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Manjeri Formation Type Section

This exposure is described in detail by Martin (1978) and Bickle et al. (1975) and only a summary is given here.
The sedimentary succession here is 130m thick with the lower part dominated by argillite and quartzite and ironstone and the other 80m by siltstone and argillite.

Kariba sillimanite quartzite Kariba Heights

The Kariba sillimanite quartzite Kariba Heights, Sample ZMB13/11 is an aluminous quartzite consisting mainly of quartz and sillimanite. The zircons have yielded concordant ages of 2.018 Ga, 2.172, 2.220 and 2.70 Ga (Master et al., 2015). The maximum age of the quartzite is 2.018 Ga, the age of the youngest concordant detrital zircon, while the other zircons reflect a provenance from older crust dated at 2.17, 2.22, and 2.70 Ga.

Pink paragneiss (meta-arkose) of the Malaputese Group

At this outcrop locality, about 10 km further NW from the previous stop, there are numerous roadside outcrops of strongly recrystallized pink paragneiss of the Malaputese Group. The gneisses are interpreted as meta-arkoses, and some show relict cross bedding. They have yielded a detrital zircon population that ranges in age from 2254 ± 18 to 2796 ± 17 Ma, with a strong age peak at ca. 2.7 Ga (Master et al., 2013a,b).

Reliance Formation Type Section

The petrography of the Type Section rocks (Martin 1978) and their chemistry (Nisbet et al., 1977) are described elsewhere and detailed information on some of the more magnesian rocks are given by Nisbet et al (1987).

The Kariba Dam Observation Point

The steps ascending to the interpretive centre (beneath the crochet work) at the Observation Point, and those beyond, reveal banded Kariba Quartzite, with apparent biotite gneiss interleaved in either bedded or thrust relationship.  It is in this situation where weathering is deep and where the dip corresponds with the hill slope, landslip took place threatening to disrupt the tailraces on the south bank.  Extensive drainage, rock bolting and slope sculpture has aleviated this threat.

Tourmalinised amphibolite schists of the Malaputese Group

This is an outcrop on the main Bulawayo to Victoria Falls road, about 3 km NW from the turnoff to Gwaai River Mine (i.e., Mabale Store).  Here there are schistose amphibolites which are strongly impregnated with tourmaline which occurs in the form of black acicular or prismatic crystals. This is one of many examples of tourmalinization in the schist belts of the Dete-Kamativi Inlier, often associated with quartz-muscovite and tin-bearing pegmatites that are of late Mesoproterozoic ca. 1.03 Ga age (Master et al., 2013b). 

Zeederbergs Formation

The outcrop shows a pavement of pillow lavas with spherulites, some patches of pillow breccia and a tuff band. The pillows are generally about 1-2m in cross-section and some 3-D exposures suggest lengths of 3-4m. The spherulites tend to be concentrically arranged, with some flow units consisting almost wholly of coalesced spherulites. In some pillows the spherulites appear to be located around cooling cracks.

Makuti Marble

Outcrop of Matuki Marble in the roadside cutting on the Zambezi escarpment

Archaean (2.71 Ga) migmatitic granitoid gneisses

These are variegated inhomogeneous, polydeformed migmatitic gneisses, with leucocratic quartzo-feldspathic leucosomes and biotitic melanosomes. These migmatitic gneisses are the westernmost dated Archaean rocks of the Zimbabwe Craton. They have zircons which an age of ca. 2.71 Ga (Master et al., 2013a,b)- and they appear to be the source of the 2.7 Ga detrital zircons in the Malaputese Formation meta-arkoses (pink paragneisses), as well as the source of inherited zircons in the Palaeoproterozoic granites intruding the western Magondi Belt.

Hokonui Formation Volcanic Vent

An outcrop interpreted as a volcanic vent is exposed in the bed of the Mtshingwe River. The outline of the “megabreccia” approximates to the river bed and finer-grained sulphidic tuffs occur along the regional strike to the north and south. However, detailed mapping has not been done. The clasts in the breccia of finer-grained, grey tuffaceous rocks (not unlike the surrounding tuffs) and larger fragments of tonalite which are lithologically and isotopically very similar to the Chingezi tonalite which intrudes the Hokonui Formation to the east.