusaka L-441 0 442 440800 8308400 35L 5HA-69 Pink granitoid Geological Survey, Lusaka L-442 0 443 432000 8306700 35L 5HA-70 Pink foliated granitoid Geological Survey, Lusaka L-443 444 432000 8298000 35L 5HA-86 Fine dark gabbro Geological Survey, Lusaka L-444 445 676000 8529000 35L 7FB-146 Granitoid (rept 20) Geological Survey, Lusaka L-445 89 446 669500 8522000 35L 7FB-153 Foliated granitoid Geological Survey, Lusaka L-446 447 669500 8522000 35L 7FB-154 Foliated granitoid Geological Survey, Lusaka L-447 448 666000 8522000 35L 7FB-155 Foliated granitoid Geological Survey, Lusaka L-448 449 680000 8529000 35L 7FB-165 Foliated granitoid Geological Survey, Lusaka L-449 450 685000 8525000 35L 7FB-172 Foliated granitoid Geological Survey, Lusaka L-450 451 684000 8527000 35L 7FB-173 Felsic, white granitoid Geological Survey, Lusaka L-451 452 35L 7FB-176 Foliated granitoid Geological Survey, Lusaka L-452 453 666000 8522000 35L 7FB-176 Schist, clay altered Geological Survey, Lusaka L-453 454 676000 8530000 35L 7FB-178 Granitoid Geological Survey, Lusaka L-454 455 676000 8529000 35L 7FB-181 Granitoid Geological Survey, Lusaka L-455 456 666000 8522000 35L 7FB-188 Gneiss Geological Survey, Lusaka L-456 457 672000 8537000 35L 7FB-189 (175) Granitoid Geological Survey, Lusaka L-457 468 35L 7GB-78 Granitoid w/ hematite/magnetite Geological Survey, Lusaka L-468 469 35L 7GB-189 Granitoid Geological Survey, Lusaka L-469 470 35L 5GB-102 Geological Survey, Lusaka L-470 35L Gabbro, coarse grained West Lusaka L-180A 74 525465 8325280 35L Quartz blobs na L-233A 80 600660 8609383 35L Nchanga Granite na L-9A 15 376000 8248000 35L Calcium-enriched porphyritic granite Hook Granite 4HD184 406500 8285000 35L Calcium-enriched porphyritic granite Hook Granite 5HC485 412000 8282000 35L Calcium-enriched porphyritic granite Hook Granite 5HC489 367000 8274500 35L Migmatitic gneisses and granites Hook Granite 4HD115 355300 8253700 35L Migmatitic gneisses and granites Hook Granite 4HD117 353000 8237500 35L Migmatitic gneisses and granites Hook Granite 4HD190 373000 8266000 35L Migmatitic gneisses and granites Hook Granite 4HD202 374500 8272500 35L Migmatitic gneisses and granites Hook Granite 4HD203 376000 8254850 35L Coarse amphibole-quartz monzonite Hook Granite 4HD139 376000 8264500 35L Coarse amphibole-quartz monzonite Hook Granite 4HD147 385000 8260500 35L Coarse amphibole-quartz monzonite Hook Granite 4HD150 345500 8243000 35L Granodiorites and tonalites Hook Granite 4HD108 349000 8237700 35L Granodiorites and tonalites Hook Granite 4HD122 371000 8247300 35L Granodiorites and tonalites Hook Granite 4HD200 363500 8244300 35L Granodiorites and tonalites Hook Granite 4HD77 381000 8274000 35L Porphyroblastic biotite granite Hook Granite 4HD159 385500 8265000 35L Porphyroblastic biotite granite Hook Granite 4HD197 408000 8286000 35L Porphyroblastic biotite granite Hook Granite 5HC343 394700 8283100 35L Porphyroblastic biotite granite Hook Granite 5HC344 405000 8278700 35L Porphyritic alkali procataclasite Hook Granite 5HC384iii 415300 8267000 35L Porphyritic alkali procataclasite Hook Granite 5HC443 400200 8264000 35L Porphyritic alkali procataclasite Hook Granite 5HC474 377000 8276000 35L fine to medium-grained biotite granite Hook Granite 4HD133 356500 8247400 35L fine to medium-grained biotite granite Hook Granite 4HD182 367000 8260000 35L fine to medium-grained biotite granite Hook Granite 4HD205 360100 8235000 35L fine to medium-grained biotite granite Hook Granite 4HD41 ID UTMEAST UTMNORTH UTMZONE ROCK LOCATION SAMPLE PAGE ANALYSIS 341500 8252500 35L Biotite quartz monzonite Hook Granite 4HD48 394000 8258500 35L Leukocratic granite Hook Granite 5HC537 395500 8256000 35L Tourmaline granite Hook Granite 5HC455 400600 8285500 35L Post-Tectonic granite Hook Granite 5HC303 402700 8277500 35L Post-Tectonic granite Hook Granite 5HC307 401200 8272250 35L Post-Tectonic granite Hook Granite 5HC317 397000 8270000 35L Post-Tectonic granite Hook Granite 5HC445 13 296925 8520339 35L granitoid Kalengwa Area Zambia 13 14 298382 8503683 35L granitoid Kalengwa Area Zambia 14 16 298276 8503764 35L granitoid Kalengwa Area Zambia 16 17 299599 8503979 35L granitoid Kalengwa Area Zambia 17 22 264690 8487350 35L granitoid Kalengwa Area Zambia 22 24 283550 8551745 35L granitoid Kalengwa Area Zambia 24 25 282635 8549632 35L granitoid Kalengwa Area Zambia 25 26 299047 8529075 35L granitoid Kalengwa Area Zambia 26 28 594794 8612062 35L granitoid Chingola, Zm 28 29 600795 8609306 35L granitoid Chingola, Zm 29 38 393638 8255771 35L granitoid Kafue Park, Hook Granite, Zm 38 39 423570 8315373 35L granitoid Kafue Park, Hook Granite, Zm 39 41 414825 8298503 35L granitoid Kafue Park, Hook Granite, Zm 41 42 411907 8297321 35L granitoid Kafue Park, Hook Granite, Zm 42 44 412093 8296082 35L granitoid Kafue Park, Hook Granite, Zm 44 45 408665 8292534 35L granitoid Kafue Park, Hook Granite, Zm 45 46 404790 8289083 35L granitoid Kafue Park, Hook Granite, Zm 46 50 402228 8276327 35L Post-Tectonic granite Kafue Park, Hook Granite, Zm 50 53 397596 8260510 35L Tourmaline granite Kafue Park, Hook Granite, Zm 53 57 440441 8343507 35L granitoid Kafue Park, Hook Granite, Zm 57 58 447852 8345457 35L granitoid Kafue Park, Hook Granite, Zm 58 423932 8316746 35L granitoid Kafue Park, Hook Granite, Zm 40I Y 426932 8316746 35L granitoid Kafue Park, Hook Granite, Zm 40ii Y 2001 398200 8529500 35L u CH-5 Kasempa area, Dale Jannek e CH-5 Y 2002 448480 8530400 35L u MUF-1 Kasempa area, Dale Jann e MUF-1 Y 2003 449400 8530400 35L u MUF-2 Kasempa area, Dale Jann e MUF-2 Y 2004 448650 8527650 35L u MUF-3 Kasempa area, Dale Jann e MUF-3 Y 2005 447750 8530090 35L u MUF-4 Kasempa area, Dale Jann e MUF-4 Y 2006 599700 8614500 35L granitoid Gray's Quarry, Nchanga Granite Gray's Quarry y 2007 649000 8606000 35L granitoid Mufulira Mufulira G y 2008 614000 8601000 35L granitoid Chambishi Chambishi G y 2009 594400 8611200 35L granitoid Nchanga Red granite Nchanga Red G y 6010 358646 8476200 35L Subvolcanic porphyritic granitoid Chit-8 Borehole, Chitampa, Kasem CHIT-8, AVMIN y 6011 387800 8481200 35L Subvolcanic porphyritic granitoid MB-34 Borehole, Chitampa, Kase m MB-34 y Table A17 Zambian samples that are located using latitude and longitude coordinates (WGS84) SAMPLE E S ROCK LOCATION PAGE ANALYSIS 8A 28.633250000 -13.715260000 Muva Quartzite Big sampl 12 12 26.485972222 -14.590916667 Hook Granite 1 na 16 12a 26.486155556 -14.591208333 Hook Granite 2 na 17 420 26.466666667 -12.250000000 5EA-11 Granitoid Geologica 0 421 26.483333333 -12.266666667 5EA-17 Granitoid Geologica 0 458 27.100000000 -15.025000000 A-1208 Pink granitoid (rept ) Geologica 90 459 27.030000000 -15.091666667 A-1247 Gabbro. Mineralized and al Geologica 460 27.050000000 -15.416666667 A-1260 Foliated granitoid (minera Geologica 461 27.013333333 -15.066666667 A-1267 Fine-grained granitoid Geologica 462 27.008333333 -15.083333333 A-1268 Fine grained granitoid Geologica 463 27.121666667 -15.321666667 A-1351 Gabbro Geologica 464 27.133333333 -15.300000000 A-1353 Massive hematite Geologica 465 27.133333333 -15.333333333 A-1360 Porous massive hematite Geologica 466 27.133333333 -15.416666667 A-1364 Med-g granitoid Geologica 467 27.216666667 -15.416666667 A-1365 Med-g granitoid Geologica Zambian samples that are located in UTM zone 36 ID UTMEAST UTMNORTH UTMZONE ROCK LOCATION SAMPLE PAGE ANALYSIS 32 189947 8531605 36L granitoid Serenje, Zm 32 u y 33 187103 8541206 36L granitoid Serenje, Zm 33 u y 34 185730 8554091 36L granitoid Serenje, Zm 34 u y 35 180902 8553214 36L granitoid Serenje, Zm 35 u y Table A18 Namibian samples that are located in UTM zone 33 (Schwartzeck) ID UTMEAST UTMNORTH UTMZONE SAMPLE PAGE DATE ROCK LOCATION ELEVATION 492 539840 7809922 na L-830 5 22403 na 493 534537 7811450 na L-831 5 22403 na 506 472892 7827884 na L-840 7 22503 na 170 470574 7745499 33K L-1015 45 30803 Mafic gtd from dike Way to Oas Farm na 170 470574 7745499 33K L-1016 45 30803 Glassy vfg rk w/ sub// vugs (lava?) + qz way to Oas Farm 889 170 470574 7745499 33K L-1016a 45 30803 Volc rk w/o vacuoles Way to Oas Farm na 170 470574 7745499 33K L-1017 45 30803 mnzd u na 171 470780 7746140 33K L-1018 47 30803 mag from sand in dry ck na na 471546 7747493 na L-1019 47 30803 Fol fg gtd Way to Oas Farm na 471562 7747737 na L-1020 47 30803 Mafic fol gtd Oas Farm house na 471474 7753169 na L-1022 47 30803 Porphyritic subvolcanic rk, dike way to Loftdal farm na 626 471408 7753443 na L-1023 49 30803 Fresh mafic fol gtd way to Loftdal farm na 637 469519 7752923 na L-1024a 30803 Carbonatite for dating Lofdal na 637 469519 7752923 na L-1024c 30803 Carbonatite for dating Lofdal na 639 469504 7752995 33K L-1025 49 30803 Mafic rk w/ radial macroxts, magnetic Lofdal bx na 641 469468 7753052 33K L-1026 49 30803 Massive magnetite Lofdal bx na 643 469468 7753081 33K L-1027 49 30803 Massive mag w/ goss vugs after sulfs Lofdal bx na 642 469465 7753077 33K L-1028 49 30803 Cg gtd w/ circular vugs Lofdal bx na 645 469360 7753119 33K L-1029 49 30803 Gossanous mag Lofdal bx na 646 469653 7752666 33K L-1030 49 30803 Large bx Lofdal bx na 646 469653 7752666 33K L-1031 49 30803 Smal bx Lofdal bx na 649 469654 7752801 33K L-1032 51 30803 Mafic fol gtd Lofdal bx na 650 469649 7752814 33K L-1033 51 30803 Mag jigsaw bx Lofdal bx na 652 469646 7752816 33K L-1034 51 30803 Mag bx w/ igneous clasts Lofdal bx na 653 469623 7752848 33K L-1035 51 30803 Ang bx Lofdal bx na 221 466169 7754051 33K L-1036 30803 Big sample of mag bx Lofdal bx na 220 469619 7752727 33K L-1036 30803 Big sample of mag bx Lofdal bx na 689 685140 7751116 33K L-1039a 57 31003 Weathered gtd Otjiwarongo na 689 685140 7751116 33K L-1039c 57 31003 Weathered gtd Otjiwarongo na 689 685140 7751116 33K L-1040 57 31003 FeOx Otjiwarongo na 617 798316 7820893 na L-1041 30703 X Carbonate bx, base of Otavi sequence Otavi na 618 798318 7820909 na L-1042 30703 Y Cg porph fol gtd Otavi na 618 798318 7820909 na L-1043 30703 Z Fg felsic porph rk w/ little foliation Otavi na 618 798318 7820909 na L-1044 30703 XX Fresh gtd Otavi na 619 798172 7821133 na L-1045 30703 Yb Fresh gtd Otavi na 619 798172 7821133 na L-1046 30703 XXb Fresh gtd Otavi na 164 471364 7740547 33K L-1047 45 30803 stwk in bn rk entrance to Oas Farm 807 na L-1048 FeOx bx Borehole AV-12-160, Kombat na na L-1049 Bx Kombat mine na na L-1050 Bx Kombat mine na na L-1051 Bx Kombat mine na na L-1052 Bx Kombat mine na na L-1053 Bx Kombat mine na na L-1054 Bx Kombat mine na na L-1055 Bx Kombat mine na 466547 7755980 na L-551 na na na 26 243590 7536839 34K L-618 9 100802 quartz veins Klein Windhoek na 26 243590 7536839 34K L-619 9 100802 quartz veins Klein Windhoek na 31 243338 7537266 34K L-624 10 100802 M-f-g Gtd Okatjepuiko na 26 243590 7536839 34K L-624a 9 100802 quartz veins Klein Windhoek na 31 243338 7537266 34K L-625 10 100802 na Okatjepuiko na 32 243335 7537261 34K L-626 10 100802 M-f-g intrusive w/ FeOx veins Okatjepuiko na 35 243343 7537284 34K L-627 10 100802 F-g chloritized gtd w/ bk hem Okatjepuiko na 35 243343 7537284 34K L-628 10 100802 F-g chloritized gtd w/ bk hem Okatjepuiko na 35 243343 7537284 34K L-629 10 100802 F-g chloritized gtd w/ bk hem Okatjepuiko na 35 243343 7537284 34K L-630 10 100802 F-g chloritized gtd w/ bk hem Okatjepuiko na 37 243050 7537104 34K L-631 10 100802 Red jasper bx Okatjepuiko na 39 243021 7537009 34K L-632 11 100802 Dk bn vf-g volc rk w/ white plag phenxt Okatjepuiko na 41 242991 7537254 34K L-633 11 100802 F-m-g gtd w/ chlorite veinlets, monzogab Okatjepuiko na 43 242977 7537404 34K L-634 11 100802 Bk-dk gn volc rk (basalt?) subvolc? Okatjepuiko na 44 242959 7537593 34K L-635 11 100802 Med gray porh vold rk Okatjepuiko na 36 243060 7537117 34K L-636 10 100802 Dk volc rk w/ pk veinlets Okatjepuiko na 36 243060 7537117 34K L-637 10 100802 Lt vold rk w/ plag & slight fol (flow ban Okatjepuiko na 42 242988 7537303 34K L-639 11 100802 na Okatjepuiko na 46 242979 7537303 34K L-640 100802 F-g pk gtd w/ bk volc rk xenoliths Okatjepuiko na 46 242979 7537303 34K L-641 100802 F-g dk gn-dk gray vold rk (xenolith? Monz Okatjepuiko na 48 243578 7536616 34K L-642 100802 F-g bk volc rk Fol. W/ mass FEOx altn Okatjepuiko na 49 243591 7536591 34K L-643 100802 Gtd w/ FeOx veinlets Okatjepuiko na 50 243566 7536780 34K L-646 100802 Bn-rk altn that masks text w/ vug white q Okatjepuiko na 50 243566 7536780 34K L-647 100802 Rd-rk altn w/ cc veinlets n stwk Okatjepuiko na 50 243566 7536780 34K L-648 100802 Bn-rk altn w/ Cu stains + goss Okatjepuiko na 50 243566 7536780 34K L-649 100802 Unid f-g rk w/ silicif + FeOx altn Cu sta Okatjepuiko na 50 243566 7536780 34K L-650 100802 Bx of bn-rk altd rk w/ cc veins Okatjepuiko na 51 244142 7537156 34K L-651 100802 Metallic hem Okatjepuiko na 51 244142 7537156 34K L-652 100802 F-g dk volc rk; pervasive FeOx altn Okatjepuiko na 653 349377 7890241 33K L-653 17 101002 Goss schist (Au?) NW of Sesfontein na 654 349377 7890241 33K L-654 17 101002 Goss schist (Au?) NW of Sesfontein na 655 348478 7890333 33K L-655 17 101002 qz from qz blob NW of Sesfontein na 656 348478 7890333 33K L-656 17 101002 Dirty ls cut by qz bxwk w/ sulfs NW of Sesfontein na 657 348478 7890333 33K L-657 17 101002 Dirty ls cut by series of qz veinlets NW of Sesfontein na 658 348478 7890333 33K L-658 17 101002 De-calcified explosive calcarous bx NW of Sesfontein na 659 348478 7890333 33K L-659 17 101002 De-calcified ls w/ FeOx after sulfs NW of Sesfontein na 660 347477 7890212 33K L-660 18 101002 Ls w/ weathered sulfs + qz veinlets NW of Sesfontein na 661 347477 7890212 33K L-661 18 101002 Qz blob w/ sulfide veinlet intersection NW of Sesfontein na 662 340091 7893346 33K L-662 18 101002 Bx w/ pink qz frags cemented by qz NW of Sesfontein na 663 340091 7893346 33K L-663 18 101002 Calc olig bx; concentric bk bands NW of Sesfontein na 664 342717 7892842 33K L-664 19 101002 Arkosic ss. Epupa Complex NW of Sesfontein na 665 342717 7892842 33K L-665 19 101002 Pk qz w/ bk hem xtal NW of Sesfontein na 666 471473 7748315 33K L-666 21 101102 Pan concentrate from loose sand Oas Farm na ID UTMEAST UTMNORTH UTMZONE SAMPLE PAGE DATE ROCK LOCATION ELEVATION 667 471473 7748315 33K L-667 21 101102 Mag concentrate fro loose sand Oas Farm na 668 471439 7748404 33K L-668 21 101102 M-g gtd cut by qz+mag veinlets Oas Farm na 669 471439 7748404 33K L-669 21 101102 Ang hyd. Bx of pk gtd w/ mag+qz Oas Farm na 670 471411 7748527 33K L-670 21 101102 M-g gray-pk gtd +mag+sulfs? Oas Farm na 671 471378 7748582 33K L-671 21 101102 F-g bn gtd +qz+sulfs vts +mag Oas Farm na 672 471378 7748582 33K L-672 21 101102 Vein qz w/ vthin rd FeOx fracs +sulfs Oas Farm na 673 471427 7748620 33K L-673 22 101102 Massive mag from qz+mag+sulfs vein Oas Farm na 674 471427 7748620 33K L-674 22 101102 M-fg pk gtd cut by qz-mag stwk Oas Farm na 675 471427 7748620 33K L-675 22 101102 M-g gtd w/ abund mag clusters +mag vein Oas Farm na 676 471408 7748649 33K L-676 22 101102 Massive mag veinlet +sulfs?, martitized Oas Farm na 677 471435 7748670 33K L-677 22 101102 Qz vein w/ bladed bk hem+sulfs? Oas Farm na 678 471455 7748666 33K L-678 22 101102 M-g pk gtd Oas Farm na 679 471435 7748670 33K L-679 22 101102 Pk gtd w/ bk mag clustes, veined Oas Farm na 680 471425 7748638 33K L-680 23 101102 Gtd w/ abund vfg mag Oas Farm na 681 471435 7748655 33K L-681 23 101102 Massive bx mag vein w/ ang rk frags Oas Farm na 682 471435 7748655 33K L-682 23 101102 F-mg gy-pk gtd w/ mag veinlet Oas Farm na 683 471435 7748655 33K L-683 23 101102 Mg pk-bn gtd cut by //bk mag veinlets Oas Farm na 684 471435 7748655 33K L-684 23 101102 Massive bx mag + sulfs? Oas Farm na 685 471491 7748732 33K L-685 24 101102 Braided network of qz +hem+sulfs? Veins Oas Farm na 686 471491 7748732 33K L-686 24 101102 Braided qz veins w/ hem+sulfs? Au? Oas Farm na 687 471491 7748732 33K L-687 24 101102 Qz vein w/ hem clusters + sulfs? Oas Farm na 688 471503 7748729 33K L-688 24 101102 F-mg bn gtd w/ little qz, magnetic Oas Farm na 689 471503 7748729 33K L-689 24 101102 Qz bx vein w/ bk massive hem layer Oas Farm na 690 471496 7748781 33K L-690 24 101102 Mg gtd w/ mafic min clusters +mag Oas Farm na 691 471519 7748783 33K L-691 25 101102 Vfg bk-dk gn rk, non-mag, dense, dike? Mo Oas Farm na 692 471549 7748814 33K L-692 25 101102 Vfg bk rk w/ abund 0.5mm cubic vugs Oas Farm na 693 471497 7748831 33K L-693 25 101102 Fg gtd, high mag, high qz Oas Farm na 694 471491 7748835 33K L-694 25 101102 Mg gy gtd, ~mag low Qz Oas Farm na 695 471513 7748845 33K L-695 25 101102 Vfg bk rk -mag cut by qz+hem veins Oas Farm na 696 471476 7748965 33K L-696 25 101102 Mfg gtd cut by qz+hem veinlets Oas Farm na 194 471477 7748923 33K L-697 101202 Mg bn-pk gtd cut by mag veins Oas Farm na 201 471494 7748955 33K L-698 101202 Fg bn-gy gtd w/ diss py Oas Farm na 202 471446 7749001 33K L-699 101202 Mg bn gtd w/ mafic min clusters Oas Farm na 203 471438 7749017 33K L-700 101202 Vuggy, gossanous qz vein. Sulfs? Oas Farm na 204 471439 7749022 33K L-701 101202 Bk intrusive w/ fine acicular needles Oas Farm na 205 471442 7749018 33K L-702 101202 Qz druzes + goss vugs in qz veins Oas Farm na 206 471454 7749083 33K L-703 101202 Qz druzes + goss vugs in qz veins Oas Farm na 207 471465 7749111 33K L-704 101202 Sheeted qz+hem veinlets Oas Farm na 471465 7749111 na L-705 Vfg bn intrusive w/ braided qz-hem veins Oas Farm na 471465 7749111 na L-706 Vein of vfg intrusive w/ vugs + goss sulf Oas Farm na 208 471464 7749143 33K L-707 101202 Mg pk gtd cut by ntwk of qz veins Oas Farm na 209 471495 7749231 33K L-708 101202 F-mg dk gn-bk intrusive, -mag, chloritize Oas Farm na 210 471456 7749236 33K L-709 101202 Fg pk intrusive cut by braided qz+chlorit Oas Farm na 211 471435 7749288 33K L-709a 101202 na Oas Farm na 163 471443 7749248 33K L-710 101202 Fg dk gn-gy intrusive cut by qz+hem+sulfs Oas Farm na 163 471443 7749248 33K L-711 101202 Fg fol gtd cut by veins +Au?+sulfs? Oas Farm na 212 471428 7749313 33K L-712 101202 F-mg gold intrusive cut by qz veins Oas Farm na 161 471417 7749439 33K L-713 101203 F-mg gtd w/ smoky qz +sulfs? Oas Farm 1011 159 471419 7749631 33K L-714 101202 Mg pk gtd w/ braided qz+sulfs? Veins Oas Farm na 214 471383 7750213 33K L-715 101202 Pk gneiss > mag Oas Farm na 215 471571 7750360 33K L-716 101202 Pk gneiss -mag Oas Farm na 216 471782 7750569 33K L-717 101202 Milky qz w/ bk joints Oas Farm na 217 472021 7750981 33K L-718 101202 Milky white qz in part s/ sugary texture Oas Farm na 218 472085 7751127 33K L-719 101202 Vfg pk intrusive w/ no mag Lofdal Farm, Field na 223 470685 7753757 33K L-720 101202 Mass mag w/ carb vein + vugs Lofdal Farm, Field na 223 470685 7753757 33K L-721 101202 Vuggy white qz w/ hem blob Lofdal Farm, Field na 224 470677 7753774 33K L-722 101202 F-mg gn carbonatite w/ xenolithic frags Lofdal Farm, Field na 226 470621 7753910 33K L-723 101202 Mikly white qz w/ abund bk joints Lofdal Farm, Field na 227 470613 7753909 33K L-724 101202 M mag, flow bands, sulf? Lofdal Farm, Field na 245 470069 7753148 33K L-744 101202 M-cg pk gtd w/ qz veinlets -mag Lofdal Farm, Field na 246 470072 7753141 33K L-745 101202 Vfg med gy intrusive > mag, internal flow Lofdal Farm, Field na 247 470081 7753115 33K L-746 101202 Carbonatite w/ braided mag veins Lofdal Farm, Field na 252 470091 7753115 33K L-747 101202 Qz w/ rd stain + thin rd-filled joints Lofdal Farm, Field na 220 469619 7752727 33K L-748 101202 Ang bx w/ vuggy surfaces + mag (Au?) Lofdal Farm, Field na 466547 7755980 na L-749 Qz w/ minor lt gn micas in batches Lofdal Farm, Field na 466547 7755980 na L-750 Mnzd samples Lofdal Farm, Field na 466547 7755980 na L-751 Mnzd samples Lofdal Farm, Field na 466547 7755980 na L-752 Mnzd samples Lofdal Farm, Field na 466547 7755980 na L-753 Mnzd samples Lofdal Farm, Field na 278 466549 7755506 33K L-754 101302 Mnzd samples Lofdal Farm, Field na 279 466552 7755496 33K L-755 101302 Bk material w/ f vugs, braided qz veins Lofdal Farm, Field na ID UTMEAST UTMNORTH UTMZONE SAMPLE PAGE DATE ROCK LOCATION ELEVATION 279 466552 7755496 33K L-756 101302 Qz + hem cut by braided bk hem veinelst, Mesopotamie Farm na 279 466552 7755496 33K L-757 101302 Qz from Qz blob Mesopotamie Farm na 312 439148 7765096 33K L-758 101302 White, gossanous, graphic granite Mesopotamie Farm na 327 438940 7765078 33K L-759 101302 Pegmatitic intrusive w/ graphic texture Mesopotamie Farm na 328 439572 7764296 33K L-760 101302 Crushed ore grade material, Cu Valley min Mesopotamie Farm na 328 439572 7764296 33K L-761 101302 Finely crushed material, Cu Valley mine Mesopotamie Farm na 328 439572 7764296 33K L-762 101302 Finely crushed material, Cu Valley mine Mesopotamie Farm na 328 439572 7764296 33K L-763 101302 Mnzd rk w/ gossan + hem Cu Mesopotamie Farm na 328 439572 7764296 33K L-764 101302 Qz vein w/ hem ntwk +sulfs Mesopotamie Farm na 328 439572 7764296 33K L-765 101302 Milky white qz q/ ntwk of bk hem + sulfs Mesopotamie Farm na 328 439572 7764296 33K L-766 101302 Qz q/ FeOx veinelts, hem blobs + sulfs Mesopotamie Farm na 328 439572 7764296 33K L-767 101302 Bx w/ qz, ang hem, martite, Cu carbs Mesopotamie Farm na 328 439572 7764296 33K L-768 101302 Qz-bk hem -Cu carbs, vugs after sulfs Mesopotamie Farm na 328 439572 7764296 33K L-769 101302 Qz=hem vein w/ abund vugs after sulfs Mesopotamie Farm na 328 439572 7764296 33K L-770 101302 Qz vein w/ FeOx ntwk, hem blobs +vugs Mesopotamie Farm na 328 439572 7764296 33K L-771 101302 Qz vein w/ rk frags and bxwk after sulfs Mesopotamie Farm na 439579 7764129 na L-772 Lt gy-white graphic granite Mesopotamie Farm 703 439579 7764129 na L-773 Pegmatitic intrusive w/ graphic texture Mesopotamie Farm na 328 439572 7764296 33K L-774 101302 Vuggy qz vein w/ dusty chalcocite + Cu ca Mesopotamie Farm na 328 439572 7764296 33K L-775 101302 Qz vein w/ chacocite + Cu carbs Mesopotamie Farm na 328 439572 7764296 33K L-776 101302 Qz w/ fine hem veinlets, goss vugs, Cu ca Mesopotamie Farm na 328 439572 7764296 33K L-777 101302 Qz + stwk of hem veinlets, grades to bx Mesopotamie Farm na 328 439572 7764296 33K L-778 101302 Gossans of different types Mesopotamie Farm na 284 443718 7762833 33K L-779 101302 Intensely fractured fol gtd Mesopotamie Farm na 330 445478 7763678 33K L-780 101402 Mass white qz from blob Mesopotamie Farm na 330 445478 7763678 33K L-781 101402 Mass qz w/ vthin hem veinlets Mesopotamie Farm na 337 445963 7766384 33K L-782 101402 Mass qz vein, no FeOx, vugs after sulfs Mesopotamie Farm na 337 445963 7766384 33K L-783 101402 Gneiss Mesopotamie Farm na 339 543938 7762661 33K L-784 101502 Coarse augen gneiss Volcanics na 340 536655 7734183 33K L-785 101502 Calcareous turbidite Volcanics na 342 531468 7735504 33K L-786 101602 Lt bn slightly foliated volc rk Volcanics na 342 531468 7735504 33K L-787 101602 Volc rk w/ vugs - gossanous texture Volcanics na 342 531468 7735504 33K L-788 101602 slightly fol volc rk w/ vugs -gossanous Volcanics na 343 531284 7735131 33K L-789 101602 Slightly mag, porph. Subvolc. Intrusive Sumas Mountains na 343 531284 7735131 33K L-790 101602 Fg bn-rd crystalline rk, cpy specks Sumas Mountains na 344 531251 7735039 33K L-791 101602 Fg laminated pk volc rk (ash?) Sumas Mountains na 343 531284 7735131 33K L-792 101602 Magnetic foliated subvolcanic rk Sumas Mountains na 355 495836 7693248 33K L-793 101602 Cg pk granitoid + mag inclusions Ugab River na 356 495856 7693220 33K L-794 101602 Pk gtd w/ slight foliation Ugab River na 358 496026 7693138 33K L-795 101602 Porphyritic gy intrusive w/ mafic cluster Ugab River na 360 496058 7693188 33K L-796 101602 Pk gtd w/ red qz clustes - mag Ugab River na 353 489966 7699063 33K L-797 101602 Mg pk gtd w/ red qz + pk felds Ugab River na 352 488901 7700138 33K L-798 101602 F-mg gy ftd Ugab River na 351 485783 7702912 33K L-799 101602 Bn porphyritic rk w. yellow qz, 50 cm diamete r in some cases) and inclus i on s of green and black schisto s e rocks. It may be a breccia zone fill ed with quartz . No sulfides or iron oxides of any type were found. The last zone, located between 19 ?52.5?S and 19 ? 51.8?S was thought to be the continua tion of a main region a l minera l iz e d frac tur e zone, as seen on Fig 4.2.1.6. That fracture is the same that has the copper sulfide dissemi na t i o n s and abundant vugs after sulfidation. S-146 L-1001: Quartz with schistose black/gr een rock with abundant vugs. S-147. Foliated, coarse-grained gr anitoids from the local basement. S-148. Outcrop on a box cut for road. L-1002 : Intensely-frac tured and quartz-veined massif of medium- g r a i ne d , pink, metalu m in o us leucoc r a t ic sodic to potass ic ferrifer ous alkali granite with biotite and amphibole . Very altered and possibly hydrothermally altered. The sample is the freshe st rock available. S-149. L-1003 : Slightly foliated, coarse-grained , metaluminous subleuc oc r a t ic sodic ferrif e r o u s quar tz latite from the basement . This rock correla t e s very well with the group of quartz mon z on i t e s . S-150. Large hill with outcrop on the road. Myarolitic cavi ties are visible in a large extensio n of the outcrop . Fine-g r a in e d subvolc an i c granit o i d ( L-1004 ). S-151. The rock of L-1004 is cutting through the brow n, foliated, coar se - g r a in ed porphy r i t ic granit o id that was seen on the Guab River. Maybe it is the same granit oid that was seen there too. It still has the angular myarolitic cavities and oc assionally grades into a breccia. 1 9 9 APPENDIX A66 FIELD NOTES ON THE N-S TRANSECT THROUGH THE OAS FARM, NAMIBIA From WPT 176 to WPT 175 there is abundant mag netite in the sand that covers the ground. On WPT 174, L-666 pan concentr a t e of magnetit e from the sand, to look for metals. L-667 is anoth er sample of magnetic substances collected with a strong hand magnet. L-668 . Reasonably fres h, brow n, medium-grained , metalumi n ou s mesocra t i c sodic ferrifer ou s syenite , with 2 feldpar s and low quartz conten t . The rock has small clus ters of biotite, amphibole and magnetite. The dominan t minerals are pink potassic feldspa r and light gray, transpa r en t plagioc la s e . The rock is cut by a 1.5cm wide quartz +magne tite veinlet that is more magnetic than rest of the rock; it is accompan ied by a stockwo r k of 1-3mm similar magneti t e - r ic h veinlets. There were no apparent sulfides. This sample was colle c t ed from a series of dense vein s of a darker intrus iv e material around a pink , coarse- g r a i ne d granito i d (See Fig photos ) . L-669 . Angular (hydrothermal?) breccia of pink, medium-g r a i ne d , metalumi no us mesocrat i c sodic ferrifer o u s syenite, cemented by a black quartz+magnet ite (mafic-rich) intrusive material . The rock is not very fresh. It was intersected by later 1mm veinlet network that does not carry sulfides. Another portion of the sample shows round clas t brecc i a and angul ar brecc ia cemen t e d by quartz+magnetite (dark-blac k) material. The rock was later over prin t e d by a network of fine black veinlet s filled by quartz+magnetite. A portion has a boxwork of magnetite blades with dark-colo red quartz in the middle. This intens ely - f r a c t ur e d and re-cemen te d pink coarse- to medium- g ra in ed granito id seems to mak e mos t of the rock in the massif. The massif has approximately 150 me ters in diameter , it is located to the east of WPT 172, and makes a rock outcrop along the road (Fig 4.2.2.1 ) . WPT 177, L-670 . Fresh, medium-grained, light gray to pink , metalumino us mesocratic sodic ferriferous nepheli n e syenite with clus ter s of light green (epidote and/ or chlorit i z e d biotite ) + m a g netite+biotite. Some very long pink plagio c la s e blades (Potas s i um feldspa r ?) 2- 3c m. Might have containe d small sulfide s , now oxidized . It comes from the massif of body E. The rock is a high-hea t producin g syenite . WPT 178, L-671 . Fine-grained, red- brow n intrus ive rock with su lfid e s (may have ?brow n- r ock? alteration). It is cut by a 1-1.5c m quartz veinlet with sulfides (now angul ar vugs +gos sans ) and magnetite. It also contains very brittle minerals with silvery, metallic lu ster (sulfide or sulfosalt) that couldn? t be identified. The sulfide is hard to scratc h ; the scratc h is not red, yellow, black or white in color. Thin, 1mm th ick quartz veinlet s radiate out of the 1.5cm quartz vein. L-672 . Quar tz from a vein with very thin, non-orien ted, red iron oxide- filled joints and angular vugs after sulfid es ; some vugs are gossano us . The vein cuts thro ugh a fine-grai n ed red, sulfide- b ea r i ng intrusiv e rock. The sample was collec t ed for fluid inclus i o n studies . By WPT 171 the abundanc e of ferroma gn e s ia ns in the rock increas es . Amphib ol e s and magnet i t e make 0.5 cm to 0.7 cm diameter clusters. The rock is spotted and looks like t he skin of a dalmati a n . WPT 179. Massive magnetite fr agments , such as that of L-673 begin to appear. Massive magnetite from a quartz +ma gne t i t e vein. The magnetit e contains some gos sano us vugs where sulfide s might have previous ly resided . Part of the quartz has a da rk gray to almost black color. WPT 179, L-674 . Medium- to fine-grained pink granitoid intersec ted by stockwork of quartz +magne tite veinlets; some 1cm, most a few mm wide. It contained di sseminated very small (<1mm) sulfides that now are leached . It also has dissemi n a t e d cluste r s of mafic minerals includ ing magnetite. L-675 . Medium - gr a i ne d , peralu m i n ou s , subleuc oc r a t i c s odic ferriferous syenite with a ?black-white? dot texture. Abundant magnetite clusters conform ?black ? and plagioc l as es + q u ar t z + m u scovite make the rest = ?white? . This rock is similar to others seen at WPT 171. Ther e may be some type of iron oxide flooding that altered a previou s rock, replacin g all the mafics: biotite , amphi b o le , etc. The rock has a small, more felsic dike with flow textures that is also partially replac ed by magnetite. A magnetite vein cu ts across the sample and carried sulfide s , now represen t e d by gossano us vugs. Thin magnetite veinlets branch from the magnetite veinlet. This rock is a very hi gh heat producer due to high Th. 2 0 0 WPT 183. L-676 . Metaluminous mesoc ratic sodic ferriferous sy enite. It contains a large mass of partly martitized magnetite from ~10c m wide veinlet with some vugs that might have been sulfides or other minerals immersed into the magnetite. The vein seems displays flow texture or banding . Note the abundant angular vugs and boxwork textures in the photo. From WPT 171 to WPT 170 to the we st, small hill of granitoid rocks. WPT 180, 947m (highest point). L-677 . Fragment of quartz vein with hematite in 2mm thick blades and very abundan t vugs after sulfides . The sample is hosted by deeply hematit i z e d , red intrusi v e rock. It was collecte d to slab and look at the iron oxide mi neralization; it could also be used to carry out fluid inclus ion studies. Two of the veins interse c t . Ther e is iron oxide + minerali z a t i o n at the intersec t i o n . The massive iron oxide vein system was orient ed 110/72 ? N. Th is was measured using the magnetic needle of a Brunton compass set to 0?; it should be correc te d for magnetic declinat i o n a nd for error due to nearby magnetic ironston es . Veins have an irregu la r texture, they norma lly are 4-12 cm wide but may open up to 40 cm, and were also oriente d in many other directions. No clear quartz veins are visible. WPT 181, 948m. * L-678 *. Fresh, medium-grained, pink-black granitoid with twinned plagioc lase (or nepheli n e ?) elonga t ed phenoc r y s t a ls in t abula r shapes . Some of the blades are 3-4c m long and 4-5mm thick. The rock has clus ter s of mafic minerals with magneti t e, and is intersec ted by diffuse 0.5c m thick magnetite- rich veinlets . It represents the whole hill. The sample ha s a xenolith of a finer-grained, pink rock without the plagioc l as e blades. WPT 180, L-679 . Pink granitoid with black accumula tions of mafic minerals including magnetite. It is cut by two dark quartz+ ma g n e t i t e paralle l veins, oriented as measured on WPT 180. Indicated with blue marker. The veins seem to have carried sulfides . Photo of the fracturing style with N and scale, taken 1 m away from WPT 181. There is a diagram (page 23 of field notebook ) of the main rock relatio n s h ip s . See photo on WPT 182, 943m. Relatio ns h i ps of L-678 , L-681 , and L-680 are indicated on the diagram. Black, lens oid veinlets cut the other granitoids almost perpendicula rly. L-680 . Fragmen t of a quartz+f e l dp a r rock with abundan t ve ry fine-gr a i ne d , black ma gnetite. It comes from a vein. L-681 . Massive black magnetit e vein with angular fragment s of host pink rock ( L-678 ) in a breccia fashion . The rock has flow foliation. Its fragments are elongat e d and show slight imbric a t i o n . A dense network of magnetit e veinlets was seen nearby. The host rock is a pink medium to fine-grained granitoid with very little observa b le texture that seems to grade from L-678. The vein?s width varies from 1 to 5cm in the hand sample . Some very vuggy textures with bl ack- d a r k brown gossano us surfac es after sulfide s . The gossano us vugs occur both on the pink host rock and black vein. 2 0 1 L-682 . Grab sample s of a fine- to medium- gr a i ne d , light gray to pink granito i d ( L-678 ) intersec t e d by a 0.7- 1.5cm magnetite-rich black veinlet with minor quartz. Fine black veinlets <1mm radiate from the main black vein. The hos t rock has some clus ters of mafic miner als , most with iron oxide (earthy goethite ) on outer surfac e . L-683 . Medium-grained , pink-brown granitoid (lik e L-678 ) with bladed twinned plagioc lases. It is intersected by series of sub-pa rallel very fine (<1mm) black magnetit e-rich veinlets+sulfide s that accoun t for a thic kness of 4cm. The outcrop showed a 3 cm black vein with intern a l subpa r a l l e l banding and many gossan o us vugs. The sample might carry free gold and needs to be assaye d . Gossan o us vugs are also pres ent in the pink host rock. Disseminated magnetite is also pr esent in the pink rock. L-684 . Massive magnetit e with angular breccioi d fragment s. Probably derived from vein. Continuous, very large vugs and abundant small vugs with gossanous textures after leached sulfides . All of the previous samples come from the ?hill?. Its perimeter was walk ed and recorded with the GPS to note its map outcro p and surface . WP TS A to I (Fig 4.2.2.1). WPT 170. Coarse ?dalmatian? rock and fine-gr ained pink intrus ive with stockwor k of magneti t e fractur es . WPT 184, 950m. Quartz veins with hematite and vugs after sulfides begin to appear. L-685 has the intersection of several such veins. It is a large sample of braided network of approximately 1c m wide quartz + h e mati t e + s u l f i de veins. The host rock seems to be a fine-gr a i ne d volcan ic rock (or dike?) . It has abundant little dips like pin pricks on a weathered surface, after weathe red disseminated sulfides. L-686 was collec te d from same site; L-687 from approximately 10 m to the east. The host rock is a fine-grained granito id. L-686 . Braided , 6-7 cm wide quartz veins with hemati t e and very abunda n t , open gossan o us vugs hosted in what seems to be a very fine-gr a in e d volcan i c rock. The sample might contain free gold if the rock ever did. Nothing in the sample is magnetic . L-687 . Quar tz vein with large clusters of hematite and associa t ed angular vugs after sulfide s . Hosted by a fine-gr ained, and intens ely brown-altered, gossano us rock. WPT 185, 971m. L-688 . Fresh, brow n-colored fine- to medium-grained granitoid with little visible quartz. It is a slightly magne tic rock cut by a 0.5mm quartz-magne tite veinlet. Fres h sample s were hard to find due to intense frac tur i n g and weather i n g . This rock was dated by SHRIMP at 762?12 Ma. Structural relation ships indicate that the rock is older than L-689 . L-689 . Quartz vein with a black, 2-3cm tabular interlay er of massive hematite. The vein contains mineral inclus i on s of minera l s , angula r rock fragme n t s and ma ybe fluid inclus ions. It has coarse angular vugs and gossans. Part of the sample is a quartz vein with less hematite, very thin red and black joints, and vuggy texture on one surfac e . WPT 186, 967m. 2 photos (ED 10120005.jpg) of ve ry thin 1.2 mm hematite with the veinlets ( L-690 ) on a wet surfac e. Less dense frac ture pattern and thinne r veinlets . The main vein orientation is 070/69? N. There are other minor sets. L-690 Relatively fresh, medium-grained intrus ive rock with clus ter s of mafic minerals+ m a gn e t i t e , that is cut by a 0.5mm magnetite veinlet. WPT 187, 965m. L-691 . Small (~1m wide) non-porph yritic, very dens e, black to dark green, very fine-gr a in e d , metalum i no us sodic ferrife r o us monzon i t i c dike that runs E-W. It contain s high copper values and was identifi e d in the field as a fine-gr ain e d g abbroid with none to very low magnetism. By WPT 168 to the W there is another intrus i v e body that makes a smal l hill. Abundant massive hematite and magnetite fragments and black veinlets cutting the coarse intrus ive rocks. L-692 . Very fine-gr a in e d black rock with abundan t angular (mos tly cubic) vugs 0.5-0.8 m m ? unifor mily spread out. It is a 3-D silica rock, with white scratc h mark and conc ho idal fracture. It is intersec ted by some 0.5mm hematite veinlets and one 3mm quartz+hematite veinlet. The origin of the rock is unknown . It could be a subvolcan i c sulfide - r i c h dike, a fine-gra in e d nepheli ne syeni te, or a leached carbonatite. In the field, it was thought to be a ?porou s? hematite (after sulfides ?) but t hat turned out to be wrong. The rock displa y s textur e s similar to angular breccias and contains very high silica. 2 0 2 WPT 188, 998m. Photograph of a subvol c an i c rock (or somet h i ng that l ooks like it) that intersec ts the main granitoid body and has a contac t breccia. Several sub-pa ra l l e l dikes, L-693* . Fres h, fine-grained, medium gray, metaluminus mesocratic sodic ferriferous, biotit e - r ic h , non-ca lc ar e o us alkali granit e , with strong magnetic content (very fine magnetit e , not seen with bar e eye) and high silica. It has no other particu l a r macros co p ic features . This rock was dated by SHRIMP at 765?4.5 Ma. Structur al relationship s indicate tha t the rock is younger than L-688* . WPT 189, 996m. Site of same dark subvolcanic intrusive as L-693* , with xenoliths and flow textures, located on the hilltop . The strike of the subvert ic a l rock is N70? E. It is 25-30 cm wide. The dike is finer-g r a in e d on the margin s . WPT 190, 982m. L-694 . Fresh, medium-grained, medium-gray, slightly magnetic , metaluminous sodic ferriferous nepheline syenite with low quartz content, clusters of mafic minerals and minor magnetite. The entire hill is made of this material. WPT 191, 991m. Highest elevation of small hill 2. 15 to 10 cm wide black dike or iented 077/69?N that cuts across the coarse granitoid (same as L-694 ). L-695 : very fine-grained, black, me talumi n ou s sodic ferrifer ou s nepheli n e syenite with no magneti c signatu r e , inters ected by at leas t 2 families of very thin <<1mm quartz +hematite veinlets. It has some minor open vugs t hat on fresh surfac e seem to corres po n d with red hematite small clusters in 3-D. The rock matrix scra tches white. See diagram of the hills on pg 25 of field notebook. WPT 192, 979m. Locate d on top of the third, smaller hill and granitoid outcrop. Same rock type and orienta t i on of dikes as on hill 2 = 69/80?N. After WPT 167, going up, we begin to see yet another h ill composed of intrus ive rocks. Maybe it is another intrusive pipe of a system. At WPT 193, 975m is t he base of this new hill. The road turns around it. WPT 194, 982m. L-697 : Fres h, represen tative medium-grained , light brown to pink, metaluminous sodic ferrife r o us syenite with clus ter s of mafic minerals+ he m atite, cut by network of magnet i t e- r ic h dark gray to black granitoid veins 0.6-0.8cm wide. The rock is a high-heat producer due to its high Th content. WPT 195, 977m. The hill of body B is surrounded by quartz veins. L-696 . 5mm quartz veinlet that intersects medium- to fine-gr a in e d syenit o i d rock, as in the othe r hills. Also cut by 1mm hematite+quartz veinlets . The sample was slabbed to see textures better. Also photo of breccia vein/dike with hematite and angular fragments . WPTS 196, 988m, 197, 980m, 198, 978m, 199, 978m, 200, 987m, and 201, 994m close the perime t e r around the base of the hill. There is a similar hill fu rther east that was not studied in great detail. Photo taken towards the S from WPT 201 of the three hills and intr usiv es of p. 25, taken towards the N. Note general geomorpho l o g y of the small intr us iv e bodies. WPT 201. Black to dark gray dike, 15 cm wide and ori ente d 150/90 ? that interse c t s other dikes 40 cm wide. L- 698 . Fres h, fine-gr ained light brown-gray metaluminous s odic ferriferous alkali granite with disseminated py clus ters in very fine nuclei. Slightly foliated in the same orientat i on as the host rock. Need to slab to describe better. WPT 202, 985m. L-699 . Medium-grained, brown, metaluminous sodic ferriferou s syenite with clusters of dark gray quartz +magnetite (and also transparen t quartz). Sli ghtly magnetic, medium color index. It was difficult to find a fresh sample of this rock. It is a high heat prod uci ng syenite due to high Th content . The sample comes from a very large ring complex (body H) with the same co mposition. The same rock is host to bodies bodies A, B and C. WPT 203, 990m. L-700 . Very vuggy, gossanous quartz vein that contained sulfides. WPT 204, 977m. L-701 . Massive, very fresh, black, non-magnetic intrusive with extremely fine needles of acic ular crysta ls in all directions (lik e rutile) that make 10-12 cm veins. Some of the vugs contain quartz druz es . The origin of the vugs is uncerta i n ; could be miarolitic cavities or amygdules . Some of the vugs have gossano us texture s . Ther e are many sim ilar bodies of rock lying around. WPT 205, 981m. L-702 . Large sampl e to slab. Quartz druz es and quartz veins 10-15 cm wide with gossano u s vugs. This sample might have carried sulfides and gold. Collected to be slabbed and assayed. 2 0 3 WPT 206, 988m. L-703 . Large sample to slab, same as previous sample. Red rock alterati o n was obs erved on both sides of the road, up to WPT 165. After WPT 165 to the west, outcrop s of calcar eo us schis ts with many red veinlets and red rock iron oxide alteration. Any carbonate rock like this makes a good host for mineralization. WPT 207, 992m. Sheeted, subparallel, 1mm quartz + hemati te veinlet s in fine-gr a i n ed igneous rock that is hard to identify ( L-704 ) . There is at least one other perpendic u l a r family of joints with black iron oxide minerals. WPT 208, 993m. Very fine-grained intrus ive rock (ori ginally mis-identified as a quartz ite) with abundant iron oxide veining stoc kwor k and main system of sheeted veins. L-705 and L-706 were collected there. L-705 is a brow n very fine-gr a in e d intrusi v e rock with thin , braided quartz black hematite (?) veinlets. L-706 is a 6cm vein (dike?) filled by very fine-grained green intrusive ma terial. It contains massive hematite, rounded vugs and gossano us texture s . Both of these samples might carry economic metal mineral i z a t i o n and they should be assayed . The same kind of veining occurs in seve ral types of rocks on the way up the road. Red rock alterat i o n also continu es along the route. WPT 208, 986m. Very ?dirty? dark gray quartz vein collected for fluid inclusio n studies . L-707 Pink, medium- grained, granitoid intersected by dense re ticle of quartz veins in all directio ns . WPT 164. Red rock alteration in foliated quartz ites. WPT 209, 994m. L-708 . Dark green-black, fine- to medium-g rained, non-magnetic , metaluminous sodic ferriferous pyroxenite. It contains some disseminated sulfides . The surface is st rongly covered by gossans and weathers orange. It also contains some carbonates. It is chloritized. WPT 210, 1010m. Fine-gr a i n e d intrusi ve rock. (same as L-705 ) L-709 . Fine-grained pink intrusive rock cut by a series of sub-pa r a l l e l and braid e d , 1mm quart z + chlori te veinlets. At least seven veinlets identified on sample ; one is 3-5mm wide. The sample has red-rock alterati o n . It was marked in blue to slab and carry out petrogr ap h ic studies . WPT 163. Some massive iron oxide rocks and vuggy quartz veins, as well as extensive iron oxide alteration. Lots of gossan on some surfac es ; see L-710 . Collect e d to slab and observe the source of gossan. Dark green-gr a y , fine-gr a in e d , non-magne t i c intrusive intersec ted by multiple s ub-parallel 1-2mm veinlets of quar tz + hematite + vugs that probably carried sulfides . W eath e r e d surfa c es show abund ant irregu lar vugs and gossanous textures. The rock reac ts with HCl; it might be a carbonatite dike. Abundant gossanou s surfaces on the way up. Iron oxide alteratio n in all rocks. L-711 . Fine-gra i n ed , foliated , dark granitoi d (gabbroid? ) with networ k of braided quartz +ear thy goethite (red- orange) <<1mm veinlets. Stockwor k texture. Most vein let s open to show crusty hematit e - du s t y red hematit e and gossanou s textures . The sample might carry free gold. WPT 211, 1021m. Vuggy, white rock with gossan and dusty limonite. This rock should be assayed for gold and base metals. It is macroscopically very similar to L-709 . WPT 212, 1005m. Some gneissos e textures (granulites?) with q uartz in veinlets. L-712 . Non-magnetic , fine- to medium- g r a i n e d , foliated , peralum i no u s leucocr a tic so dic ferrife r o us alkali granite cut by 1cm thick, white quartz veinlets . Maybe the ?foliation? is due to very clos e quartz braided veining in a non-folia t e d granito i d . WPT 162. Many very thin quartz veinle ts (2-5 cm wi de) and persis t e n t red iron oxide surfac es . The veins might have contained sulfides. Ther e are no evident fresh sulfides . WPT 161. L-713 . Fine- to medium-grained, brown to dark gray , non-magnetic , metalumino us sodic ferriferous quartz syenite, with abundant gray smoky quartz. the rock might have carried some sulfides , now oxidized . It contains 1 cm-diame ter plagioc lase phenocrystals with ghos t borders and general fuzzy texture. This rock probably is intensely hydrothermally altered. From here onward, less iron oxide on the rock surfac es. Less gossanous textures. Migmatitic rocks ~ foliated. WPT 160. Brown, coarse-g rained intrusive rock. 2 0 4 WPT 159. Fine grained, brown, pera luminous sodic ferriferous , biotite alkali granite. Ten meters after that, L- 714 : foliated, medium- to coarse-grained , pink, metalu mi n o us leucoc r a t i c sodic magnes i an granit e with series of sub-parallel, black, braided very thin <<1mm veinle ts of quartz+sulfi d es that are now gossa no us vugs and coar se quartz elonga t e d crys ta l s . Severa l orient a t io n s of intersecting fractures. Some with minor black hematite. After WPT 159, red rock alteration increases once more. Up to WPT 158, foliated intrusive rocks (?). Similar br own, fine-grained intrus ives with very thin, <1mm quartz veinlets. WPT 157. Red-roc k and brow n-r oc k alterat i o n persis t s . Pink granitoids with some minor foliation planes and minor dark fac ies . WPT 156. Abundant subpar allel 1 cm quartz veining. WPT 155. Red rock alteration persis ts. Some strong l y - b a nd e d cement e d rocks. ~ submil l im e t r i c black and white banding . Brown rock. Red color does not continu e further . No co arse quar tz veins. No gossan s . Ocassio n a l dark-g r e en to black gabbr os. WPT 154. Foliated, banded, black-pink granitoids. After sedimentar y rocks? WPT 213, 1044m. Gossanous rocks wi th quartz veinle ts; red rocks. WPT 153. Banded intrusive rocks (gneissos e ) . With black iron oxide banding. WPT 153. Outcrop s of hematit e pods. There are some quartz vuggy veins with massive black hematite and gossans; probably after sulfides . Red rock alterati on is abundant . Some of the red granitoi ds have subparal l e l black hematite veinlets. Banded black and white igneous (?) rocks along the way. No hills or evidence of granite plugs. WPT 214, 1046m. L-715 : Very magnetic sample of black and white, foliated, metaluminous mesocratic sodic- p o t a s s ic ferrife r o us biotite granite . G neiss- l i k e texture with black bands of biotite + magnetite + quartz. Seems to have a metamorphic segr egation origin. The main rock is a pink coar se-grain ed granitoid . WPT 152. Some quartz float. Black and white dike 25-30 cm wide, 18m after fence. Banded intr us i v e rocks. WPT 150. Same as befor e. Quartz float and red-roc k altera t i o n . Some gossan o us rocks. WPT 149. Some black, foliated dikes. WPT 215, 1043m. L-716* . Fres h, gneiss ic brow n to pink /b l ac k , fine-gr a in e d , metalu m in ou s subleuc oc r a t ic sodic ferriferous biotite granite with evident rock foli atio n . Pink potassiu m feldspar + quartz + biotite + no apprecia b l e magnetit e . Very strongly ox idized, with gossanous surfaces and no visible sulfides. The rock is similar to others seen befor e . There is some quartz float lying around. L-716* was dated by SHRIMP at 745?5 Ma. WPT 148. Quartz float is abundant and rocks have brown- rock alteration. Foliated granitoi d s . Dark green ?porous ? gabbros with red oxidati o n . WPT 147. Very abundant quartz float. No good outcrops available. WPT 146. Coarse quartz float and gabbros. Red iron oxide on most rock surfaces . 2 0 5 WPT 216, 1028m. L-717 . Abundant quartz float is presen t in the en virons . Quartz milky fragments, some with joints filled by black materia l . They were collect e d for fluid inclusion work. Maybe the fluid inclus ions in the quartz can be used as an explora t i o n tool for iron oxid e-c o p pe r - g o ld (or other ty pes?) of mineralization. WPT 145. Some gabbro (green) fragmen t s are pres en t in the enviro n s . No in situ out cro p . Only angula r gravel terraces. Minor iron oxide in coar se, angular gravel. Relatively flat topograph y. WPT 143. Not much outcrop . Some dark green dikes. WPT 217, 1029m. Abundan t coar se quartz float. L-718 . Milky white quartz in part with coar se ?sugar y? texture is found on the ground. Collect e d for fluid incl us ion work. No true outcrops along the way. WPT 142. Abundant quartz float. WPT 218, 1036m. Fine-grained pink intr usives . L-719 . S160 (See on Fig M21). All the way up to here from t he main road from Khorixas there is a lot of coarse quartz with gossano us vugs. S161. Outcrop of fine-gr a in e d schists after volcanic rocks , with some plagiocla s e porphyroc l as t s . Abundant quartz with gossanous vugs lies on the ground. There might be some sort of epitherma l mineraliz a t i o n , there is no more time available for evaluation. The road is rough for a 4WD vehicl e . Good outcrops on the hills. They are easy to traverse and have very little vegetation. Flat plateaus full of quartz. Photos with abundant quartz. S162. Photo with hammer and Welw itschia for scale. Another photo with car for scale in a flat flateau that is 100% made of quartz from quartz pod. S163. Extremely iron oxide-rich fracture (?) in shales or volcan ic rocks. Outcrop along a dry creek bed. S164, 807m. Entrance to road to Oas farm from the ma in road. Hand sample for example of stockwor k in brittl e quartz i te s L-1047. S165. Very abundan t quartz with gossanou s vugs . Also abundant rocks such as L-1047 with many intersec ting quartz veins . S166. Brown rock alteration and abundan t quartz veins with gossanous vugs . S167. Abundan t calc ret e covers rock s. Some quartz is still visible. S168, 876m. Entrance to Oas farm. Calcrete and brow n rock alteration. S169. Quartz and brown-rock altered, fine-gr ained rock make all the ground. Maybe the quartz is evidence of silicific ation ~ veining. S170, 889m. Outcrop of strange rock ( L-1016 ) that after microscopic analys is turned out to be a quar tzite. Glassy, very fine-gr ained with subparallel vugs, such as vesicular lava would have, intersec t e d by abundan t network of quartz veins. The surfac e colo r is brow n; ins ide its color is white or light gray. Very fresh; it gives a bell tinge when struck by the hammer. L-1047 is from that same type of rock . Photo (photo 03080007) with pencil of sub-pa rallel vugs and stockwor k of of quartz veins. L-1015 for chemic al analysis . Much of the quartz in veins of the brown-su rfac e rock has vuggy textures, after sulfides. Photo (photo 0308000 8) with hamme r that shows aspects of the quartz stoc kwork in brown-white rock. Veins with abundant iron oxide and vugs after sulfides. L-1017 . 2 0 6 S171. L-1018 . Magnetite from sand found in the active bed of a dry creek. Several sample s of subvolcanic intrus io ns were observ e d along the creek. S172. Another dry creek with subvolc a n ic intrus i v e s along it. S173, 199m. Sand-covered flat savannah with abundant magnetit e clas ts concentr a t e d along drainage . S174. L-1019 . Foliated, fine-gr ained, metaluminous, subleuco c r a t i c sodic alkali granit e with pyroxe n e and amphibo le. Its chemical compos ition is similar to L-1021 . Goats withou t earing s were observ e d on the site. The ?earings ? are spec ial appendic e s that hang from the goat?s neck when they feed on soils with high arseni c conten t. S175. Farm house. L-1020. Foliate d , metalum i n o us mesocra t i c sodic amphibol e- r i c h granite with high sodium and copper contents. S176. Many quartz veins that cut gneissic, meta lum in o us subleuc o c r a t i c sodic biotit e granit e L-1021 . S177, 993m. Sulbvolcan ic porphyritic, peraluminou s me socra t i c sodic-p o t as s ic fe rrife r o us nepheli n e syenite dike that runs @ 070? strike 2 m wide, cuts road. L-1022 . It is very similar in composition to L-161 . L-716* was conside r e d to be a repr es en t a t i v e sample of t he ?basement? to the syenite intrus ions of the Oas farm, but it tu rned out to be much younger. A definitive age for this sample is not yet completely interpreted. Neverthe l es s , several xenoc rys t i c zircons with an age of 1692 Ma were found. 2 0 7 APPENDIX A67 FIELD NOTES FROM THE LOFDAL FARM, NAMIBIA WPT 220, 1022m. Large outcrop of gos sanous, strong ly magnetic, silicified , angular clast, polymictic hydrother m a l breccia. Some of the clasts have diameter greater than 20 cm. L-719 . Fres h, very fine-grained pink granitoid, with no magnetite. WPT 223, 973m. Large fragments of magnetite that is turnin g into hematite (martite). L-720 . The outcrop is located in front of a house. Massive magnetite with in terna l layerin g is intersec t e d by a white carbona t e veinlet. All surfaces are strongly altered and full of vugs. L-721 . Small quartz fragments with coar se magnetite/hematit e clus ters inside . Pebble of vuggy white quartz, with round nugget of enclosed hematite. This is the surface expres sion of a quartz pod. WPT 224, 972m. L-722 . Brown, fine- to medium-grained, massive intrusi v e carbona t e rock. It has white calc ite veinlets, inclus ions of black magnetite and xenoliths of some silice o us , igneous - l oo k in g rocks. All consti tu e n t minera l s seen are brow n-c o l o r ed carbona t e s and abunda n t r ed, dusty hematit e . Nothing else is visible , except for magnetite. See photo on Fig 4.4. 2.18. The rock is a carbonatite. The environs contain abundan t black m agnetite-hematite ~1mm wide veinlets in a brow n carbona t i t e , just as sampled above. There is abundant float of anker ite and iron oxide gossans. WPT 225, 1980m. Many piled fragments of unidentified co arse white micas, pink plagioc lase, quartz and light green miner al s that cannot be recogn iz e d in what seem to be pegmati t e s . These minerals were mined for their rare earth conten t . WPT 226, 985m. Up to here, abundant quartz float. L-723 . Milky white quartz with abundant very thin <<1mm black iron oxide veinlets . The sample was taken for fluid inclus io n s studies . It may be part of a mineraliz ed syste m . L-724 . Milky, white quartz intersec ted by a dense se t of braided, 0.1 ? 3mm, somewhat hematitized magnetite veinlets, with very porous vuggy textures and gossan ous vugs. Thes e probably were sites of old sulfides. Collected to slab and make thin/opaque section. WPT 227, 986m. Coar se white body of quartz with sheeted hematite veins that may carry gold. WPT 228, 987m. Coarse crystals of tan-pink plagioclase. L-725 . Very coarse (10c m ?) , single plagiocla s e crys tal with coarse quartz inclus ions. Part of a pegmatite. Some float of quartz veins with dissemi n a t e d ?dalmat i a n ? hematit e spots 3-6mm diamete r . Veins are 5 cm wide. WPT 229, 1000m. L-726 . Coar se- to fine-gr a in e d granito i d with abund ant myar olitic cavities filled by brow n, druz y hemat i te . The rock is spongy and has light density as if leached . It mi ght carry gold. Quartz and feldspar in coar se pegmatite with hematite/limon ite vugs that may be sulfide remnants . Located just by a ridge of intrus i v e rocks. The rocks seems to have been etched by an acid selectively disolving a portion of the rock out. WPT 230, 1002m. L-727 . Gossano us fractur es with goethit e in ligh t, foliated, fine-gr ained, pink granitoid; densely intersec ted by quartz-hematite veinlets with abundan t gossan o us vugs after sulfid e s . Part of the quartz in the veins is dark and smok ey. This rock mi ght contain gold. Quar tz and pink potassiu m feldspar reac t slow ly to HCl along the pores. WPT 231, 1002m. L-728 * . Fresh sample of fine-gra i n ed , banded, dark pink to red-br ow n , fine-gra in e d , metaluminous, subleucocratic sodic ferrifer ou s granite . Same as describ e d above for L-727 . Intersec ted by two (at leas t) very fine quartz veins and brow n- oc h r e hem atite - r ic h veinlets . Zircons from this sample were dated by SHRIMP U-Pb at 1750?5 Ma. 2 0 8 WPT 232. 1002m. L-730 . Large sample of intens el y - fr a c t ur ed , fine- to medium-g r a i ne d intrusiv e rock cut by a dense 3-D networ k of gossan ou s , vuggy quartz + hematit e + sulfid e s (?) veinle t s ~1mm wide. The sample seems to have carried sulfid e s . It was collec t e d for sl abbin g and detaile d observati o n . Breccio id texture . L-729 . Breccia of similar char ac te r is t i c s to the previous sample ( L-730 ) . Fine- to medium-g r a i n ed , pink, metalum i no us subleuc oc r a t i c sodic to potassi c ferrife r ous biotite granite. The sample is cut by several subparallel sets of 1mm or thinner quartz veinlets with abundant vugs and gossanous texture. Collected for slabbin g and observi n g texture s . WPT 233, 993m. Photo that was taken towards 064? of a fracture-fill br eccia with leached sulfide vugs and gossanous surfaces . The fracture zone is approxim a te l y 1m wide. Fig (Photo) shows a subver t i c a l , 25-30 cm breccio i d vein with abund ant dusty goethite-filled vugs after sulfides . It contains quartz, black, massive hematite and sulfides . There is calcite in the veins. Note coarse texture of the breccia vein, angular fragments, etc. Taken from S to N and downward from WPT 233. Orientation of veins is 150?. Clos e-up photo of the same breccia vein, with card for scale and no north arrow. L-731 . Abundan t 2-3 cm-wide , non- mag n e t i c , coarse- gr a i ne d , brown to deep red carbona t iti c dikes that run subparallel to each other in 165/80?W. Dikes are spaced every 40-45 to 80 cm and occur in large numbers. The carbonatite dikes contain plagioc lase, clear calcite and quar tz needles as intra-fragmen ts. Dikes intersect a medium- to coar se - gr a in e d , porphy r it i c , white to light gray granit o i d rock. Both contac t s are pres ent in sample . Some vugs in the host rock now are filled by red materia l . See also photo in section 4.2.2 with camera bag for scale, for a general image of the dikes. Located 80 m N of WPT 233. Dark green (brown ) dikes 065/79 ? S subpar a l l e l . 65 m N, from WPT 233. Foliated, dark gray carbonatit e dikes 2.5 cm wide, 15-20 cm wide, sub- p ar a lle l to each other. Some run parallel and atta ched to white quartz veinlets. See L-732 . 2-3mm lens of quartz enclo sed by carbonatite (Fig 4.2.2. 1 9 photo L-732; a clos e-up view of sl abb ed sample can be seen on Fig 4.2.2.16 ) . These are not simple ankerite veins, becaus e at times the dikes thicke n and displa y clear igneous textures. L-733 . Tabular magnetit e crys tals , 5 mm thick and 10 cm lo ng, with aleatory orientation. They occur in a brow n carbonat i t e dike with white calcit e porph yr oc l as t s or xenocry s t s (Fig, photo L-733d ) . Located 50 m NE of WPT 233. Elephant skin weathering texture on surface. Note white color of the fresh surfac e and dense network of magnetite-filled fractures. L-734 . White quartz veinlet with angular crystals of magnet ite, brow n dolomite, corroded fragments of slightly magnetic hematite, and transpar en t calcite xenocrysts. It looks like the ?slurry veins? that are common in Carlin mineralized environments, Nevada, U.S.A. L-735 . Non-magnetic , angular breccia vein from WPT 233 with gossano us vugs and some 1-2 mm hematit e veinlet s and quartz . Medium- gr a i ne d pink igneous rock (syenite?) that seems to have been ?chewed up? by something. Some 1cm ?, clus ters of brown calcite are found within the intrus ive texture. Very irregular outer surfac e, with black iron oxide-rich la yer. Collected to slab and observe textures. WPT 234, 998m. L-736 . Foliated medium- to fine-grained biotite-ri ch granitoid cut by at least two different famili e s of 1-2 mm wide very vuggy, gossan ou s quartz ?magnetite-sulfides veinlets that make a dense mineralized stockwor k. The veinlets display red iron ox ide alterat i o n haloes. This sample may be mineraliz e d with disseminated prec ious metals. WPT 235, 998m. L-737 . White quartz veinlet intersec ted by three families of magnetite banded veinlets. There is paired zonation from the center outward. The thic ke r vein is 8-9mm wide; th inner ones are millimetric. The quartz is full of voids, like big bubbles . Try fluid inclus ion studies . WPT 236, 1002m. Photos (sever al , 1 close- up, one long distance, another short distance. All with hammer for scale. ) L-738 . For slabbing. Fine-grained, foliated, pink gr anitoid intersected by braided (or sheeted) magnetite+ hematite+qua rtz veinlets 1-0.3 cm wide, that intersec t each other and anastomo s e . Note iron oxide alteration of host rock near some veinlets and progress ive over pr inting from one side of the sample to the 2 0 9 o t h e r . Almost every single vein has vugs with gossanous infill that probably contained sulfides. Magnetite is partiall y martitiz e d . Foliation is 130/76 ?N. The same ori entat i o n and similar features are often seen around this site. The rock is very similar to rocks from around the Hook Granite batho li t h , Zambia and to mineraliz e d stockworks from the Tevrede iron oxid e-co pp e r - go l d deposit in Namibia. WPT 237, 997m. L-739 . Extremely vuggy coar se-grained igneous rock in a gossanous breccia vein. Very similar to that of WPT 233, collected to compare. Pro bable orientation = 070?. No reac tion to HCl. The sample is intersec ted in multiple directions by thin (< <1mm) magnetite-quartz veinlets that probably contained sulfides . An important portion of the rock seems to have been dissolved out. It should be assayed for gold. 2 1 0 APPENDIX A67.1 Cross Section Through Series of Ultramafic Dikes, Lofdal farm, Namibia WPT 238, 997m. WPT 239, 980m. Near farm worker ?s house. WPT 240, 963m. WPT 241, 1007m. L-740 . Fres h, very fine-grained, glassy, gr ay-red d is h to dark pink -br o w n , ~1m wide, peraluminou s sodic ferriferous trac hy phonolite dike wi th disseminated fine magnetite and no reac tion to HCl, that runs 056? azimuth. It has conc hoidal fracture and shar p edges. Well indurated. WPT 242., 1005m. L-741 . Subvertical, magnetic , dark gray to bl ack subvolc a n ic , metalum i n o us potass i c ferriferous trachy phonolite dike. It has an extremel y fine-gr ained matr ix, plagioc lase porph yries, open vacuole s , and does not react to HCl. The dike is orient e d 078?. Typica l nephel in e blades are 2-3mm wide, but range up to 2cm. The rock has a strong chloritic alteration. WPT 243, 1052m. Black to dark brown carbon a t i t e dike with hematitic banding along the foliation, coarse hematit e cluster s and gossano us texture. Or iented 60?/78?S. Very abundant iron oxides. WPT 244, 1002m. L-742 . Fres h, very fine-grained, medium gray, foliated, metaluminous sodic magnes ian biotite granite, with slightly magnetic char ac ter. It lies exactly halfway between cons ecutive subparallel carbonatite dikes. Maybe the magnetis m is due to hydrothermal alteration. WPT 245, 1002m. L-743 . Very magnetic, appr oximately 1m wide, brow n carbonatite dike with abundant earthy goethite (after sulfides?), that seems to have inte rnal flow banding. Oriented 085/52? S. It reacts to HCl. No more macroscopic features visible. L-744 . Non-magn e t ic , somewhat foliated , medium- to coarse - gr ai n e d pink granito i d cut by by quartz veinlet s . The rock is reasonably fresh for petrography and dati ng. It should be the same rock as L-742, and was collecte d to check for hydrothe r ma l alterati o n and chemical variation in the host rock due to carbonatitic dikes. WPT 246, 1012m. L-745 . Fres h 4-5 cm wide, strong ly magnet i c , very fine-grained, medium gray carbonatite dike with internal flow banding and no visible iron oxides that intersects rock L-742 . Orientation is 095/49 ?S. This rock could be dated. There is an alteration halo around the dike, and the sample has two ?quenche d ? margin s . It was slabbed across for detaile d petrogr a p h ic study. The sample has dip and strike indicat i o ns written on it to correct for erroneo us compass measur e me n t . The average strike was defined using several GPS readings , to bypass rock magnetism. WPT 247, 1002m. Carbona t i t e dike with abundant foliat e d (or braided? ) , black magneti t e bodies that might contain sulfide mineraliz a t io n . It runs parallel to the road and produc es an elonga t e d ridge. Oriente d 064/83? S . As seen on photo, the iron oxides seem to be foliate d along the dike. WPTs 248, 249 and 250 were taken are along the same dike. Minimun outcrop length is 400 m. Compar e the orient a t io n wi th that measured by the compa ss . L-746 was collecte d across the northe rn half of the carbonatite dike. Note the orientation of the sample . It contains an iron oxide gossan on one side. The weath e r i ng surfa c e s show clusters of iron oxide- r i c h subs tance that do not weathe r as much; that is due to magnetite-alteration. The surfac e is brow n/yellow and has a very irregula r texture like lapiez corrosio n in karstic environm e n ts . Dozens of satelli t e dikes run subparallel to the main ones that were sampled. A typic a l cros s secti o n of the variou s dikes is show n a nd discus s e d on sectio n 4.2. 2, Fig 4.2.2.15. In other locations, dikes are clos er together and very abundant. WPT 251, 1001m. Site of another subverti c a l carbonat i t e dike. 25-30 cm wide with abundan t iron oxide and red-rock alterati o n in the host rocks. WPT 252, 1002m. Subvertical, 10-15 cm wide, quartz vein with iron oxide and black frac tur es that is oriente d 050?. It seems to be younger than other nearby, quartz-less, carbona t i t e dikes sampled ; but that is not proven, due to insufficient outcrop. It could also be contem po r ar y with the ultrama f ic dikes. Sample L-747 of quartz with red stain and thin red-fill e d joints and some bl ack-filled joints, taken to study fluid inclus ions. 2 1 1 APPENDIX A67.2 Magnetite-Cemented, Polymictic Hydrothermal Breccia that Makes a Diatreme WPT 220. L-748 . Highly magnetic , coarse-grained, polymictic, angular hydrothermal breccia with gossanous surfac e. It is extremely difficult to find a fresh repres entative sample. Many of the clasts display corros io n edges and hydroth er m a l alterat i o n . Most of the sample surfac es are magnetic . The dimens ions of the sample collecte d were 25 x 15 x 20 cm. It was slabbed every 2cm to study clas t composit i on and angular variatio n . The gossanous surfac e was all left of the abundant contained sulfides. It may carry economic metallic mineralization and it should be eval uated . See Photos on Chapter 8. WPT 635. Photo with hammer and view of the flat land. Note textures. WPT 636. 2 photos of bare outcrop. WPT 637. L-1024 . Outcrop of carbonat i t e inside the breccia b ody. This rock does not seem to be a dike, but a massive volume of carbonatite. The sample contains hi gh values of rare earths, Y, Cu, Sc, Ce and La; low Al 2 O 3 , Na 2 O and Rb. WPT 636, 639, 640 (from south to north end) waypoin t s along a subvertical, black, magnetic , metaluminous, sodic ferrifer ou s undersa t u r a t e d olivine gabbro dike with extremely large radial pyroxene crystals. L-1025 was collec t e d from the dike, on WPT 639. The rock has a de cimetric , radial, conic crys tal struc ture. It might indicate paleo -orientation of verticality at the time of emplac e me nt . The sample has anomalo u s enricheme n t in Ti, P, Zn and V; very high Sr, Sr and Nb; low Al 2 O 3 , K, Na and Rb. Its copper conten t is also signifi c a n t . The dik e is two meters wide at times , but thins . The field map of Fig 4.2.2.20 shows it location. WPT 641. L-1026 . Massive magnetite. WPT 642. L-1028 . Abundan t massive black magne ti t e with gossano us vugs after sulfides and occasio n a l quartz veins. WPT 643. L-1027 . First outcrop of possibl e host rock to the diatreme. It is a coarse-grained , metaluminous mesocra t i c potassi c ferrifer o us nepheline syenite with lo ts of circular vugs , and contains high K, LOI, Zr, Zn and Nb. WPT 644. Abundan t fragmen t s of magnet i t e lying on the ground. Most with gossanou s textures and quar tz or white clay. WPT 645. All the way from WPT 64 4 with abundant gossano us magneti t e . L-1029 , massive magnetite with small hole. WPT 646. 2 sample s of magnetite-matrix, very coar se-grained, round-clas t, polymictic hydr othermal breccia for chemical analysis and assaying. L-1030 is large, L-1031 is small. Both for slabbing and assaying. WPTs 647, 648, 649. Thes e waypoints were ma de along the strike of the foliation of L-1032 , a massive, very dark, green to black, foliated, meta lu m in o us mesocr a t i c sodic ferrif e r ou s unders a t ur a t ed olivin e gabbro that seems to confor m the host rock of the magnet i t e brecci a body (diatreme) . The average dip of the foliation is 65? to the SE; meas ured indirectly, due to the rock?s strong magnetism. The rock has similar chemis try to L- 1023 an d L-754 . WPT 650. L-1033 . Magnetite-matrix in coar se-grained, polymic tic hydrotherma l breccia to slab, assay, and evaluate composition of fragments and matrix. WPT 652. L-1034 . Magnetite-matrix, coarse-grained polymictic hydro t h er m a l brecc i a with igneo us clas t s and abundant chlorite. Sampled to evaluate corros ion of clast margin and assay. WPT 653. L-1035 . Center of a large magnetite-matrix, co ar s e - gr a i ne d polymic t i c hydr oth e r m a l breccia outcrop with well-pac k e d angular fragment s . L-1036 , Very large sample of the magneti t e - c em e n t ed br ecci a . Collec t e d to make large- a r e a slabs and study the corros ion of round clas ts. Also for assaying . WPT 277. Pitch black dike or vein with quartz to be described later. 2 1 2 WPT 278, 970m. L-754 . A one-mete r wide, fine-gr a i n ed , dark gr ay to black, metalum i n o us potass ic , ferrif e r o us diorit e dike that produc es a slight re ac ti o n with HCl and does not contai n quartz (Fig photo L-754 ) . Strongly-foliated: 070/55?S. The surface weathers with subpar a ll e l ridges and valley s . Other near by dikes seem to have lamprophyric compos ition. L-749 . Quartz with minor light green micas in small batc hes. This comes from a rare-eart h- b ea r i n g pegmatit e . WPT 279, 970m. L-755 . Pitch black, non-magnetic , ~40 cm wide, extremely fine-gr ained dike, oriented 076/74?S. It is made of an unidentified black silicate subs ta nc e that scratc hes white. The black material is full of very small vugs, and many submillimetric veinlets of braided quartz . Some 5mm, white quartz lenses; coar se r portio n s show pris ma t i c amphib o l es + q u ar t z + p l ag ioclases. Another portion of the sample has more quartz and less black materi a l . The sample was slabbe d to observ e its textur e in det ail. No massive hematite was presen t in the rock and it did not produce any reaction to 10% HCl. The rock extends for at leas t 50 m along strike . There are a few astomos in g black veinle t s in white quartz. One part of the sample is a quartz pod, the other part is a breccia . WPT 281, 883m. Site along a dry creek with dense 3-D network of quartz veinlets. Some of them are vuggy. The host rock is a silicif ied, fine-grained granitoid . WPT 282. Abundant quartz is lying on the ground, located by a farm gate. It may be from a quartz pod or a pegmatite. WPT 283. Graniti c rock outcrop . 0443882 / 7 7 6 29 6 9 WPT 284. End of igneous rock outcrop. 0443718/77 62833. L-756 . Quartz with hematite 1-2cm ? particl es inters e c t ed by networ k of at least 2 families of braided, submillimetric black hematite veinlets. All (par ticles and veinlets) contain gossanous vugs after sulfides, and should be assayed for their gold/metal/rare earth content. S175. Farm house. L-1020 . Mafic, foliated rock with high Na and Cu. WPT 151 is a gate in the fence. S176. Many quartz veins cut gneissic , metalum i no us , subleuc o c r a t i c sodic ferrife r o us biotite granite ( L-1021 ). Similar to L-1019 . S177, 993m. L-1022 . Outcrop s of a subvolc a n ic , porphyr i t i c , peralu m in o us mesocr a t ic sodic- po t a s s i c ferriferous trac hytic dik e. It is 2m wide, strik es 07 0?, and cuts the road. Its chemis try is similar to L-161 . S178 WPT 623, 995m. Just by windmill, gate of fence. S179. Entrance to site of abandoned water borehole that is marked #W96911 . Cased in 6-inch diamet e r iron pipe. A strati gr a p h ic column of the boreho l e might be av ailabl e with the farm owner or a Namibian governme n t institution. Many magnetic dikes were seen around here. WPT 624. House on road. WPT 625. Located on the road. WPT 626. On dry river. L-1023 . Reas onably fres h, flat-lying, black, non-magne tic, foliated rock. It might be a pyroxenite? If it is a dike, it is more than 5 meters wide. The chemis tr y of this sample is very similar to that of L-1032 and L-754 . It contains high Ca, Fe2O3, Co, Ni, Zn, and V. WPT 627. Along road, severa l mafic or ultram a f ic black dikes were crosse d . S180 Gate on fence to enter the Lofdal fa rm. Black ultr am a f ic rock makes the ground . Zinc enric hme n t seems to be a particula r featur e of some syenite s . Nepheli ne syenites from the sodalit e syenite quarry in Zambia also contain high zinc. Gabbr oic rocks in general are zinc-enr ic h ed ; high-Zn rocks from other suites in the Greater Lufilia n Arc tend to be gabbroids. Such is the case for the Kamanjab batholith and Okatjepuiko. 2 1 3 APPENDIX A68 PARTIAL FIELD NOTES COLLECTED AT THE MESOPOTAMIE FARM, NAMIBIA WPT 312, 726m. L-758 . Gossanous, quartz -rich, white, coar se-gra ined granite with graphic texture. There are several pegmatit i c phases of the same rock made of coar se biotite, plagioclase and quar tz that displa y partial graphic texture; its crys tals va ry from 5-10 cm in diameter . A zircon concentrate of this sample was dated using SHRIMP U-Pb methods and gave an age of emplac ement of 750?5 Ma. Xenocrystic zircon s produce d an age of 1692?10 Ma. They record the igneous protolith from which the graphic granite was made. The sample was collec t ed near the NW corner of the farm, as seen on Fig 4.2.3.3. WPT 327, 682m. L-759 . Peraluminous leuc ocratic potass ic ferriferous , muscovite-rich granite that intersec ts schists. It is very similar to the previo us outcro ps along road ( L-758 ). On 0439579/7 7 6 41 2 9 , 703m on a hill located just above the old mine plant site, L-772 is one of several ligh t gray to white, 70 cm wide, metalumino us potassic ferrif erou s graphic alkali granite veins that intrude a coarse, pegmat i t i c peralu m in o us leucoc r a t i c so dic ferrifer ou s pegmatit i c granite ( L-773 ). The main orientation of the veins is 032/82 ? NW. They have many 2-3 cm long tabula r white to light pink plagiocl as e phenoc rys t a l s . WPTs 283 to 284 L-779 . Outcrop of an intens ely-fractured and har d to sample gneissos e granitoid rock that probably is the regional basement. On the NE corner of the Mesopot a m ie farm, several quartz pods were observe d . L-780 to L-782 come from quartz pods. WPT 337, L-783 . Peralum i n o us mesoc r a t ic sodic to potass i c fe rriferous , muscovite-biotite gneissic granite outcrop on the northeastern portion of the Mesopotamie farm. WPT 338, 790m. L-784 comes from a coar se -g r a in ed , metal u m ino u s mesoc ra ti c sodic to potas s ic ferri fero u s augen granite gneiss that probab l y makes the regio nal basement. It has pink potassium feldspar phenocr y s t a ls (with white nucleus ) in a biotite+amphybole+ plagioclas e, dark gray, fine-grained matr ix. The granitoid ?s main foliation is 154/51? E. It is macroscopically very similar to L-779 . 2 1 4 APPENDIX A69 FIELD NOTES, UGAB RIVER, NAMIBIA WPT 346. Gate WPT 347. Flat outcrop of granitoids. WPT 348. WPT 349. E flat outcrop of granitoid s WPT 350. NE flat WPT 351. WPT 352. S outcrop WPT 353. S Good, large outcrop WPT 354. Long, pano ramic photograph radiating from 070? to 045?. To the left, in the Ugab River valley, there are small, red intrusive bodies that seem to be young (L-7 93, L-796 and L-797). Next comes a soft, round hill, the road, and other small hills that are probably made of the same red intrusive rock. The large rolling hills to the right are made by gray, old intrusiv e rocks (L-795, L-798, L-799 and L-802) . Fig Field drawing of some structural re lationships at the Ugab River site, Namibia . Located on geological station WPT 359, as described in the tex t. S e e p h o t o graph of the same outcrop on the n ex t page. W P T 359, 648 m. Orient e d photogr a ph of porphyritic ?gray? granitoid. The ar row points toward magnet i c north. It has a 10 cm thick vein that contains a quartz + feldsp ar inclus io n . A white/pin k , banded dike is limited by a biotite halo (K alteration ?). There is also a black, biot ite-rich xenolith. The orientat ion of the dike is 127/90?. Some thin, black veins are oriented 083/77? S. A ll is shown on the Fig above. The photogr a ph is perpendicular to the main rock foliation in this place, but few location s show similar foliatio n. The ?foliati o n ? might be due to local flow textures. Roy Miller, consultant to the Namibian Geological Su rvey, suggested that I should visit the well-exposed outcro p of intrus i v e rocks near the Ug ab River bridge . It is a good site to observe the contact between two intrus i v e bodies . The river was comple tely dry at the time of the vis it. WPT 361, 614 m. Parking spot. WPT 355, 633 m. L-793 . Coar se pink, metalumin o us sodic ferrifer o us biotite granite with magnetit e in abundant clus ters. It may be a coarse facies of the pink intrus ive body. 2 1 5 W PT 356, 630 m. L-794 . Typical texture of the pink granitoid with very little magnetite. The rock has a slight foliation due to deformation; deformation is especially seen on the quartz. The rock is not extremely fres h, but is the best availab l e for samplin g . 2 1 6 WPT 357, 632 m. Fig is a photograph of contact the bet ween both intrusiv e rocks. The red intrusiv e is fine grained near the contact (~chill ma rgins). The gray granitoid is ol der, as observed on the outcrop. WPT 358, 646 m. L-795* . Two fragmen ts of the gray, coarse, porphy ri t i c intrusive body with abundant biotite and magnetite clusters. Most of the rock has int ens e chemic a l and mechanic a l weather i ng . A zircon conc en t r a t e from the sample was dated by U-Pb S HRIMP II at approximately 540 Ma; it also containe d xenocry s t i c zircon s with ages around 1200 Ma. Geochro n o l o g y has not been complete d at the time of writing this doc ument. WPT 360, 647 m. L-796* . Fres h pink granito i d from opposit e side of the road, behind a small, informa l crafts shop. The sample contains red quartz clusters, no m agnet i t e and zoned red plagio c la s e . A zircon conc en tr a t e from the sample was dated by U-Pb SHRIMP II at ap pr oximately 750 Ma. That age came as a surprise, for the foliated, porphyritic rock seemed to be older. Ther e mi ght be two generations of pi nk granito i d s at the Ugab River outcro ps . WPT 353. L-797 . Fres h, pink, medium-grained , peraluminous sodic-potassic ferriferous biotitic granite with pink feldspars, rare magnetite and red quartz . WPT 352. L-798 . Very fres h, fine to medium-grained, gray, peral umi n o us leuc oc ra t ic sodic-po t a s s i c ferrifer o us granite with no pink feldspar present. It may be facies of the ?pink? granitoid ( L-796 , L-797 ). WPT 351. Two types of granitoid s . A non-magne t i c , m edium-grained, gray granitoid with coarser-grained gray/ p i nk felds pa r ( L-800 , the same as on WPT 350) that intr ude s medium- to coarse- g r a i n ed , brow n, porph y r i t i c , peralum i n o us sodic- p o t a s s ic ferrif e r o us biotit e granit e ( L-799 ) with yellow quartz, some magnetit e and transparent to yellow plagioc lase. WPT 349. L-801 Granitoid with dark red, tabular , soft ma crocr y s t a l s and medium gray quartz . The gray granitoid progressively changes into a more pink rock. WPT 348. L-802 . Fine to medium-grained, pink, non-magnetic , per alu m i n ou s sodic- p o t as s ic ferrif er o us granit e that grades from the previou s gray gr anitoid (L-801). It contains small sp indl e- s ha p ed , biotit e - rich xenolit h s and coarse biotite ?eyes?. 2 1 7 APPENDIX A70 FIELD NOTES, OKWA RIVER, BOTSWANA WPT 001 Car stop near a ?bridge? over a dry river bed. Very low profile outcrops as rock pavement surrounded by calc rete . WPT 002. Granite outcrop WPT 003. Granite outcrop WPT 004. Calcrete cover WPT 005. Granite outcrop WPT 006. Boulder of calcrete with granite clasts in it. (See map on page 8.) WPT 007. Granite outcrop along the river bed WPT 008-012 . Delimit the perimeter of foliated gr anite outcrop. Main rock foliation is 131/87 ?N. WPT 013. Small 10m diameter outcrop ( L-600A ) Fresh, light pink , slightly fo liated, porphyritic, peraluminous sodic-potassic ferriferous alkali granite that is cut by a pink dike. Note zoned plagioc lases and intense brown alteration in the fine-gr ained matrix. WPT 014. L-601, Foliated granitoid sampled in situ from the freshe s t rock possible . Main rock foliatio n is 121/88?N. WPT 015. L-602 : Dark gray-gr ee n is h, fine- to medium- g r a in e d , metalum i n ou s mesocra t i c sodic-p o t ass i c ferriferous granite. This roc k was so da rk that in the field, it was cons id e re d to be a gabbr o id ins te a d of a granite. WPT 016. L-603 . Fres h, non-foliated, fine-gr ained intr usive surrounded by foliated, coarse-grained (dike?). WPT 017. L-604 . Fres h, foliated granito id. WPT 018. L-605 . Coarse-grained, foliated, metaluminous leuc oc ratic sodic ferriferous clinopyroxene granite. WPT 019. L-606 . Composit e , medium-gr a i n ed , metalu mi n o us mesocr a t i c sodic ferrif e r o us biotit e granit e that is not as strongly foliated. Most of the foliated rocks contai n dark gray to black xenoliths. Abundant fragments of green, glassy volcanic rock are lying in the ground. These probably are Karoo age volc anic rocks . This type of rock turned out to be quite common and widesp read , as indicated on the main text of the chapter comparing Okwa River rocks to those from t he Grootfontein Inlier, the Ugab River and others. 2 1 8 APPENDIX A71 FIELD NOTES, GROOTFONTEIN INLIER, NAMIBIA WPT 602. Site wher e vehicle was parked . WPT 603 to 610, 620 and 621: route along a railroad. WPT 611 and WPT 612 travers ed over coarse granito id s . WPT 613. Over fine-grained porphyritic granitoid. WPT 614. Over coarse-gr ai n e d granitoi d in forest. WPT 615 and 616. From the highest point reac hed . In situ outcrop of carbonat es with no evidence of intrusions or metamorphism. Bedding planes have normal polarity. WPT 617. L-1041 : Carbonat e breccia from the base of the Otavi sequenc e with fragmen t s of rounded granitoid s. This is eviden ce that the Katangan rocks were unconformably laid over the granitoid s. WPT 618. L-1042 : Coar se- gr a i ne d , porph yr i t i c , slightly foliated, peralumin o u s subleu c o c r a t i c potassic ferriferous biotite granite with fuzzy mineral borders and 1cm long euhedr a l white to light yellow plagioc la s e phenocr y s t a ls . The sample was the leas t altered rock that could be found. L-1043* : Fine, felsic, porphyritic, almost un-foliated, peral u m i no us , suble uc oc r a t i c pot ass ic ferr ife ro us biotite granite. Zircon s conc entr a t e d from this rock were dated by laser ablation ICPMS at the Memorial University in Newfound l a nd , Canada. They gave a U-Pb age of 1939? 64 Ma, with xenocrystic zircons that dated 2544?78 Ma. Geoc hr on o l o g ic a l data for this sample was extr emel y comple x to interpret , and furthe r work may end up refining the ages. W P T 619. The rock repres en t e d by L-1043* intrudes into L-1044 i n sever a l location s . L-1044 is a coarse- grained, porphyritic, peralumi n o u s leucocra t ic sodic fe rriferous biotite granite with alligned 2-3 cm long, pink feldspa r euhedra l phenocr y s t a l s . L-1045 : Fres h, very light gray to light yellow-pink, ve ry fine-grained, metaluminous sodic ferriferous clinopyroxene quartz monzonite with small vugs that may be sulfides (?). L-1046 : Fresh, porphyritic, gneissose, peraluminou s subleuco cratic potassic ferriferous biotite granite with white to yellow-p in k potassic feldapar augen phenocrys t a l s . 2 1 9 APPENDIX A72 TRANSCRIPTION OF FIELD NOTES FROM OKATJEPUIKO, NAMIBIA Route with several fences and brooches. Sparse outcrop. WPT 26 + 27 Outcrop . WPT 28, brooch. WPT 29 Borehole OP-2-17- 1 0 0 100- 17m 0243000/ 75 3 7 05 5 1544 m WPT 30 Borehole OP-1, (to south). There is a pole with ro ck outcrop. The salt pan (called ?malachite pan?) is located to the east of WPT 30. The coor dinates t hat I get for borehol e OP-1 are 0243351 / 7 5 37 2 56 ? 1 5 4 4 meters of elevation. WPT 31 L-624 : Medium- to fine-grained fresh intrus ive rocks L-625 : Metalumi n o us subleuco c r a t i c potassic ferrifer o u s granite. WPT 32 L-626 : Fres h, medium- to fine-gra i ne d , peralu mi n o us me socrat i c potassic ferrifer ou s granite with iron oxide veins. Large sample, packed in two bags. WPT 33 Pole on OP-2 steel material over a concre te BM. This is the loc ation of borehole OP-2. WPT 034 Small outcrops of similar intrusi v e rock. Ma ybe outcrop is 20 m in diamete r around all above stati o ns . WPT 035 [34K 0243343 / 75 3 7 28 4 ] L-627 , L-628 , L-629 and L-630 were collected here. They are different hand samples with iron oxide, black hematite and fine- to medium-grained, chloritized igneous rock. On WPT 036: A dark green-bl ac k , fine grained gabbro cuts a much lighter gabbro with foliatio n . WPT 037 L-631 : Red jasper breccia WPT 038 Site to sample later. WPT 039 L-632 : Gabbro or basalt (?) with white porphyries of plagioc lase (or amygdules) in a very fine- graine d , dark green matrix. WPT 041 L-633 : Fine of medium- gr a i ne d metalum ino u s mesocra ti c potassic ferrife r o us monz o-g a bb r o with chlorite veinlets . WPT 042 Outcrop of medium-g r a in e d gabbro or amphibole - r i c h rock. L-639 : Black to dark green gabbro to NE of power line. WPT 043 and 040 Poles for power line. Cables. L-634: Gabbro cut by thin, lighter 2mm intrusive veinlet. WPT 044 Power line tower. L-635 : Medium gray, porphyritic metalu minous potassic ferrife r o us quartz latite. It outcrops in a 10 m diameter around wpt. L-636 : Dark gabbro with pink veinlets . L-637 : Lighter (than L-636 ) fine-gr a i n ed , metalum i no u s mesocrati c potassic ferrifer o us biotite granite with higher plagioc l as e content and very slight foliati o n (or fl ow-banding?). In the field it seemed to be a different facies of the same gabbroi c body of L-636 . Fig (photo L-637A ) shows the main features of the rock and illustr a t e the surfac e weather i ng and strong red surfac e colorat i o n . WPT 045 L-638 : Pink , fresh, medium- to fine-gr a in e d , metalum i n o us leucoc r a t ic potassic ferrifer o us alkali granite. Contains fine green (chlor ite?) and black (m agnetite+ biotite?) veinlets . It outcrops along the road, beneat h a power line. WPT 046 L-640 : Pink and fine grained granito id with black gabbro xenolit hs ~rounded edges. Also some black hematit e (?) veinle t s . 2 2 0 In the same site, L-641 : Fine-gr ained, dark green to dark gray, metalu m i n ou s mesocra t i c potassi c ferrifer o us monzo-gabbro. Seems to be a xenolit h into the pink granitoid of L-640 . WPT 048 L-642 : Small fragments of fine-grained, black ga bbr o. Foliate d rock with massive iron oxide alteration (hematitization) of sedimentary rock or folia ted metamo rphic rock. Also contains fragment of quar tz + iron oxide pod. None of the samples are in situ , but collected from 5 m diameter around the WPT. WPT 049 L-643 : Small sample of granitoid with iron oxide veinlets. No more outcrop available at site of sample #130 of Eckhart Freyer. On WPT 050 and 10 m around it, many sample s of intens ely-hematitized rock with quartz veins, vuggy quartz veins, calc ite veinlets in networks, near a ?T? junc ti on and fenc e intersection . Deep red color extends along the road. Some of the rocks display round-c l as t breccia t i o n overprin t e d by extreme red hematite alterati o n . (See L-644 and L-645 : Brown-red, metalumino us me soc ra ti c pota ss ic ferr i fe ro us nephe l i n e syeni te ) with stron g hydrot h er m a l altera t i o n . The rock name is probab l y wr ong. Intens e sodic alterati o n , added to the large iron oxide hydrothe rmal input have largely modified the origi nal rock chemistry. The trace element chemis try is not from a nepheli n e syenite . The origina l type of rock wa s hard to identify in the field. It seemed to have been fine-grained gabbro, or a dark sedimentary rock. It c ould also be a hydroth e r ma l breccia cemented by nephelin e syenite. As seen on Fig the photogra ph , the origi n a l clasti c textur e of the rock has almost vanish ed , to be replaced by a pervasive brown- r ed hematit e alterat i o n that progres s i v e l y replac es matrix and clasts of the breccia . The photogr ap h of L-645 also helps to illustrate the red-rock alteration. In this case, original texture is easier to identify. Both L-644 and L-645 are mass ive, extr emely well cemented rocks. L-646 (Big sample) : has deep purple- br o w n iron oxide colo r that masks previou s rock texture out comple tely. A vuggy, white quartz vein intersects it and the oxidized vugs seem to have contained some sort of sulfides. L-647 : Red-rock altered roc k with calc ite th in veinlets in a stockwork fashion. L-648 : Brow n iron oxide massive alteration in metaluminous mesoc r a tic potass ic ferr i fe r ou s alkal i grani te with some Cu stains & gossans . L-649 : Fine-grained, metalu minous subleuc ocratic potassic ferrifer ous granite with silic ification and massive iron oxide alteration; with chlorite and possible CuCO 3 stains . Very difficult to identify in the field. As show n on the photogr ap h of L-649 , a very dense three dimens i o na l network of iron oxide-r ic h sub- mill i m e t r i c veinle t s , along with chlorite and sulfides of copper and iron were overpr i n t e d on a granitoi d rock. L-650 : Breccia of brown-a l t e r e d rock with quartz and calc ite veins. On WPT 051 entering the pan along a road, there is a ~20 m diameter outcrop of black to dark green and dark brow n / r e d possib l e porph yr i t i c (mafic ?) volca n ic rocks with massiv e iron oxide altera t i o n . Some rocks even displa y massive metallic hematite. L-651 : Several grab sample s with metallic iron oxide (hematite). L-652 : Several grab samples of the different varieties of rock in the outcr o p . Note possib le vacuo l es and porph y r ob l a s ts as well as flow textur e s and/or beddin g . Some rocks may be breccio i d , but their textur e is masked by pervasive iron oxide alteration. The rocks are immersed in white CaCO 3 calcrete. Light gray color in roads that cover the pan. Some with Cu stains! WPT 052 On the change of road, ballas t color varies fr om from red/brow n to light gray. This might indicate the areal extension of iron oxide alteration. WPT 053 Change of soil color from brown to oc hre. The brow n soil has large rock boulde r s that were not sampled , but are thought to be similar to the brow n ro ck iron oxide pervasive alte rat i o n that was previou s l y describ e d . WPT 054 Entrance to farm house. Very friendly manager. WPT 055 Possible intrus ive rocks. 2 2 1 APPENDIX I OTHER INFORMATION A73 Persons interviewed for preparation of fiel dwork, during fieldwor k , and when proc es s in g information, 223 A74 Rock names of samples from the Greater Lufilian Arc Granitoi d project, 224 A75 Experiment to test quality of chemic al laborator y, 229 A76 Heat production capa city of intrusive rocks from the Greater Lufilian Arc at the time of their emplac eme n t, 231 2 2 3 APPENDIX A73 PERSONS INTERVIEWED FOR PREPARATION OF FIELD WORK, DURING FIELD WORK AND WHEN PROCESSING INFORMATION Armstrong, David; Kitwe, Mopani Coppe r Mines Ltd. Ashwall, Lew; Johannes bu r g , Univ ersity of the Witwatersrand Badenhorst, Frik; Navachab mine, Anglogold Corporation, Namibia Bantu-Bons e, Frederick; Kalulushi, Zambian Chamber of Mines Borg, Gregor; Windhoek, Johannesbur g, Ma rtin Luther Univer sity, Halle, German y Bouda, Steven; Lumwana, Equi nox Corpora t i o n , Zambia Buxton, Mike; Johannesburg, Windhoek, Lubumbashi, A ngl o America n Corpor a t i on S outh African exploration offic e Carruthe rs, Hugh; Kitwe, First Quantum Corpor ation Clark, Alan, H., Queen?s University, Kings ton, Ontario, Canada; met in Toronto Corner , Branko; Swak opmund, Private consultant in applied geophysics Corran s, Roy; Johannesbur g, geolog ical cons ultant Freyer, Eckart; Windhoek, Manager of AngloAmerica n Corporat i o n explorat i on office in Namibia Greyling, Lynette; University of the Witwatersrand G?nz el, Arno; Windhoek, Otavi, Lubumba shi, Ongopolo Corpor ation Hoffmann, Karl; Windhoek, Namibian Geological Survey Hunt, John Paul; University of the Witwatersrand Injoque, Jorge; Lima, via e-mail, geological cons ultant, Lima, Peru Jebrak, Michel, University of Quebec in Montreal, Canada Kabengele, Matthias, Lubumbashi, D.R. Congo Kamona, Fred; Windhoek and Lubumbas hi, Univer sity of Namibia Khunuch ab , Julius Kinnaird, Judith; Johannesburg, Zambia, University of the Witwatersrand Klinge, Thoren ; Kumba Resour ces, South Africa Lauderda le, John, Kitwe, Lubumba shi, AVMIN exploration office in Zambia Liyungu, Kennedy; Lusaka, Director, Zambian Geolog ical Survey Lombaard, Andrus ; Otavi, geolog ical consul t an t to Ongopo l o Corpor a t i o n Lombard, Anton; Windhoek, manager of AVMIN exploration office in Namibia MacKen zie, Chris; Windhoek, Manager of BAFEX corpor ation Mann, Peter; Kitwe, Anglo American Cor poration exploration office in Zambia Mariano, Anthony; Windhoek, geological cons ultant Martin, Robert, McGill Univ ersity, Montrea, Canada Master , Sharad; Johannes b u r g , various portions of Zambia and Bots wana, Lubumbahi, Univer sity of the Witw a ters r and Matthews, Alexander, Kitwe, Lusak a, Lubumbash i, AVMIN exploration office in Zambia Mendels oh n , Felix; Johanne s bu r g , geolog i c a l cons ult an t Miller, Roy; Windhoek, Geol ogical consultant to the Namibian Geological Survey Murphy, John; Johannesburg, AVMIN Mweti, Albert Nex, Paul; Johannesburg, Univ ersity of the Witwatersrand Niku-Paavola, Vicky; Windhoek, Namibian Geological Survey Nyambe, Imas iku; Lusaka, Lubumbashi, Jo hannesburg, University of Zambia Pelly, Peter; Johannesburg, Kitwe, Windhoek, Lubumbas hi, BHPBilliton exploration office in South Africa Philpot, Hilton; Johannesburg, Exploration Manager, AVMIN Porada , Hubertus; via e-mail, University of W?rsburg, German y Prinsloo, Tinus; Kombat Mine, Ongopolo Corporation Rainaud , Christi n e ; Johanne s bu r g , University of the Witwatersrand Richards, Michael; Lumwana, Equinox Corpor ation Schneider, Gaby; Windhoek, Director, Namibian Geological Survey Sillitoe, Richard; Kitwe, geological consultant Steven, Nick; Johannes bu r g , privat e geologi c a l consult a n t , Capetow n Tembo, Francis; Lusaka, Head of Geology, University of Zambia Tsengua, Simon Whitfield, Gavin; Johannesbur g, geological cons ultant Williams , Tim; Chingola , Nchanga Mine, Nchanga Copper Corpor ati o n Wilton, John; Otjiwarongo, AVMIN exploration office in Namibia Woodhead, John; Kitwe, Lubumba shi, Anglo Americ an Corpor ation exploration office in Zambia TABLE A74 ROCK NAMES, GRANITOID SAMPLES COLLECTED, LUFILIAN PROJECT, ZAMBIA AND NAMIBIA By Alberto Lobo-Guerrero S, Geologist, M.Sc., Min.Ex., Feb. 2004, Johannesburg Sample Middlemost de la Roche IUGS Sample Middlemost de la Roche IUGS L-005a granite L-163 foid gabbro syeno-gabbro foid diorite L-012 syenite quartz syenite syenite L-166 granite granite granite [high-K] L-012 A syenite quartzmonzonite syenite L-167 foid monzodiorite syeno-diorite foid monzodiorite L-020 granite alkali granite granite [high-K] L-168 granite alkali granite granite [high-K] L-023 granodiorite granodiorite tonalite L-170 granodiorite granite granite [high-K] L-024 gabbro gabbro-diorite gabbro [subalkali] L-172 granite alkali granite granite [high-K] L-025 granite granite granite [high-K] L-173 granite alkali granite granite [high-K] L-026 granite granite granite [high-K] L-175 granite granite granite [high-K] L-027 granodiorite granodiorite granodiorite [medium-K] L-181 gabbro s. olivine gabbro gabbro [subalkali] L-028 monzonite quartz monzonite monzonite [Na2O-21.33Fe+4.4] L-032 diorite gabbro-diorite diorite [high-K] L-208 granite alkali granite granite [high-K] L-034 syenite ? syenite L-209 gabbro alkali gabbro gabbro [alkali] L-036 granodiorite syenite granodiorite [low-K] L-210 quartzmonzonite syenite syenite L-037 foid syenite out of plot (far from gtd field) nepheline sodalite syenite [peralkaline] L-212 syenite-quartzmonzonite quartz sye nite syenite L-038 foid syenite nepheline syenite nepheline sodalite syenite [peralkaline] L-213 syenite syenite syenite L-039 foid syenite nepheline syenite nepheline sodalite syenite L-214 syenite syenite syenite L-040 foid syenite nepheline syenite nepheline sodalite syenite [peralkaline] L-215 granite syenite granite [Peralkaline, Al2O3>1.33Fe +4.4] L-041 foid syenite nepheline syenite nepheline sodalite syenite L-217 granite-granodiorite granodiorite granite [medium-K] L-044 foid syenite nepheline syenite nepheline sodalite syenite [peralkaline] L-218 quartzmonzonite quartz syenite syenite L-045 foid syenite nepheline syenite nepheline sodalite syenite L-222 granodiorite alkali granite tonalite L-046 foid syenite nepheline syenite nepheline sodalite syenite L-223 granodiorite granite tonalite L-047 quartzmonzonite quartz syenite syenite L-224 diorite alkali granite tonalite L-049 gabbro saturated olivine gabbro gabbro [alkali] L-237 granite granite granite [high-K] L-050 gabbro undersaturated olivine gabbro gabbro [alkali] L-238 granite granodiorite granite [high-K] L-060 gabbro saturated olivine gabbro gabbro [subalkali] L-239 granite granite granite [high-K] L-060 gabbro saturated olivine gabbro gabbro [subalkali] L-241 foid out of plot L-060 granite granite granite [Peralkaline, Al2O3>1.33Fe+4.4] L-242 granite out of plot granodiorite granite [medium-K] L-063 essexite foid gabbro (ol<10%) L-248 granodiorite granodiorite granodiorite [medium-K] L-064 essexite foid gabbro (ol<10%) L-248-LG granite granite granite [high-K] L-065 theralite nepheline syenite L-249 granite granite-granodiorite granite [high-K] L-075 quartzmonzonite L-257 granite granite granite [high-K] L-076 quartzmonzonite quartz monzonite quartzmonzonite L-259 quartzmonzonite granite granite [high-K] L-077 quartzmonzonite quartz monzonite quartzmonzonite L-259-B quartzmonzonite granite granite [high-K] L-078 granodiorite tonalite L-263 quartzmonzonite quartzmonzonite quartzmonzonite L-079 quartzmonzonite granite - limit with granodiorite quartzmonzonite L-268 granodiorite granite? L-079 granite L-269 granite granite? L-139 granite alkali granite granite [high-K] L-273 granodiorite granodiorite L-150 monzodiorite syeno-diorite monzodiorite [Na2O-21.33Fe+4.4] L-325 monzonite granite L-437 monzonite syeno diorite monzonite [Na2O-21.33Fe+4.4] L-362 granodiorite granodiorite granodiorite [medium-K] L-602 granite granite granite [high-K] L-363 granodiorite granodiorite tonalite L-605 granite granite granite [high-K] L-364 granite alkali granite granite [high-K] L-606 granite granite granite [high-K] L-365 granite granite granite [high-K] L-625 granite granite granite [medium-K] L-366 quartzmonzonite granite quartzmonzonite L-626 granite granite granite [low-K] L-367 granodiorite granodiorite granite [medium-K] L-633 monzo-gabbr o monzo-gabbr o monzogabbro [Na2O-2>=K2O] L-368 quartzmonzonite granite quartzmonzonite L-635 monzonite quartzmonzonite syenite L-369 granite granite granite [high-K] L-637 granodiorite granite granite [low-K] L-370 granite granite granite [high-K] L-638 granite alkali granite granite [high-K] L-371 granite granite granite [high-K] L-641 gabbro monzo-gabbr o gabbro [subalkali] L-372 monzo-diorite monzo-gabbr o monzodiorite [Na2O-2>=K2O] L-645 monzonite nepheline syenite monzonite [Na2O-2>=K2O] L-373 granite granite granite [high-K] L-648 granite alkali granite granite [peralkaline, Al2O3>1.33Fe+4.4] L-374 granite granite granite [high-K] L-649 granite alkali granite granite [medium-K] L-375 granite granite granite [high-K] L-668 diorite syenite syenite L-376 syenite syenite syenite L-669 granodiorite syenite syenite L-377 quartzmonzonite quartz syenite granite [peralkaline, Al2O3>1.33Fe+4.4] L-670 diorite-gabbroic diorite nepheline syenite monzonit e [Na2O-2>=K2O] L-378 granite granite granite [high-K] L-675 diorite syenite syenite L-379 granite alkali granite granite [peralkaline, Al2O3>1.33Fe+4.4] L-676 diorite syenite syenite L-380 granite alkali granite granite [high-K] L-691 gabbro monzonite monzodiorite [Na2O-21.33Fe+4.4] L-403 quartzmonzonite quartzmonzonite syenite L-694 diorite nepheline syenite syenite L-405 gabbroic diorite s. olivine gabbro gabbroic diorite [medium-K] L-695 gabbro nepheline syenite foid diorite L-406 gabbro alkali gabbro gabbro [alkali] L-697 diorite syenite syenite L-407 monzonite gabbro-diorite monzonite [Na2O-21.33Fe+4.4] L-408 granite granite granite [high-K] L-699 granodiorite syenite syenite [comenditic] L-409 quartzmonzonite granite-alkali granite granite [high-K] L-700B granodiorite quartz monzonite L-410 granodiorite granite tonalite L-708 gabbro out of plot, gabbro gabbro [alkali] L-411 out of plot, foid off plot, ultramafic foidolite L-712 granite alkali granite granite [medium-K] L-416 gabbro-diorite gabbro norite gabbroic diorite [medium-K] L-713 granodiorite quartz syenite granite [peralkaline, Al2O3>1.33Fe+4. 4] L-420 granite granite granite [medium-K] L-714 granite granite-alkali granite granite [high-K] L-421 quartzmonzonite granite granite [high-K] L-714 granodiorite granite granite [high-K] L-433 monzodiorite syeno gabbro monzodiorite [Na2O-21.33Fe+4.4] L-898 quartzmonzonite granite granite [high-K] L-729 granite granite granite [high-K] L-899 granite granite granite [high-K] L-740 monzodiorite nepheline syenite monzonite [Na2O-21.33Fe+4.4] L-742 granodiorite granite granodiorite [low-K] L-903 granite alkali granite granite [high-K] L-754 gabbroic diorite gabbro diorite gabbroic diorite [medium-K] L-904 granite alkali granite granite [high-K] L-759 granite granite granite [high-K] L-905 granite alkali granite granite [high-K] L-772 granite alkali granite granite [peralkaline, Al2O3>1.33Fe+4.4] L-906 granite alkali granite granite [high-K] L-773 granite granite granite [medium-K] L-907 granite granite granite [high-K] L-783 granite granite granite [high-K] L-908 syenite syenite L-784 granite granite granite [high-K] L-909 granite alkali granite granite [high-K] L-789 syenite quartz syenite syenite L-910 granite alkali granite granite [high-K] L-791 granite alkali granite granite [high-K] L-911 granite out of plot, high Si granite [high-K] L-791 granite alkali granite granite [high-K] L-912 granite granite granite [high-K] L-793 granite granite granite [high-K] L-917 granite granite granite [high-K] L-797 granite granite granite [high-K] L-919 out of plot, high Si out of plot, high Si granite [high-K] L-798 granite granite granite [high-K] L-920 foidolite syenite foidolite L-799 granite granite granite [high-K] L-922 quartzmonzonite granite quartzmonzonite L-802 granite granite granite [high-K] L-923 granite granite granite [high-K] L-808 granite granite granite [high-K] L-924 granite granite granite [high-K] L-809 granite alkali granite granite [high-K] L-938 granite granite granite [high-K] L-810 granite granite granite [high-K] L-939 quartzmonzonite granite quartzmonzonite L-812 granite granite granite [high-K] L-940 quartzmonzonite gabbro-diorite syenite L-813 granite granite granite [high-K] L-943 granite granite granite [high-K] L-814 out of plot, high Si out of plot,high Si granite [low-K] L-945 quartzmonozonite granite granite [high-K] L-815 granite-quartz monzonite granite granite [high-K] L-946 quartzmonozonite granite granite [high-K] L-816 granite granite granite [medium-K] L-948 granite granite granite [high-K] L-816 granite L-951 syenite nepheline syenite syenite [comenditic] L-832 granite alkali granite granite [peralkaline, Al2O3>1.33Fe+4.4] L-952 quartz monzonite nepheline syenite syenite [comenditic] L-834 foid syenite syenite foid syenite L-955 quartz monzonite nepheline syenite syenite [comenditic] L-835 quartzmonzonite quartzmonzonite syenite L-956 monzonite syenite monzonite [Na2O-2>=K2O] L-836 quartzmonzonite granite quartzmonzonite L-957 granite granite granite [high-K] L-838 quartzmonzonite granite quartzmonzonite L-958 gabbro under-saturated olivine gabbro gabbro [subalkali] L-839 granite alkali granite granite [high-K] L-963 out of plot, high Si out of plot, high Si granite [low-K] L-840 granite granite granite [high-K] L-965 quartz monzonite quartz syenite quartzmonzonite L-842 quartzmonzonite granite L-966 quartz monzonite quartz syenite quartzmonzonite L-843 granite alkali granite granite [high-K] L-967 granite granite granite [high-K] L-844 quartzmonzonite granite granite [high-K] L-967a gabbro L-846 quartzmonzonite granite quartzmonzonite L-968 granite granite granite [high-K] L-849 granite alkali granite granite [high-K] L-969 foid syenite nepheline syenite foid syenite L-850 granite granite granite [high-K] L-971 syenite nepheline syenite syenite L-855 granite alkali granite granite [peralkaline, Al2O3>1.33Fe+4.4] L-973 granite granite granite [high-K] L-857 granite granite granite [high-K] L-975 granite granite granite [high-K] L-863 granodiorite granodiorite tonalite L-976 granite alkali granite granite [high-K] L-864 n.d. L-977 granite alkali granite granite [peralkaline, Al2O3>1.33Fe+4.4] L-864 granodiorite granodiorite tonalite L-978 granite alkali granite granite [peralkaline, Al2O3>1.33Fe+4.4] L-865 granodiorite granodiorite tonalite L-979 quartzmonzonite quartzmonzonite quartzomonzonite L-868 quartzmonzonite granite quartzmonzonite L-980 quartzmonzonite quartzmonzonite quartzomonzonite L-874 off plot out of plot, high Si granite [low-K] L-982 quartzmonzonite quartzmonzonite syenite L-874- quartzmonzonite granite quartzmonzonite L-983 granite granite granite [high-K] L-875 quartzmonzonite granodiorite quartzmonzonite L-985 granite granite granite [high-K] L-877 quartzmonzonite granite quartzmonzonite L-987a gabbro alkali gabbro gabbro [alkali] L-878 quartzmonzonite granite granite [high-K] L-987b foidolite theralite foid diorite Sample Middlemost de la Roche IUGS Sample Middlemost de la Roche IUGS L-990 monzodiorite monzo-gabbr o diorite [high-Mg, low-alkali, Boninite] LL2a granite alkali granite granite [high-K] L-991 gabbro under-saturated olivinie gabbro gabbro [subalkali] LL2b syenite quartz syenite granite [high-K] L-992 monzogabbr o under-saturated olivinie gabbro monzogabbro [k mzgb., Na2O-21.33Fe+4.4] P-13 quartzmonzonite quartz syenite syenite L-998 quartzmonzonite quartzmonzonite syenite P-17 quartzmonzonite quartz syenite syenite L-999 quartzmonzonite granite granite [high-K] P-25 monzodiorite essexite monzodiorite [Na2O-2>=K2)] L-1000 quartzmonzonite granite granite [high-K] P-26 granite quartz syenite granite [Peralkaline, Al2O3>1.33Fe+4.4] L-1002 granite alkali granite granite [high-K] P-28 syenite nepheline syenite syenite [comenditic] L-1003 quartzmonzonite quartzmonzonite syenite P-29 granite granite granite [high-K] L-1005 granite granite granite [high-K] P-32 granite alkali granite granite [peralkaline, Al2O3>1.33Fe+4.4] L-1007 quartzmonzonite quartzmonzonite syenite P-33 quartzmonzonite quartz syenite syenite [comenditic] L-1009 quartzmonzonite quartzmonzonite quartzmonzonite P-35 granite granite granite [high-K] L-1010 quartzmonzonite quartzmonzonite syenite P-39 granite alkali granite Granite [Peralkaline, Al2O3>1.33Fe+4.4] L-1011 quartzmonzonite quartzmonzonite syenite P-40i granite granite granite [high-K] L-1012 quartzmonzonite quartzmonzonite syenite P-40ii quartzmonzonite quartz syenite syenite [comenditic] L-1013 quartzmonzonite quartzmonzonite P-46 granite alkali granite granite [Peralkaline, Al2O3>1.33Fe+4.4] L-1014 granodiorite granodiorite granite [high-K] P-50 granite granite granite [Peralkaline, Al2O3>1.33Fe+4.4] L-1016 granite out of plot, high Si granite [lok-K] P-53 granite granite granite [high-K] L-1016a granite out of plot, high Si granite [peralkaline, Al2O3>1.33Fe+4.4] P-57 out of plot, foid nepheline syenite foid syenite [pe ralkaline] L-1019 granite alkali granite granite [peralkaline, Al2O3>1.33Fe+4.4] P-58 quartzmonzonite granite quartzmonzonite L-1020 granite granite granite [high-K] X-43 granite [high-K] L-1021 granite granite granite [high-K] X-44 granite [high-K] L-1022 foid monzosyenite nepheline syenite foid syenite X-45 quartzmonzonite L-1023 gabbro under-saturated olivine gabbro gabbro [alkali] X-46 granite [high-K] L-1024a out of plot, high Ca out of plot, high Ca foidolite X-47 granite [high-K] L-1024c out of plot, high Ca out of plot, high Ca foidolite X-48 granite [high-K] L-1025 peridot gabbro alkali gabbro peridot gabbro X-49 syenite L-1027 foid monzosyenite nepheline syenite foid monzosyenite X-50 syenite L-1032 gabbro alkali gabbro-under saturated oli v gabbro [alkali] X-51 syenite L-1037 quartzmonzonite quartzmonzonite syenite X-52 quartzmonzonite L-1038 quartzmonzonite granite quartzmonzonite X-53 granite [high-K] L-1039 granite alkali granite granite [high-K] X-54 granite [high-K] L-1039a granite granite [high-K] X-55 granite [high-K] L-1039c granite granite [high-K] X-56 tonalite L-1042Y granite granite granite [high-K] X-57 quartzmonzonite L-1043Z granite granite granite [high-K] X-58 granite [high-K] L-1044X X granite granite granite [high-K] X-59 granite [high-K] L-1045Yb quartzmonzonite quartzmonzonite syenite X-60 granite [high-K] L-1046XX b granite granite granite [high-K] X-61 granite [high-K] LJ1 quartzmonzonite granite quartzmonzonite X-62 syenite LL1 granite granite granite [high-K] X-63 syenite LL10 monzonite nepheline syenite monzonite [Na2O-2>=K2O] X-65 granite [high-K] LL11 granite granite granite [high-K] X-66 granite [high-K] LL13 diorite out of plot, high Ca, high Si diorite [low-K] X-67 granite [high-K] LL14 monzonite nepheline syenite monzonite [Na2O-2>=K2O] X-68 granite [high-K] LL15 syenite syenite syenite X-69 monzonite [Na2O-2=K2O] X-87 monzogabbr o syeno gabbro monzogabbro [Na2O-2>=K2O] X-88 foid-gabbro essexite melanephelinite X-89 foid-gabbro essexite foid diorite 2 2 9 APPENDIX A75 EXPERIMENT TO TEST THE QUALITY OF THE CHEMICAL LABORATORY: An experiment was carried out to test the chemical labor atory of the School of Geo sc ie nc es of the Univers i t y of the Witwatersrand. Samples L-012 and L-012A were used as double contro l sample s . The test was also designed to evaluat e the repr es e n t at i v i t y of single rock analys i s on the variou s diagra ms used for geochemic a l interpre t a t i o n in the Greater Lufilian Arc granitoi d resear ch project. Five kilogr a ms of rock sampl e were colle c te d from tw o outcrops of a large, well exposed pluton in the Hook Granite Batholith, Zambia . Macroscopically, the outcrop seemed to be very uniform in composition and grain size. Two types of experiments were carried out during the Lufilian Arc Granitoid project. Some were intend ed to evaluate the repr es entativity of single samples in a la rge outcro p . Another one was designed to evalua t e the accuracy of the laboratory. Only the second experiment will be de scribed here. Samples L-012 and L-012A were carefully crushed, ground and quartered. Thre e sample s were obtaine d from the fine powder of L-012 and sent along with the first three batches of sample s for analysis at the laboratory. Thes e were labeled L- 200B , L-400B and L-700B . L-012 and L-012A were analysed in the same batch of samples. Labora t or y resul t s are listed on Table 1. They plot as show n on Figs 1 and 2 on a logarit h m i c scale. Arithme t i c scales display simil ar resul ts . Fig 3 show s arith m e ti c- s cale diagrams of major oxides and trace elements for the five samples . Main conclu sions of the experiment were: 1) The quality of the laboratory is acceptab le for the type of resear ch intended, 2) Sample repeatability and general qua lity control of the laborator y were adequate for the type of resear ch , 3) The samples collecte d may be taken as represen tative of large granitoid bodies , and 4) Dispersion in results from analysis of the major oxides was very small. Assuming that instrume n t a l error is neglig i b l e , some ox ides tend to have greater dispersion than others. For example, TiO 2 , MnO, Na 2 O and P 2 O 5 are more variabl e than SiO 2 , Al 2 O 3 , MgO or K 2 O (Figs 1 and 3). Minor elements show somewha t similar results : Co, Ni, Cu, Zn and V display large dispersion, while Rb, Sr, Y,Zr, Cr and Ba are almost the same in all cases (Figs 1 and 3). The variatio n may be due to the mineral s that contain the given element s , and the size of those minerals in the rock. A few coarse- gr a in e d minera l s contain a large proportion of the total iron, Mn, P, Co, Cu, Zn, V and Cr. Fig 1 Logarithmic chemical data diag ram for five portions of the same sample. 0.01 0.10 1.00 10.00 100.00 1000.00 %SiO2 %TiO2 %Al2O3 %Fe2O3 %MnO %MgO %CaO %Na2O %K2O %P2O5 %LOI %TOTAL ppm Rb ppm Sr ppm Y ppm Zr ppm Nb ppm Co ppm Ni ppm Cu ppm Zn ppm V ppm Cr ppm Ba L- 012 L- 012A L- 200B L- 400B L- 700B 2 3 0 Fig 2 Logarithmic web representation of chemi cal data for five portions of the same sample Table 1. Duplicate analysis to evalua te precision of analytical results Sample SiO2 TiO2 Al2O3 Fe2O3 MnO MgO CaO Na2O K2O P2O5 LOI TOTAL Rb Sr Y Zr Nb Co Ni Cu Zn V Cr Ba L-012 6 4 . 19 0.6 6 17. 47 3 . 4 5 0.0 30 1.1 2 2.5 5 4 . 3 4 6 . 1 4 0 . 1 8 0 . 3 0 1 0 0 .4 3 1 4 1 5 2 9 3 8 3 8 7 3 6 7 9 7 42 46 3 6 9 6 8 L-012A 6 4 . 38 0.6 1 17. 86 3 . 1 8 0.0 30 1.1 3 2.4 0 4 . 1 0 6 . 2 4 0 . 1 5 0 . 3 2 1 0 0 .4 0 1 4 3 5 3 6 3 6 3 6 0 3 2 9 10 9 28 33 3 6 9 4 0 L-200B 6 3 . 93 0.6 7 17. 66 3 . 8 9 0.0 30 1.1 0 2.5 5 3 . 9 8 6 . 2 2 0 . 1 7 0 . 3 2 1 0 0 .5 2 1 4 0 5 2 7 3 8 3 6 2 3 5 9 9 12 41 46 3 6 9 4 0 L-400B 6 3 . 85 0.6 5 17. 33 3 . 8 4 0.0 40 1.1 1 2.4 9 4 . 2 7 6 . 0 6 0 . 1 8 0 . 3 0 1 0 0 .1 2 1 3 9 5 2 6 3 8 3 5 7 3 6 8 8 8 34 40 3 3 9 5 6 L-700B 6 4 . 12 0.6 6 17. 78 3 . 8 3 0.0 30 1.0 6 2.5 3 3 . 9 1 6 . 0 8 0 . 1 9 0 . 2 9 1 0 0 .4 8 1 4 0 5 2 9 3 7 3 7 4 3 5 8 8 10 29 44 3 2 9 4 4 Average 6 4 . 09 0.6 5 17. 62 3 . 6 4 0.0 32 1.1 0 2.5 0 4 . 1 2 6 . 1 5 0 . 1 7 0 . 3 1 1 0 0 .3 9 1 4 0 .6 5 2 9 .4 3 7 . 4 3 6 8 3 4 . 8 8.2 8.8 9.2 34. 8 41. 8 3 4 . 6 9 4 9 .6 Fig 3 Distribution of major oxides and minor el ements for five portions of the same sample. 0 .0 1 0 .1 0 1 .0 0 1 0 .0 0 1 0 0 .0 0 1 0 0 0 .0 0 L -0 1 2 L -0 1 2 A L -2 0 0 BL -4 0 0 B B % S iO 2 % T iO 2 % A l2 O 3 % F e 2 O 3 % MnO % Mg O % C aO % Na2 O % K 2 O % P 2 O 5 % L O I % T O T A L p p m R b p p m S r p p m Y p p m Z r p p m Nb p p m C o p p m Ni p p m C u p p m Z n p p m V p p m C r p p m B a 0 .0 0 .1 0 .2 0 .3 0 .4 0 .5 0 .6 0 .7 0 .8 L- 0 1 2 L- 0 1 2 A L- 2 0 0 B L- 4 0 0 B L- 7 0 0 B A ver ag e % Ti O2 % M nO % P2 O5 % LOI 0 2 4 6 8 1 0 1 2 1 4 L- 0 1 2 L- 0 1 2 A L- 2 0 0 B L- 4 0 0 B L- 7 0 0 B A v er ag e % F e2 O3 % M g O % C aO % N a2 O % K2 O p p m C o p p m N i p p m C u 0 2 0 0 4 0 0 6 0 0 8 0 0 1 0 0 0 1 2 0 0 L- 0 1 2 L- 0 1 2 A L- 2 0 0 B L- 4 0 0 B L- 7 0 0 B p p m R b p p m Sr p p m Z r p p m B a 0 1 0 2 0 3 0 4 0 5 0 6 0 7 0 L- 0 1 2 L- 0 1 2 A L- 2 0 0 B L- 4 0 0 B L- 7 0 0 B A v er ag e % Si O2 % A l 2 O3 p p m Y p p m N b p p m Z n p p m V p p m C r Sample number U (ppm ) Th (ppm) K (%) Time (BA) Heat producing value (H(t) muW-m3) U/Th Sample number U (ppm ) Th (ppm) K (%) Time (BA) Heat producing value (H(t) muW-m3) U/Th ppm ppm (%) t (BA) H(t) muW- m U/Th ppm ppm (%) t (BA) H(t) muW- m U/Th West Lusaka, Zambia L-410 7 32 4.34 0.55 2.966 0.22 L-175 3 25 4.6 0.55 2.400 0.12 L-411 3 7.5 0.35 0.55 0.649 0.40 L-181 3 7.5 0.24 0.55 0.635 0.40 L-433 7 7.5 2.33 0.55 1.016 0.93 L-195 8 7.5 5.03 0.55 1.389 1.07 L-434 3 7.5 4.77 0.55 1.212 0.40 L-199 8.85 38.67 0 0.55 2.927 0.23 L-435 3 7.5 6.45 0.55 1.426 0.40 L-207 0 0 6.27 0.55 0.799 L-436 26 99 4.81 0.55 8.202 0.26 L-207 pr o 9 132 6.27 0.55 10.181 0.07 L-437 3 7.5 4.4 0.55 1.165 0.40 L-208 9 132 6.13 0.55 10.163 0.07 L-438 7 22 3.75 0.55 2.199 0.32 L-209 3 7.5 1.91 0.55 0.848 0.40 L-439 19 90 5.46 0.55 7.462 0.21 L-210 7 74 0.09 0.55 5.327 0.09 L-440 3 7.5 2.19 0.55 0.884 0.40 L-212 8 79 7.04 0.55 6.587 0.10 L-441 6 19 5.3 0.55 2.161 0.32 L-213 12 163 4.87 0.55 12.232 0.07 L-442 3 44 7.61 0.55 4.097 0.07 L-214 7 104 3.92 0.55 7.889 0.07 L-443 3 100 6.79 0.55 7.863 0.03 L-215 3 193 0.19 0.55 13.450 0.02 L-444 6 7.5 1.98 0.55 0.943 0.80 L-217 3 7.5 2.97 0.55 0.983 0.40 L-458 8 7.5 6.94 0.55 1.632 1.07 L-218 8 99 5.43 0.55 7.764 0.08 L-459 3 7.5 1.16 0.55 0.752 0.40 L-222 7 20 4.74 0.55 2.187 0.35 L-460 3 20 2.33 0.55 1.765 0.15 L-223 8 21 5.2 0.55 2.344 0.38 L-461 3 15 5.34 0.55 1.803 0.20 L-224 8 19 5.69 0.55 2.268 0.42 L-462 3 16 5.19 0.55 1.853 0.19 L-416 6 7.5 0.73 0.55 0.784 0.80 L-463 3 7.5 1.01 0.55 0.733 0.40 X-90 5.9 0.55 0.752 L-464 29 7.5 0.52 0.55 1.417 3.87 X-90 pro x 8 19 5.9 0.55 2.295 0.42 L-465 24 7.5 0.43 0.55 1.262 3.20 Hook Granite, Zambia L-466 3 23 4.5 0.55 2.249 0.13 L-012 4.27 50.39 6.14 0.55 4.388 0.08 L-467 3 67 5.45 0.55 5.412 0.04 L-012A 3 49 6.24 0.55 4.268 0.06 X-43 5.46 0.55 0.696 L-079 0 0 4.98 0.55 0.635 X-44 5.77 0.55 0.735 L-237 3 26 5.44 0.55 2.576 0.12 X-45 4.63 0.55 0.590 L-238 6 24 6.16 0.55 2.616 0.25 X-46 4.57 0.55 0.582 L-239 6 24 6.16 0.55 2.616 0.25 X-47 6.08 0.55 0.775 L-242 7 7.5 1.96 0.55 0.969 0.93 X-48 4.44 0.55 0.566 L-248 6 7.5 2.1 0.55 0.958 0.80 X-49 4.57 0.55 0.582 L-248-L G 3 27 4.49 0.55 2.525 0.11 X-50 6.04 0.55 0.770 L-249 3 20 4.5 0.55 2.042 0.15 X-51 7 0.55 0.892 L-257 16 74 5.29 0.55 6.248 0.22 X-52 5.3 0.55 0.675 L-259 7 21 6.11 0.55 2.431 0.33 X-53 5.64 0.55 0.719 L-259-B 10 29 5.35 0.55 2.973 0.34 X-54 5.49 0.55 0.700 L-263 3 19 5.55 0.55 2.107 0.16 X-55 5.6 0.55 0.714 L-341 3 20 0.95 0.55 1.590 0.15 X-56 4.6 0.55 0.586 L-343 3 35 1.11 0.55 2.647 0.09 X-57 5.1 0.55 0.650 L-344 6 24 1.83 0.55 2.064 0.25 X-58 6.3 0.55 0.803 L-345 6 7.5 7.65 0.55 1.665 0.80 X-59 5.5 0.55 0.701 L-346 11 24 5.99 0.55 2.738 0.46 X-60 5.5 0.55 0.701 L-347 9 29 0.45 0.55 2.320 0.31 X-61 4.65 0.55 0.593 L-348 3 40 3.37 0.55 3.280 0.08 X-62 6.03 0.55 0.768 L-349 3 23 4.97 0.55 2.309 0.13 X-63 4.3 0.55 0.548 L-352 3 19 4.96 0.55 2.031 0.16 X-64 3.3 0.55 0.421 L-353 6 20 5.05 0.55 2.198 0.30 X-65 5.35 0.55 0.682 L-354 3 22 4.06 0.55 2.124 0.14 X-66 5.25 0.55 0.669 L-355 8 21 5.57 0.55 2.391 0.38 X-67 5.9 0.55 0.752 L-402 6 21 1.14 0.55 1.769 0.29 X-68 7.44 0.55 0.948 L-403 8 17 4.38 0.55 1.963 0.47 X-69 7.36 0.55 0.938 L-405 3 7.5 1.08 0.55 0.742 0.40 X-70 5.91 0.55 0.753 L-406 3 7.5 0.8 0.55 0.706 0.40 X-71 7.33 0.55 0.934 L-407 7 26 3.86 0.55 2.490 0.27 X-72 6.03 0.55 0.768 L-408 12 32 5.24 0.55 3.224 0.38 X-73 3.53 0.55 0.450 L-409 13 53 5.43 0.55 4.728 0.25 X-74 3.07 0.55 0.391 Table A76 Heat production capacity of intrusive rocks from the Greater Lufilian Arc at the time of their emplacement (Based on equation No. 4 by Gibson, 2002 ) Sample number U Th K Time Heat Cap U/Th Sample number U Th K Time Heat Cap U/Th X-75 4.92 0.55 0.627 L-029 3 7.5 2.5 1.89 1.308 0.40 P-39 19 71 5.57 0.55 6.163 0.27 L-030 16 40 5.91 1.89 4.989 0.40 P-46 10 46 6.89 0.55 4.345 0.22 L-047 6 7.5 4.75 1.89 2.031 0.80 P-50 62 256 4.88 0.55 20.096 0.24 L-049 3 7.5 0.93 1.89 0.888 0.40 P-53 21 43 5.92 0.55 4.329 0.49 L-050 3 7.5 0.89 1.89 0.877 0.40 P-57 10 51 5.52 0.55 4.516 0.20 L-060 4.91 46.54 1.12 1.89 3.714 0.11 P-58 4 24 4.27 0.55 2.318 0.17 L-060 3 7.5 5.74 1.89 2.175 0.40 P-40i 6 20 4.05 0.55 2.071 0.30 L-060 1.09 1.89 0.292 P-40ii 1 15 5.77 0.55 1.801 0.07 L-063 3 7.5 0.15 1.89 0.679 0.40 Kalengwa-Kasempa Area, Zambia L-064 3 7.5 0.05 1.89 0.652 0.40 L-139 3 26 7.87 0.55 2.886 0.12 L-065 3 7.5 0.12 1.89 0.671 0.40 L-311 8 7.5 0.84 0.55 0.855 1.07 L-357 3 7.5 3.59 1.89 1.600 0.40 L-313 7 7.5 0.8 0.55 0.821 0.93 L-358 3 7.5 2.31 1.89 1.257 0.40 L-314 3 7.5 0.36 0.55 0.650 0.40 L-359 3 7.5 4.84 1.89 1.934 0.40 L-318 3 7.5 0.56 0.55 0.676 0.40 L-360 3 7.5 6.02 1.89 2.250 0.40 L-321 3 7.5 0.05 0.55 0.611 0.40 L-361 3 7.5 2.06 1.89 1.190 0.40 L-322 3 27 7.57 0.55 2.917 0.11 L-366 3 7.5 4.28 1.89 1.785 0.40 L-323 3 30 8.21 0.55 3.206 0.10 L-368 3 7.5 4.64 1.89 1.881 0.40 L-324 13 48 6.29 0.55 4.492 0.27 L-371 3 7.5 4.06 1.89 1.726 0.40 L-325 6 27 6.75 0.55 2.899 0.22 L-374 3 7.5 3.92 1.89 1.688 0.40 P-13 10 56 3.89 0.55 4.653 0.18 L-380 3 18 5.94 1.89 2.955 0.17 P-17 11 48 5.62 0.55 4.350 0.23 L-420 13 37 2.98 1.89 3.876 0.35 P-25 1 2 1.71 0.55 0.385 0.50 L-421 3 57 6.69 1.89 5.851 0.05 P-26 6 76 0.03 0.55 5.429 0.08 Nepheline Sodalite Quarry, Zambia X-76 7.34 0.55 0.935 L-032 3 7.5 3.13 0.5 0.992 0.40 X-77 5.07 0.55 0.646 L-034 3 20 4.47 0.5 2.022 0.15 X-78 4.48 0.55 0.571 L-036 3 36 0.25 0.5 2.605 0.08 X-79 1.14 0.55 0.145 L-037 9 17 5.51 0.5 2.114 0.53 X-80 3.32 0.55 0.423 L-038 8 32 4.32 0.5 2.975 0.25 X-81 2.96 0.55 0.377 L-039 9 30 4.63 0.5 2.903 0.30 X-82 1.05 0.55 0.134 L-040 8 30 6.14 0.5 3.062 0.27 X-83 3.2 0.55 0.408 L-041 11 22 5.41 0.5 2.504 0.50 X-84 0.87 0.55 0.111 L-044 10 31 4.28 0.5 2.957 0.32 X-85 0.61 0.55 0.078 L-045 7.24 17.82 4.16 0.5 1.953 0.41 X-86 1.46 0.55 0.186 L-046 3 29 5.27 0.5 2.743 0.10 X-87 0.32 0.55 0.041 X-88 5.24 0.55 0.668 Basement to the Copperbelt, Zambia X-89 2.7 0.55 0.344 Muliashi Porphyry Northwestern Zambia Region, Zambia L-075 3 16 5.1 1.9 2.600 0.19 Archean rocks L-076 3 17 5.1 1.9 2.669 0.18 L-372 3 7.5 2.25 2.3 1.412 0.40 L-077 3 14 5.06 1.9 2.451 0.21 L-373 3 17 4.2 2.3 2.724 0.18 L-078 3 18 3.78 1.9 2.382 0.17 L-375 3 21 5.81 2.3 3.541 0.14 L-157 3 18 6.95 1.9 3.236 0.17 L-376 3 7.5 4.94 2.3 2.316 0.40 L-158 6 26 7.11 1.9 3.952 0.23 Paleoproterozoic rocks L-159 11 24 6.8 1.9 3.932 0.46 L-027 3 7.5 1.72 1.89 1.099 0.40 L-160 3 15 5.69 1.9 2.689 0.20 L-023 3 7.5 3.6 1.89 1.602 0.40 X-01 4.83 1.9 1.300 L-025 3 7.5 4.8 1.89 1.924 0.40 X-02 6.12 1.9 1.648 L-026 3 7.5 4.51 1.89 1.846 0.40 X-03 3.03 1.9 0.816 L-362 3 7.5 2.15 1.89 1.214 0.40 X-04 2.13 1.9 0.573 L-363 3 7.5 3.37 1.89 1.541 0.40 X-05 4.7 1.9 1.265 L-369 3 7.5 3.83 1.89 1.664 0.40 Chambishi Mine Area L-370 9 52 4.07 1.89 5.045 0.17 L-155 3 7.5 6.03 0.5 1.351 0.40 L-377 8 45 5.45 1.89 4.890 0.18 X-42 4.04 0.5 0.501 L-364 8 44 5.07 1.89 4.719 0.18 X-06 2.5 0.5 0.310 L-365 3 26 4.87 1.89 3.221 0.12 X-07 0.66 0.5 0.082 L-378 6 33 4.18 1.89 3.641 0.18 X-08 0.2 0.5 0.025 L-020 10 62 5.85 1.89 6.253 0.16 X-09 0.2 0.5 0.025 L-379 10 7.5 2.92 1.89 1.701 1.33 X-10 1.55 0.5 0.192 Other X-11 1.4 0.5 0.174 L-367 3 7.5 2.41 1.89 1.284 0.40 Samba "Porphyry" 0.5 0.000 L-023 3 7.5 3.6 1.89 1.602 0.40 L-268 3 19 4.53 1.9 2.653 0.16 L-024 6 7.5 0.43 1.89 0.874 0.80 L-269 3 7.5 3.67 1.9 1.627 0.40 L-028 3 17 3.07 1.89 2.117 0.18 L-273 3 7.5 3.12 1.9 1.479 0.40 Sample number U Th K Time Heat Cap U/Th Sample number U Th K Time Heat Cap U/Th L-279 6 20 3.08 1.9 2.453 0.30 L-898 5.14 1.8 1.309 Nchanga Granite L-899 3 16 3.72 1.8 2.170 0.19 X-34 5.01 0.88 0.766 L-900 3 16 4.01 1.8 2.244 0.19 X-35 4.9 0.88 0.750 L-902 3 25 4.81 1.8 3.070 0.12 X-36 4.4 0.88 0.673 L-903 3 25 4.99 1.8 3.116 0.12 X-37 4.9 0.88 0.750 L-904 3 21 4.81 1.8 2.794 0.14 X-38 2.9 0.88 0.444 L-905 3 22 1.54 1.8 2.030 0.14 X-39 11.9 0.88 1.821 L-906 3 19 5.97 1.8 2.951 0.16 X-40 15.5 0.88 2.371 L-907 3 16 5.07 1.8 2.514 0.19 P-28 13 98 5.32 0.88 7.989 0.13 L-908 3 15 2.63 1.8 1.824 0.20 P-29 9 65 5.56 0.88 5.621 0.14 L-909 3 18 4.96 1.8 2.625 0.17 L-151 11 65 5.54 0.88 5.680 0.17 L-910 3 7.5 4.24 1.8 1.715 0.40 L-153 11 44 4.89 0.88 4.129 0.25 L-911 3 19 5.19 1.8 2.752 0.16 L-154 3 44 5.78 0.88 4.018 0.07 L-912 3 16 5.3 1.8 2.573 0.19 L-162 3 7.5 4.92 0.88 1.364 0.40 L-917 3 7.5 4.48 1.8 1.777 0.40 Nchanga Mine L-919 3 7.5 2.09 1.8 1.168 0.40 L-150 6 7.5 6.12 0.5 1.447 0.80 L-920 3 7.5 2.72 1.8 1.328 0.40 L-167 12 37 8.7 0.5 3.977 0.32 L-922 3 16 4.88 1.8 2.466 0.19 L-168 3 7.5 7.61 0.5 1.547 0.40 L-923 3 21 4.67 1.8 2.758 0.14 L-170 10 7.5 5.02 0.5 1.425 1.33 L-924 3 19 3.97 1.8 2.442 0.16 L-172 5.31 48.48 7.48 0.5 4.429 0.11 L-938 3 7.5 4.11 1.8 1.682 0.40 L-173 7 58 7.51 0.5 5.139 0.12 L-939 3 7.5 5.28 1.8 1.980 0.40 Mufulira Granite L-940 3 7.5 3.4 1.8 1.501 0.40 X-41 4.65 0.5 0.576 L-943 3 28 5.72 1.8 3.509 0.11 L-166 3 15 4.54 0.5 1.685 0.20 L-945 3 19 5.08 1.8 2.724 0.16 Other L-946 3 7.5 5.01 1.8 1.912 0.40 L-163 3 7.5 3.69 0.5 1.061 0.40 L-948 3 15 4.47 1.8 2.292 0.20 L-161 3 30 6.26 0.5 2.935 0.10 L-951 3 22 0.33 1.8 1.722 0.14 X-12 0.5 0.000 L-952 3 7.5 0.35 1.8 0.725 0.40 X-13 0.8 0.5 0.099 L-955 3 7.5 0.19 1.8 0.684 0.40 X-14 0.86 0.5 0.107 L-956 3 7.5 0.01 1.8 0.638 0.40 Serenje, Zambia L-957 3 26 4.9 1.8 3.162 0.12 P-32 1 7 6.61 1.8 2.206 0.14 L-958 3 7.5 0.36 1.8 0.727 0.40 P-33 1 16 6.09 1.8 2.696 0.06 L-963 3 7.5 1.77 1.8 1.086 0.40 P-35 2 8 2.54 1.8 1.278 0.25 L-965 7 30 5.73 1.8 3.806 0.23 L-966 5.82 27.15 5.68 1.8 3.551 0.21 X-15 5.21 1.8 1.327 L-967 8 36 5.05 1.8 4.087 0.22 Kamanjab Inlier, Namibia L-967a 3 20 0 1.8 1.500 0.15 L-832 3 19 5.23 1.8 2.762 0.16 L-968 3 23 4.79 1.8 2.927 0.13 L-834 7 25 14.1 1.8 5.582 0.28 L-969 6 29 14.3 1.8 5.883 0.21 L-835 3 15 4.48 1.8 2.295 0.20 L-971 3 7.5 8.51 1.8 2.803 0.40 L-836 0 0 4.77 1.8 1.215 L-973 3 18 9.97 1.8 3.901 0.17 L-838 3.98 21.25 4.48 1.8 2.765 0.19 L-975 3 21 5.4 1.8 2.944 0.14 L-839 3 16 5.28 1.8 2.568 0.19 L-976 5.29 1.8 1.347 L-840 3 18 4.93 1.8 2.617 0.17 L-977 3 16 5.21 1.8 2.550 0.19 L-842 3 16 3.5 1.8 2.114 0.19 L-978 3.59 19.11 5.19 1.8 2.783 0.19 L-843 3 21 4.39 1.8 2.687 0.14 L-979 3 7.5 3.67 1.8 1.570 0.40 L-844 6 16 4.35 1.8 2.448 0.38 L-980 3 7.5 3.48 1.8 1.522 0.40 L-846 3 19 4.59 1.8 2.599 0.16 L-982 3 7.5 3.57 1.8 1.545 0.40 L-849 3 16 5.57 1.8 2.642 0.19 L-983 3 19 4.95 1.8 2.691 0.16 L-850 3 46 4.96 1.8 4.560 0.07 L-985 1.49 17.09 4.25 1.8 2.322 0.09 L-855 3 7.5 4.06 1.8 1.670 0.40 L-987a 3 7.5 1.59 1.8 1.040 0.40 L-857 3 7.5 4.21 1.8 1.708 0.40 L-987b 3 7.5 0.79 1.8 0.837 0.40 L-863 3 17 3.86 1.8 2.275 0.18 L-990 3 7.5 0.32 1.8 0.717 0.40 L-864 3.14 13.43 4.14 1.8 2.105 0.23 L-991 3 7.5 0.46 1.8 0.753 0.40 L-864 3 7.5 0 1.8 0.636 0.40 L-992 0.24 0.89 1.87 1.8 0.547 0.27 L-865 3 16 4.38 1.8 2.339 0.19 L-993 3 17 5.33 1.8 2.650 0.18 L-868 3 7.5 4.38 1.8 1.751 0.40 L-994 3 7.5 5.07 1.8 1.927 0.40 L-874 6 17 0.31 1.8 1.488 0.35 L-995 3 7.5 0.53 1.8 0.770 0.40 L-874a 4.99 1.8 1.271 L-996 2.82 14.88 4.78 1.8 2.356 0.19 L-875 3 7.5 4.25 1.8 1.718 0.40 L-997 3 33 5.33 1.8 3.756 0.09 L-877 3 17 4.74 1.8 2.499 0.18 L-998 3 7.5 4.03 1.8 1.662 0.40 L-878 3 17 4.58 1.8 2.459 0.18 L-999 3 16 4.65 1.8 2.407 0.19 L-895 3 7.5 4.61 1.8 1.810 0.40 L-1000 3 20 5.11 1.8 2.801 0.15 Sample number U Th K Time Heat Cap U/Th Sample number U Th K Time Heat Cap U/Th L-1002 3 28 4.97 1.8 3.318 0.11 L-1016a 3 7.5 0.13 0.75 0.627 0.40 L-1003 3 15 5.26 1.8 2.494 0.20 L-1019 1.82 17 3.79 0.75 1.769 0.11 L-1005 3 18 4.47 1.8 2.500 0.17 L-1020 3 19 3.14 0.75 1.850 0.16 L-1007 3 22 3.92 1.8 2.636 0.14 X-21 5.27 0.75 0.750 L-1009 3 16 4.42 1.8 2.349 0.19 X-22 5.64 0.75 0.803 L-1010 3 7.5 4.24 1.8 1.715 0.40 X-23 6 0.75 0.854 L-1011 3 17 4.43 1.8 2.420 0.18 X-24 5.19 0.75 0.739 L-1012 3 17 3.94 1.8 2.296 0.18 X-25 0.77 0.75 0.110 L-1013 3 19 4.72 1.8 2.633 0.16 X-26 1.1 0.75 0.157 C-1 5.09 1.8 1.296 Lofdal Farm, Namibia C-2 5.3 1.8 1.350 L-722 6 27 0 0.75 2.046 0.22 C-3 4.42 1.8 1.126 L-728 4.64 20.88 0.86 0.75 1.704 0.22 C-4 6.35 1.8 1.617 L-729 4.96 0.75 0.706 C-5 5.5 1.8 1.401 L-740 27 18 4.68 0.75 2.719 1.50 C-6 4.71 1.8 1.200 L-741 19 7.5 7.21 0.75 2.114 2.53 C-7 4.4 1.8 1.121 L-742 3 21 1.17 0.75 1.708 0.14 C-8 5.93 1.8 1.510 L-754 3 7.5 1.02 0.75 0.753 0.40 C-9 5.67 1.8 1.444 L-1021 3 18 4.02 0.75 1.906 0.17 C-10 3.6 1.8 0.917 L-1022 8 7.5 7.25 0.75 1.790 1.07 C-11 5.2 1.8 1.324 L-1023 3 7.5 0.87 0.75 0.732 0.40 C-13 (weath 1) 5.71 1.8 1.454 L-1024a 19 20 0.15 0.75 1.973 0.95 C-14 1.05 1.8 0.267 L-1024c 20 18 0.04 0.75 1.849 1.11 Felsic volcanics, Namibia L-1025 86.4 19.53 0.56 0.75 4.017 4.42 X-16 0.13 1.8 0.033 L-1027 3 7.5 6.88 0.75 1.588 0.40 X-17 0.3 1.8 0.076 L-1032 3 7.5 0.75 0.75 0.715 0.40 X-18 5.36 1.8 1.365 LR25 24 7730 0.01 0.75 535.017 0.00 X-19 5.18 1.8 1.319 LR23 15 130 0.1 0.75 9.450 0.12 X-20 5.02 1.8 1.279 LR20 0 36 0.04 0.75 2.494 0.00 Ugab River 2, Namibia LR5 26 2347 0.53 0.75 163.080 0.01 L-793 12 61 5.24 0.75 5.322 0.20 LR4 28 1593 0.04 0.75 110.953 0.02 L-797 6 37 4.63 0.75 3.396 0.16 AM-1 11 1019 0.75 70.777 0.01 L-798 7 27 5.17 0.75 2.812 0.26 Mesopotamie Farm, Copper Vallei Mine, Namibia L-799 7 7.5 4.84 0.75 1.417 0.93 L-759 3 7.5 5.54 0.75 1.397 0.40 L-802 3 15 4.55 0.75 1.774 0.20 L-772 3 7.5 10.1 0.75 2.042 0.40 Owka River, Botswana L-773 3 7.5 3.07 0.75 1.045 0.40 L-600A 3 43 5.55 0.75 3.852 0.07 L-783 3 27 5.15 0.75 2.689 0.11 L-602 3 36 4.54 0.75 3.225 0.08 L-784 7 26 5.07 0.75 2.729 0.27 L-605 3 42 5.47 0.75 3.772 0.07 Other alkaline and gabbroic rocks to compare with (used by Frets) L-606 3 38 5.19 0.75 3.455 0.08 X-27 0.75 0.75 0.107 Summas Mountains, Namibia, (Volcanic Rocks) X-28 3.81 0.75 0.542 L-789 8 15 5.21 0.75 2.018 0.53 X-29 5.57 0.75 0.793 L-791a 6 32 5.16 0.75 3.126 0.19 X-30 5.86 0.75 0.834 L-791b 8 17 5.85 0.75 2.248 0.47 X-31 4.4 0.75 0.626 Oas Farm, Namibia X-32 5.1 0.75 0.726 L-668 7 22 4.79 0.75 2.412 0.32 X-33 5.36 0.5 0.664 L-669 9 31 4.8 0.75 3.096 0.29 Otjiwarongo Environs, Namibia L-670 17 46 3.35 0.75 4.166 0.37 L-1037 3 105 7.49 0.55 8.298 0.03 L-675 10 78 6.41 0.75 6.603 0.13 L-1038 3 112 6.45 0.55 8.649 0.03 L-676 3 19 5.55 0.75 2.193 0.16 L-1039 3 26 5.51 0.55 2.585 0.12 L-691 3 7.5 2.82 0.75 1.010 0.40 L-1039a 3 7.5 6.14 0.55 1.387 0.40 L-693 2.29 8.612 4.46 0.75 1.299 0.27 L-1039c 3 32 5.94 0.55 3.055 0.09 L-694 3 7.5 4.89 0.75 1.304 0.40 LJ1 1 95 7.17 0.55 7.509 0.01 L-695 3 7.5 3.51 0.75 1.108 0.40 LL1 0 5 6.24 0.55 1.141 0.00 L-697 15 51 4.59 0.75 4.628 0.29 LL10 9 25 4.86 0.55 2.606 0.36 L-698 3 7.5 4.1 0.75 1.192 0.40 LL11 3 55 6 0.55 4.652 0.05 L-699 15 50 4.73 0.75 4.579 0.30 LL13 4 5 0 0.55 0.460 0.80 L-708 3 7.5 1.77 0.75 0.860 0.40 LL14 22 83 5 0.55 7.005 0.27 L-712 3 7.5 1.95 0.75 0.886 0.40 LL15 3 26 5 0.55 2.520 0.12 L-713 3 7.5 5.66 0.75 1.414 0.40 LL16 3 33 5 0.55 3.004 0.09 L-714 3 16 0.76 0.75 1.304 0.19 LL17a 5 3 7 0.55 1.243 1.67 L-714a 0 0 0.94 0.75 0.134 LL17b 4 18 5 0.55 1.996 0.22 L-715 3 19 4.88 0.75 2.098 0.16 LL18 5 4 7 0.55 1.312 1.25 L-716 7 24 3.98 0.75 2.435 0.29 LL2a 2 4 4.86 0.55 0.953 0.50 L-1016 3 7.5 0.09 0.75 0.621 0.40 LL2b 0 2 10.4 0.55 1.464 0.00 Sample number U Th K Time Heat Cap U/Th LL3a 0 7 5.93 0.55 1.240 0.00 LL3b 1 0 9.09 0.55 1.187 LL4 4 52 5.74 0.55 4.440 0.08 LL5 5 11 3.46 0.55 1.345 0.45 LL9 2 3 5.63 0.55 0.982 0.67 AVMIN Pegmatitic Granitoids, Namibia L-808 3 7.5 3.67 0.55 1.072 0.40 L-809 3 7.5 7.52 0.55 1.563 0.40 L-810 3 7.5 5.44 0.55 1.298 0.40 L-812 17 30 4.17 0.55 3.093 0.57 L-813 13 21 5.59 0.55 2.537 0.62 L-814 3 7.5 0.31 0.55 0.644 0.40 L-815 42 16 5.59 0.55 3.024 2.63 Grootfointein Inlier, Otavi Mountains, Namibia L-1014 L-1042 3 35 6.14 0.55 3.288 0.09 L-1043 3 44 5.77 0.55 3.863 0.07 L-1044 3 36 5.94 0.55 3.331 0.08 L-1045 3 57 1.7 0.55 4.243 0.05 L-1046 3 42 5.45 0.55 3.684 0.07 Okatjepuiko, Witvlei, Namibia L-625 3 7.5 2 1.1 0.961 0.40 L-626 3 7.5 1.04 1.1 0.795 0.40 L-633 3 7.5 1.69 1.1 0.908 0.40 L-635 3 7.5 0.22 1.1 0.654 0.40 L-637 3 7.5 0.76 1.1 0.747 0.40 L-638 3 7.5 3.73 1.1 1.260 0.40 L-641 3 7.5 0.62 1.1 0.723 0.40 L-645 3 7.5 0.16 1.1 0.643 0.40 L-648 3 7.5 1.32 1.1 0.844 0.40 L-649 3 7.5 1.86 1.1 0.937 0.40 L-816 3 7.5 1.96 1.1 0.954 0.40 Spitzkoppe Complexes, Namibia X-92 5.23 0.2 0.549 X-93 4.93 0.2 0.517 X-94 4.84 0.2 0.508 X-95 6.29 0.2 0.660 Erongo Complex, Namibia 0.2 0.000 X-96 5.07 0.2 0.532 Brandberg Complex, Namibi a 0.2 0.000 X-97 4.69 0.2 0.492 X-98 5.53 0.2 0.580 X-99 5.6 0.2 0.588 X-100 5.66 0.2 0.594 X-101 5.15 0.2 0.541 Nigerian Ring Complexes 0.2 0.000 AMN24 27 5.74 0.15 2.452 0.00 RN75 111 4.31 0.15 8.112 0.00 PAN112 25 5.17 0.15 2.256 0.00 JON147 41 5.32 0.15 3.377 0.00 B34 40 5.77 0.15 3.354 0.00 MD333 66 4.53 0.15 5.024 0.00 NG208 63 5.1 0.15 4.875 0.00 T15A 69 4.59 0.15 5.238 0.00 DR11 61 3.58 0.15 4.582 0.00 DW1 42 3.56 0.15 3.267 0.00 FG5 39 4.45 0.15 3.150 0.00 KD12 36 4.39 0.15 2.937 0.00 2 3 7 APPENDIX J RAW DATA FOR NEW GEOCHRONOLOGY A77.1 Raw data obtaine d for SHRIMP II U-Pb dating at the Australian National Univer sity, Canberra , 238 L-030, 238 L-075, 238 L-158, 238 L-160, 239 L-207, 239 L-213, 240 L-638, 240 L-688, 241 A77.2 Raw data and proc es s in g for zircon dating using U-Pb laser- a b l a t io n ICP-MS techniq u e , 242 L-855, 242 L-868, 242 L-943, 242 L-969, 242 L-993, 243 L-1013, 243 L-1043, 243 A78 CONCORDIA DIAGRAMS, 244 A78.1 Sample L-030, 244 A78.2 Sample L-047, 244 A78.3 Sample L-075, 245 A78.4 Sample L-158, 245 A78.5 Sample L-160, 246 A78.6 Sample L-207, 246 A78.7 Sample L-213 Conc or d i a diagra m for high U zircons + rims , 247 A78.8 Sample L-213 Conc or di a diagram for cores and rims, 247 A78.9 Sample L-638 Conc or d i a diagram for all zircons includ i n g xenocrys t s , 248 A78.10 Sample L-638 Conc or dia diagram for main clus ter of zircons, 248 A78.11 Sample L-688 Conc or di a diagram for all zircons, 249 A78.12 Sample L-688 Histog ram of all 12 ages in main clus ter, 249 A78.13 Sample L-693, 250 A78.14 Sample L-868, 250 A78.15 Sample L-855 Conc or di a diagram for all zircons, 251 A78.16 Sample L-855 Conc or dia diagram for main clus ter of ages, 251 A78.17 Sample L-943 Conc or di a diagram for all zircons, 252 A78.18 Sample L-943 Conc or dia diagram for main clus ter of zircons, 252 A78.19 Sample L-969, 253 A78.20 Sample L-993, 253 A78.21 Sample L-1013 first, 254 A78.22 Sample L-1013 second, 254 A78.23 Sample L-1043 concord ia diagram for older group of zircons , 255 A78.24 Sample L-1043 concordia diagram fo r younger group of zircons , 255 A78.25 Sample L-1043 concord ia diagram for all zircons 2, 256 A78.26 Sample L-1043 concord ia diagram for all zircons 1, 256 page 1/ 4 Grain spot % 206Pbc ppm U ppm 232Th/ 238U 232Th/ 238U ppm20 6Pb* (1) 206Pb/ 238U error (1) 207Pb/2 06Pb error % discordant (1) 207Pb/206 Pb ?% (1) 207Pb/2 35U ?% (1) 206Pb/2 38U ?% err corr 1.1 0.04 827 452 0.56 235 1841 15 1925 4.4 5 0.11793 0.25 5.375 0.94 0.3306 0.91 0.964 2.1 8.18 319 82 0.27 61.6 1209 19 1868 180 54 0.114 10.00 3.25 10.00 0.2064 1.80 0.172 3.1 1.53 3305 732 0.23 495 1021.8 9.4 1609 64 57 0.0992 3.40 2.349 3.60 0.1718 10.00 0.28 4.1 2.40 2406 315 0.14 441 1220 14 1655 140 36 0.1017 7.40 2.92 7.60 0.2083 1.30 0.17 5.1 0.03 520 272 0.54 149 1859 14 1932.6 6.1 4 0.11842 0.34 5.459 0.92 0.3343 0.85 0.928 6.1 0.51 523 465 0.92 122 1543 12 1935 12 25 0.11861 0.66 4.421 1.10 0.2703 0.88 0.798 7.1 2.18 2193 255 0.12 286 893 7 1706 48 91 0.1045 2.60 2.141 2.80 0.1486 0.84 0.306 Grain spot % 206Pbc ppm U ppm 232Th/ 238U 232Th/ 238U ppm20 6Pb* (1) 206Pb/ 238U error (1) 207Pb/2 06Pb error % discordant (1) 207Pb/206 Pb ?% (1) 207Pb/2 35U ?% (1) 206Pb/2 38U ?% err corr 1.1 0.08 194 176 0.94 55.8 1858 11 1864.9 8.9 0 0.11405 0.49 5.253 0.84 0.334 0.68 0.812 2.1 0.06 171 135 0.81 49.7 1872 11 1856.1 8.2 -1 0.11349 0.45 5.273 0.82 0.3369 0.68 0.833 3.1 0.09 116 81 0.72 33.5 1869 17 1863 11 0 0.11392 0.63 5.284 1.20 0.3364 1.10 0.862 3.2 0.06 174 99 0.59 52 1924 13 1869.1 9.5 -3 0.11431 0.53 5.482 0.92 0.3478 0.75 0.819 4.1 0.06 175 130 0.77 51 1884 12 1857.1 9.3 -1 0.11356 0.52 5.315 0.88 0.3395 0.72 0.811 5.1 0.01 226 206 0.94 63.6 1828 11 1869.7 7.4 2 0.11435 0.41 5.168 0.80 0.3278 0.69 0.859 6.1 0.04 281 231 0.85 82.2 1889 12 1870.8 7 -1 0.11442 0.39 5.373 0.84 0.3406 0.74 0.886 7.1 0.06 142 143 1.04 41.2 1878 12 1860 11 -1 0.11373 0.61 5.304 0.97 0.3382 0.75 0.774 8.1 0.08 143 136 0.98 40.6 1837 12 1862.6 9.4 1 0.1139 0.52 5.178 0.91 0.3297 0.75 0.822 9.1 0.41 361 401 1.15 93.8 1696.8 9.6 1859 23 10 0.1137 1.20 4.719 1.40 0.3011 0.64 0.457 9.2 0.24 163 148 0.94 43.2 1729 14 1882 14 9 0.11514 0.75 4.885 1.20 0.3077 0.95 0.782 Error in Standard calibration was 0.23% ( not incuded in above errors, but re q uired when com p arin g data from different mount s Grain spot % 206Pbc ppm U ppm 232Th/ 238U 232Th/ 238U ppm20 6Pb* (1) 206Pb/ 238U error (1) 207Pb/2 06Pb error % discordant (1) 207Pb/206 Pb ?% (1) 207Pb/2 35U ?% (1) 206Pb/2 38U ?% err corr 2.1 2.84 159 153 1.00 32.7 1347 12 1893 59 29 0.1158 3.30 3.71 3.40 0.2324 0.98 0.286 2.2 0.06 340 320 0.97 99.7 1891 16 1865.7 7 -1 0.1141 0.39 5.362 1.00 0.3408 0.95 0.925 3.1 0.01 118 153 1.34 34.7 1897 19 1891 11 0 0.11574 0.62 5.461 1.30 0.3422 1.10 0.878 3.2 0.05 121 216 1.84 34.6 1847 27 1872.3 9.1 1 0.11452 0.50 5.239 1.80 0.3318 1.70 0.959 4.1 0.72 173 286 1.71 47.6 1785 15 1914 22 7 0.1172 1.20 5.155 1.60 0.3189 0.94 0.603 5.1* 32.83 3365 244 0.07 392 562 18 1360 1200 142 0.087 62.00 1.09 64.00 0.0911 3.30 0.052 6.1 0.17 320 364 1.17 92.7 1872 26 1883.4 7.7 1 0.11522 0.43 5.352 1.70 0.3369 1.60 0.967 7.1 0.10 108 150 1.44 31.3 1873 27 1879.5 9.3 0 0.11498 0.51 5.345 1.70 0.3372 1.60 0.955 8.1 4.32 607 154 0.26 127 1349 22 1745 92 23 0.1067 5.00 3.43 5.30 0.2328 1.80 0.334 9.1 0.71 196 224 1.18 50 1666 24 1862 17 11 0.1139 0.96 4.629 1.90 0.2949 1.60 0.859 10.1 0.08 224 274 1.26 63.8 1843 27 1868.3 7.2 1 0.11427 0.40 5.214 1.70 0.3309 1.70 0.973 11.1 0.05 258 306 1.23 70.4 1775 25 1873.9 6.1 5 0.11462 0.34 5.01 1.60 0.317 1.60 0.978 12.1 0.24 158 236 1.54 42.5 1749 25 1852 13 6 0.11324 0.70 4.867 1.80 0.3117 1.60 0.92 13.1 5.88 144 153 1.10 33.7 1473 23 1808 120 19 0.1105 6.80 3.91 7.00 0.2568 1.70 0.249 14.1 3.09 223 210 0.97 50 1454 21 1825 63 20 0.1116 3.50 3.89 3.80 0.253 1.60 0.423 * = emba y ment. (Errors are 1-sigma; Pbc and Pb* indicate the common and radiogenic portions, respectively. (1) Common Pb corrected using measu red 204Pb.) Data provided by Richard Armstrong, PRISE Institute. Table A77.1 Raw data obtained for SHRIMP II U-Pb dating at the Australian National University, Canberra L-158 L-075 L-030 page 2/ 4 Grain spot % 206Pbc ppm U ppm 232Th/ 238U 232Th/ 238U ppm20 6Pb 206Pb/ 238U error 207Pb/2 06Pb error % discordant 207Pb/206 Pb ?% 207Pb/2 35U ?% 206Pb/2 38U ?% err corr L-160 1.1 0.03 201 172 0.89 59.3 1906 15 1860.1 7.6 -2 0.11374 0.42 5.394 1.00 0.3439 0.93 0.91 2.1 0.04 201 154 0.79 59.1 1896 13 1863.6 8.4 -2 0.11397 0.47 5.375 0.92 0.342 0.79 0.862 3.1 0.18 39 62 1.61 11.4 1862 18 1874 21 1 0.1146 1.20 5.293 1.60 0.3349 1.10 0.691 4.1 0.04 181 171 0.98 52.1 1866 12 1871.9 8.4 0 0.11449 0.46 5.299 0.85 0.3357 0.71 0.841 5.1 0.04 220 181 0.85 63.5 1865 11 1866.9 7.6 0 0.11418 0.42 5.281 0.81 0.3354 0.69 0.853 6.1 0.04 435 344 0.82 124 1851 10 1871.4 5.5 1 0.11446 0.31 5.25 0.70 0.3326 0.63 0.898 7.1 0.06 149 151 1.05 43.6 1892 14 1868 10 -1 0.11427 0.57 5.373 1.00 0.341 0.85 0.831 7.2 0.03 111 108 1.01 31.9 1863 16 1857 10 0 0.11357 0.58 5.246 1.10 0.335 0.98 0.86 7.3 0.01 259 237 0.95 73.9 1851 15 1869.4 7 1 0.11433 0.39 5.244 0.99 0.3327 0.91 0.921 8.1 0.04 287 184 0.66 77.8 1767 10 1856.7 6.8 5 0.11353 0.38 4.938 0.75 0.3154 0.65 0.864 Error in Standard calibration was 0.23% ( not incuded in above errors, but re q uired when com p arin g data from different mount s Grain spot % 206Pbc ppm U ppm 232Th/ 238U 232Th/ 238U ppm20 6Pb* (1) 206Pb/ 238U error (1) 207Pb/2 06Pb error % discordant (1) 207Pb/206 Pb ?% (1) 207Pb/2 35U ?% (1) 206Pb/2 38U ?% err corr 1.1 0.03 3670 619 0.17 266 521.5 2.8 544.4 6.4 4 0.05839 0.29 0.6784 0.64 0.0843 0.57 0.888 2.1 - 4107 924 0.23 302 529.8 2.9 541.3 6.5 2 0.05831 0.30 0.6887 0.64 0.0857 0.57 0.887 3.1 - 4469 997 0.23 326 525.2 2.9 540.9 5.1 3 0.05829 0.24 0.6882 0.61 0.0849 0.57 0.923 4.1 0.02 3236 415 0.13 239 531.1 2.9 536 6.3 1 0.05817 0.29 0.6887 0.64 0.0859 0.57 0.893 5.1 0.02 1592 217 0.14 117 528.4 3.1 534 12 1 0.05811 0.55 0.6884 0.82 0.0854 0.61 0.741 6.1 0.01 1392 760 0.23 242 513.5 3 550.2 6.3 7 0.05854 0.29 0.6693 0.67 0.0829 0.60 0.901 7.1 - 5836 1568 0.28 435 536 2.9 542 4.5 1 0.05833 0.21 0.6973 0.60 0.0867 0.56 0.939 8.1 - 3562 1465 0.42 257 520 2.8 537.8 5.7 3 0.05821 0.26 0.6742 0.63 0.0884 0.57 0.908 9.1 0.00 17119 29182 1.76 1530 637 16 531.8 4.2 -17 0.05805 0.19 0.831 2.70 0.1038 2.70 0.997 10.1 0.00 3280 362 0.11 237 520.4 3.3 531.7 6.3 2 0.05805 0.27 0.6729 0.72 0.0841 0.66 0.916 11.1 0.01 2305 482 0.22 165 515.6 3 547.1 8.6 6 0.05846 0.40 0.6712 0.72 0.0833 0.60 0.834 12.1 0.00 1076 235 0.23 79.5 531.8 3.2 536 11 1 0.05816 0.50 0.6896 0.80 0.086 0.62 0.776 13.1 0.00 659 96 0.15 48.9 533.3 3.2 540 13 1 0.05827 0.61 0.6928 0.87 0.0862 0.63 0.72 14.1 0.08 749 60 0.08 54.5 524.4 3.1 530 16 1 0.05802 0.72 0.6779 0.95 0.0847 0.63 0.655 15.1 0.03 2825 625 0.23 204 519.9 2.9 524 7.2 1 0.05785 0.33 0.6699 0.67 0.084 0.58 0.869 Error in Standard calibration was 0.23% ( not incuded in above errors, but re q uired when com p arin g data from different mount s L-207 Raw data obtained for SHRIMP II U-Pb dating at the Australian National University, Canberra Data provided by Richard Armstrong, PRISE Institute. (Errors are 1-sigma; Pbc and Pb* indicate the common and radiogenic portions, respectively. (1) Common Pb corrected using measu red 204Pb.) page 3/ 4 Grain spot % 206Pbc ppm U ppm 232Th/ 238U 232Th/ 238U ppm20 6Pb* (1) 206Pb/ 238U error (1) 207Pb/2 06Pb error % discordant (1) 207Pb/206 Pb ?% (1) 207Pb/2 35U ?% (1) 206Pb/2 38U ?% err corr 1.1 2.76 441 945 2.21 23.7 380.3 3.9 517 150 26 0.0577 7.00 0.483 7.10 0.0608 1.10 0.149 2.1c 0.05 308 263 0.88 90.5 1895 14 1869.6 6.4 -1 0.11435 0.36 5.388 0.95 0.3418 0.88 0.927 2.2c 0.06 781 486 0.64 235 1933 27 1864.7 3.9 -4 0.11404 0.22 5.498 1.60 0.3497 1.60 0.991 3.1 0.15 447 503 1.16 32 516 4.4 562 23 8 0.05886 1.00 0.6764 1.40 0.0833 0.89 0.647 3.2 0.18 492 791 1.66 34.6 506.4 7.8 537 20 6 0.05818 0.90 0.656 1.80 0.0817 1.60 0.873 4.1 0.14 336 315 0.97 24.1 515.9 5.3 555 29 7 0.05866 1.30 0.674 1.70 0.0833 1.10 0.62 5.1 1.64 595 1616 2.81 46.6 553.8 5 521 82 -6 0.0578 3.70 0.715 3.90 0.0897 0.95 0.245 6.1c 0.14 216 256 1.23 60.8 1826 26 1877.9 8.1 3 0.011487 0.45 5.188 1.70 0.3275 1.60 0.963 7.1 4.18 685 1617 2.44 46.8 473.7 7.4 486 200 3 0.0569 8.90 0.598 9.10 0.0763 1.60 0.179 8.1 7.00 2457 7179 3.02 69.5 194.4 3.5 522 330 63 0.0578 15.00 0.244 15.00 0.0306 1.90 123 9.1c 0.03 157 215 1.41 43.8 1812 26 1891.7 7.1 4 0.11576 0.39 5.181 1.70 0.3246 1.60 0.972 9.2c 0.01 167 205 1.26 43 1687 24 1882.8 7.6 10 0.11519 0.42 4.75 1.70 0.2991 1.60 0.968 10.1 0.46 601 899 1.54 40.1 479.3 8.1 575 47 17 0.0592 2.20 0.63 2.80 0.0772 1.70 0.625 11.1c 0.02 457 260 0.59 124 1764 25 1863.5 6.3 5 0.11396 0.35 5.945 1.60 0.3147 1.60 0.977 12.1 ### # 2336 6723 2.97 183 500.9 8.5 694 490 28 0.063 23.00 0.7 23.00 0.0808 1.80 0.076 c = core Grain spot % 206Pbc ppm U ppm 232Th/ 238U 232Th/ 238U ppm20 6Pb* (1) 206Pb/ 238U error (1) 207Pb/2 06Pb error % discordant (1) 207Pb/206 Pb ?% (1) 207Pb/2 35U ?% (1) 206Pb/2 38U ?% err corr 1.1 0.60 171 91 0.55 27.5 1105.1 10 1095 16 -1 0.076 0.80 1.96 1.30 0.187 1.00 0.785 2.1 1.43 258 149 0.60 42 1104.7 9.6 801 68 -28 0.0658 3.20 1.7 3.40 0.1869 0.90 0.281 3.1 0.02 462 439 0.98 73.9 1098.9 8.8 1102 11 0 0.0763 0.50 1.95 1.00 0.1859 0.90 0.854 4.1 0.13 188 109 0.60 29.7 1087 11 1090 23 0 0.0758 1.10 1.92 1.50 0.1837 1.10 0.683 5.1 0.05 133 86 0.67 32.2 1193.9 11 1133 17 -5 0.0775 0.80 2.17 1.30 0.2035 1.00 0.768 6.1 - 291 252 0.90 46.5 1101.3 9.1 1095 12 -1 0.076 0.60 1.95 1.10 0.1863 0.90 0.843 7.1 0.01 164 99 0.62 25.8 1083 9.5 1086 15 0 0.0757 0.80 1.91 1.20 0.1829 1.00 0.786 8.1 - 275 257 0.96 78.5 1849.7 14.2 1871 6.8 1 0.1144 0.40 5.24 1.00 0.3323 0.90 0.92 9.1 - 205 131 0.66 33 1107.1 9.8 1091 18 -1 0.0759 0.90 1.96 1.30 0.1874 1.00 0.733 10.1 0.17 167 100 0.62 26.9 1105.3 11 1100 24 0 0.0762 1.20 1.97 1.60 0.187 1.10 0.662 11.1 0.08 347 309 0.92 54.2 1076 8.8 1090 12 1 0.0758 0.60 1.9 1.10 0.1817 0.90 0.827 12.1 0.03 311 241 0.80 50.3 1111.6 9.1 1094 11 -2 0.076 0.60 1.97 1.10 0.1882 0.90 0.842 13.1 - 299 232 0.80 48 1105.9 9.1 1113 11 1 0.0767 0.60 1.98 1.10 0.1871 0.90 0.844 Error in Standard calibration was 0.29% ( not incuded in above errors, but re q uired when com p arin g data from different mount s L-638 L-213 Data provided by Richard Armstrong, PRISE Institute. (Errors are 1-sigma; Pbc and Pb* indicate the common and radiogenic portions, respectively. (1) Common Pb corrected using measu red 204Pb.) page 4/4 Grain spot % 206Pbc ppm U ppm 232Th/ 238U 232Th/ 238U ppm20 6Pb* (1) 206Pb/ 238U error (1) 207Pb/2 06Pb error % discordant (1) 207Pb/206 Pb ?% (1) 207Pb/2 35U ?% (1) 206Pb/2 38U ?% err corr 1.1 6.61 2382 1633 0.71 90.44 260.6 2.4 647 280 60 0.0612 13.00 0.348 13.00 0.0413 0.95 0.072 2.1 0.20 216 67 0.32 22.6 738.9 6.6 774 31 5 0.06499 1.50 1.088 1.80 0.1214 0.95 0.537 3.1 7.34 2563 3230 1.30 123 324.5 3.1 745 300 56 0.0641 14.00 0.456 14.00 0.0516 0.98 0.069 4.1 0.04 283 265 0.97 29.8 746.1 7.1 745 18 0 0.06411 0.85 1.085 1.30 0.1227 1.00 0.763 5.1 0.00 189 135 0.74 20.5 765.3 8.2 754 20 -1 0.06436 0.93 1.119 1.50 0.126 1.10 0.772 6.1 0.07 175 148 0.87 19.2 774.1 7.2 775 22 0 0.06503 1.00 1.144 1.40 0.1276 0.98 0.689 7.1 0.66 229 78 0.35 21.3 658.2 6 726 51 9 0.0635 2.40 0.941 2.60 0.1075 0.96 0.368 7.2 0.41 509 381 0.77 48.7 678 5.6 738 27 8 0.0639 1.30 0.977 1.50 0.1109 0.88 0.57 8.1 7.64 1536 2115 1.42 91.9 401.9 3.9 732 310 45 0.0637 15.00 0.565 15.00 0.0643 0.99 0.068 9.1 0.31 397 451 1.17 39.7 707 6 764 24 7 0.06468 1.20 1.034 1.50 0.1159 0.89 0.612 10.1 0.11 171 137 0.83 18.4 758.7 7.4 755 24 0 0.06442 1.20 1.109 1.50 0.1249 1.00 0.666 11.1 - 275 234 0.88 29.7 763.4 8.2 771 16 1 0.0649 0.78 1.125 1.40 0.1257 1.10 0.825 12.1 0.16 152 102 0.70 15.2 708.3 6.7 754 30 6 0.06436 1.40 1.031 1.70 0.1161 1.00 0.581 13.1 0.00 78 37 0.49 8.11 735 14 770 31 5 0.06488 1.50 1.08 2.50 0.1207 2.00 0.8 14.1 0.01 608 399 0.68 64.8 754.2 6.1 769 12 2 0.06483 0.56 1.109 1.00 0.1241 0.86 0.84 Error in Standard calibration was 0.29% ( not incuded in above errors, but re q uired when com p arin g data from different mount s L-688 (Errors are 1-sigma; Pbc and Pb* indicate the common and radiogenic portions, respectively. (1) Common Pb corrected using measu red 204Pb.) Raw data obtained for SHRIMP II U-Pb dating at the Australian National University, Canberra Data provided by Richard Armstrong, PRISE Institute. page 1/2 SAMPLE 2 ? % 2 ? % 2 ? % spot # file 207/235 7/5 err 206/238 6/8 err Rho 207/206 7/6 err 207/235 206/238 207/206 7/5 age 1 sigma 6/8 age 1sigma 7/6 age 1 sigma 17 de07a73 1 3.8861689 0.2723272 0.2181177 0.0154914 0.5719453 0.0474051 0.1490011 0.0151776 14.015202 14.20461 20.372445 1610.8123 56.591665 1271.9214 81.982128 2334.4934 174.38964 18 de07a74 1 5.8943952 1.0937442 0.3293116 0.1008497 0.9584352 0.95 0.12692 0.0115705 37.111329 61.248819 18.232759 1960.409 161.08292 1835.04 41 489.06453 2055.7429 160.90729 20 de07a76 1 5.7359715 0.4308339 0.3494882 0.0222455 0.8483357 -0.148335 0.1222516 0.0048565 15.022176 12.730309 7.9451708 1936.8046 64.94407 2 1932.154 106.26507 1989.3445 70.655851 21 de07a78 1 5.9298652 0.4346084 0.3630994 0.022412 0.8827698 0.7536593 0.1175504 0.0038614 14.658289 12.344814 6.5698489 1965.6195 63.680024 1996.8483 105.99144 1919.3124 58.908056 22 de07a79 1 5.5746854 0.2218629 0.3430592 0.0106765 0.7941551 0.9566402 0.1215528 0.0028948 7.9596572 6.2242983 4.763049 1912.1965 34.264127 1901.37 51.245124 1979.1435 42.407829 25 de07a82 1 5.7703022 0.34888 0.3647025 0.0199801 0.8351765 0.3830381 0.1172916 0.0042315 12.092261 10.956951 7.2153921 1941.9665 52.323639 2 004.425 94.379716 1915.3593 64.726662 26 de07a83 1 2.2541158 0.2621079 0.1059486 0.0163581 0.9519029 0.95 0.1559413 0.0077499 23.255937 30.879257 9.9394641 1198.0714 81.785625 649. 17625 95.348855 2412.1205 84.400941 27 de07a84 1 5.6765228 0.4230757 0.3652015 0.0203673 0.8606453 0.95 0.1176787 0.003883 14.906155 11.154012 6.5993234 1927.8035 64.342452 2006. 7819 96.173431 1921.269 59.158596 28 de07a85 1 6.0652984 0.3150475 0.3533505 0.0213286 0.828722 -0.730174 0.1235805 0.0050376 10.388523 12.072204 8.1527167 1985.2721 45.276764 1950.5777 101.5945 2008.5532 72.340187 27 de07a59 1 5.6814046 0.2714572 0.3477042 0.0193947 0.8395116 -2.092603 0.1261072 0.0045526 9.5559906 11.155887 7.2202198 1928.5457 41.25376 4 1923.6262 92.770017 ######### ######### 4 de07a60 1 5.8364594 0.2499059 0.3562104 0.0136202 0.7730637 -1.409699 0.1176722 0.0036919 8.5636146 7.6472704 6.2748793 1951.8403 37.117204 1964.1861 64.740227 1921.1691 56.250835 5 de07a61 1 5.6451029 0.2597258 0.3525353 0.0138085 0.1532033 -13.67142 0.1777832 0.044917 9.201811 7.8338504 50.530055 1923.0138 39.686553 19 46.6933 65.813874 2632.2986 419.82811 7 de07a70 1 5.5665511 0.3622369 0.3634626 0.0151121 0.6938889 0.2887536 0.1145689 0.0049434 13.014769 8.3156224 8.6295234 1910.9395 56.012536 1998.5654 71.449538 1873.1152 77.804437 8 de07a64 1 5.5555309 0.3968726 0.3497276 0.0188052 0.8562946 0.4650214 0.1194884 0.0038753 14.287475 10.754187 6.48656 1909.234 61.4714 1933. 2978 89.815153 1948.5864 57.960307 9 de07a65 1 5.7973008 0.4583302 0.3465556 0.0261189 0.4123277 -0.137801 0.15018 0.0250085 15.811847 15.073443 33.304681 1946.0076 68.465513 19 18.1299 125.04009 2347.9771 284.68857 10 de07a66 1 5.7187663 0.3694023 0.3596408 0.0198537 0.6735214 0.6411648 0.1153613 0.0069892 12.918951 11.040878 12.117002 1934.2078 55.82644 4 1980.4708 94.131841 1885.5348 109.08495 11 de07a67 1 5.827115 0.3255682 0.3380223 0.0246191 0.8456335 -1.330556 0.1288558 0.0059238 11.174251 14.566574 9.1944238 1950.4515 48.421108 1877.1482 118.61172 2082.4203 80.896854 12 de07a68 1 5.6436119 0.353291 0.3624487 0.0171024 0.7614459 0.8891728 0.1151226 0.0046244 12.520033 9.4371225 8.0339408 1922.786 53.995586 1 993.77 80.91968 1881.804 72.359016 13 de07a69 1 5.8262672 0.3385881 0.3611168 0.0174379 0.71151 0.7020767 0.1181978 0.0056368 11.622816 9.6577658 9.5378563 1950.3254 50.363787 1 987.4652 82.588044 1929.1557 85.420724 1 de07a37 1 5.5790795 0.3447373 0.3394403 0.015608 0.3102493 -0.745717 0.1441734 0.0203134 12.358215 9.196332 28.179083 1912.8749 53.205077 18 83.9764 75.117806 2277.9373 242.66225 4 de07a32 1 5.2631163 0.2877905 0.3381076 0.0218543 0.8463948 -0.761206 0.1215086 0.0049418 10.936126 12.927443 8.1340149 1862.9008 46.656902 1877.5594 105.28458 1978.4959 72.426712 5 de07a33 1 5.1460642 0.2912204 0.2320183 0.0126158 0.7475899 0.6604485 0.169195 0.0081732 11.31818 10.87487 9.6612601 1843.7446 48.112136 134 5.0685 66.011168 2549.6957 80.915097 6 de07a34 1 5.1903189 0.3398781 0.2870648 0.0227464 0.5482055 0.3639471 0.1541875 0.0186391 13.096616 15.847592 24.177127 1851.0297 55.749379 1626.8446 113.92814 2392.8942 205.70575 7 de07a35 1 5.1738748 0.4968662 0.3364605 0.02677 0.2080789 0.4083423 0.1001822 0.0374684 19.206733 15.912698 74.80048 1848.3288 81.716828 186 9.6195 129.12491 1627.4691 695.38114 11 de07a40 1 7.9292555 0.9601647 0.3533551 0.0426658 0.9740681 0.9967587 0.1660353 0.0046567 24.218281 24.148969 5.6092835 2223.0117 109.1843 5 1950.5999 203.22936 2518.069 47.12564 12 de07a41 1 4.8701803 0.3640734 0.2875914 0.0244424 0.9167832 -0.128503 0.1300729 0.0048159 14.951126 16.998001 7.4049702 1797.1116 62.97488 9 1629.4816 122.37251 2098.9476 65.03097 13 de07a42 1 5.1178 0.3229215 0.3369483 0.018361 0.8206989 -0.721338 0.1173243 0.0044509 12.619545 10.898382 7.5873253 1839.0644 53.595908 187 1.9716 88.531713 1915.8598 68.059091 14 de07a43 1 5.0802446 1.1563019 0.3410673 0.0732018 0.9616655 0.95 0.1171194 0.0071679 45.521506 42.925103 12.240373 1832.812 193.09904 1891. 8022 351.87556 1912.7224 109.83837 15 de07a44 1 6.1755834 0.5920532 0.3012298 0.034479 0.7555957 0.7820836 0.1770828 0.0175715 19.174 22.892148 19.845575 2000.9992 83.778658 169 7.4041 170.81211 2625.7373 164.99018 1 de07a09 1 5.2244037 0.3166229 0.3280679 0.0179158 0.8656311 -1.089433 0.114913 0.0036297 12.120919 10.922004 6.3173037 1856.6052 51.650491 1 829.0099 86.962896 1878.5201 56.920284 6 de07a05 1 5.5423445 0.6026643 0.3254451 0.0125216 0.3007831 0.4711928 0.1421572 0.0173422 21.747631 7.6950477 24.398673 1907.1895 93.53453 1 816.2665 60.899754 2253.6501 210.65463 8 de07a07 1 5.5265467 0.2904833 0.3334539 0.0188007 0.3436379 -2.983624 0.1381832 0.0212915 10.512291 11.27636 30.816316 1904.7347 45.192637 1 855.1006 90.889756 2204.5608 267.4816 9 de07a08 1 5.0661801 0.3795521 0.3070497 0.0223789 0.8658847 0.1220115 0.1192419 0.0050209 14.983757 14.576717 8.4213412 1830.4606 63.531041 1726.172 110.37341 1944.8949 75.281166 10 de07a18 1 5.0433297 0.2765725 0.3246592 0.0154257 0.7143129 -4.791581 0.1135063 0.0052837 10.967854 9.5027038 9.309986 1826.6286 46.468927 1812.4431 75.068716 1856.2954 84.110027 13 de07a12 1 5.481676 0.5443276 0.3209244 0.0197536 0.6355912 0.2026786 0.1269908 0.0094944 19.859897 12.310422 14.952949 1897.7297 85.271314 1794.2419 96.401969 2056.7277 131.94758 15 de07a14 1 5.354477 0.3405239 0.3228988 0.0203466 0.888929 -0.663536 0.1157783 0.0037592 12.719222 12.602441 6.4937525 1877.6053 54.412378 1 803.8702 99.147705 1892.0283 58.415426 16 de07a15 1 5.6757555 0.2567558 0.3318133 0.020104 0.8558245 -1.760238 0.1202999 0.0044054 9.0474575 12.117647 7.3239908 1927.6868 39.052579 1847.1645 97.309882 1960.6726 65.350245 17 de07a16 1 5.6701703 0.2306803 0.3128281 0.0181811 0.8590636 -2.86665 0.1268333 0.0043922 8.1366286 11.623671 6.925907 1926.837 35.115882 17 54.6086 89.274903 2054.5367 61.130755 L-855 L-868 Table No. 77.2 Raw data and processing for zircon dating using U-Pb laser-ablation ICP-MS techniques. Work was done by Marc Poujol at the Memorial University of Newfoundland, Canada. CONCORDIA COLUMNS AGES Ma I N T E R C E P T V A L U E S L-943 L-969 page 2/2 SAMPLE 2 ? % 2 ? % 2 ? % spot # file 207/235 7/5 err 206/238 6/8 err Rho 207/206 7/6 err 207/235 206/238 207/206 7/5 age 1 sigma 6/8 age 1sigma 7/6 age 1 sigma 10 de07a18 1 5.0433297 0.2765725 0.3246592 0.0154257 0.7143129 -4.791581 0.1135063 0.0052837 10.967854 9.5027038 9.309986 1826.6286 46.468927 1812.4431 75.068716 1856.2954 84.110027 18 de07a17 1 5.2155825 0.2930756 0.3158416 0.0173751 0.4079038 -0.71912 0.1355637 0.0166927 11.238462 11.002402 24.627049 1855.1652 47.877094 1769.3888 85.121921 2171.2761 214.54103 22 de07a21 1 5.0282414 0.243085 0.31959 0.0166628 0.8518812 0.284619 0.1125839 0.0036088 9.6687875 10.427599 6.4108689 1824.0903 40.944674 178 7.7268 81.400434 1841.5386 58.021946 23 de07a22 1 4.9479696 0.3144167 0.3282694 0.0143464 0.7705624 -0.420794 0.1091408 0.0039453 12.708916 8.7405969 7.2297144 1810.4787 53.67434 1 1829.9881 69.626338 1785.1235 65.88648 24 de07a23 1 5.2793953 0.2655679 0.3357591 0.0120442 0.6889278 0.3933588 0.1125297 0.004247 10.060544 7.1743009 7.5481758 1865.5366 42.94254 1 866.235 58.125594 1840.6674 68.322438 25 de07a24 1 5.3047917 0.2611458 0.3246616 0.0179237 0.8383324 -15.7668 0.1175756 0.0042211 9.8456579 11.041485 7.1801703 1869.6349 42.057383 1812.4545 87.225132 1919.6971 64.377516 26 de07a25 1 5.1905442 0.2834624 0.3196162 0.0178786 0.8516318 0.6341477 0.115049 0.0039608 10.922261 11.187545 6.885422 1851.0667 46.493958 1 787.8544 87.338171 1880.6523 62.023267 27 de07a26 1 4.9359082 0.3400392 0.3238592 0.0164922 0.7417392 -0.175981 0.1101967 0.0050741 13.778182 10.184811 9.2092143 1808.4176 58.16633 7 1808.5487 80.307412 1802.6527 83.745301 28 de07a27 1 5.5585206 0.2408556 0.3244011 0.0178945 0.7820466 0.2933926 0.1163312 0.0051138 8.6661749 11.03234 8.7917715 1909.697 37.288997 1 811.1866 87.100089 1900.5956 79.006617 1 de07a88 1 5.3112417 0.2912953 0.3155266 0.0232072 0.9275001 0.95 0.1191242 0.0035313 10.96901 14.710171 5.9288395 1870.6731 46.864998 1767.8 454 113.72142 1943.1291 53.010899 4 de07a91 1 5.1785406 0.2955598 0.3304206 0.0140517 0.9067522 0.95 0.1152943 0.0022801 11.414792 8.5053578 3.9552178 1849.0959 48.572383 1840. 4198 68.086175 1884.4879 35.611853 5 de07a92 1 4.8936428 0.4375046 0.3210772 0.020323 0.8464205 0.95 0.1070732 0.0042639 17.880529 12.659236 7.9644026 1801.1619 75.375243 1794.9 877 99.169235 1750.1876 72.897143 6 de07a93 1 5.0513482 0.4307734 0.3277303 0.0169057 0.7531384 0.95 0.1106088 0.0049839 17.055781 10.316809 9.0116747 1827.9749 72.281423 1827. 3711 82.080564 1809.4393 81.880738 7 de07a94 1 4.8492316 0.4395616 0.3218411 0.018785 0.8392279 0.95 0.1092804 0.0041329 18.129123 11.673447 7.5638402 1793.4815 76.304618 1798.7 14 91.611408 1787.4518 68.911665 8 de07a95 1 4.8370614 0.5257475 0.307162 0.0226887 0.9289885 0.95 0.1167672 0.0034362 21.7383 14.77314 5.8856102 1791.3667 91.456131 1726.7262 111.89203 1907.3169 52.848229 9 de07a96 1 5.3529454 0.3228036 0.3255053 0.0239632 0.8558893 0.9904111 0.117708 0.005236 12.060783 14.723663 8.896568 1877.3606 51.593275 181 6.5593 116.54153 1921.7153 79.74766 10 de07a97 1 4.9559367 0.3235049 0.2999937 0.0234993 0.8794396 0.200595 0.1199461 0.0050856 13.055245 15.6665 8.4797405 1811.8378 55.15192 169 1.2775 116.52821 1955.4162 75.709431 14 de07a87 1 5.1252415 0.4973133 0.3362542 0.0247572 0.8885686 0.95 0.1134834 0.0043136 19.406434 14.725259 7.6022493 1840.2987 82.439771 1868 .6244 119.43451 1855.9312 68.684696 1 de07a45 1 5.4648859 0.2598163 0.3256634 0.0216861 0.9041929 -0.528848 0.1243149 0.0039105 9.5085734 13.318089 6.2912223 1895.0961 40.807079 1817.3278 105.45465 2019.0614 55.755188 2 de07a46 1 5.2914589 0.2751321 0.3165815 0.0166182 0.2904635 -2.796617 0.1632353 0.028228 10.399102 10.498507 34.585671 1867.4854 44.403767 1 773.0127 81.367973 2489.4508 291.39556 3 de07a49 1 12.092751 0.7941725 0.5029125 0.0425009 0.9605512 0.95 0.1830016 0.0044776 13.134686 16.901918 4.8935183 2611.6248 61.590513 2626.3006 182.29843 2680.2618 40.47313 4 de07a50 1 4.0401862 0.4094227 0.2286349 0.0284983 0.8858599 0.9988996 0.1394286 0.009102 20.267518 24.929046 13.056127 1642.3242 82.481257 1 327.3408 149.52492 2220.1229 113.13371 5 de07a51 1 4.6064705 0.3039321 0.2443014 0.014603 0.9654131 0.95 0.1452107 0.0023441 13.195879 11.954915 3.2286111 1750.4406 55.044886 1409.0 203 75.654564 2290.2762 27.766459 6 de07a52 1 5.1658876 0.5445519 0.2565876 0.0203743 0.9276599 0.95 0.1526757 0.0048802 21.082608 15.881005 6.3928395 1847.0144 89.675457 1472. 3597 104.52233 2376.1119 54.486401 7 de07a53 1 3.8084903 0.6267278 0.1967121 0.011892 0.2083014 0.95 0.1361647 0.0386512 32.912138 12.090734 56.771199 1594.5405 132.34274 1157.6 334 64.05931 2178.9799 494.14889 8 de07a54 1 9.3724075 0.5987481 0.4068449 0.0320976 0.9708126 0.95 0.1718203 0.0033489 12.776826 15.778799 3.8981554 2375.1324 58.613073 2200.4807 147.07702 2575.4537 32.565816 9 de07a55 1 3.0315512 0.2247834 0.1914939 0.0141233 0.7243399 0.9441589 0.1259064 0.0088386 14.829594 14.750626 14.039977 1415.5975 56.613747 1129.4624 76.412022 2041.5793 124.10601 10 de07a58 1 6.6686291 0.7825919 0.2888674 0.0430327 0.9921435 -0.231836 0.1661435 0.0031209 23.470849 29.794058 3.7568973 2068.4753 103.62094 1635.8667 215.23263 2519.1632 31.559646 11 de09a12 1 6.0133045 1.3234738 0.3703881 0.0462822 0.7741406 0.95 0.1262575 0.0129005 44.018187 24.99118 20.435255 1977.7722 191.61194 2031.2265 217.71506 2046.5007 180.53518 12 de09a17 1 4.8438518 0.7226037 0.2615149 0.0351093 0.8375949 0.9771022 0.1416091 0.0123996 29.835913 26.850671 17.512405 1792.5472 125.5541 1497.588 179.41034 2246.9769 151.30817 13 de09a18 1 5.7567967 1.6103982 0.2498894 0.064653 0.9839455 0.95 0.1611289 0.0075615 55.947718 51.745251 9.3856202 1939.939 242.00388 1437.9055 333.45328 2467.5409 79.250877 14 de09a15 1 5.9249064 0.9703973 0.2470443 0.1672451 0.9129523 0.95 0.1528901 0.0462637 32.756545 135.3968 60.518887 1964.8927 142.28712 1423.2149 864.54897 2378.5034 515.67701 15 de09a16 1 3.8012578 0.6072876 0.259721 0.0343578 0.7506087 0.95 0.1101086 0.0128221 31.951928 26.457439 23.289993 1593.0121 128.43083 1488.4143 175.82017 1801.198 211.82872 16 de09a13 1 6.8573273 0.5616457 0.3853195 0.0366172 0.8925806 0.9995402 0.1305711 0.006268 16.380893 19.006139 9.6009701 2093.1579 72.580095 2101.0848 170.39354 2105.66 84.252757 17 de09a14 1 5.3946515 0.3896944 0.3471454 0.024745 0.7886113 0.9875615 0.1214013 0.0067474 14.447437 14.256249 11.115812 1884.0046 61.87814 1920.953 118.41056 1976.9224 98.99534 16 de07a45 1 5.4648859 0.2598163 0.3256634 0.0216861 0.9041929 -0.528848 0.1243149 0.0039105 9.5085734 13.318089 6.2912223 1895.0961 40.80707 9 1817.3278 105.45465 2019.0614 55.755188 17 de07a46 1 5.2914589 0.2751321 0.3165815 0.0166182 0.2904635 -2.796617 0.1632353 0.028228 10.399102 10.498507 34.585671 1867.4854 44.403767 1773.0127 81.367973 2489.4508 291.39556 20 de07a49 1 12.092751 0.7941725 0.5029125 0.0425009 0.9605512 0.95 0.1830016 0.0044776 13.134686 16.901918 4.8935183 2611.6248 61.590513 2626 .3006 182.29843 2680.2618 40.47313 21 de07a50 1 4.0401862 0.4094227 0.2286349 0.0284983 0.8858599 0.9988996 0.1394286 0.009102 20.267518 24.929046 13.056127 1642.3242 82.481257 1327.3408 149.52492 2220.1229 113.13371 22 de07a51 1 4.6064705 0.3039321 0.2443014 0.014603 0.9654131 0.95 0.1452107 0.0023441 13.195879 11.954915 3.2286111 1750.4406 55.044886 1409. 0203 75.654564 2290.2762 27.766459 23 de07a52 1 5.1658876 0.5445519 0.2565876 0.0203743 0.9276599 0.95 0.1526757 0.0048802 21.082608 15.881005 6.3928395 1847.0144 89.675457 1472 .3597 104.52233 2376.1119 54.486401 24 de07a53 1 3.8084903 0.6267278 0.1967121 0.011892 0.2083014 0.95 0.1361647 0.0386512 32.912138 12.090734 56.771199 1594.5405 132.34274 1157. 6334 64.05931 2178.9799 494.14889 25 de07a54 1 9.3724075 0.5987481 0.4068449 0.0320976 0.9708126 0.95 0.1718203 0.0033489 12.776826 15.778799 3.8981554 2375.1324 58.613073 2200 .4807 147.07702 2575.4537 32.565816 26 de07a55 1 3.0315512 0.2247834 0.1914939 0.0141233 0.7243399 0.9441589 0.1259064 0.0088386 14.829594 14.750626 14.039977 1415.5975 56.61374 7 1129.4624 76.412022 2041.5793 124.10601 30 de07a58 1 6.6686291 0.7825919 0.2888674 0.0430327 0.9921435 -0.231836 0.1661435 0.0031209 23.470849 29.794058 3.7568973 2068.4753 103.6209 4 1635.8667 215.23263 2519.1632 31.559646 L-1043 CONCORDIA COLUMNS AGES Ma L-993 L-1013 2 5 7 APPENDIX K GEOCHRONOLOGICAL CORRELATION DIAGRAMS A79 Correlation of dated events, Zambian locations, 258 A80 Correlation of dated events, Namibian locations, 259 A81 Correlation of dated events, Greater Lufilian Arc, 260 A82 Correlation of dated events, Greater Lufili an Arc, first portion (3000 to 1400 Ma), 261 A83 Correlation of dated events, Greater Lufili an Arc, second portion (1400 to 0 Ma), 262 Contact information of the author Last Name: Lobo-Guerrero Sanz Name: Alberto e-mail addresses: ageo@iname.com ageo@logemin.com Paper mail address: Calle 127A No. 53A-28, office 309 Bogota, Colombia Home address: Calle 109 No. 13-98 Bogota, Colombia Business telephone: +57-1-6435364 Home telephone: +57-1-6586040