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Kamoa

Katanga, Dem. Rep. Congo

Main commodities: Cu
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The Kamoa sediment hosted copper deposit lies on the western margin of the Central African Copperbelt, in the Democratic Republic of Congo (DRC), ~25 km west of Kolwezi and 270 km west of the provincial capital of Lubumbashi (#Location: 10° 46'S, 25° 15'E).

Regional Setting

For details of the regional setting of the Kamoa deposit, the Central African/Congolese Copper Belt and the Lufilian Arc, see the Central African Copperbelt - Congolese/Katangan Copperbelt record.

Geology

The Kamoa deposit is located <10 km SSW of the tip of the Nzilo block, a regional NNE-SSW trending, and broadly SSW plunging basement ridge of Kibaran (1.3 to 1.1 Ga) metasedimentary rocks.
   Aeromagnetic data defines a major NNE-SSW trending feature, the ~3 km wide Kansoko Trend, that appears to define the eastern margin of both the Kamoa deposit, and the Nzilo block. This trend is underlain by a thick, 15 to 21° easterly-dipping sequence of weakly carbonaceous and pyrrhotite-bearing diamictite and siltstone, with subordinate andesitic/mafic sill-like bodies to the NE. It is interpreted to represent a major syn-depositional fault zone that has been subsequently reactivated, and now occurs as an east-dipping monocline (Schmandt et al., 2013; Hitzman et al., 2012). It also marks the approximate boundary between a thick, deformed, eastern basinal sequence, comprising well developed Roan Group carbonate and siliciclastic rocks, and a western, shallow-dipping and condensed, siliciclastic sequence of Mwashya Subgroup rocks of the upper Roan Group, unconformably draping onto basement on the basin rim (the Western Foreland of Key et al., 2001).
   The western edge of the Kamoa deposit is bounded (or downfaulted) by the west-side-down West Scarp normal fault (and magnetic feature), with a vertical displacement of 350 to 400 m. This fault also apparently corresponds to the western margin of the exposed Nzilo block, although it does not appear to have been active during deposition of the upper Mwashya Subgroup and lower Nguba Group (Schmandt et al., 2013). It marks the eastern margin of a deep graben (or half graben) that has preserved a thick section of the diamictite of the basal Nguba Group Grand Conglomérat and associated sedimentary rocks, which dip at <10° to the west and south.
   Within the Kamoa deposit area there are a number of curved, but generally ENE-WSW trending faults with minor, generally <10 m of normal offset to the south, some of which may have been active during Katangan deposition.
   Kamoa therefore, overlies a present day NNE-SSW elongated horst that is ~7 to 9 km wide, located along the western edge of the Katangan basin. The host sequence over the horst represents a broad, undulating plateau, punctuated by a series of gentle domes (including the main Kamoa and Makalu domes), where the Grand Conglomérat has been eroded, and the underlying Mwashya Subgroup sandstones are exposed (Schmandt et al., 2013; Parker et al., 2013).
   The NNE-SSW elongated Makalu dome, in the south, covers an area of ~7.5 x 3 km, while the southern lobe of the dumbbell shaped Kamoa dome, 3 km to the NNE, is 4 x 1.5 km, aligned east-west, connected on its northeastern edge by a narrow NNE-SSW neck, to a larger north-south elongated, 10 x 8 km window to the north. The indicated + inferred resource outline of the Kamoa deposit covers an area of ~22 x 12 km, that extends from the southern tip of the Makalu dome, along its eastern margin, reaching its maximum width between the two domes, surrounding the southern half of the Kamoa dome and then extending up the western margin of the northern lobe of the Kamoa dome to taper near that structures northern extremity (2013; Parker et al., 2013).
   These domes are windows, exposing the redox boundary between the underlying hematitic (oxidised) Mwashya Subgroup sandstones in the core of the structures, and the overlying carbonaceous and sulphidic (reduced) Grand Conglomérat, the host to mineralisation, which dips outward from the domes at ~5°.
   The deposit was developed where the thick Katangan sequence markedly thinned as it draped onto the basin margin, in a manner somewhat analogous to the Roan Group pinch-out onto the margin of the Kafue anticline basement high in the Zambian Copperbelt (see the Zambian Copperbelt record).
   The host sequence and basement at Kamoa are autochthonous, located just beyond the outer edge of the mainly allochthonous to para-allochthonous External Fold and Thrust Belt of the Lufilian Arc (as at Kolwezi, 25 km to the east) that was transported north during the Lufilian orogeny, to overlie the Western Foreland (see the Congolese Copperbelt record). While the NNE-SSW aligned Kansoko Trend may have represented a growth fault during deposition of the Katanga Supergroup, it may also have been re-activated as a transfer fault, accommodating differential displacement during the later Lufilian orogenesis, separating autochthonous rocks to the west, from the north directed transport of the allochthonous External Fold and Thrust Belt to the east.
Komoa geology
The geological sequence in the Kamoa district is as follows, from the base (after Schmandt et al., 2013; Parker et al., 2013):
Kibaran basement - quartzite, weakly metamorphosed ferruginous siltstone and greywacke, and minor mafic rocks, exposed to the north of Kamoa within the Nzilo block, deposited between 1.3 and 1.1 Ga (François, 1973; Kokonyangi et al., 2006; Broughton and Rogers, 2010).
angular unconformity
Roan Group (R-4) - which was deposited post 880 Ma, is well developed to the east in the Kolwezi klippe and Tenke-Fungurume Roan window, where it is over 1500 m thick and comprises, from the oldest unit, the R.A.T. Subgroup (R-1), oxidised, purple to red, chloritic and dolomitic detrital sedimentary rocks; the Mines Subgroup (R-2), interbedded reduced and evaporitic stromatolitic dolostone, dolomitic siltstone and argillites containing the bulk of the Cu-Co ores in its lower sections, immediately above the R.A.T.-Mines subgroups redox boundary; the overlying Dipeta Subgroup (R-3), which is lithologically similar, but generally barren; and the uppermost Mwashya Subgroup (R-4), largely composed of dolomitic silty shales/siltstones/sandstones, grey to black, pyritic carbonaceous shales and an upper suite of pink to green feldspathic sandstone, arkose or conglomeratic arkose, alternating with variable amounts of shale or siltite.
   At Kamoa, however, only the Mwashya Subgroup (R-4), is represented, varying from several tens to several hundreds of metres in thickness, made up of the following:
* Poudingue (Roan Grit and Conglomerate), (R-4.1), which rests unconformably on Kibaran basement quartzite to the north. It includes thin to >10 m thick conglomerate bands within pebbly, angular grit and sandstone beds, in a sequence that is typically immature and poorly sorted, with the exception of some conglomerate bands that have a weak feldspathic cement.
* Roan Feldspathic Sandstone, (R-4.2) - compositionally and texturally immature feldspathic sandstones, arkoses and silty arkosic greywacke, which are massive to very coarsely bedded, with beds ranging in thickness from centimetres to several metres. The feldspathic sandstones/greywackes are composed of rounded to subangular grains of quartz and feldspar, commonly with quartz overgrowths, cemented with intergranular quartz and fine-grained muscovite, chlorite and biotite, sometimes containing rare pyrite. They are often gritty and pebbly, with some diffuse, relatively fine-grained conglomeratic bands (≤1m thick), containing pebbles that are generally <1 cm in diameter and dominantly comprise quartz with lesser basement schist and gneiss, basalt, sandstone and limestone. Very fine-grained sandstone, thin dark-coloured, biotite-rich, non-pyritic laminated siltstones and thin hematitic silty bands, with irregularly developed undulating and anastomosing laminae, are locally interbedded with the greywackes, but account for <5% of the unit. The greywackes are normally well cemented, although the top 1 to 5 m below the mineralised diamictite, is often friable and porous, with obvious weathering of feldspar and dissolution of probable dolomite, accompanied by kaolinisation, mostly due to secondary, geologically recent, processes. Symmetric and asymmetric ripples, trough cross bedding, planar stratification and water escape structures are evident to varying degrees, and beds both fine and coarsen upward. These high and low energy traction current sedimentary structures, occasional pebble conglomerates and the compositional immaturity, suggest deposition in a marginal marine to possibly subaerial fluvial environment.
Nguba Group (Ng) - commencing with the Grand Conglomérat (Ng-1.1) - which overlies the Mwashya Subgroup sediments across a sharp contact, suggesting erosion of the underlying, poorly lithified Mwashya Subgroup sediments. The Grand Conglomérat comprises:
* Basal Diamictite Package, (Ng-1.1.1), composed of a basal, 0 to 30 m thick, clast-rich, sandy diamictite (Ng-1.1.1.1) with 20 to 40% clasts; 0 to 5 m of sandstone-siltstone to lithic greywacke, (Ng-1.1.1.2), which is thinly bedded, and only locally present; 0 to 15 m of clast-poor, silty/muddy and weakly carbonaceous diamictite (Ng-1.1.1.3), with only 10 to 20% clasts, that is generally well mineralised and distributed over most of the Kamoa deposit area, although the thicknesses varies, being thicker to the SW. It contains good reductants which catalyse precipitation of copper and is key to the resource.
   It is uncertain, from the source literature, as to how much pre-ore diagenetic pyrite was present within the Basal Diamictite Package (Ng-1.1.1), which hosts the bulk of the post-diagenetic, hydrothermal copper sulphide deposit. The overlying units (Ng-1.1.2 to 1.1.4) contain substantial early diagenetic pyrite, both as fine framboidal and secondary cubic pyrite. Copper sulphides are observed to replace framboidal pyrite in Ng-1.1.1, where unreplaced cores remain, while diagenetic pyrite and copper sulphides of the orebody display overlapping isotopic values, suggesting the latter inherited reduced sulphur from earlier formed diagenetic pyrite (Schmandt et al., 2013). Consequently, it seems likely, the Basal Diamictite Package (Ng-1.1.1) also contained significant diagenetic pyrite prior to ore deposition.
   A 2 to 10 cm thick, thinly laminated mudstone draping the top of the Basal Diamictite Package is a distinctive marker horizon across the central portion of the deposit. It is composed of 1 to 3 mm thick, alternating pale and dark grey laminations made up of mud, composed mostly of fine-grained quartz (up to 20 µm), and lacks diagenetic pyrite.
* Kamoa Pyritic Siltstone-Sandstone (Ng-1.1.2), which is 15 to 45 m thick - the lower pyritic siltstone-sandstone unit, which is predominantly well stratified and laminated, with bedded pyrite. The basal contact with diamictite is frequently characterised by a thin (<20 cm) clast-supported quartzitic conglomerate. The lower portion always includes mudstone beds with abundant shale pellets. This unit contains 5% to >25% pyrite, both as very fine grained, framboidal disseminations, and as secondary, very coarsely recrystallised, subhedral to euhedral crystals. The lowermost 3 to 5 m generally contains only fine grained pyrite, but it may also locally host copper mineralisation
* Middle Diamictite Package (Ng-1.1.3) - with clasts that usually range between 2 and 200 mm across, rarely in the 50 to 200 cm range, and are frequently dominated by quartzite, very fine-grained sandstone, shale and black argillite, very variable amounts of mafic rocks (mainly dolerite), with subordinate vesicular lava, quartz and scattered granitic and schistose basement cobbles. Coarse feldspathic sandstone clasts are rare and tend to be preferentially weathered. Rare clasts of Roan dolomite have also been recorded.
* Upper Laminated Pyritic Siltstone (Ng-1.1.4) - similar to the Kamoa Pyritic Siltstone-Sandstone (Ng-1.1.2)
* Uppermost Diamictite Package (Ng-1.1.5) - which is farthest removed from mineralisation and the least altered diamictite in the deposit area, with a matrix of quartz, chlorite, plagioclase, potassium feldspar, mica (muscovite and biotite), carbonate minerals (calcite and minor ankerite) and minor heavy minerals (tourmaline, rutile, apatite), with minor disseminated pyrite. Clasts are similar to the Middle Diamictite.

Igneous activity that is temporally and spatially associated with the host sequence includes, basaltic flows, pillow breccias and hyaloclastite breccias, together with gabbroic and doleritic textured mafic igneous rocks, occurring within the Mwashya Subgroup and the base of the Grand Conglomérat, directly northeast of the Kamoa deposit (Schmandt et al., 2013). These are described as one or more, 5 to 80 m thick, apparently concordant tabular bodies, which may be sills or flows, in the Kansoko Trend to the north of the deposit, and as >200 m of vesicular to massive, brecciated and altered, pale green to light grey-green lava grading into a fine-grained igneous rock, probably of andesitic composition, encountered in drilling adjacent to the deposit (Parker et al., 2013).

Diamictite units represent the most volumetrically abundant lithofacies in the Grand Conglomérat at Kamoa, and vary from 10 to 300 m in thickness, with strike lengths in excess of several kilometres. Clasts range from ~2 mm to 3 m in diameter and from well rounded to angular. They include exotic lithologies such as quartzite, quartz-mica schist, phyllite, limestone, dolostone, argillaceous dolostone and gabbro as well as locally derived basalt, Mwashya Subgroup greywacke, and Grand Conglomérat siltstone, greywacke and diamictite. The matrix is composed of silt (2.5 to 20 µm) that varies from light to dark grey or grey-green in colour (Schmandt et al., 2013).
   Framboidal and secondary pyrite in diamictites are most common low in the Grand Conglomérat and probably largely grew in situ, although some may be detrital grains derived from erosion of underlying pyritic sediments (Schmandt et al., 2013).
   Sedimentary structures and the matrix-supported nature of the diamictites, suggest deposition by mass transport or sediment gravity flow processes, e.g., slumping and debris flow, while rare graded beds indicate occasional turbidity currents (Schmandt et al., 2013).
   Dark grey to grey lithic greywacke lenses are irregularly interbedded through all of the diamictite packages, and range from ~3 to 30 m in thickness, extending discontinuously over strike lengths up to 3 km, though most persist for <1 km along strike. They generally have sharp lower and gradational upper contacts with diamictite, and are composed of silt to pebble size (3 µm to 2 cm) grains and clasts, with grains that average 0.2 to 1 mm of mainly quartz, with lesser feldspar and carbonate (calcite and ankerite) minerals. Sedimentary structures indicate deposition by turbidity currents, while their geometry suggests deposition in channels or between diamictite lobes, derived from glacial outwash flows or from reworking of unlithified diamictite (Schmandt et al., 2013).
   Two similar laminated pyritic siltstone units (Ng 1.1.2 and Ng 1.1.4) within the Grand Conglomérat sequence, are continuous across the deposit area, and range from 2 to 40 m in thickness. Individual laminae vary from millimetres to centimetres and are planar laminated or massive, and normally or reverse graded, with occasional asymmetric and symmetric ripples. They are interpreted to have been deposited by turbidity currents. They include intervals with minor millimetre to a few centimetres thick interbeds of sandstone or conglomerate and diamictite beds up to 15 cm thick. The laminated pyritic siltstones are composed of quartz, pyrite, K feldspar, chlorite, carbonate (ankerite >>dolomite), muscovite and biotite, while interbedded sandstones comprise quartz grains cemented by ankerite. Pyrite is abundant throughout the laminated siltstones, particularly in coarser grained graded beds, with some bands containing >60 vol.% pyrite, mostly framboidal, ranging from <2 to ~20 µm, averaging 5 to 10 µm. Secondary diagenetic pyrite overgrows pyrite framboids, and is mostly cubic, occasionally up 5 mm in diameter, and often concentrated in distinct, cm-scale layers. Rip-up clasts of siltstone within overlying diamictite layers commonly contain framboidal pyrite, indicating pyrite precipitation during early diagenesis (Wilkin et al., 1996; Schmandt et al., 2013).

The Katangan rocks in the Kamoa area contain chlorite, and are weakly metamorphosed to lower greenschist facies.

Diagenesis and Alteration

At Kamoa, diagenetic minerals occur across the district, throughout the stratigraphy, while hydrothermal minerals are most abundant in and near the ore zone.

Petrography suggests that prior to diagenesis and hydrothermal alteration, the greywackes, siltstones and conglomerates of the Mwashya Subgroup were composed of detrital quartz, feldspar and clay, whilst the Grand Conglomérat diamictites and siltstones were mostly composed of fine-grained rock flour and detrital grains of quartz and feldspar, as well as a variable range of lithic clasts (Schmandt et al., 2013 and references cited therein).
   During burial diagenesis at depths of <2 km, and temperatures of <~100°C, they would have undergone recrystallisation of quartz, formation of chlorite from clay, feldspar overgrowths on detrital feldspar, and precipitation of quartz and carbonate cements. With increased burial and temperature, albitisation of feldspar would be expected, together with dolomitisation of calcite. Any external heat input, e.g.,  the intrusive or extrusive mafic magmatism known in the sequence, or the influx of hydrothermal fluids, could produce an increased temperature gradient and form the deeper assemblages, but at shallower depths (Schmandt et al., 2013 and references cited therein).

In addition to these diagenetic assemblages, the uppermost Mwashya Subgroup rocks and the basal portion of the Grand Conglomérat currently contain significant hydrothermal muscovite, K feldspar and biotite, as well as lesser ankerite, and lack plagioclase or significant calcite. The absence of significant plagioclase and the abundance of potassium feldspar and biotite in these rocks indicate they have undergone potassic alteration. The presence of ankerite suggests relatively high temperature alteration in the presence of reduced pore fluids (Schmandt et al., 2013 and references cited therein).
   Hydrothermal alteration occurs in two styles, comprising fine-grained alteration mineral assemblages within the diamictite matrix and prominent rims of coarse-grained minerals surrounding lithic clasts within the Grand Conglomérat diamictites. These coarse grained rims are thickest and most abundant within and proximal to the ore zone within the basal diamictite.
   Hydrothermal alteration mineral assemblages at Kamoa are zoned relative to the contact between the Mwashya Subgroup and the Grand Conglomérat, with the most intense alteration and mineralisation occurring at the base of the Grand Conglomérat, indicating that the hydrothermal fluids utilised the underlying Mwashya Subgroup arenitic siliciclastic rocks as an aquifer.
   Both the fine and coarse grained mineral assemblages comprise quartz, muscovite, K feldspar, biotite, Mg-rich chlorite, ankerite and sulphides at the base of the mineralised zone, and grade upwards to a suite dominated by calcite and Fe-rich chlorite at the top of the zone of alteration. These assemblages suggest three sequential types of hydrothermal alteration affected the rocks (after Schmandt et al., 2013):
i). potassic - an intense potassic alteration event (accompanied by silicification), which post-dated diagenetic (framboidal) sulphide precipitation, was focused in the lower stratigraphic units of the Grand Conglomérat, and is characterised by an increased abundance and size of K feldspar and biotite in the matrix and in clast/grain rims, as well as the increase in matrix muscovite toward the base of the Grand Conglomérat. These minerals, which are concentrated within and adjacent to the ore zone, are commonly intergrown with Cu sulphides, and hence this event was temporally associated, at least in part, with copper mineralisation. The hydrothermal fluids responsible for copper precipitation had temperatures of ~225°C.
ii). silicification - occurring as coarse grained quartz rims and silicification of clasts toward the base of the Grand Conglomérat, generally coeval with the potassic alteration and Cu sulphides.
iii). magnesian - magnesian chlorite is pervasive throughout the stratigraphic sequence and commonly forms the exterior layer on clast rims, indicating it is paragenetically late, relative to potassic alteration, silicification and most sulphide precipitation. However, overall, this phase produced extensive chlorite alteration at stratigraphically higher levels in the Grand Conglomérat than those affected by the earlier potassic alteration and silicification event. Minor copper mineralisation continued during this phase, as evidenced by chlorite intergrown with copper sulphides.
   A later, overprinting, bleached, probably albitic-dolomitic alteration is locally present adjacent to quartz-carbonate-sulphide veins in the west of the deposit, near the West Scarp Fault (Parker et al., 2013).

Mineralisation

Mineralisation at Kamoa is located immediately above the redox boundary at the contact between the oxidised Mwashya Subgroup arenites and the base of the overlying reduced diamictites of the lower Grand Conglomérat, and is capped by the hanging wall Kamoa Pyritic Siltstone-Sandstone (Ng-1.1.2) unit (Schmandt et al., 2013; Parker et al., 2013).
   The host sequence comprises several interbedded units that appear to control the distribution of mineralisation. The lowermost clast-rich diamictite unit (Ng-1.1.1.1) is thought to have been only weakly reduced, and generally hosts low-grade (<0.5% Cu) mineralisation throughout. Copper sulphides tend to be most abundant where this unit is thin or absent, such that the overlying reduced units are in direct contact with the underlying oxidised Mwashya Subgroup sandstones. Most of the higher-grade mineralisation occurs within the more strongly reduced clast-poor, carbonaceous and pyritic diamictite unit (Ng-1.1.1.3), or in the intervening sandstone and siltstone (Ng-1.1.1.2) which is frequently absent (Schmandt et al., 2013; Parker et al., 2013).

Tenke Fungurume lithologies

High grade intersection at Kamoa showing lenses of chalcopyrite-bornite (e.g., as indicated by arrowheads) within the weakly deformed host siltstones and reworked glacial sedimentary rocks that constitute the main host in the Grand Conlomérat of the basal Nguba Group.   Photographs by Mike Porter.


   Sulphide mineralisation was precipitated in two main stages (after Schmandt et al., 2013):
i). the earliest took place during diagenesis, and formed abundant fine framboidal and coarse secondary cubic pyrite, most commonly in the lower units of the Grand Conglomérat, which contains unusually high amounts of early diagenetic framboidal pyrite. This pyrite probably largely grew in situ, and is mostly preserved in the laminated pyritic siltstones and to a lesser extent in some greywacke lenses and diamictites. The coarse, secondary diagenetic pyrite overgrows pyrite framboids, and is mostly cubic, occasionally anhedral, and up to 5 mm in diameter, and is often concentrated in distinct, centimetre scale layers. Framboidal and secondary diagenetic pyrite may be either uniformly distributed within individual beds, or mimic sedimentary structures.
ii). a later period of dominantly hydrothermal copper sulphide mineralisation, which affected the uppermost Mwashya Subgroup rocks, the lower diamictite package (Ng-1.1.1) of the Grand Conglomérat and, locally, the lower siltstone unit, the Kamoa Pyritic Siltstone-Sandstone (Ng-1.1.2). Associated ore stage pyrite is distinguished from diagenetic secondary cubic pyrite by its more anhedral shape as well as its occurrence in mineral rims to lithic grains and clasts. Copper sulphides both overgrow, and replace diagenetic framboidal and secondary cubic pyrite.
   δ
34S isotopic values from diagenetic pyrite, both framboidal and secondary cubic varieties (-11 to -1‰), closely overlap values for copper sulphides in the lower Grand Conglomérat (-12 to +3‰ with most values between -12 and -5‰). This suggests the copper sulphides inherited reduced sulphur from earlier formed diagenetic pyrite. Inheritance of sulphur during copper sulphide replacement is also supported by the textures of some fine-grained copper sulphides in the diamictite matrix and siltstones that are similar in size and shape to framboidal pyrite. Coarse-grained copper sulphides also share the same light sulphur isotope values, suggesting that they also derived at least some of their reduced sulphur from framboidal pyrite (Schmandt et al., 2013).
   However, due to lack of preserved framboidal pyrite, and complete replacement of pre-ore minerals by copper sulphides, Schmandt et al. (2013) suggest petrographic analysis has not been able to demonstrated that the Grand Conglomérat contained a sufficient volume of diagenetic pyrite to account for the observed volumes of both fine- and coarse-grained copper sulphides by the replacement of diagenetic pyrite (c.f., in Michigan, USA - see the separate White Pine record).
   Hydrothermal fluids responsible for copper precipitation at Kamoa were moderately saline (~23 to 26 wt.% NaCl 
equiv.) and had temperatures of ~225°C (Schmandt et al., 2013).
   The total thickness of the hypogene sulphide zone at a 1% Cu cutoff, varies from 2 to 15 m. Copper mineralisation occurs as a low grade (generally <1% Cu) sheet over thicknesses that rarely exceed 1 m within the footwall Mwashya Subgroup sandstones, with the bulk of the ore in the overlying Basal Diamictite Package (Ng-1.1.1), as well as locally within the base of the overlying Kamoa Pyritic Siltstone-Sandstone (Ng-1.1.2). The lowermost 3 to 5 m of the Ng-1.1.2 unit may locally host copper mineralisation, but generally only contains pyrite, occurring mainly as very fine-grained, framboidal disseminations, with lesser coarsely recrystallised, subhedral to euhedral grains (Schmandt et al., 2013; Parker et al., 2013).
   The principal sulphide minerals within the orebody are chalcocite, bornite, chalcopyrite and pyrite, which share common bedding and replacement textures, ranging from semi-massive accumulations, to disseminations, to very coarse blebs, and occasionally occur as veins. Sulphides commonly mantle and or partially replace clasts in the diamictite (Schmandt et al., 2013).
   Copper sulphides are zoned, relative to the Mwashya Subgroup-Grand Conglomérat contact, upward, from chalcocite (Cu
2S), through bornite (Cu5FeS4) to chalcopyrite (CuFeS2), then pyrite and, finally, minor sphalerite and/or galena. The upper pyrite zone, locally with abundant sphalerite in its lower sections, commonly extends for hundreds of metres above the copper ore zone, although this is principally early diagenetic, and not hydrothermal pyrite. A similar mineral and elemental zonation occurs laterally outward (Schmandt et al., 2013).
   The three copper sulphide species and pyrite form overlapping zones, such that the lower, more copper-rich sulphide generally mantles or partially replaces the overlying, more copper-poor sulphide (e.g. chalcocite mantles bornite in the overlap between these two mineral zones), particularly on the up-section side of clasts in the diamictite, where there may have been more permeability (low-pressure shadow) (Parker et al., 2013; Schmandt et al., 2013).
   Copper sulphide mineral zonation is poorly developed below the Grand Conglomérat-Mwashya contact, but is a mirror image of that in the diamictite, with chalcocite and bornite giving way to chalcopyrite and finally pyrite down section. Sphalerite and galena are rarely present. These sulphide zoning patterns suggest that hydrothermal fluids, at least locally, moved laterally along the contact between these two units (Schmandt et al., 2013).
   Trace element geochemistry (Schmandt, 2012) indicates that minor enrichment of Pb and Co occur at the outer/upper edge of the main copper zone, in the Grand Conglomérat, although the Co appears to be contained within pyrite. The overall outward metal zoning pattern is Cu-Co-Pb-Zn. Unlike the other deposits in the Congolese Copperbelt, Kamoa is not known to contain carrollite, and the overall Co content in ore samples rarely exceeds several hundred ppm (Schmandt et al., 2013; Parker et al., 2013).
   Chalcocite, bornite and chalcopyrite constitute between 5 to almost 15 vol.% of the rock in the ore zone, occurring as both i). very fine grained (<50 µm) disseminations, usually anhedral and equidimensional, distributed throughout the diamictite matrix and ii). coarse-grained crystals that rim, or partially to completely replace clasts, particularly those of mafic igneous rocks. These rimming sulphide minerals are generally anhedral and may form crystals up to 5 cm in length, although they generally represent <10% of the total sulphide content of the rocks. Sphalerite and galena occur stratigraphically above well-developed copper sulphide zones, with textures that mimic those of the copper sulphides (Schmandt et al., 2013; Parker et al., 2013).
   Similar sulphide mineral assemblages are generally recognised in both styles at a particular location, and are intergrown with a similar suites of alteration minerals. These relationships suggest that both the fine disseminated and coarse-grained 'rim' sulphides were precipitated simultaneously. Vein-hosted sulphide minerals are rare to absent at Kamoa. Coarse-grained sulphides in rims to lithic clasts within the lower diamictite are often intergrown with and locally appear to replace chlorite, biotite, potassium feldspar, quartz and ankerite (Schmandt et al., 2013).
   Sulphides are preferentially distributed along the coarser-grained, more permeable layers within the basal greywacke lenses (Parker et al., 2013).
   Throughout much of the deposit, there is a sharp increase from <0.5% Cu to >1% Cu at the top and bottom of continuous zones grading >1% Cu, representing a natural cut-off (Parker et al., 2013).

Supergene enrichment has taken place below a leached cap, where the Kamoa ore zone intersects the present day surface, over a strike length of several kilometres. The leached cap has a vertical thickness of ~10 to 50 m, generally ~30 m, and contains only trace amounts of copper within a vuggy zone where feldspar has been altered to clay. Supergene chalcocite, which mantles iron-bearing sulphides (chalcopyrite and pyrite), is accompanied by minor native copper and cuprite. It defines a supergene-enriched zone that extends to depths of ~100 m below the surface, but locally to as much as 250 m, and to ~400 m within fracture and fault zones, and along the basal diamictite-sandstone contact. The main supergene ore mineral chalcocite, overprints, replaces and upgrades the hypogene chalcocite, bornite and chalcopyrite zones of the dipping hypogene orebody, with a mixed supergene-hypogene interface. Cuprite (Cu
2O) is uncommon, and occurs as tiny specks and blebs in contact with supergene chalcocite, and as fracture fillings and along rare bedding planes, most commonly just above the top of the Mwashya Subgroup sandstones. Native copper occurs as crystalline plates along oxidised joints and occasionally as specks and veinlets, particularly within a few decimetres above the top of the Mwashya Subgroup sandstones. It commonly replaces chalcocite in this position, and has been found as bedding-parallel veinlets in siltstone and replacement blebs in weathered basal diamictite. Grades of >5% Cu are common within supergene zones. Malachite, azurite, chrysocolla and libethenite occur locally, mostly in fractures related to faults and joints, and as a weathering product of supergene chalcocite (Parker et al., 2013; Schmandt et al., 2013).

Published NI 43-101 compliant mineral resources as of January, 2013 (Ivanplats website, 2013), applying a 3 m thickness cutoff, and different grade limits, were:
  1% Cu cutoff
      indicated resources - 739 Mt @ 2.67% Cu;
      inferred resources - 227 Mt @ 1.96% Cu.
  2% Cu cutoff
      indicated resources - 550 Mt @ 3.04% Cu;
      inferred resources - 93 Mt @ 2.64% Cu.
  3% Cu cutoff
      indicated resources - 224 Mt @ 3.85% Cu;
      inferred resources - 19 Mt @ 3.04% Cu.

Information in this summary has in part been taken from "Parker et al., March 2013, Kamoa Copper Project, Katanga Province, Democratic Republic of Congo, NI 43-101 Technical Report on Updated Mineral Resource Estimate", prepared for Ivanplats Limited.

The most recent source geological information used to prepare this summary was dated: 2013.     Record last updated: 19/9/2013
This description is a summary from published sources, the chief of which are listed below.
© Copyright Porter GeoConsultancy Pty Ltd.   Unauthorised copying, reproduction, storage or dissemination prohibited.


  References & Additional Information
 References to this deposit in the PGC Literature Collection:
Hitzman M W, Broughton D, Selley D, Woodhead J, Wood D and Bull S,  2012 - The Central African Copperbelt: Diverse Stratigraphic, Structural, and Temporal Settings in the Worlds Largest Sedimentary Copper District: in Hedenquist J W, Harris M and Camus F, 2012 Geology and Genesis of Major Copper Deposits and Districts of the World - A tribute to Richard H Sillitoe Society of Economic Geologists   Special Publication 16, pp. 487514
Schmandt D, Broughton D, Hitzman M W, Plink-Bjorklund P, Edwards D, Humphrey J,  2013 - The Kamoa Copper Deposit, Democratic Republic of Congo: Stratigraphy, Diagenetic and Hydrothermal Alteration, and Mineralization: in    Econ. Geol.   v.108 pp. 1301-1324


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