The Ventersdorp Contact Reef, one of the major gold-bearing conglomerate horizons in the Witwatersrand Basin, occurs as a distinct horizon between the overlying Klipriviersberg Group lavas (2714 Ma) and the underlying Central Rand Group rocks (<2894 to >2714 Ma). The Ventersdorp Contact Reef has been metamorphosed and hydrothermally altered under greenschist facies conditions (290–350 °C and 0.2–0.3 GPa). A study of S, O, and H isotopes was carried out to constrain the sources of hydrothermal fluids and gold mineralization in the Ventersdorp Contact Reef. A narrow range of δ 34 S values (−1.5‰ to +1.8‰) for authigenic pyrite, pyrrhotite, chalcopyrite, sphalerite, and galena from the Ventersdorp Contact Reef and its hanging-wall and footwall lithologies suggests a reconstitution of detrital sulfides during fluid circulation at peak metamorphic conditions. The δ 18 O values of authigenic quartz and calcite range from +8.9‰ to +11.3‰, and the δ 18 O and δD values of muscovite separates are between +7.2‰ and +8.4‰ and −62‰ and −31‰ respectively. The estimated δ 18 O (+4.8‰ to +6.1‰) and δD (−27‰ to −39‰) values of the fluids in equilibrium with these minerals under the relevant P-T conditions suggest a metamorphic origin for the fluid. It is concluded that the metamorphic fluids involved were probably derived from the Basin itself, and allogenic sulfides in the Ventersdorp Contact Reef were reconstituted during fluid circulation at peak metamorphic conditions. Accordingly, gold appears to have been locally remobilized and possibly derived from pre-existing placer concentrations.

Abstract Hydrothermal and placer origins for Witwatersrand gold have been debated ever since the discovery in 1886 of the Central Rand goldfield in South Africa. The hydrothermal model is supported by recent findings of a complex postdepositional history for the Witwatersrand Supergroup, including extensive deformation, greenschist facies metamorphism with widespread alteration and associated gold mobility. Critical to the debate is the association of half the Witwatersrand gold with migrated hydrocarbons that were not in their present position at the time of sedimentation. Gold is mined from planar reefs that are centimeters to meters thick and of several hundred square kilometers in area. The mineralogy of the reefs is unusual in having negligible iron oxides, hydrocarbons, and abundant round pyrite. The host rocks to gold include conglomerates and sandstones, with no single depositional environment or inferred depositional process that correlates with high gold-grade areas across the basin. In contrast, the chemical association of pyrite and/or migrated hydrocarbons is ubiquitous in the orebodies. Regional metamorphism in all goldfields generated assemblages including pyrophyllite, chloritoid, chlorite, muscovite, and pyrite, with more restricted kyanite, biotite, kaolinite, and pyrrhotite. Peak temperatures of 300° to 400°C have been inferred with isograds semiparallel to stratigraphy. A period of hydrothermal alteration near the peak of metamorphism has overprinted much of the Central Rand Group in the goldfields, extending 300 km around the basin margin. This alteration has involved loss of Si, Fe, Mg, and Ca, with addition of K and Rb. Geometrically, this hydrothermal alteration coincides vertically and laterally with the distribution of economic gold and with areas of widespread sulfide distribution in all sedimentary rock types. The hydrothermal alteration is distinguishable from weathering by its geometry and the addition of K, Rb, and sulfur. The hydrothermal model invokes uranium introduction in meteoric waters along the uplifted basin margin. During burial diagenesis, thermal maturation of organic material in Witwatersrand shales generated hydrocarbons that were carried by the migrating fluids and precipitated near unconformities, commonly in association with preexisting uranium minerals. Gold-bearing H 2 O-CO 2 -H 2 S fluids at 300° to 400°C were introduced to the Central Rand Group along major basin-bounding thrust faults and were channeled between the overlying Klipriviersberg lavas and the underlying marine shales of the West Rand Group. Fluid flow was controlled by bedding subparallel fracture networks and the sedimentary architecture of the basin that favored flow along lithologically complex reef packages on unconformity surfaces. The hydrothermal model predicts the distribution of gold in the Witwatersrand reefs through sulfidation of detrital iron-rich heavy minerals and precipitation with the migrated hydrocarbons. Hydrothermal gold mineralization is inferred to predate Platberg extensional faulting that displaces the orebodies. The hydrothermal replacement model implies significant potential for exploration in younger sedimentary basins with similar tectonic and thermal histories. Basin architecture, structure, alteration, and suitable chemical traps are important exploration criteria.

Abstract The Witwatersrand gold fields of South Africa account for more than a third of the world's total gold production since mining started there in 1886: 48,000 t Au. These gold fields dominated production throughout the twentieth century, but production peaked at 1,000 t in 1970 and has steadily declined since that time. The regional geologic framework is well understood as a consequence of intensive study and virtually unrivalled three-dimensional information derived from drilling and underground openings, supplemented by seismic data. Advancements of the last decade have come from the integration of stratigraphy, sedimentology, structural evolution, and a much greater appreciation of thermal and fluid processes. Gold has been produced from seven major gold fields located around the northern and western margin of the 350-km-long Witwatersrand basin. Each gold field consists of one major and commonly several minor reef horizons that have been mined semicontinuously for up to 400 km2. Mineralized zones range from 1 cm to several meters in thickness, and the host rock varies from quartz pebble conglomerate and carbon seam to polymictic conglomerate and pyritic quartzite. All reefs are either on or within a few meters above unconformity surfaces, and the major reefs are part of a very distinctive reef package of footwall, unconformity, conglomerate, quartz-rich sandstone and/or shale. The actual distribution of gold has been poorly represented in the literature owing to grade coding, inappropriate averaging, and omission of important features that are critical to understanding the controls on the gold. High grades and remarkable lateral continuity have nevertheless facilitated economic exploitation. The mineralogy of the Witwatersrand reefs is dominated by pyrite with lesser pyrrhotite and arsenopyrite, widespread nickel and cobalt sulfarsenides, and low base metal sulfides. A distinctive mineral assemblage of pyrophyllite-chloritoid-muscovite-chlorite-quartz-rutile-pyrite is found in and around the reef package in all gold fields. This assemblage has been used to constrain peak metamorphic temperatures to just above 300°C to the south and east of the basin, and closer to 400°C in the northwest corner west of the basin near Johannesburg. Two characteristics of the metamorphic event are the nearly strata-parallel distribution of metamorphic grade and an extremely high geothermal gradient. The presence of pyrophyllite and chloritoid in conglomerate, quartzite, shale, basalt flows, and some dikes has been used to indicate an alteration halo embracing the gold fields and approximately 300 km by 50 km (into the basin) by 3 km (of sequence). Quartz veins of up to a few centimeters thickness are common within this alteration halo especially in the reef horizons, but veins of meters thickness are rare. Ubiquitous pyrite throughout the alteration zone indicates elevated levels of sulfur in solution. The elements most closely associated with gold are Fe and C; uranium is also associated with many reefs and extensively mined as a coproduct. A consensus appears to be developing in support of a paragenetic sequence of uranium, then hydrocarbons, then gold. The origin of the Witwatersrand has been of great interest to economic geologists and a source of great contention. Historically, placer and hydrothermal theories have competed, and much more regional and mine-scale data have been used in the debate during the last decade. In the 1980s and especially the 1990s, models shifted from the unmodified to the modified placer model, and from both placer models to a hydrothermal model. Challenges still facing the placer models include regional alteration, structural control on gold, the chemical process of gold remobilization, and the poor match with modern gold placer processes. Moreover, the outstanding issues remain a source area for the gold and a convincing demonstration that processes during sedimentation concentrated gold at all. The hydrothermal replacement model invokes transport of gold into the Witwatersrand Supergroup during metamorphism and associated widespread alteration by a reduced, low-salinity fluid, analogous to other gold-only deposits. Fluids were channeled by structures, unconformity surfaces, and bedding, and gold precipitation was dominated by reaction with carbon- or iron-bearing rocks. These Fe- and C-rich rocks are concentrated immediately above unconformity surfaces. This model proposes that crustal rocks (probably mafic) beneath the Witwatersrand Supergroup are the source of gold. The hydrothermal model links the tectonic evolution of the basin to mineralizing processes, and can thus be used to target other basins with potential for similar mineralization. From the hydrothermal model arise a number of factors that contribute to the enormous size of the Witwatersrand gold fields: The age of the Witwatersrand basin, which predates a major period of gold introduction, The retroarc foreland basin, Major thrust structures around the basin margin, Unconformities in the upper Witwatersrand, Iron-rich nodules on unconformity surfaces, Carbon distribution, High geothermal gradient during gold deposition, Metamorphism and regional alteration, and Limited erosion. Special source regions for detritus and special sorting processes during sedimentation do not appear to have been critical. The Witwatersrand gold formed by the optimization of a set of processes found in other gold provinces, not by unique processes unrepresented elsewhere.

The first serious suggestion that the Archean atmosphere was reducing was based on the interpretation of round uraninite and pyrite grains in the Witwatersrand Basin in the early 1950s. It was then inferred that these minerals were detrital and that they reflected equilibrium with a reducing Archean atmosphere. Over the past 20 years the understanding of the Witwatersrand Basin has changed dramatically with more integrated studies of the basin and the recognition of widespread alteration in close spatial association with the mineralization in every goldfield. Post-depositional mobility of gold, sulfur, and uranium during alteration is widespread and supports hydrothermal ore genesis, or at least substantial modification of the original mineral assemblage. Pseudomorphic replacements of pre-existing detrital minerals (e.g., pyrite after titano-magnetite), and precipitation and/or chemical rounding to generate round mineral shapes (e.g., uraninite in carbon seams) have all been documented. The recognition that the carbon seams formed by the post-depositional introduction and maturation of migrated hydrocarbons is a dramatic departure from earlier models of coalified algal material deposited with the sediments. The enrichment of both gold and uraninite in carbon seams implies that these minerals are hydrothermal and that their shapes do not reflect detrital processes. Uranium mobility in basinal waters may in fact require a relatively oxidizing atmosphere. None of the existing arguments for the Witwatersrand mineralization unambiguously support a placer or modified placer model for the mineralization. Consequently, round uraninite and pyrite of the Witwatersrand Basin do not provide support for a reducing Archean atmosphere.