Where is tenor reef

At the current level of exposure, the Southeastern lobe appears to lack the lower two zones. The Western Bushveld lobe is effectively separated into two parts Southwestern and Northwestern by the later intrusion of the Pilanesberg alkalic intrusion. A fourth compartment Far Western Bushveld lies west of the Pilanesberg. Here, except for one or two minor localities, only marginal rocks of the layered series are preserved; another fully developed lobe probably existed in this area, but has been mostly removed by erosion.

The fifth compartment, the Northern Limb, may well be part of another lobe although the rocks exposed along it exhibit some differences from those of the other bodies. Rocks that can be equated with the Lower and Critical Zones elsewhere are observed only in the extreme south of the limb south of the Ysterberg—Planknek fault, van der Merwe, The Main and Upper Zones are present along much of the limb, although somewhat attenuated in comparison with the Eastern and Western lobes Ashwal et al.

The various zones and units vary greatly in thickness throughout the complex, and are absent in some areas. The lower zones vary in thickness partly because of their transgressive nature and appear to have had the most restricted development. In many places, the Critical Zone transgresses over a wider area of the Bushveld floor than the Lower Zone, and the Main Zone a still wider area. Von Gruenewaldt and Kruger have attributed the transgression to the progressive addition of new magma as the Complex crystallized, equating the emplacement to the progressive filling of saucer-like structures.

Drawing on the data of Eales et al. They proposed that the missing magma escaped up the sides of the structure, interacting with the country rocks on the way, and that this has given rise to Platreef and other zones of marginal mineralization. Seabrook et al. They concluded that two different magmas were present during the crystallization of these cyclic units, one of Main Zone type referred to as T-type subsequently contributing plagioclase and one of Critical Zone type U-type contributing orthopyroxene.

They stressed that the compositions of the rocks of the Merensky and Bastard cyclic units are the result of the mixing of minerals, not magmas. Before describing the Merensky Reef it is necessary to define what is meant by the term. In this study we adopt the definition of Cawthorn et al. We are mainly concerned with the Reef as it occurs in the northwestern and southwestern segments of the complex. Aspects of the geology within — m of the Reef that are important to the interpretations presented in this study are summarized below.

A major change in the stratigraphic sequence of rocks within the interval between the top of the UG-2 and the Merensky Reef occurs at about the position of the much younger Pilanesberg intrusion see Fig. This is illustrated in Fig. In general, large thicknesses of norite, leuconorite and anorthosite are present in the south, interrupted by more mafic horizons, whereas in the north the more felsic intervals are significantly thinner and less abundant, and the mafic units are both thicker and richer in pyroxene and olivine.

The latter is an olivine—orthopyroxene—plagioclase cumulate with a distinctive platey fabric. Note the greater overall thickness of anorthosite and norite in the former. The Merensky cyclic unit is overlain by the Bastard cyclic unit, which is similar in many respects, except that the sulfides at its base are both less abundant and have much lower PGE tenors see below.

The Bastard unit is overlain by rocks belonging to the Main Zone. Olivine is much more prevalent in the Reef in the northwestern Bushveld, although it also occurs intermittently throughout the southwestern portion.

In some areas a third chromite layer may occur within the pegmatoid or in the pyroxenite above the pegmatoid. Figure 4a shows an example of pegmatoidal Reef, surrounding an elliptical zone with a normal cumulus texture. These are illustrated schematically in Figs 5 and 6. In the SE Eastern Platinum Mines , up to 10 m of Pre-Merensky cyclic unit pyroxenite is present, overlying interbanded norite and anorthosite. A chromite layer and uneconomic amounts of PGE-rich sulfides may be present at this contact.

The Pre-Merensky pyroxenite is overlain by a thin chromite layer, which is taken to mark the contact with the overlying Merensky pyroxenite.

This layer is completely missing in some areas and intermittent in others. Significant amounts of disseminated PGE-rich sulfide are present at the contact between the Pre-Merensky and Merensky pyroxenites, extending up to 1 m both above and below the contact see data on TN72 discussed below. Reef thicknesses decrease progressively from 10 m to less than 1 m over a distance of about 4 km west from Eastern Platinum mine.

Variations from one type to another occur over lateral distances of m or less, and tend to show a relationship to structures, such as faults and horst and graben structures, that pre-date or are contemporaneous with emplacement of the Bushveld Complex.

Whereas thick reef is predominant to the east and adjacent to the Pilanesburg in the extreme NW, reef types vary locally elsewhere, and tend to be related to structurally induced irregularities in the Merensky footwall. The vertical bars indicate the types of Reef investigated in this study.

Schematic section through the stratigraphic succession including the Merensky Reef in the NW Bushveld. In some areas it cuts through the Tarentaal and lies on the underlying anorthosite and in others, particularly at Union Section, it cuts through the anorthosite and underlying pyroxenite and harzburgite into a pyroxenite that is part of the UG-2 cyclic unit.

The downcutting of the Merensky cyclic unit is also arrested by an intermediate anorthosite horizon, the Footwall Marker, and where it does this the Reef is referred to as NP2 Reef. Where the Merensky pyroxenite is in contact with, or close to, footwall anorthosite units these show the development of olivine that has been described by Smith et al.

This section should be viewed in conjunction with Fig. Figure modified after Viljoen Normal Reef is as described above. It thins towards the area of regional pothole, where the upper chromite layer and overlying Merensky pyroxenite cut down through the stratigraphy to level out at different horizons within the underlying footwall. Horizons that appear to have been particularly favoured are a feldspathic harzburgite the Tarentaal and an intermediate-level mottled anorthosite.

Smith et al. Their data show that, even within the regional pothole, the down-cutting is irregular, and that down-dip to the SE the Reef reverts to its normal position in the stratigraphy.

Distribution of Reef types at Northam after Smith et al. Although the Regional Pothole Reef is the most dramatic illustration of irregularities between the Merensky Reef and the underlying cumulates, potholing on a smaller scale, forming structures typically 50— m in diameter and 3—12 m deep Viljoen et al.

Furthermore, the base of the Reef is very commonly unconformable with respect to igneous layering in the footwall rocks. Figure 4b shows the marked unconformity between the Reef and the underlying banded norites and anorthosites at Western Platinum mines.

In places discrete masses of footwall rock project up into the Merensky pyroxenite Fig. The basal chromite of the Reef can be observed to thicken on some of the steps into the rolls, giving the impression that the chromite was carried as a bottom load, and became concentrated in hydraulic traps Fig. An interesting aspect of the northwestern Bushveld is the interaction between the magma responsible for the formation of the Merensky pyroxenite and the footwall rocks.

Roberts et al. They concluded that the fine grain size, textural relations between minerals and the distribution of sulfide and olivine are better explained by the reaction of the footwall rocks with a downward infiltrating magmatic liquid than by the upward streaming of aqueous volatiles. Locally, sulfides occur in the footwall norites and anorthosites, apparently having settled from the overlying pyroxenite. The extent to which this has happened is variable.

The precise positioning of the two deflections with respect to each other in the plane of the Reef is not known, but would not be greater than a few metres. At least two influxes of magma, the Pre-Merensky and Merensky magmas, have contributed to the formation of the Merensky Reef. These appear to have been hot, energetic pulses that physically and thermally eroded the footwall rocks in many places to cause single potholes or, in the northwestern Bushveld, regional pothole reef.

The presence of olivine in the cumulates ascribed to the Pre-Merensky cyclic unit in the northwestern Bushveld indicates that here this magma was more primitive and probably hotter than its equivalent in the southwestern Bushveld.

This interpretation is contrary to that of Seagrove et al. Rather, they proposed that a layer of T-type magma was injected beneath the Merensky magmas, and that the pyroxene grains settled through this to come to rest on the footwall see discussion on density considerations below.

The locations of the 25 drill-hole profiles that have studied from the Western Bushveld are shown in Fig. Sampling was constrained by the amount of material available. Where this had not been sampled in the course of routine mine sampling, we were able to take half-core samples; in this case samples were selected at 10 cm intervals.

Where half-core had been taken previously for mine sampling, we restricted ourselves to quarter-core samples, 20 cm in length. This scale of sampling is unsuitable for studying the fine structure across profiles through thinner sections of the Merensky Reef, but gives a reasonable picture of broad variations through the Merensky and Pre-Merensky cyclic units. In a number of cases we also obtained samples from underground that were sliced at 2 cm intervals see below to show the finer structure within the Reef.

Location of drill holes sampled for this study. Samples were crushed and milled at the analytical facility operated by Anglo American at their Research Laboratory in Johannesburg, where samples were also analysed for sulfide Ni, using the ammonium citrate leach technique see discussion below.

Detection limits for PGE were better than 2 ppb for all elements. As discussed above, our sampling of the southwestern Bushveld was aimed to investigate four main aspects of PGE distribution: 1 variation across the Merensky Reef, the overlying pyroxenite of the Merensky cyclic unit and the immediately underlying footwall rocks; 2 detailed variation within or very close to the Merensky Reef; 3 variation between the Merensky Reef and the top of the UG-2 cyclic unit intermittent 30 cm samples ; variation within the Merensky cyclic unit and thick Pre-Merensky cyclic unit at Eastern Platinum and Western Platinum mines.

The primary objective of this study was to examine the variation in tenor of sulfides that make up the Merensky Reef. The primary mineralogy of the major sulfides is pyrrhotite po , pentlandite pn and chalcopyrite cp , and the total amount of sulfide present in each sample has been calculated on the basis of analyses for S, Ni and Cu using the method outlined by Naldrett , p.

The assumption that all but a negligible amount of the Ni is in the sulfide phases is not justified in the case of samples with a low sulfide content and high olivine or pyroxene content; thus many of the samples have been analysed for sulfide Ni as well as total Ni, and the former figure has been used in the calculation.

It was found that the technique used for determining sulfide Ni ammonium citrate leach gave unreliable results when the samples were altered particularly when serpentinized ; some Ni appears to have been leached from minerals other than sulfide, with the consequence that too much sulfur is used up in calculating the Ni as pentlandite, and the remnant sulfur is a negative value, leading to a negative quantity of pyrrhotite.

This value is typical for sulfide-rich assemblages in which any Ni leached from non-sulfide environments is very small in comparison with that in sulfide. A potentially more serious problem lies in the assumption that the present S content is the same as the original S content.

Li et al. As already mentioned, our samples were collected away from the more hydrothermally affected areas surrounding potholes. We sampled only those drill-hole intersections that appeared in hand-specimen to be entirely fresh, in which the sulfides showed sharp contacts with silicates and occupied interstitial locations characteristic of magmatic sulfide.

As a further check on this aspect, we have determined the Se contents of those of our samples that have sufficient Se to be analysed with reasonable precision. Results are shown in Fig. The sulfides of the UG-2 samples are highly altered, with all of the pyrrhotite replaced by pyrite.

This is taken as evidence that the MR samples are relatively unaltered and that the present S content is close to the original content.

An important aspect of the interpretation of the tenor of PGE in the sulfides of the Merensky Reef is whether any given sample contains excess sulfides, or merely sulfide that has been forced out of solution during the crystallization of trapped intercumulus liquid.

A reasonable S content for a magma that has evolved to the stage of that responsible for the Merensky Reef of the Bushveld Complex is ppm Cawthorn, b. Where the calculated sulfide content of our samples lies well above the shaded area, it is likely that this is due to the presence of excess sulfide; where the points fall within or below this area, excess sulfides are unlikely to have been present. Before discussing the variations across the Merensky Reef, it is important to understand variations in the footwall rocks to the Reef.

Here, as discussed above, rocks of the Merensky cyclic unit are present at much lower levels in the stratigraphy than their normal position.

As discussed above Fig. Where the Merensky Reef rests on these units, at first sight it appears to comprise two chromite layers and associated sulfide, although the lower chromite, some of the sulfide, and the enclosing rocks are not from the Pre-Merensky cyclic unit, but belong to the footwall units.

Their shape suggests that they settled as masses with a gelatinous consistency that sagged as they came to rest within a partially consolidated layer of cumulus plagioclase. Only one pyroxenite boulder was intersected in PDL, and this is characterized by a fairly high Pt content ppb , and a higher than ambient sulfide content. In general, the sulfide contents are low between the Footwall Marker 10 Fig.

One of the most striking aspects of Fig. The two dark vertical lines in Fig. As mentioned above, the evidence points to an influx of fresh, relatively primitive, orthopyroxene-bearing, sulfide-saturated magma at this level over the top of a somewhat viscous magmatic plagioclase-bearing mush. Sulfides and PGE appear to have been absorbed into the host, plagioclase-bearing magma, and Fe-sulfide has been dissolved and removed, leaving the host magma enriched in PGE in a manner analogous to that proposed to explain variations in TN72 see Electonic Appendix 3 and discussion below.

In hole W-1, the Reef is immediately underlain by 16 m of anorthosite, leuconorite and norite that have low sulfide and PGE concentrations, and relatively constant metal ratios.

This interval is underlain by a chromite layer that is part of the P2 cyclic unit. Two peaks in sulfide concentration occur within the P2 unit, one associated with the chromite at the norite—feldspathic harzburgite contact and the other at the lower contact with the underlying anorthosite.

The upper sulfide concentration constitutes the P2 Reef. The P1 cyclic unit, comprising anorthosite and underlying pegmatoidal olivine pyroxenite, forms the footwall to the P2 cyclic unit. A chromite layer and associated PGE-enriched sulfides P1 Reef occur within the olivine pyroxenite, just below the anorthosite of this unit. Cawthorn et al. Each influx deposited chromite followed by orthopyroxenite and sulfide. We accept these interpretations, and refer to the lower chromite and overlying pyroxenite as the Pre-Merensky cyclic unit, and the upper chromite, and overlying pyroxenite, norite and anorthosite as the Merensky cyclic unit.

Data for samples from this hole, and for a hand sample from Townlands shaft, are given in Table 1. Figure 11 shows data for the overlying Bastard Reef from the same hole.

The hatched area in Fig. Sulfide contents lying within or to the left of this zone indicate samples with little or no excess sulfide, and those lying to the right of it are interpreted to contain sulfide in excess of that that could be dissolved in the intercumulus liquid.

The data shown by the lines with a series of small dots are 2 cm samples from a hand sample from the same shaft, but not the same position. They are discussed below. The grey dots and continuous line are data from the hand specimen that was sampled at 2 cm intervals; the black squares, open diamonds and black dots are from our 20 cm sampling of the drill core. These figures show data plotted in the same manner as in Fig.

Representative analyses the full dataset is given in Electronic Appendix 1. All of our results for the southwestern Bushveld are shown on plots similar to that of Fig. Because disruption to the normal stratigraphy of the Reef is known to occur in potholes, holes within or close to these structures were avoided during our sampling. Where possible, two deflections of a given hole were analysed to provide an indication of the representativeness of our data. It is standard practice in Bushveld exploration to drill a single hole and, a few metres above important horizons such as MR or UG-2, to insert wedges in the original hole to deflect the drill bit once it is reinserted and resumes drilling, so that more than a single intersection through the horizon is obtained.

In some cases results from both deflections are shown in the figures, but where no significant differences existed between the two deflections, the results have been averaged on the basis of their position in the stratigraphy. In some cases e. Although only Pt tenor is shown in Fig. TN72 is an exception to this and is discussed below.

In some cases the ratio increases, in some cases it does not. They noted that the PGE tenors in the Pre-Merensky pyroxenite appear to be partly dependent on the extent of the mingling. Holes TN72 and WP32 show much more systematic tenor variations, which are discussed in detail in Electronic Appendix 3. The main aspects of these variations are as follows: a high-tenor sulfides appear up to 1 m below the chromitite that is regarded as marking the contact between the Pre-Merensky and Merensky pyroxenites, showing a progressive upward decrease in tenor across the chromitite and into the Merensky pyroxenite; b these high-tenor sulfides are underlain by a zone up to 2 m thick that is sulfide poor but PGE-enriched; c at the base of the Pre-Merensky pyroxenite in both holes there is a 20—30 cm thick sulfide-poor zone also enriched in PGE.

Because so much of the northwestern Bushveld consists of a regional pothole, the sampling here also included Pothole Reef. As noted above, the pyroxenite and basal chromitite of the Pre-Merensky cyclic unit are not present in the area affected by the regional pothole, and, although a second chromite layer is often present in the zone of mineralization forming the Reef, this is the P2 chromite, and the mineralization associated with it very probably belongs to the P2 Reef, perhaps modified to some extent by mineralization associated with the Merensky as opposed to Pre-Merensky pulse.

The Reef is significantly thicker in the northwestern Bushveld than in the southwestern, and the spacing of our sampling across Normal Reef should have provided enough resolution to examine ratio and tenor variations related to the bottom chromite seam Pre-Merensky chromite.

Given the necessary coarseness of most of our sampling, and the small distances over which variations in metal tenor and ratio have been observed, it is reasonable to ask whether, if the sampling had been more closely spaced, we would have reached the same generalizations.

For this reason we collected some large samples of rock providing profiles across the Reef in a number of localities. These were then sliced at 2 cm intervals to provide more detailed profiles across the Reef.

Pt tenor and metal ratio data for hole TLU 10 cm Reef, Townlands shaft, southwestern Bushveld are compared with data for hand samples from roughly the same locations in Fig. Despite the fact that the positions of the hand sample and drill hole are not the same, the trends for the two Townlands locations are very similar.

The close correlation between the presence of sulfide and PGE enrichment has always dominated ideas about the genesis of the Merensky Reef Vermaak, , and references thererin; von Gruenewaldt, ; Campbell et al. Evidence bearing on whether mixing of a U- and T-type magma occurred at the level of the Merensky Reef has an important bearing on the origin of the PGE mineralization. Campbell et al. Subsequently, as better sulfur solubility data became available, considerable debate developed as to whether the mixing of two magmas with U- and T-type compositions could produce sulfide immiscibility Li et al.

Hanley et al. Pt solubility increased with increasing temperature and decreased markedly with increasing NaCl concentration. Wilmore et al.

These concepts are summarized in Fig. Any discussion of the relative merits of these two basic hypotheses would have to be comprehensive, and would be beyond the scope of this paper. Models for the origin of the Merensky Reef from Naldrett et al. As Cawthorn et al. The difference in the distance between the upper and lower chromite layers is attributed to the magma responsible for the Merensky cyclic unit variably eroding the pyroxenite of the Pre-Merensky unit.

Partial erosion resulted in as much as 10 m of the latter remaining in some areas Eastern Platinum Mines area , whereas complete erosion, or non-deposition, resulted in none remaining in other areas contact Reef. The pegmatoidal recrystallization characteristic of the Reef in some areas is particularly developed where the upper chromite layer is less than 50 cm above the lower layer, suggesting that heat from the later influx is partly responsible for the recrystallization.

It was pointed out above Fig. It is assumed that sulfides are settling from an overlying body of magma, and that their settling rate is rapid with respect to the speed with which they are segregating, so that any Pt depletion experienced by the magma as the result of sulfide segregation affects the Pt content of subsequently segregating sulfide. Theoretical scenarios involving fractional segregation of sulfide. If sulfides segregate fractionally from a body of magma, one would expect the PGE to become depleted in the magma much more rapidly than base metals such as Cu.

Maier et al. Of the profiles shown in Fig. In profile PDL Fig. This is also the case with the Haakdoorndrift profile of Contact Reef Fig. In the Contact Reef profile from Impala mine Fig. These sulfides have a uniform, high Pt tenor which suggests that they could have resulted from a bottom load, but, alternatively, could have resulted from mixing during the settling process.

In general, it appears that there is little substantive evidence of the magma carrying a substantial bottom load of PGE-enriched sulfide. In many of the profiles shown in Fig. Mining operations commonly include rock several tens of centimetres below the lower chromite layer in recognition of this.

Godel et al. The exceptions are: the underground sample from Townlands shaft Fig. Boreholes TN72 and WP32 are discussed in the following section.

Thus, in this case, there is evidence that fractional segregation of sulfide also occurred from the influx of Pre-Merensky magma, although this single example is insufficient to claim that this can be considered as a global observation. The Bastard Reef, as seen in Fig.

Provided that, as shown in Fig. The most primitive sulfides settled farthest, followed by successively more fractionated material. The intercumulus liquid of the Pre-Merensky pyroxenites was probably unsaturated in sulfur, so that as the initial sulfides settled, iron sulfides were partially dissolved, raising the tenor of those elements more chalcophile than Fe.

As the settling sulfides penetrated deeper into the unconsolidated Pre-Merensky pyroxenite mush, an increasing amount of sulfide was dissolved, with the result that PGE tenors in the remaining portion of sulfide increased progessively with settling.

This is thought to be the consequence of the settling of MCU sulfides, which became progressively enriched in PGE as a result of dissolution during downward percolation.

The model curves reproduce the observed trends very closely. Considering the spike in PGE present at the lower contact of the Pre-Merensky pyroxenite, as discussed above, this occurs with no spike in sulfide.

It is suggested that the first wave of Pre-Merensky cyclic unit magma deposited PGE-enriched sulfides here, but that subsequent Pre-Merensky magma was unsaturated in sulfide as evidenced by the low concentrations present in most of the Pre-Merensky pyroxenite and dissolved Fe sulfide away, but not significant amounts of PGE, giving rise to the PGE spike and the very high calculated tenors present at this contact.

The settling of sulfides below the top chromite layer in WP32 is significantly less than has occurred in TN72, although the high tenor of the interstitial sulfides that extends nearly 1 m below the chromite layer is probably due to the resorption of Fe sulfide but not PGE as has been discussed for TN72 above.

The exponential decay of Pt, and Pt and Pd tenors is also interrupted by a spike in these parameters 50 cm above the top chromite layer, which again can be explained if the MCU magma was the result of at least two surges, the second causing a refreshment in the PGE content of the initial MCU magma. It is suggested that the movement of PGE by settling sulfide that becomes progressively dissolved as it settles into or becomes engulfed by sulfide-unsaturated magma is an important process in the distribution of PGE in the Bushveld Complex.

Data for Pt tenors over 1 m true distance close to and above the top chromite layer of the MR are shown on a non-logarithmic scale in Fig.

The maximum tenors found in the Union and Amandelbult areas, and in the profiles of thicker Reef in the Styldrift area, are much higher than those of much of the southwestern Bushveld. Values of the maximum tenor are plotted along with the location of the profile in Fig. In the Union—Amandelbult area, there appears to be a decrease in tenor towards the NE reaching ppm at Haakdoorndrift and to the SW reaching ppm of this area.

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