Highly metamorphosed Malmesbury rocks in other parts of the area comprise metaquartzite, amphibolite, and different types of gneiss and granulite containing numerous aplite and pegmatite veins. The gneiss and granulite consist mainly of quartz and orthoclase; most varieties contain garnet and some are also rich in biotite. 

The sediments, occurring mainly in the central portion of the area, lie with a sedimentary contract on a very uneven floor of older formations. 

The Kuibis Series consists of 100 to 400 feet of quartzite with lenticular shale bands and conglomerate locally at the base.

The Schwarzkalk Series is divided into 3 stages according to lithology. The lower stage consists of siltstone, mudstone, and shale with interbedded bands of sandstone, grit and conglomerate. The middle stage is made up mainly of shale, mudstone and siltstone with interbedded bands of sandstone and greywacke. A thin sandstone zone is locally developed at the top. The upper stage comprises tillite, boulder-clay, conglomerate, clay-pellet conglomerate, grit, sandstone, shale and mudstone. A zone of arenaceous strata follows the glacial deposits in some localities, but the entire stage is missing in some places.

The Schwarzrand Series consists of a thick succession of mudstone with lenticular bands of siltstone, sandstone, grit and rarely limestone. The Fish River Series consists of sandy sediments with interbedded lenses of shale, mudstone and siltstone.

The different types of mud structures, local unconformities, rill-marks, ripple-marks and cross-bedding point to the deposition in the littoral zone of sedimentation. Glacial conditions prevailed during the upper Schwarzkalk time.

Only the Table Mountain and the Bokkeveld Series represent the Cape System. The latter is comprised of shale only. The Table Mountain Series consists mainly of feldspathic sandstone with subordinate conglomerate layers. It rests discordantly on the Nama sediments. The maximum thickness of Table Mountain Sandstone is 350 feet; it thins out completely northwards due to original conditions of deposition and denudation by ice in Dwyka times.

The basal Karoo strata rest uncomfortably on all the older formations. The Dwyka Series and the Lower Ecca Stage underlie the eastern quarter of the area. The Dwyka tillite was deposited on a very uneven floor with a regional slope eastwards. Glacial striae show that the ice moved towards the southeast.

The Lower Dwyka Stage, with a maximum thickness of 700 feet, consists mainly of tillite. A well-developed zone of sandstone is found some 50 feet above the base of the stage. Lenticular bands of sandstone, shale and siltstone are found on all horizons. Calcareous concretions and replacements of tillite by limestone are often found. 

The Upper Dwyka Stage consists of two portions. At the base is thick shale with sandstone lenses, isolated pebbles and chertified layers. At the top is the black shale of the White Band, which contains secondary gypsum, limonite and limestone lenses and weathers white.

The Lower Ecca Stage with a maximum thickness of 550 feet consists only of greenish shale and mudstone with chert lenses.

Scree and fanglomerate occupy large areas along the escarpment of the Bokkeveld Plateau, on the slopes of other mountains and on areas underlain by Dwyka tillite. Small isolated foothills off the Bokkeveld Plateau are capped by scree and stand out above the plains with younger deposits of similar nature. 

Surface quartzite, sandstone, and surface-conglomerate occur in many places below the Great Escarpment. According to Lamont the silcrete is of Miocene age.

Surface limestone is of widespread occurrence. Some of it must be the oldest superficial deposit of surface-conglomerate overlies it on one locality. Other occurrences are of more recent origin and still form on the calcareous matrix of Dwyka tillite.

River-terrace gravel is well developed on terraces of two different ages along the Sout River and its tributaries. The lower terrace is only a few feet above the streambeds. The thin gravel upper terrace lies some fifty feet above the streambeds. The lower portion of the deposit, which consists of sandy clayey silicified beds with interbedded gravel, is up to 30 feet thick. The upper portion, consisting of course gravel, rests discordantly on the lower portion and must be much younger. Along the edge of the Bokkeveld Plateau the coarse river-terrace gravel grades into scree and fanglomerate. 

Large quantities of alluvium occur along all the major rivers. The western portion of the area is covered by Aeolian sand to a large extent.

Sills and dykes of dolerite are plentiful in the eastern half of the area where they are intruded in all the formations, but mainly in the Karoo sediments. The sills range in thickness from 30 to 300 feet; the thick ones are prominent in the topography. Dykes are from 1 ft to 50 ft wide with exceptional ones of 250 ft that extend for 28 miles. Some of the dolerite is olivine-bearing. 

The sediments on the contact of dolerite intrusions have been indurated or rechrystallised. Calcite was formed in Dwyka shale and garnet in calcareous shale. In some localities country-rock was assimilated and hybrid rocks were formed. Rheomorphic veins occur near dolerite contacts in many places. Prehnite, calcite and epidote have replaced the dolerite in some instances. 

Rocks of the Malmesbury Formation have been folded to varying degrees of intensity. The fold axes trend from west-northwest-southeast in the Knersvlakte. The Nama sediments dip to the southwest consistently and are faulted down to the northeast in every case. The Nama sediments are also folded; the incompetent Schwarzkalk beds are more intensely folded than the Kuibis quartzite. Several large faults that trend from southeast to northwest delineate a graben in the surroundings of Brandkop. The sediments are intensely folded in these faults.

Defamation of the Nama sediments when they were still in a plastic state is reflected in intraformational folding, contortion of beds, brecciation and faulting due to slumping. Moving ice masses also caused folding.

The Cape and Karoo sediments have a low regional dip to the east. A few relatively small faults, in which there are dolerite dykes, displace the Karoo sediments and dolerite sheets.