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Chapter 6 Provenance of Detrital Zircons from the Wolkberg Group and Transvaal Supergroup

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Chapter 6 Provenance of Detrital Zircons from the Wolkberg Group and Transvaal Supergroup Provenance of detrital zircons from the Wolkberg Group and Transvaal Supergroup Chapter 6 Provenance of Detrital Zircons from the Wolkberg Group and Transvaal Supergroup 6.1 Introduction The Wolkberg Group and Transvaal Supergroup (Fig 6.1) are sequences that preserve a ca. 600Ma long, almost continuous record of late Archean (ca. 2.7Ga) to Paleoproterozoic (ca. 2.1Ga) sedimentation (Fig 6.2) on the Kaapvaal Craton. In an attempt to trace source populations of detrital zircons for the Wolkberg Group and Transvaal Supergroup, representative samples of zircons from several prominent quartzite successions were analysed by SHRIMP (sensitive high resolution ion microprobe) in order to obtain 207Pb/206Pb radiometric ages. Based on these results two 94 Provenance of detrital zircons from the Wolkberg Group and Transvaal Supergroup 95 Provenance of detrital zircons from the Wolkberg Group and Transvaal Supergroup important geological issues in South African geology are to be addressed in this chapter namely: a) Whether the Wolkberg and correlative Buffelsfontein Group belong to the Transvaal Supergroup and if the sediments could have been sourced from the Limpopo Metamorphic Belt. b) What are the ages of source areas (provenance ages) of different unconformity- bounded sequences in the Pretoria Group of the Transvaal Supergroup? Radiometric ages of between 2670 and 2600Ma (Gutzmer and Beukes, 1998; Barton et al., 1995) suggest that deposition of the Wolkberg Group and Schmidtsdrif Subgroup of the Transvaal Supergroup in Griqualand West (Fig 6.1) occurred concurrently with granulite facies metamorphism in the Limpopo metamorphic complex (Fig 6.2). It is widely accepted that granulite facies metamorphism in the Limpopo Mobile Belt occurred at ca. 2660Ma (Barton and Van Reenen, 1992). However, a period of ca. 2000Ma granulite facies metamorphism has also been identified in the Limpopo Belt (Holzer et al., 1998). It therefore remains uncertain when the Zimbabwe and Kaapvaal cratons became connected. Many studies of the Limpopo Belt have identified magmatic and metamorphic zircon with radiometric ages between 2.7-2.6Ga (i.e. McCourt and Armstrong, 1998; Kröner et al., 1999; Barton et al., 1992; Barton et al., 1994; Kreissig et al., 2001). If the collision between the Kaapvaal and Zimbabwe cratons occurred at ca. 2.7-2.6Ga, then one would expect to find a large population of 2.7-2.6Ga zircons in the Wolkberg Group. This is one of the hypotheses to be tested in this chapter of the thesis. Furthermore, the recently proposed revised correlation for the Transvaal Supergroup in the Griqualand West and Transvaal areas (Beukes et al., 2002) can be tested. The correlation subdivides the Transvaal Supergroup into six sequence stratigraphic units (Fig 6.2), based on the presence of major unconformities in the succession (Coetzee, 2001, Beukes et al., 2002). Amongst other consequences, the Dwaal Heuvel Formation of the Pretoria Group is now regarded laterally equivalent to the beds of the Gamagara/Mapedi Formation in Griqualand West (Fig 6.2)(Beukes et al., 2002). Measuring the radiometric ages of detrital zircons within each of the unconformity-bounded sequences, may help 96 Provenance of detrital zircons from the Wolkberg Group and Transvaal Supergroup understand the ages of rocks that sourced the sequences and also perhaps place age constraints on the boundaries of sequences. In addition, the variation in detrital zircon populations may indirectly provide some information about the plate tectonic history of the Kaapvaal craton during the deposition of the Wolkberg and Transvaal successions. In other words, data may provide some insights into the tectono-sedimentary events that led to formation of the unconformity-bounded sequences. 6.2 Stratigraphic Setting 6.2.1 Wolkberg Group and Correlatives The Wolkberg Group is an up to 2000m thick sedimentary succession (Button, 1973, Bosch, 1992), that crops out in the Limpopo Province, South Africa (Figs 6.1 and 6.3). It consists of alternating feldspathic quartzites and argillaceous sedimentary rocks, coarse quartz arenites, some conglomerates, basaltic lava and minor stromatolitic carbonate beds (Fig 6.3)(Button, 1973, Bosch 1992). It is correlated with the Buffelsfontein Group of the Thabazimbi area (Fig 6.1)(Tyler, 1979). The Wolkberg Group comprises from the base upwards the Sekororo, Abel Erasmus, Schelem, Selati, Mabin and Sadowa Formations (Fig 6.3)(Button, 1973 and Bosch, 1992). The basal Sekororo Formation overlies Archean basement granite and greenstone of the Kaapvaal craton with an erosional unconformity (Button, 1973). Barton et al. (1995) obtained an age of 2664±0.7Ma for rhyolitic lava in the Witfonteinrand Formation of the Buffelsfontein Group that is thought to be correlative to the Abel Erasmus lavas (Fig 6.3)(Tyler, 1979). The basement granites and greenstone belts to the Wolkberg Group have radiometric ages that vary from 2.78 (Henderson et al., 2000) to greater than 3Ga (De Wit et al., 1992; De Wit et al., 1993; Brandl and De Wit, 1997; De Wit and Ashwal, 1997; Armstrong et al., 1990; Nelson et al., 1999). It appears, as if the Kaapvaal craton was mildly flexed prior to the deposition of the Wolkberg Group (Button, 1973; Beukes, 1983). The formations of the Wolkberg Group thicken in pre-Transvaal trough structures, and thin and pinch out against pre-Wolkberg basement domes (Button, 1973). The Wolkberg Group thickens towards the northeastern margin of the present day Kaapvaal craton, suggesting that it covered a much larger area 97 Provenance of detrital zircons from the Wolkberg Group and Transvaal Supergroup 98 Provenance of detrital zircons from the Wolkberg Group and Transvaal Supergroup during its deposition. Paleocurrent directions for the Wolkberg Group are predominantly from the northeast and north (Button, 1973; Bosch, 1992). The Wolkberg and Buffelsfontein Groups could perhaps be correlated with the Schmidtsdrif Group in Griqualand West. This correlation is based on recent zircon ages of 2669±5Ma and 2650±8Ma from tuffaceous beds within the Schmidtsdrif Subgroup (Fig 6.3)(Gutzmer and Beukes, 1998). These ages are similar to the age of the Buffelsfontein Group rhyolite obtained by Barton et al. (1995). It therefore appears as if the Wolkberg Group and Schmidtsdrif Subgroup are time equivalent successions, deposited simultaneously on different parts of the Kaapvaal craton (Fig 6.3). The Schmidtsdrif Subgroup consists predominantly of quartzite, shale, carbonate and some lava, in contrast to the predominantly coarse-grained siliciclastic rocks of the Wolkberg Group (Fig 6.3). The differences in lithologies could indicate that the Wolkberg Group and Schmidtsdrif Subgroup were deposited in two subbasins separated by the Ganyesa dome (Fig 6.3). Only after the deposition of the Motiton Member in Griqualand West did these two basins become connected. The Motiton Member is suggested here to be equivalent to the Black Reef Formation that marks the onset of Transvaal Supergroup deposition at approximately 2590Ma (Fig 6.3). Previously, it was suggested that the Wolkberg Group is equivalent to the Ventersdorp Supergroup (Eriksson et al., 1993). However, the basal Vryburg Formation of the Schmidtsdrif Group overlies the upper Allanridge Formation of the Ventersdorp Supergroup with a marked erosional unconformity (Fig 6.3). It is therefore unlikely that the Wolkberg Group is equivalent to the Ventersdorp Supergroup. A SHRIMP 207Pb/206Pb zircon age of 2709±4Ma (Armstrong et al., 1991) has been obtained for quartz porphyry of the Makwassie Formation of the Ventersdorp Supergroup (Winter, 1976) and is thus markedly older than the Wolkberg Group. 99 Provenance of detrital zircons from the Wolkberg Group and Transvaal Supergroup 6.2.2 Transvaal Supergroup 6.2.2.1 Chuniespoort and Ghaap Groups The Wolkberg Group is unconformably overlain by the Black Reef Formation, which marks the base of the Transvaal Supergroup in the Transvaal area and southeastern Botswana (Fig 6.3)(Button, 1973). Given new geochrological restrictions the most likely correlative to the Black Reef quartzite in the Northern Cape Province becomes the quartzite of the Motiton Member at the top of the Monteville Formation (Figs 6.2 and 6.3)(Beukes, 1978). This is a very different concept from the commonly accepted idea that the Black Reef quartzite in the Transvaal area corresponds to the base of the Vryburg Formation in Griqualand West (Beukes et al., 2002). Radiometric 207Pb/206Pb ages of 2602±14Ma (Gutzmer and Beukes, 1998) obtained for the Monteville Formation (top of the Schmidtsdrif Group) and 2550±3 (Walraven and Martini, 1995) and 2583±5 (Martin et al., 1998) for the Oak Tree Formation (base of the Malmani Subgroup) suggest that the deposition of the Black Reef Formation in the Transvaal area commenced at ca. 2590Ma (Figs 6.3 and 6.4A). According to the new correlation, deposition of the Black Reef Formation of the Transvaal Supergroup in the Transvaal area commenced at the same time as the onset of the deposition of the Motiton Member on top of the Monteville Formation, in Griqualand West. This contact represents a 2nd order sequence boundary in the Transvaal Supergroup (Fig 6.2)(Coetzee, 2001). Present day outcrop of the Transvaal Supergroup suggests that the erosional surface along the sequence boundary covered the whole of the Kaapvaal Craton (Fig 6.4A). Lithostratigraphic correlation is unequivocal between the Ghaap Group in Griqualand West (Beukes, 1978) and the Chuniespoort Group (Obbes, 1995) in the Transvaal
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