An AMF-PGC International Study Tour
Developed & Managed by Porter GeoConsultancy
Africa-B 2001
Mineral Deposits of Southern & Central Africa
10 June - 5 July 2001 - In Two Separate Modules
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This tour, which was developed, organised, managed and led by TM (Mike) Porter of Porter GeoConsultancy Pty Ltd (PGC), as a joint venture with the Australian Mineral Foundation Inc. (AMF), included:


PART A - Zambian Copper Belt
Sunday 10 to Saturday 16 June 2001 PART B - Zinc, Lead & Copper in South Africa & Namibia,
Sunday 17 to Sunday 24 June 2001

Northern Cape Scene

For information on the remainder of the tour,
see the Deposit Descriptions for Module 2
Module 1, Part A, was managed by PGC (in joint venture with the AMF), in cooperation with  AMIRA International  to double as the non-confidential segment of its Sponsors Field Meeting for research project P544, "Proterozoic Sediment Hosted Copper Deposits".

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MODULE 1 - PART A - Zambian Copper Belt

Geological Overview

The Zambian Copperbelt is part of the larger Central African Copperbelt, and extends north into the neighbouring Democratic Republic of Congo (DRC), to continue as the Congolese Copperbelt. It closely coincides with the southern half of a complex, arcuate structural zone, the late Neoproterozoic to early Cambrian Lufilian Arc. Although part of the same curvilinear trend, the Zambian Copperbelt deposits, are hosted by non-evaporitic, rift facies siliciclastic rocks that are not temporally or lithologically equivalent to the mainly carbonate hosts of the Congolese Copperbelt. In addition, the structural architecture in Zambia is characterised by thrusted Palaeo- to Mesoproterozoic metamorphic basement inliers and folded Neoproterozoic sedimentary host rocks, in contrast to the thin skinned deformation of the hosts in the DRC, without involvement of basement.
   Mineralisation within the Central African Copperbelt is hosted within the Neoproterozoic Katanga Supergroup, an intracontinental rift basin sequence, comprising the Roan, Nguba and Kundelungu groups. A period of extension commenced after ~900 Ma, and in Zambia, the sedimentary sequence began after 880 Ma, with the Lower Roan Subgroup oxidised rift facies clastic rocks, deposited in a series of restricted sub-basins controlled by extensional normal faults, including the thin reduced argillites of the Copperbelt Orebody Member near the middle of the unit. The succeeding sag phase Upper Roan Subgroup, is dominantly made up platformal mixed carbonate and clastic rocks, but also included a <500 m thick evaporite/salt bed. To the north, in the DRC, the sag phase sequence transgresses beyond the main rift margin, to become the basal unit of the Roan Group, where the Upper Roan Subgroup equivalents are divided into three. The lowest of these, the R.A.T. Subgroup, comprises the red, silt- and sand-sized residue after dissolution of a thick (>500 m) evaporite/salt bed deposited in a restricted sub-basin, separated from the open sea by a stromatolitic reef. This is overlain by the Mines Subgroup dolostones and shales, including a number of reduced units near the base. The uppermost of the three Roan Group units in the DRC is the Dipeta Subgroup, comprising a lower regressive suite, including oxidised, evaporitic rocks, followed by transgressive carbonate rocks with some reduced intervals.
   During deposition of the late Upper Roan and Dipeta subgroups, a period of 'renewed extension' commenced, reflected by a ~30 to 100 km wide by ~500 km long corridor of gabbroic and lesser felsic intrusions, and an associated volcanic belt of thin mafic lavas and tuffs emplaced from ~765 to 735 Ma. During the same event, an arcuate metamorphic core complex formed, embracing the gabbroic intrusive corridor, marked by a series of basement domes capped by mylonitic detachments. During this period, deposition transgressed further onto basement, and the Dipeta Group passed upwards into a sequence of carbonaceous argillites of the Mwashya Subgroup, the uppermost unit of the Roan Group in both Zambia and DRC. This was overlain by glacial diamictites and interbedded pyritic black argillites of the basal Nguba Group Grand Conglomérat. The remainder of the Nguba Group carbonate and siliciclastic rocks were overlain in turn by the Kundelungu Group basal diamictites and then carbonate rocks, passing up into siliciclastic rocks.
   The main Katanga Supergroup deposition was terminated by the Lufilian orogenic event after ~600 Ma, with NE vergent D
1 folding and thrusting and D2 strike-slip folding to produce the Lufilian Arc. Prior to this event, possibly during late 'renewed extension', uplift of the Domes core complex to the SW, coupled with deepening of the basin to the NE (in response to extension), and dissolution of the R.A.T. Subgroup salt beds (as the increasing temperature and pressure allowed fluids to penetrate the salt beds), led to northward mass gravity gliding of the Upper Roan/R.A.T., Mines and Dipeta subgroup successions towards the main basin centre. This gravity gliding, slumping, salt dissolution and diapirism, produced a regional scale megabreccia of large clasts up to several km in length of Mines Subgroup rock in a matrix of R.A.T. Subgroup and comminuted Roan Group rock fragments to rock flour.
   During the late Lufilian event, a complex of anorogenic granites was emplaced in the inner Lufilian Arc to the SW from ~560 to 530 Ma, with minor coeval mafic to ultramafic intrusions. This was followed after ~530 Ma by orogenic relaxation that lasted until after 500 Ma.
   Stratabound and vein ore emplaced after 880 Ma is found in rocks from the Palaeoproterozoic Lufubu Metamorphic Complex to the Kundelungu Group. However, large, stratabound sediment hosted Cu-Cu±U deposits are restricted to the stratigraphic interval from the Lower Roan Subgroup to the basal Nguba Group, specifically where it occurs in association with rocks that contain (or contained) in situ or mobile hydrocarbons at the following stratigraphic levels: i). the Copperbelt Orebody Member (including secondary positions within 100 m above and below this member), where the great bulk of the Zambian Copperbelt deposits are hosted; ii). the base of the Mines Subgroup (including a subsidiary position within ~100 m higher in the sequence) in the Congolese Copperbelt, accounting for the bulk of ore in the DRC; iii). the upper Dipeta Subgroup (e.g., Mutanda, Deziwa; iv). Mwashya Subgroup (e,g, Frontier, Kansanshi); and v). Grand Conglomérat of the Nguba Group (e.g., Kamoa, Fishtie).
   However, almost invariably, ore is only found at the first reduced unit overlying an oxidised arenaceous (or otherwise permeable) sequence, separating it from basement, e.g., ore is only found within the Mwashia Subgroup or Grand Conglomérat where no reduced Roan Group unit exists in the underlying sequence (e.g., Frontier, Kamoa).
   Regional scale alteration includes an early i). calcic-magnesian phase that redistributed carbonate and anhydrite from the evaporite beds to porous rocks throughout the basin; ii). intense potassic alteration that overlapped the Ca-Mg stage, and preceded and overlapped ore; and iii). a later, but multipulse sodic-calcic phase that pervasively overprinted early ore and predominantly affected Nguba and Kundelungu group rocks, but also locally Roan Group lithologies.
   Sulphide mineralisation was emplaced in a number of generations, including: i). early pyrite, developed either during early diagenesis in association with bacterial sulphate reduction (BSR) in carbonaceous argillites, or late diagenesis after emplacement of oil or gas reservoirs. ii). early diagenetic pyrite was overprinted and partially replaced by weak regional copper mineralisation derived from diagenetic, saline K-Mg brines circulating and scavenging metal from the basin; iii). significant, late diagenetic and pre-folding, generally fine-grained, disseminations (mostly bedding controlled) and veins containing Cu-Co sulphides and pyrite, concentrated in fluid traps along basement growth faults. These sulphides usually have isotopic signatures suggesting low temperature BSR associated with brines at temperatures of from 80 to 150°C; iv). early tectonic syn-folding sulphides, occurring as coarser veins and lesser disseminations of Cu-Co sulphides associated with brines at temperatures of 150 to 250°C that are replacing earlier, and generating new, sulphides by thermochemical sulphate reduction (TSR); v). post-folding, coarser veins and lesser disseminations of copper sulphides, that formed at the end the main Lufilian Orogeny during orogenic extensional relaxation. This generation was associated with calcic-sodic brines at temperatures of 250 to 400°C, replacing existing sulphide and producing ones by TSR, concentrated in reduced rocks, including those with pre-existing mineralisation. These brines were also responsible for IOCG and hybrid IOCG-sediment hosted copper mineralisation.
   Most significant sediment hosted Cu-Co deposits in the Central African Copperbelt can be shown to contain early pyrite, overprinting pre-folding, early to late diagenetic Cu-Co sulphides in disseminations and veins, and syn- to post-folding coarser veins and lesser disseminations. From the evidence available it can be inferred that significant Cu-Co mineralisation was emplaced by a major influx of metalliferous brines scavenged from both the basement and Katanga basin during: i). the renewed extension coeval with or soon after deposition of the Grand Conglomérat of the Nguba Group, at ~765 Ma; ii). during the early stages of the Lufilian compression from ~585 to 575 Ma; and iii). during orogenic relaxation from ~530 to ~500 Ma. Not all deposits have experience all three generations (e.g., Kansanshi), although most of the large high grade deposits are the product of at least two.
   The Central African Copperbelt is the largest and highest grade sediment-hosted stratabound copper province known in the world. Mineralisation is hosted in a variety of rocks and fluid traps, and emplaced by a number of events spread over a period of ~200 Ma. The key however, is the large amount of Cu-Co, necessarily scavenged from a very large volume of rock with lithologic and structural permeability. The structural preparation of basement permeability, and the generation and circulation of brines required both a large scale source of salts/evaporites, and significant pulses of energy to promote basement faulting (both listric and compressional detachments) and to elevate thermal gradients. These energy pulses were provided by the 'renewed extensional' event, particularly the metamorphic core complex and gabbroic magmatism, and the Lufilian compression and related anatectic magmatism. Without one or both of these two events, the result may have been a regionally distributed low grade to anomalous copper shale.

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Kitwe Seminar - The Setting, Geology & Metallogeny of the Zambian Copper Belt

The seminar included presentations covering the following topics:
  • The setting & geology of the Damaran-Katangan System in Africa and the place of the Lufilian Arc & Copper-Belt within it.
  • The tectonics, geology, structure, metallogeny and mineralisation of the Copper Belt in Zambia and the Cupriferous Arc in the neighbouring Democratic Republic of the Congo (DRC) and how they are related.
  • Descriptions of the important DRC deposits and their characteristics.
  • The stratigraphy, structure, occurrence and controls of copper mineralisation within the Copper Belt in Zambia.
  • Details of the main deposits that are not to be visited and how they compare to those orebodies on the itinerary.
  • Aspects of exploration on the Copper Belt - the expression of mineralisation in outcrop, geochemistry, geophysics, etc.

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Mufulira - Cu-Co

The Mufulira stratabound, sediment-hosted, copper-cobalt deposit is located 30 km north of the town of Kitwe, in the Zambian Copper Belt of central Zambia. It is also one of the 'classic' Zambian Copperbelt deposits, located on the eastern margin of the Kafue Anticline, hosted by the Lower Roan Subgroup of the Neoproterozoic Katangan Supergroup. Copper sulphides occur at 21 distinct stratigraphic positions within the Mufulira mine, of which only three are economically exploited, termed the 'A', 'B' and 'C', within the 30 to 80 m thick "Ore Formation". The Ore Formation overlies the westward thinning "Footwall Formation", which is equivalent to the Mindola Clastics Formation on the western flank of the Kafue Anticline. The 'C' Orebody is the lowest and most extensive, having lateral dimensions of 5800 m, continuous down dip for >1300 m, to at least the 1500 m level, and is up 23 m thick, averaging ~14 m.
   The ore at Mufulira is almost exclusively within 'arenites' and not in the intervening and overlying finer sedimentary rocks. Copper sulphides occur as discontinuous bands of 'fly speck' disseminations following bedding planes and as irregular angular clots of weak to dense interstitial disseminations of sulphides whose elongation is influenced by bedding, but may also be markedly transgressive. Chalcopyrite dominates in the 'C' Orebody (although in sections this grades to bornite dominant), whilst in the 'B' Orebody, the predominant ore mineral is bornite. The uppermost 'A' Orebody is also the highest grade, with bornite and chalcocite. Total production + resources were estimated in 1988 as 335 Mt @ 3.3% Cu. ..... MORE

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Nkana - Cu-Co

The Nkana-Mindola stratabound, sediment-hosted, copper-cobalt deposits are exploited from four open pit and four underground mines, from north to south, the North Mindola, Mindola, Nkana Central and Nkana SOB (Southern Ore Body). Mineralisation, is more or less continuous over a strike length of 14 km, with narrow 'barren gaps', on the SW margin of the Kafue Anticline, immediately to the east of the town of Kitwe and is hosted within the 21 to 23 m thick Copperbelt Orebody Member, or 'Ore Shale'. The Copperbelt Orebody Member is the basal unit of the Kitwe Formation, predominantly composed of dark grey dolomitic argillite, overlain by quartzites and dolomitic argillites of the main bulk of the Kitwe Formation. It overlies an eastward thinning sequence of oxidised sandstones and conglomerates that comprise the Mindola Clastics Formation, which rest on basement gneisses.
   Orebodies are distributed throughout the Copperbelt Orebody Member. Overall, the best grades of primary mineralisation (~4% Cu) are found to the NE in the Mindola orebody, dropping off to nearer 2.2% Cu at depth to the south in the SOB (South Orebody), where the host then passes into black carbonaceous shale, with only low grade chalcopyrite, carrollite and pyrite, then to pyrite with scattered chalcopyrite. To the north and up-dip of this facies gradation, the primary ore is chalcopyrite dominant, passing into a bornite-chalcopyrite in the Mindola deposit. At Mindola, bornite accompanies chalcopyrite at the base of the ore zone, decreasing upwards. Total production + resource were estimated in 1988 as 690 Mt @ 2.5% Cu. ..... MORE

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Nchanga - Cu-Co

The Nchanga-Chingola stratabound, sediment-hosted copper-cobalt deposits are located on the northern section of the western margin of the Kafue Anticline in Zambia. Mineralisation is hosted by the Neoproterozoic Lower Roan Subgroup, where its lower members lap onto a palaeo-basement high that corresponds to the core of the current Kafue Anticline. Primary copper mineralisation is found at five overlapping levels over a total stratigraphic interval of 150 m, occurring as 'Footwall ore' in the Mindola Clastics Formation, the lowermost unit of the Lower Roan Subgroup, in the Lower Banded Shale (equivalent to the regional Copperbelt Orebody Member) at the base of the overlying Kitwe Formation, and in succeeding members of the latter formation. Mineralisation, which is generally found at progressively higher stratigraphic positions from south to north, is hosted by a variety of lithologies, including micaceous and dolomitic feldspathic quartzite, coarse grained arkose and greywacke, and, to a lesser extent, by siltstones and shales which cap these arenite units. Primary sulphides, which include chalcopyrite, bornite, chalcocite and pyrite, occur mainly as disseminations within the arenitic units and as disseminations orientated along bedding or cleavage planes, and in quartz veins, within the finer facies. Much of the sulphides have been oxidised to depths of over 300 m, with malachite and secondary chalcocite being ubiquitous. Total production + resources at the Nchanga-Chingola cluster is 1080 Mt @ 2.16% Cu. .... MORE

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Konkola - Cu-Co

The Konkola-Kirila Bombwe and Konkola Deep stratabound, sediment-hosted, copper-cobalt deposits, which are ~15 km to the north of Nchanga on the northwestern extremity of the Kafue Anticline in Zambia, are part of the Konkola Copper Mines operation which also includes Nchanga-Chingola. The Konkola mineralisation continues north at depth, becoming the neighbouring Lubambe (previously Konkola North) mine that emerges on the eastern margin of the Konkola Dome to the NW, following the rim of dome northwestward into the DRC, as the Musoshi deposit. The ore is predominantly hosted by banded siltstones and sandy shales of the up to 60 m thick Lower Roan Subgroup Copperbelt Orebody Member, equivalent to the Lower Banded Shale facies that hosts some of the ore at Nchanga. Total production + resources from Kirila Bombwe to Musoshi is estimated to total >1000 Mt @ ~3% Cu. ..... MORE

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Chambishi - Cu-Co

The Chambishi Main, West and Southeast sediment hosted copper-cobalt deposits are developed within the Lower Roan Group in the Zambian Copper Belt. They are located on the southwestern margin of the 'Kafue Anticline', approximately half way between the Nkana-Mindola and Nchanga mining complexes in northern Zambia. They are ~360 km north of Lusaka and 28 km NW of Kitwe. Chambishi Southeast is centred on a point ~10 km NW from the Mindola mine, while the Main and West deposits, which are separated by a narrow barren gap, are a further ~7 km to the NW (#Location: 12° 39' 36"S, 28° 3' 21"E).

The Chambishi Main deposit was discovered in 1902, with underground access being developed in 1927, although operations were suspended in 1931 due to depressed copper prices. Operations were not restarted until an open pit was initiated in 1963, with the first ore treated in 1965, to be supplemented by underground production from 1972. The open pit was closed in 1978, and the underground mining were suspended in 1987. Non-Ferrous Corporation Africa (NFCA) aquired the operation in 1998, and commissioned a new undeground mine in 2003. Construction commenced on the Chambishi West underground mine in 2007, with first production in 2010. Exploration at Chambishi Southeast has sporadically taken place since 1903, with the main discovery drilling from 1975 to 1982. Production was scheduled to begin in 2016.

Regional Setting

For details of the regional setting of Chambishi, the Chambishi-Nkana basin, the Central African/Zambian Copper Belt and the Lufilian Arc, see the separate Zambian Copper Belt record.

The Chambishi deposits are hosted by the Neoproterozoic Lower Roan Group Ore Formation of the Katanga Supergroup, within the Chambishi-Nkana basin, located on the mid-southwestern flank of the 'Kafue Anticline'. The 'Kafue Anticline' is a late-tectonic structural feature within the Domes Region of the Lufilian Arc, centred on a basement high of Palaeo- and Mesoproterozoic gneisses and schists, over which the Katangan sedimentary rocks were draped. The Chambishi-Nkana basin is essentially a NW-SE elongated, doubly plunging, structural basin, predominantly surrounded by pre-Katangan basement. The basinal structure cuts across the generally NW-SE trending facies boundaries within the Lower Roan Group. The Chambishi deposits lie on the northeastern and northern margins of the Chambishi-Nkana structural basin.

Geology & Mineralisation

The stratigraphy of the Lower Roan Group at Chambishi can be summarised as follows, from the base, where it unconformably overlies the Palaeo- to Mesoproterozoic basement complex, which is predominantly a grey, microcline-biotite-granite and numerous aplite dykes, with a few Lufubu schist xenoliths, overlain by Mesoproterozoic Muva conglomerate, quartzite and quartz-schist (after Garlick in Mendelsohn, 1961):

Mindola Clastics Formation or Footwall Formation, 0 to 150 m thick - at surface the Mindola Clastics Formation is thin, but thickens down-dip, and comprises:
Basal Conglomerate, 0 to 65 m thick - a sporadically developed boulder bed near the surface, where it is a metre or so thick, overlying Muva schist east of the orebody, increasing to 65 m in thickness above granite basement deeper in the basin, under the West Orebody.
Footwall Aeolian Quartzite, up to 33 m thick - quartzites with large scale cross bedding (most likely aeolian), with upper beds which are coarser grained, feldspathic to arkosic and with considerable small scale crossbedding suggesting a provenance from the SW. Includes a layer of anhydrite lenses. Laps against granitic basement highs in many places where the Basal Conglomerate is absent.
Footwall Transition Arenites, 0 to 18 m thick - arkose, grading upwards into argillaceous arenites and thin argillites. The unit contains local, thin zones of disseminated chalcopyrite and pyrite, and a few fekdspar, quartz and sulphide veins.
Cobble Conglomerate, 0 to 20 m thick - a conglomerate with granite and quartzite cobbles up to 8 and rarely 25 cm in diameter in a carbonate and anhydrite-rich sandy matrix which leaches to a porous manganiferous material near surface. A few drill holes intersected traces of disseminated bornite and chalcopyrite in parts of this member.
Arkose and Argillite, 12 to 25 m thick - poorly bedded, white to pink arkose and layers of grey, generally schistose sandy argillite. Under the shallower parts of the Main orebody and farther east the argillite beds are absent.
Footwall Conglomerate, 0.5 to 10 m thick - this member has a variable composition and thickness. Where thickest it is a coarse arkose with pebbles and rare cobbles, and near the surface large fragments of granite and schist. In places there are scree like granitic deposits flanking granitic palaeo-hills. Elsewhere it is 1 to 3m thick and comprises light grey and rarely pink, poorly sorted, porous, pebbly arkose. In many drill holes, down dip this member is a thin gritty arkose or feldspathic quartzite, difficult to differentiate from the underlying quartzites of the 'Arkose and Argillite' and 'Footwall Quartzite' members.
Chambishi Basin
Kitwe Formation, which commences with the:
Copperbelt Orebody Member, previously known as the Ore Formation or Ore Shale, 0 to 30 m thick - where fully developed, the basal 1 to 3 m of the Copperbelt Orebody Member is a dolomitic-schist, a rock rich in carbonate which is intensely contorted and schistose and cut by quartz-dolomite-anhydrite veins. The major part of the Copperbelt Orebody Member is a fine grained, biotite-quartz argillite, with well developed banding due to differences in grain size and the varying minor dolomite content. A pronounced flow-cleavage is parallel to the axial planes of small and large drag folds. In the west, the cleavage is less prominent. Over considerable areas small lenticules of dolomite, anhydrite and minor quartz, commonly with sulphides, are prominent in the upper parts of the Copperbelt Orebody Member. The upper 3 to 6 m is commonly more sandy, and may show graded bedding. Near the surface and near granitic promontories, cross bedded arkosic lenses in scours herald the approach of the hangingwall arenites. Down dip, a brownish vuggy dolomite bed up to 1 m thick occurs 2.5 m from the top. West of the Chambishi West Orebody, the Copperbelt Orebody Member becomes black, carbonaceous and pyritic.
    In the folded section of the Main Orebody, and in the West Orebody, the Copperbelt Orebody Member averages close to 30 m in thickness, but down dip, thins to 20 m. Against resistant granite ridges, both east and west of the Main Orebody, the shale thins to 6 m, as the lower beds become sandy or arkosic, which in the absence of 'Footwall Conglomerate' may not be distinguished from footwall arenites. Rarely is argillite found in contact with granitic basement. East of the easternmost granitic promontory, the Copperbelt Orebody Member is 6 to 9 m thick for 1.5 km, beyond which it becomes sandy or quartzitic and may not be differentiated from the overlying or underlying arenites.
    In the Main Deposit, where the Copperbelt Orebody Member is above the eastern granite ridge, it is barren and contains numerous arkosic layers, which thin down-dip and to the west, accompanied by the appearance of disseminated chalcocite in the lower third of the Copperbelt Orebody Member. Chalcocite gives way to bornite down-dip, while in the basal dolomite-schist, chalcopyrite appears, accompanied by abundant bornite. Coarse aggregates of both bornite and chalcopyrite are distributed along bedding planes, with associated cross-cutting quartz-dolomite veins carrying the same sulphides. The basal dolomitic-schist thickens down-dip and to the west, to become a 3 m thick layer with grades of up to 10% Cu. This high grade compensates for the progressive down-dip decrease in copper grade in the overlying argillite, as bornite passes into chalcopyrite. Further down-dip and to the west, chalcopyrite in the upper Copperbelt Orebody Member gives way pyrite. Bornite again appears as the western granite ridge is approached, and over which the Copperbelt Orebody Member thins to ~6 m, and is barren for a strike interval of ~200 to 300 m. Grades in the chalcopyrite, chalcopyrite-bornite and bornite zones generally average ~2%, 2 to 4% and >4% Cu respectively. The Main orebody is laterlly limited by the two basement granite ridge. It has a strike length of ~800 m, expanding to 1500 m at a depth of ~300 m, with a thickness of up to 30 m, averaging 8 m, and an overall dip of 15 to 75°W with a series of drag fold-related reversals (Fleischer et al., 1976; SRK 2012).
    The West Deposit, occurs to the west of the 200 to 300 m wide barren gap over the western granite ridge. As the Copperbelt Orebody Member thickens again, the sulphide mineralogy is dominated by chalcopyrite disseminations, with only minor bornite appearing again. The deposit has a strike length of ~1800 m, persists down dip for ~600 m, varies from 2 to 17 m in thickness, averaging 8 m, and is lower grade, containing ~2% Cu. A small ore lense is also found in arkose below the Cobble Conglomerate where these beds abut the western granite ridge. While the eastern margin of the West Deposit is influenced by the barren gap over the western granite ridge, its western margin corresponds to a facies change within the Copperbelt Orebody Member to a thick pyritic and carbonaceous shale, that persists to the western margin of the Nkana-Chambishi structural basin (Fleischer et al., 1976; SRK 2012).
    There is an ~20 km long, largely barren gap to the south, separating the Chambishi Main deposit and Mindola. Within the middle of this interval, the Chambishi Southeast resource has been outlined, comprising two orebodies distributed over an 8 km by 1 to 2 km NW-SE trending zone. The North body is 4500 m long, 570 to 1240 m wide, dips at 5 to 15°NW and is 1.4 to 23 m thick, averaging 10 m, with ~55 Mt @ 2.3 to 2.4% Cu, 0.074% Co. The south body is 3540 m long, 800 to 1600 m wide and lower grade, with ~50 Mt @ 1.6% Cu, 0.0125% Co. The deposits are flat lying to shallowly dipping, and completely blind. They are located on the flanks of a palaeo-hill over which the Ore Formation becomes dolomitic. Cobalt mineralisation appears within the Copperbelt Orebody Member on the flanks of the basement palaeo-hill. Away from the palaeo-hill, the Mindola Clastics Formation again comprises quartzites, grits and conglomerates, and the overlying Ore Formation consists of interbedded dolomite shale/siltstones and argillites with organic carbon. The mineralisation occurs as fine disseminations (5 to 1500µm, with most between 25 and 400µm) or concentrations of chalcopyrite, distributed along bedding planes with minor amounts of carrollite, cobaltiferous pentlandite and skutterudite, and bornite/linnaeite in certain areas. Beyond the copper mineralisation, sulphides are principally pyrrhotite and pyrite (Garlick, 1961; Fleischer et al., 1976; Fleischer, 1984; SRK 2012).
Chambishi Main section

The remainder of the Kitwe Formation, above the Copperbelt Orebody Member, was previously known as the "Hanging wall Formation", which is 40 to 80 m thick, and is subdivided into,
Hangingwall Quartzite, 3 to 12 m thick - an eastward thickening unit of white feldspathic quartzite and arkose beds with streaks of detrital iron oxides and silty and argillaceous layers.
Interbedded Quartzite and Argillite, 25 to 35 m thick - over the Main and West Orebodies this comprises a 25 m thick argillite unit with two quartzite members near the middle, each of around 3 m thickness. Above these middle quartzites, there are 12 to 15 m of schistose shale and dolomite. To the east, the quartzites thicken at the expense of the intervening argillites.
Upper Quartzite, 12 to 25 m thick - a coarse white to pink feldspathic quartzite, with in places a few pebbles. Near the base and top there are some thin silty and argillaceous beds. Magnetite and other detrital minerals mark the cross bedding, with intense concentrations on lower foresets and bottomsets. Generally it is 14 to 15 m thick, but thickens to the east due to an increase in the arenaceous content of the underlying and overlying units. It is also characterised by a chalky white appearance from the weathering of its high feldspars content.

Upper Roan Group, averaging 350 m thick - comprising, ~25 m of interbedded schist and quartzite; 12 to 24 m of cherty dolomite, 75 to 90 m of sandy talc-schist, and up to 400 m of white to pink dolostone, that includes some cherty layers with talc, and shale bands with disseminated pyrite. Around 100 m above the base of the latter dolostone unit in the northern and western parts of the Nkana-Chambishi Basin, a ~170 m thick metagabbro sill occurs, plus ~52 m of granophyre and ~8 m of magnetite. Chlorite-amphibole shear zones within the gabbro, contain dolomite, sparse pyrite, pyrrhotite and minor chalcopyrite.
Mwashia Group, 550 m thick - comprising ~300 m of grey argillite, overlain by ~240 m of black carbonaceous argillites, with substantial disseminated pyrite and minor chalcopyrite.
Nguba Group, ~1000 m thick - diamictite, dolomite and shale.


The Lower Roan is strongly deformed in the vicinity of Chambishi Main and West, the main structure being the Chambishi Monocline, which parallels the Kafue Anticline margin in the vicinity of the western granite ridge. Conspicuous east-west drag folds associated with this structure are seen to the east of the ridge. The most intense folding is in the Ore and Hangingwall Formations, with the Upper Quartzite in the upper limb commonly thrust over the adjacent syncline. Fold geometries and plunges are influenced by the granite ridges also.

Published production, reserve and resource figures include:
    Total production + resource as at 1988 - 240 Mt @ 2.3% Cu (Freeman, 1988);
    Total production to 1988 - 33 Mt @ 2.88% Cu (Freeman, 1988);
    Mineral resources at the end of 1997 (Northern Miner, Jan 26, 1998) were:
      Chambishi Main Mine, proved reserves - 33.5 Mt @ 2.55% Cu;
      Chambishi West Mine, resources - 47 Mt @ 2.27% Cu;
      Chambishi Southeast Mine, resources - 69.7 Mt @ 2.59% Cu, 0.13% Co;
    Total remaining ore reserves and mineral resources at 31 December 2011 (China Non Ferrous Metal Industries, 2012) were:
      Chambishi Main Mine
        sulphide, proved + probable reserves - 8.7 Mt @ 1.92% Cu;
        sulphide, measured + indicated resources - 10.7 Mt @ 2.5% Cu;
        sulphide, inferred resources - 8.1 Mt @ 2.42% Cu;
      Chambishi West Mine
        proved + probable reserves - 25.3 Mt @ 1.44% Cu;
        oxide, indicated resources - 6.2 Mt @ 1.11% Cu;
        sulphide, measured + indicated resources - 25.3 Mt @ 2.06% Cu;
        inferred resources - 17.3 Mt @ 2.09% Cu;
      Chambishi Southeast Mine
        probable reserves - 29.7 Mt @ 1.44% Cu, 0.10% Co;
        sulphide, indicated resources - 35.4 Mt @ 2.30% Cu, 0.12% Co;
        sulphide, inferred resources - 125.6 Mt @ 1.82% Cu, 0.10% Co.
      TOTAL measured + indicated resources - 77.6 Mt @ 2.16% Cu;
      TOTAL inferred resources - 151.0 Mt @ 1.88% Cu.

For detail consult the reference(s) listed below.

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Chibuluma - Cu-Co

The Chibuluma East, West and South copper-cobalt deposits are located some 10 km to the SW, 12 km WSW and 18 km SW of Nkana respectively, in the Zambian Copper Belt of northern Zambia (#Location: Chibuluma South 12° 54' 49"S, 28° 4' 49"E; Chibuluma West 12° 49' 52"S, 28° 6' 20"E; Chibuluma East 12° 50' 29"S, 28° 8' 27"E).

The Chibuluma East and West deposits were discovered in 1939 and 1941 respectively. Chibuluma East commenced production in 1956. The Chibuluma West mine, 2 km to the west, began operations in 1963. Discovery and production was by Roan Selection Trust (RST). The Chibuluma South orebody was discovered by RST in 1969, as a strike extension to the small Chifupu deposit (discovered in 1967), which was ~1.7 km to the SW. The Chibuluma mines were nationalised in 1970 and became part of the state owned Zambian Consolidated Copper Mines (ZCCM), before being privatised and sold to Metorex Limited in 1997. The Chibuluma East mine was closed prior to 1997, while the Chibuluma West mine ceased operation in 2005. The Chibuluma South mine achieved steady state production as an underground mine by mid 2007.

For details of the regional setting of Chibuluma, the Chambishi-Nkana basin, the Central African/Zambian Copper Belt and the Lufilian Arc, see the separate Zambian Copper Belt record.

The Chibuluma deposits are hosted by the Neoproterozoic Lower Roan Subgroup of the Katanga Supergroup, within the Chambishi-Nkana basin, located on the mid-southwestern flank of the 'Kafue Anticline'. The 'Kafue Anticline' is a late-tectonic structural feature within the Domes Region of the Lufilian Arc, centred on a basement high of Palaeo- and Mesoproterozoic gneisses and schists, over which the Katangan sedimentary rocks were draped. The Chambishi-Nkana basin is essentially a NW-SE elongated, doubly plunging, structural basin, predominantly surrounded by pre-Katangan basement. The basinal structure cuts across the generally NW-SE trending facies boundaries within the Lower Roan Subgroup. The Chibuluma East and Chibuluma West deposits lie on the southwestern margin of the Chambishi-Nkana structural basin, ~10 and ~14 km to the NW of the main Nkana Central headframe. Chibuluma South is 10 km south of Chibuluma West, on the opposite margin of the NW-plunging anticlinal basement nose that forms the southwestern margin of the Chambishi-Nkana structural basin.

These deposits are hosted by Lower Roan Subgroup sedimentary rocks that are further removed from the shoreline of the Roan sedimentary basin than Nkana-Mindola and other major deposits of the Zambian Copper Belt. The basement to the Lower Roan Group is composed of Palaeoproterozoic Lufubu System quartz-biotite schists, quartz-microcline-biotite granite gneisses and related granites, and Mesoproterozoic Muva conglomerate, quartzite and quartz-schist. At Chibuluma South, the immediate basement is described as a variably foliated, coarse-grained, grey quartz-biotite-microcline-porphyritic granite, with pink phenocrysts and aligned biotite clots, and local leuco-granite dykes.

The unconformity surface below all three of these deposits includes hills and ridges of granite gneiss, that have influenced the shape and distribution of the host sequence and mineralisation, and subsequent deformation.
Chambishi Basin

The stratigraphy of the Lower Roan Subgroup within the Nkana-Chambishi Basin can be summarised as follows (after Garlick, in Fleischer, Garlick and Haldane, 1976; Metorex, 2010), from the base:

Mindola Clastics (Footwall) Formation at Chibuluma East and West is subdivided into,
Basal Conglomerate, 0 to 1.5 m thick - angular boulders of granite and quartz-biotite gneiss in a sandy matrix, flanking basement hills, and at Chibuluma West, filling gullies between hills.
Aeolian Quartzite, 0 to 130 m thick - well banded feldspathic arenite with large scale cross bedded cossets up to 5 m thick and at angles of over 30°. Quartz, albite, minor biotite, iron oxide and rutile with variable carbonate and anhydrite cement, are the usual constituents. At Chibuluma West, the basement projects above the top of this unit.
Aqueous Arkose, 1 to 5 m thick - overlying an undulating, and in places, deeply pot-holed surface in the aeolianites, are feldspathic grits with pebbles up to 7 cm in diameter, crossbedded arkoses and minor shale beds. Small scale cross bedding, ripple marks, pebbles, gritty and muddy layers are common.
At Chibuluma South, the Footwall Formation, below the Ore Member, comprises,
Basal Conglomerate, 0 - 1.5 m thick - biotite-quartz schists and biotite quartzites, usually containing unsorted boulders and pebbles of basement rocks.
Footwall Sandstone, 10 to 100 m thick - dark pink and grey, mottled and laminated, feldspathic, argillaceous sandstones which are interbedded with biotite quartzites and biotite-quartz schists, and occasional 2 m thick beds of conglomerate with well-rounded cobbles of granite, which are matrix-supported in feldspathic argillaceous sandstone. There are occasional minor interbeds of dark and pale, hard, feldspathic quartzite.
Chibuluma Ore Member, generally 0 to 7 m, but locally up to 30 m thick - a layer of arkose with scattered quartz and quartzite pebbles is discontinuous at the base and generally carries disseminated Cu and Fe sulphides. The overlying sedimentary rocks are feldspathic arenites with sulphides, and argillaceous material now represented by sericite and biotite. Crossbedding is common in places. The host rock to the orebody is a pebbly sericitic feldspathic sandstone or grit with schistose shales. Lithologically it is very similar to the underlying aqueous arenites, except that where mineralised it is conspicuously of a more schistose nature with a higher mica content (Garlick 1962). Where not mineralised it is a pebbly arkose.
    The Chibuluma East orebody has a strike length of 330 m and persists down dip for ~1500 m to a depth of 900 m, with a maximum thickness of 23 m, averaging 7.5 m. At surface the deposit dips at ~10°N. It was deposited in a channel cutting into the underlying Aqueous Arkose. At the base of the Chibuluma East orebody, there are marker beds of sulphidite (rock with >33% sulphide), each 7 to 120 cm thick, consisting of cobaltiferous pyrite, carrollite and minor chalcopyrite in a matrix of detrital quartz and feldspar. These sulphidite bands extend over the whole length of the orebody and grade upwards into normal disseminated chalcopyrite. Conglomeratic pebbles within the sulphidite are matrix supported. Dense intergranular and authigenic tourmaline is common within sections of the sulphidite. The overlying disseminated sulphides are evenly distributed along any one bed, but vary considerably across the sequence. In some sections, the chalcopyrite zone is separated from barren intervals by a bornite-chalcopyrite phase. There is a general zoning across the orebody, parallel to strike, of barren to chalcopyrite to pyrite to chalcopyrite to barren.
    At Chibuluma West, the orebody is similar, except for the absence of sulphidite layers, and that the ore is bounded by basement hills which protrude through the Chibuluma Ore Formation. The ore bearing rocks lap onto basement, occurring in a 'moat' on the north, east and south sides of a basement hill. To the north and east, the ore rests on barren aqueous arenites, but to the south, the 'moat' was deep, and the ore rests on the aeolian arenites and to the north on the scree slopes of the basement hill. Mineralisation can be very rich with intersections of up to 25 m @ 15% Cu. The underlying arenite may also locally be mineralised. At the orebody fringes, distant from basement ridges the ore grades abruptly into disseminated pyrite with lenses of chalcopyrite, which within 30 m fades into barren arkose, that on the southern fringe is a dark flinty quartzite. Where resting on basement the immediately underlying scree and basement schist may be mineralised for up to 7 m below the unconformity.
    At Chibuluma South, the mineralisation is predominantly copper with only very minor cobalt. The orebody is hosted by the competent Orebody Quartzite unit, directly overlain by argillites and dolomites of the Upper Roan Subgroup. The Orebody Quartzite is described as a 0 to 30 m thick unit composed of hard, creamy and pale grey, coarse- to medium-grained, well sorted, feldspathic quartzite, which may be argillaceous and pebbly, with muscovite clots, and sometimes small vugs after carbonate. The orebody occurs over a strike length of 300 m, dipping at ~38°NW, and varies in thickness from a few metres to locally >30m. It persists to a maximum depth of 600 m where it pinches out against a basement high. Mineralisation occurs as oxide (dominantly malachite) to a depth of 60 m and as sulphides (bornite, chalcopyrite and chalcocite) below that level. Supergene chalcocite occurs immediately below the oxide cap in the sulphide zone. Bornite dominates in the thickest and richest central portion of the orebody and is the predominant sulphide mineral with primary chalcocite below the 400 m level. Chalcopyrite accounts for ~20% of the sulphides and becomes more evident towards the fringes. Pyrite dominates in the barren margins. Cobalt mineralisation is patchy.
Hangingwall Quartzite, 0 to 9 m thick - a hard pyritic feldspathic arenite overlies the orebodies, followed by pyritic gritty arenites and argillaceous interbeds. In places this unit has disseminated chalcocite or chalcopyrite, locally forming a second patchy ore horizon. At Chibuluma South the hanging wall sequence is described as a 0 to 30 m thick suite of pink and green banded chlorite-dolomite and quartz schists, interbedded with dark pink feldspathic argillaceous quartzites, overlain directly by the Upper Roan Subgroup to the west.
Hangingwall Conglomerate, up to 9 m thick - this unit has been correlated with the Lower Conglomerate (of the Mindola Clastics Formation) at Nkana to the east. At Chibuluma East it is a compact porous conglomerate, in places directly overlying the orebody where the intervening quartzite was eroded. It contains considerable disseminated pyrite. It is absent at Chibuluma West, where a possible tectonic breccia forms the contact with the overlying Upper Roan Subgroup.

The Hangingwall Conglomerate is overlain directly by the Upper Roan Subgroup, with a chlorite and talc schist at the base, probably a tectonic feature. In the Chambishi-Nkana basin, the Upper Roan is made up of a sequence, from the base, of interbedded schist and quartzite; cherty dolomite; sandy talc-schist; and up to 400 m of white to pink dolostone, that includes some cherty layers with talc, and shale bands with disseminated pyrite. Around 100 m above the base of the latter dolostone unit, in the northern and western parts of the structural basin, an ~170 m thick metagabbro sill occurs, plus ~52 m of granophyre and ~8 m of magnetite. At Chibuluma South, the Upper Roan Subgroup is described as >250 m of dolostones, dolostone breccias and chlorite-dolomite schists intruded by massive metagabbro and gabbro-dolomite breccias.

Mineralisation at Chibuluma East and West is entirely within the Footwall Formation, which is overlain directly by the Upper Roan Subgroup. The 'Ore Shale' that is characteristic of the main Copper Belt deposits was not developed at Chibuluma and the Hangingwall Formation of the Lower Roan Subgroup pinches out ~2 km to the east of Chibuluma East. The mineralisation at Chibuluma East and West is capped by up to 15 m of quartzites and conglomerates, followed by the Upper Roan Subgroup carbonates.

Chibuluma is an example of a Footwall Orebody (e.g., below the Nkana Southern Orebody - see the separate Nkana-Mindola record), which are usually characterised by lower tonnages, but higher grades. Footwall orebodies on the Copper Belt are generally characterised by being markedly more transgressive, not confined to any particular stratigraphy and may even extend into the basement.

Published production, reserve and resource figures include:
    Chibuluma East & West
        total production + resource as at 1988 - 28.4 Mt @ 4.12% Cu, 0.19% Co (Freeman, 1988);
        total production to 1988 - 20 Mt @ 4.53% Cu, 0.19% Co (Freeman, 1988);
        Chibuluma West - remaining down dip resource 1998 - 0.92 Mt @ 5.33% Cu, 0.11% Co (Crew Development Corp., 1998);
        Chibuluma East - original pre-mining resource - 28 Mt @ 4.1% Cu (Arthurs, 2009);
        Chibuluma West - original pre-mining resource - 8.4 Mt @ 3.2% Cu, 0.19% Co (Arthurs, 2009);
    Chibuluma South (after Metorex, 2010) in 2000
        original pre-mining ore reserve - 9.3 Mt at 3.6% Cu;
    Chibuluma South (after Metorex, 2010) at the end of 2009
        measured + indicated resource - 4.9 Mt @ 4% Cu;
        inferred resource - 6.9 Mt @ 3.8% Cu;
        proved + probable reserve - 3.9 Mt @ 3.6% Cu;

Chibuluma is currently held by Metorex (85%) and Zambian Consolidated Copper Mines Ltd, 15%.

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Kalulushi Core

An extensive core storage facility at Kalulushi houses a collection of drill core that may be used to illustrate the stratigraphy of the Copper Belt. Although surface exposures will be inspected during the tour, outcrop in general is poor and the core provides a convenient substitute for surface traverses.

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MODULE 1 - PART B - Zinc, Lead & Copper in South Africa & Namibia

Geological Overview

A series of large zinc, lead and copper deposits are known over an interval of 500 km on the south-western and western margins of the Kaapvaal/Kalahari Craton in the Northern Cape Province of South Africa and in southern Namibia. These are found in both the late Palaeo- and Meso-Proterozoic metamorphics of the Namaqua Mobile Belt and in the late Neo-Proterozoic sediments and volcanics of the Gariep Province in Namibia.

The Namaqua Mobile Belt is part of an extensive U-shaped fringe that extends around the southern, western and northern margins of the Kaapvaal/Kalahari Province, from the Indian Ocean, to the Atlantic and back into central Africa and is composed of late Palaeo-Proterozoic and Meso-Proterozoic gneisses, schists and granitoids after volcanics, sediments and intrusives that were metamorphosed in the late Meso-Proterozoic from 1200-1000 Ma. These rocks in part form the basement to the Damara-Katangan that hosts the deposits of Module 1 Part A.

The Gariep, an inlier on the western margin of the Kalahari Craton along the Atlantic coast, is part of the Damaran-Katangan System, resting unconformably on Namaqualand metamorphics and intrusives. These comprise a variety of sediments from mixtites through arenites and argillites to carbonates, with variable but generally lesser mafic rocks, and felsite-rhyolite volcanics.

The western segment of the Kalahari Craton to the north and east of the Namaqua Mobile Belt and Gariep Complex is occupied by a thick sequence of poorly deformed volcanics and intrusives, the Rehoboth Complex of granitic, intrusives cutting volcanics of from andesitic to acid composition with intercalated sediments ranging from 1700 to possibly 1050 Ma in age. These are in part equivalent to the metamorphosed volcanics and sediments of parts of the Namaqua Mobile Belt

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Black Mountain/Swartberg - Cu-Pb-Zn

The Black Mountain or Swartberg deposit is some 6 km west of Broken Hill within the Aggeneys District of the Northern Cape Province of the Republic of South Africa.

It had an original geological resource of 82 Mt @ 0.75% Cu, 2.7% Pb, 0.6% Zn, 30 g/t Ag. It occurs on Swartberg (or Black Mountain), a hill characterised by a black colouration due to the magnetite (and to a lesser extent the manganese) content of the exposed mineralisation.

The regional geology is as described for the Broken Hill (Aggeneys) record.

Black Mountain comprises two conformable "orebodies", separated by 0 to >30 m of waste. Both "orebodies" comprise large high-grade sulphide lenses, enveloped by lower-grade magnetite-rich rocks, which, in turn, are over- and underlain by weak schist and quartzite. The main sulphide minerals are galena, sphalerite, chalcopyrite and pyrrhotite.

Mineralisation is hosted by the Aggeneys Ore Formation, which at Black Mountain is separated from the underlying schists and quartzites by an inferred shear and from the base is composed of:

i). a 5 m thick lower "ore unit" of baritic schist with disseminated magnetite and sulphide;
ii). a 30 to 65 m thick package of mixed schists (banded quartz-aluminous-schist, and garnet-quartz-schist) and garnet-quartzite (quartz-almandine);
iii). 0 to 25 m of barite-magnetite quartzite (20 to 75% barite with quartz & 10% magnetite and sulphides) and barite-quartz schist (with more muscovite, biotite and chlorite);
iv). 0 to 20 m of magnetite-quartzite (with minor garnet);
v). 0 to 25 m of amphibole-magnetite (magnetite with cummingtonite/grunerite and lesser pyroxmangite, quartz, hedenbergite, garnet, fayalite and apatite); and
vi). 1 to 30 m of amphibolite and medium grained quartzo-felspathic rocks.

This sequence has been subjected to four phases of deformation, resulting in variable dips and thicknesses.   A tight, isoclinal F2 fold nose has been developed in the vicinity of the orebody. Higher grade, coarser, mineralisation is present as an elongate body concentrated down the plunge of the F2 fold axis and occurs in garnet-quartzite, magnetite-quartzite and amphibole-magnetite rocks. In this zone ore occurs as heavily disseminated pyrite and ore sulphides (galena, sphalerite and chalcopyrite) in magnetite and amphibole rich quartzose metamorphics, with finer grained, banded sulphides on the limbs aligned with the foliation of the magnetite-quartzite and amphibole-magnetite hosts.

There is a zoning from a Cu bearing garnet-quartzite, to chalcopyrite-galena rich magnetite-quartzite to an upper galena-sphalerite dominant amphibole-magnetite in the core of the fold hinge,

The deposit has been mined for a period in the past, but is not currently being worked (2001).

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Broken Hill - Pb-Zn-Cu

The Broken Hill mine at Aggeneys has exploited one of the three main ore deposits (Black Mountain, Broken Hill and Gamsberg) within the Aggeneys District of the Northern Cape Province of the Republic of South Africa. It lies some 16 km to the west of Gamsberg and 6 km east of Black Mountain.

All three are hosted by the Bushmanland Group of the Namaqualand Metamorphic Complex, which in turn lies within the broader Namaqua Mobile Belt on the south-western and southern margin of the Kaapvaal/Kalahari Craton. This complex comprises an older metamorphic suite (locally a quartzo-feldspathic augen gneiss) dated at around 2000 to 1900 Ma, overlain by a 1700-1600 Ma (?) supra-crustal succession. This latter succession comprises a lower intrusive to extrusive l euco-gneiss, the Hoogoor Suite, and an upper schist/quartzite succession, the Bushmanland Group. The latter is extensive, and is largely preserved as infolded enclaves or thrust slivers, and is relatively thin, generally less than 1000m thick. At Aggeneys the Bushmanland Group comprises a lower 80 m thick aluminous schist, the Namies Schist composed of quartz-muscovite-k feldspar, locally with up to 25% sillimanite and biotite. This is overlain by a 5 to 900 m thick white crystalline white to grey quartzite, followed by the up to 200 m thick Aggeneys Ore Formation and amphibolite, leucocratic grey gneiss and conglomerates.

The Aggeneys Ore Formation is strongly deformed and in general comprises a footwall schist of sillimanite-quartz-biotite with minor garnet. This is followed by a ferruginous garnet-quartzite composed of bands of garnet and magnetite in a matrix of quartz. This zone is in turn followed by an interval containing magnetite-quartzite (medium grained magnetite & quartz) and amphibole-magnetite (quartz, spessartine, magnetite, ortho-pyroxene, grunerite, cummingtonite & fayalite) with some bands of ferruginous garnet-quartzite. The lower massive sulphide falls within this interval. Above this amphibole-magnetite is the main massive sulphide body and sulphide-quartzite. This is in turn overlain by magnetite-quartzite and amphibole-quartzite, another zone of ferruginous garnet-quartzite and the hangingwall sillimanite-quartz schist.

The massive sulphides (>25% sulphide) generally contain <10% magnetite and range from banded to brecciated textures to heavy disseminations. Pyrrhotite and galena dominate, followed by sphalerite, chalcopyrite and pyrite. The gangue is predominantly quartz, with variable garnet and some barite.

Reserve and reource figures include:
    Initial pre-mining resource - 85 Mt @ 0.34% Cu, 3.6% Pb, 1.8% Zn, 48 g/t Ag,
    including the reserve of 38 Mt @ 0.45% Cu, 6.4% Pb, 2.9% Zn, 82 g/t Ag.
    Reserves in 2000 were ~8.7 Mt @ 0.5% Cu, 5.5% Pb, 2.9% Zn, 78 g/t Ag.

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Gamsberg - Zn

The Gamsberg deposit is located some 16 km to the east of Broken Hill/Aggeneys in the Northern Cape Province of South Africa.

Economic reserves are quoted as 90 Mt @ 6.3% Zn, 0.5% Pb, amenable to open cu extraction. The current feasibility study (2000) is considering the development of an integrated mine and zinc refinery, potentially the largest such complex in the world.

The project is owned and managed by Anglo American plc - Base Metals Division.

Mineralisation occurs within the Gams Ore Formation, which is a direct correlative of the Aggeneys Ore Formation that hosts the ore at Broken Hill, and is a member of the Bushmanland Group (for detail see the Aggeneys/Broken Hill records). The Gams Ore/Iron Formation comprises three units, namely:

i). a lower member composed of a diverse suite of quartz-felspar-garnet-clinopyroxene rock, garnet-clinopyroxene-feldspar marble and garnet-clinopyroxene-quartz-magnetite rocks;
ii). a middle sulphide zone with quartz-garnet-amphibole rocks and graphitic quartz-sillimanite-muscovite-feldspar containing major amounts of pyrite, pyrrhotite, sphalerite and galena; and
iii). an upper unit of diverse garnet, pyroxenoid, clinopyroxene, orthopyroxene, amphibole, quartz, apatite, carbonate, magnetite, hematite and barite bearing rocks.

It is underlain by a thick, massive recrystallised white quartzite with minor schists and conglomerate which succeeds the Hoogoor Suite leuco-gneisses.

Deformation is complex, with the Gamsberg mineralisation falling within a major 'sheath fold' several kilometres across, on whose margin the deposit is located at the contact between the underlying quartzite and overlying mafic gneisses of the Nousees/Koeris Formation.

The mineralised sulphide zone of the Gamsberg Iron Formation is intermittently present within the sheath fold structure and is generally weakly mineralised containing 1 to 4% Zn. The intervals of weaker mineralisation include a number of higher grade 'ore shoots' with +7% Zn embracing smaller cores of +10% Zn.

The measured and indicated resource is 140 Mt @ 5.8% Zn, 0.5% Pb, within a geological resource of 170 Mt.

The sphalerite rich pyrrhotitic-pyritic ore is found towards the centre of the Gams Iron/Ore Formation, flanked by iron sulphides, predominantly pyrite below and pyrrhotite above. These sulphides are in turn sandwiched by two magnetite to hematite rich zones towards the outer margins of the Gams Iron Formation.

The ore zone sphalerite occurs as intergranular disseminations within a quartz-sericite-sillimanite grading up with increasing zinc grade to a quartz-garnet-grunerite host. An impediment to the development of Gamsberg is the high Mn content of the sphalerite, which contains 2 to 3% Mn within its lattice.

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Rosh Pinah - Zn-Pb

The Rosh Pinah Zn, Pb, Ag deposit is located in the Namib Desert of south western Namibia, in southern Africa.

It is basically a stratabound deposit, hosted by the Rosh Pinah Formation arkoses and quartzites, in the lower sections of the late Proterozoic to early Palaeozoic Gariep Complex, an equivalent of the Damaran Supergroup. In this area the basement to the Gariep Complex is made up of Richtersveld Sub-province (Vioolsdrif Terrane) igneous rocks of the Namaqualand Metamorphic Complex.

The type section of the Rosh Pinah Formation, which forms the base of the Gariep Complex, comprises a thin basal mixtite/conglomerate overlain by a thin unit of mafic volcanics. These are succeeded by thicker felsite and rhyolite lavas, pyroclastics and epiclastics, followed by a thin dark argillitic arkose, more felsic volcanics and then the main thick sequence of arkoses, comprising arkose, graded quartzite, argillite and dolomite. A further felsic volcanic unit is found near the top of these arkoses. These rocks of the Rosh Pinah Formation are overlain by further formations composed of limestones, conglomerates, grit, sandstone and argillite.

In the mine area the Rosh Pinah Formation is 1220m thick. The ore zone is in the lower sections of the Formation, underlain by at least 200m of quartzites. The ore occurs just below the dark argillitic arkose and felsites which occupy the middle and upper section of the formation.

The ore bed consists of a well banded to massive carbonaceous cherty zone or micro-quartzite, in places grading into an argillite; various carbonate bearing rocks; sugary quartzite; lenses and bands of massive mixed pyrite, sphalerite and galena; argillite and intercalations of generally poorly mineralised quartzite. The microquartzites are fine grained and dark due to their carbonaceous content. Barium rich carbonate is an important constituent in places. The lower sections of the ore bed are generally Zn rich micro-quartzite, overlain by further micro-quartzites or carbonates with a higher Pb:Zn ratio, while the hangingwall is another micro-quartzite grading to argillite. Most ore is within the micro-quartzites and seldom in the argillites.

The ore minerals are generally present as intergranular disseminations and discrete blebs associated with a fine grained sugary quartz-carbonate matrix, or as thin bands from 1 mm to a few cm's thick of massive sulphide. Irregular barite-carbonate or dolomite lenses are present in the central or lower part of the ore bed.

Massive sulphide bands may be up to a few metres thick in sections of the mine within micro-quartzites and occasionally argillites, and may grade laterally into disseminated ore within the micro-quartzites or carbonates.

In contrast to the hangingwall quartzite which is generally little fractured, the footwall quartzite is intensely fractured forming a breccia, which is silicified and carries sulphide and carbonate veining.

The ore deposit comprises a number of lenses distributed over an area of some 2 x 3 km, each of 150 000 t to 2 to 3 mt. The structure is variable with orebodies ranging from steeply dipping to flat to folded.

The operation is owned (in 2001) and managed by Iscor Limited Base Metals strategic business unit and lies near the southern border of Namibia with South Africa.

Production since 1969 has been 14.5 Mt @ 7% Zn, 2% Pb, 0.1% Cu, 11 g/t Ag. In 1999 proven and probable reserves were quoted at 6.59 Mt @ 8.7% Zn, 2.5% Pb, within a resource of 15 Mt @ 7.5% Zn, 2.2% Pb.

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Field Inspection

A half field traverse of the host lithologies/sequence of the Rosh Pinah District is undertaken.

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Porter GeoConsultancy Home Page | More on This Tour | Other Tours | New Tours | About AMF

For more information contact:   T M (Mike) Porter, of Porter GeoConsultancy   (

This was another of the International Study Tours designed, developed, organised and escorted by T M (Mike) Porter of Porter GeoConsultancy Pty Ltd (PGC) in joint venture with the Australian Mineral Foundation (AMF).  While the reputation and support of the AMF contributed to the establishment of the tours, after it ceased trading at the end of 2001, PGC has continued to develop, organise and manage the tour series.

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