70-694: The Hottentots Holland Mountains are part of the Cape Fold Belt in the Western Cape , South Africa . The mountain range forms a barrier between the Cape Town metropolitan area and the southern Overberg coast. The range is primarily composed of Table Mountain Sandstone , and lies between the eastern Cape Town suburbs of Somerset West and Gordon's Bay to the west, and the Elgin valley to
140-707: A major earthquake , originating from movement of the northern end of the Worcester Fault. Another major (inactive) fault runs for 300 km along the southern edge of the Swartberg Mountains. The Swartberg Mountains were uplifted along this fault, to such an extent that in the Oudtshoorn region the rocks that form the base of the Cape Supergroup are exposed. These are locally known as the "Cango Group", but are probably continuous with
210-526: A maximum thickness of 2000 m, was laid down. These sandstones are very hard, and erosion resistant. They therefore form the bulk of mountains and steep cliffs and rugged crags of the Cape Fold Belt, including the upper 600 m of the 1 km high Table Mountain , below which Cape Town is situated. It contains no fossils. The Peninsula formation can be traced from 300 km north of Cape Town (i.e. about 50 km north of Vanrhynsdorp on
280-421: A maximum width of about 50 km (mostly only 15–30 km wide). Almost all of these ranges consist of hard erosion resistant Peninsula Group rocks. The valleys tend to be floored by Bokkeveld Group mudstones. A remarkable feature of these ranges is that the 1500 m high mountains (from base to crest) are cut through by very narrow, almost vertically walled defiles , not much more than 50–70 m wide at
350-644: A mountain range of immense proportions to the south of the former rift valley. The folded Cape Supergroup formed the northern foothills of this towering mountain range. The weight of the Falkland-Cape Supergroup mountains caused the continental crust of Southern Africa to sag, forming a retroarc foreland system, into which the Karoo Supergroup was deposited. Eventually much of the Cape Supergroup became buried under these Karoo deposits, only to re-emerge as mountains when upliftment of
420-556: A road cutting between Durban and Pietermaritzburg , particularly at the Marian Hill Toll Plaza. Most of the group has been deeply eroded by numerous rivers creating the ragged plateaus and scarps of the Durban-Pietermaritzburg region. With the widening and deepening of the rift valley, the entire southern portion of what was to become South Africa, as far as a line extending from Calvinia in
490-515: A thin layer (on average only about 60 m thick ) in the Peninsula Formation rocks of the more inland mountains to the west of a line between Swellendam and Calvinia . These diamictite rocks are composed of finely ground mud, containing a jumble of faceted pebbles. They can easily be recognized at a distance as this formation readily erodes into fertile, gently sloping, green swaths in a landscape where this contrasts starkly with
560-553: A variety of brachiopods , as well as trilobites , molluscs , echinoderms (including starfish , crinoids , and the extinct blastoids and cystoids ), foraminifera and fish with jaws ( placoderms ). The upper layers of the Bokkeveld Group become increasingly more sandy, grading into the sandstone of the Witteberg Group , named for the range of mountains to the south of Matjiesfontein and Laingsburg in
630-460: Is Afrikaans for mountain; its plural is berge .) 33°24′S 22°00′E / 33.4°S 22°E / -33.4; 22 Ellsworth Mountains The Ellsworth Mountains are the highest mountain ranges in Antarctica , forming a 350 km (217 mi) long and 48 km (30 mi) wide chain of mountains in a north to south configuration on the western margin of
700-563: Is a World Heritage Site with an area of 70,000 hectares from Elgin to north of Villiersdorp , between the Stellenbosch Mountains and the Groenland mountains . The reserve functions as a conservation area for mountain fynbos, with about 1300 plant species, of which some are rare and endemic. About 110 species of bird have been recorded, and a variety of indigenous animals, some of which have been reintroduced. Altitude in
770-803: Is a fold and thrust belt of late Paleozoic age, which affected the sequence of sedimentary rock layers of the Cape Supergroup in the southwestern corner of South Africa . It was originally continuous with the Ventana Mountains near Bahía Blanca in Argentina , the Pensacola Mountains (East Antarctica), the Ellsworth Mountains (West Antarctica) and the Hunter-Bowen orogeny in eastern Australia. The rocks involved are generally sandstones and shales , with
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#1732780099361840-551: Is attested to by the fact that the 1 km high Table Mountain on the Cape Peninsula is a syncline mountain , meaning that it formed part of the bottom of a valley when the Cape Supergroup was initially folded. The anticline , or highest elevation of the fold between Table Mountain and the Hottentots-Holland Mountains (1.2 to 1.6 km elevation), on the opposite side of the isthmus connecting
910-751: Is the Howard Nunataks Formation of quartzites, the Mt. Liptak Formation of quartzites, and the Mount Wyatt Earp Formation of quartzites. Major deformation of the sedimentary rocks occurred during the Gondwanide orogeny , followed by later uplift . The temperatures in the Ellsworth Mountains average around -30 °C (-20 °F). The best time for expeditions are November through January, mid-summer in
980-522: Is truncated by the overlying Dwyka sediments of glacial origin. The latter forms part of the Karoo Supergroup . Therefore, the Witteberg Group forms the uppermost layer of the Cape Supergroup. It tends to form the most inland outcrops of the Cape Supergroup, and can be traced eastwards as far as the Bokkeveld Group can be traced (i.e. to Port Alfred), about 120 km beyond the Cape Fold Belt. The Bokkeveld and Witteberg groups do not occur in
1050-618: The Argentinian and British ones. The mountains were discovered on November 23, 1935, by the American explorer Lincoln Ellsworth in the course of a trans-Antarctic flight from Dundee Island to the Ross Ice Shelf . He gave them the descriptive name Sentinel Range. The mountains were mapped in detail by the U.S. Geological Survey from ground surveys and U.S. Navy aerial photography, 1958–1966. When it became evident that
1120-663: The Cape Supergroup , which is more extensive than the Fold Belt. The Supergroup is divided into several distinct Groups. The western and southern extents of the Supergroup have been folded into a series of longitudinal mountain ranges, by the collision of the Falkland Plateau into what would later become South Africa (see diagrams on the left). However, the entire suite in this region slopes downwards towards
1190-723: The Cape Town City Bowl and Table Bay. The Pakhuis Formation is also well exposed on the road along Michell's Pass just below the Tolhuis, and especially on the Pakhuis Pass near Clanwilliam , from which the formation derives its name. The glaciers which formed the Pakhuis and Cederberg formations came from the north west, in the direction of the South Pole which was located in the neighborhood of Cameroon at
1260-494: The Carboniferous and early Permian periods. After closure of the rift valley, and rucking of the Cape Supergroup into a series of parallel folds, running mainly east-west (with a short section running north-south in the west, due to collision with eastward moving Patagonia), the continued subduction of the paleo-Pacific Plate beneath the Falkland Plateau and the resulting collision of the latter with Southern Africa, raised
1330-649: The Cederberg 200 km to the north of the Cape Peninsula , and then along the south coast as far as Port Elizabeth , 650 km to the east (see the two maps one above the other on the right). The rocks were laid down as sediments in a rift valley that developed in southern Gondwana , just south of Southern Africa, during the Cambrian - Ordovician Periods (starting about 510 million years ago, and ending about 330–350 million years ago). (See
1400-584: The Gondwana rifting when South America and the Falkland Plateau separated from Africa. Patagonia was to the west of Cape Town and the Falkland Islands were to the south during the Jurassic Period prior to separation. Most of these faults are inactive today, but on 29 September 1969 the towns of Ceres and Tulbagh , about 160 km north-east of Cape Town, were severely damaged by
1470-593: The Ou Kaapse Weg (road) goes up the slope from Westlake on to the Silvermine plateau. In the cutting one can also see the abrupt and obvious transition into the Peninsula Formation above it. Looking up the slope from below to the first hairpin bend, the granite basement on which the Graafwater formation rests is visible. And in the cutting at the first hairpin bend, the ocher-colored, gritty clay into which
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#17327800993611540-732: The Ronne Ice Shelf in Marie Byrd Land . They are bisected by Minnesota Glacier to form the Sentinel Range to the north and the Heritage Range to the south. The former is by far the higher and more spectacular with Mount Vinson (4,892 meters (16,050 ft)) constituting the highest point on the continent. The mountains are located within the Chilean Antarctic territorial claim but outside of
1610-544: The Tradouws Pass , Kogmanskloof, Garcia's pass, the Gourits River gorge (which does not have a road running through it), and Michell's Pass , which is, however, more V-shaped than the others, but impressive nevertheless. In addition several roads and highways crest the mountains over cols, or go through them via tunnels. A number of parallel faults still run roughly parallel with the coast, having formed during
1680-491: The " Malmesbury Group " that forms the base of Table Mountain on the Cape Peninsula , and similar outcrops in the Western Cape . In the Little Karoo the outcrop is composed of limestone , into which an underground stream has carved the impressively extensive Cango Caves . The following is a list of the largest individual ranges within the Cape Fold Belt include from west to east. (Translations in brackets; berg
1750-472: The 7,500 meters (24,600 ft) thick Early Cambrian - Middle Cambrian Heritage Group overlain by the 3,000 meters (9,800 ft) thick Late Cambrian - Devonian Crashsite Group; the 1,000 meters (3,300 ft) thick Permo-Carboniferous Whiteout Conglomerate (black diamictite ) from Gondawanaland glaciation; and the 1,000 meters (3,300 ft) thick Permian Polarstar Formation consisting of black argillite , siltstone , sandstone , and coal. Within
1820-502: The Cape Fold Belt, being made up of the local lowest (oldest) strata of the Cape Supergroup, composed predominantly of quartzitic sandstone which forms the impressive, almost vertical cliffs which characterize the mountain and the rest of the range which constitutes the backbone of the Cape Peninsula . The degree to which the original Cape Fold mountains (formed during the Carboniferous and early Permian Periods) have been eroded
1890-602: The Cape Supergroup sediments, but also the southern portions of the Dwyka and Ecca Groups of the Karoo Supergroup. By the time Gondwana broke up about 150 million years ago, the Falkland Mountains had been all but eroded away, before drifting south-westwards to their present position off the coast of southern South America , close to Cape Horn , leaving behind only the submarine Agulhas Bank along
1960-675: The Dwarsberg plateau) and summer temperature maxima rarely exceeding 25 °C. Snow is not unusual on the higher peaks, like Verkykerkop, Somerset Sneeukop ( Afrikaans : Snow Peak ) at 1590 m high and The Triplets in the northern section of the range. This area and the other ranges to the south are considered the hub of the Cape floristic region with the most biodiversity in the entire fynbos biome. The surrounding lowlands have rich alluvial soils supporting viticulture and other deciduous fruit farms. The Hottentots Holland Nature Reserve
2030-586: The Fold Belt into the Eastern Cape and northern KwaZulu-Natal , where no folding took place. The initial sedimentation into the rift valley which developed in southern Gondwana (see diagram at top left) was confined to the western and eastern ends of the rift. Rivers diverted into these early rifts deposited sand and gravel to form the Klipheuwel Group in the west, and the Natal Group in
2100-1040: The Heritage Group is the Union Glacier Formation of ashflow tuff - lahar deposits, the Hyde Glacier Formation of graywacke -argillite-conglomerate, the Drake Icefall Formation of black shales and marble, the Conglomerate Ridge Formation of conglomerate and quartzite , the Liberty Hills-Springer Peak-Frazier Ridge Formations of quartzite-argillite, and the Minaret Formation of marble. Within the Crashsite Group
2170-522: The Karoo's Ecca Group . During these Ecca times continued collision of the Falkland Plateau into Southern Africa, and subduction of oceanic crust under the plateau caused the formation of a range of mountains of Himalayan proportions to the south of South Africa. The Cape Fold Mountains became fully formed during this period to become the northern foothills of this enormous mountain range. The folding that occurred during this period therefore involved not only
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2240-477: The Peninsula Formation sediments, the western portion of the region was covered for a geologically brief period by glaciers. The diamictite sediments that were laid down by these glaciers, or in glacial lakes, are known as the Pakhuis and Cederberg Formations . A small patch of Pakhuis tillite occurs on the top of Table Mountain at Maclear's Beacon , but most of the Pakhuis and Cederberg Formations are found as
2310-765: The Peninsula to the Mainland, has been eroded away. The Malmesbury shale and granite basement on which this anticline mountain rested also formed an anticline; but being composed of much softer rocks, readily eroded into a 50 km wide flat plain, (now covered with dune sands) called the "Cape Flats". The Cape Fold Belt (i.e. the mountain ranges) extends from about Clanwilliam (approximately 200 km north of Cape Town), to about Port Elizabeth (approximately 650 km east of Cape Town). The Cape Supergroup sediments beyond these points are not folded into mountain ranges, but do, in places, form steep cliffs or gorges, where
2380-594: The West Coast), southwards to Cape Town and then eastwards to northern KwaZulu-Natal , a total distance of approximately 1800 km, roughly along the South African coastline. Only the section between Clanwilliam (approximately 200 km north of Cape Town) and Port Elizabeth (approximately 650 km east of Cape Town) is folded into the Cape Fold Mountains. During the laying down of
2450-640: The Worcester-Robertson valley in the middle of the Fold Belt. Although the Dwyka and Ecca sediments adjoining the Cape Fold Mountains were subjected to the same compression forces that gave rise to the Cape Mountains, they do not form the same mountain ranges as do the Cape Fold Mountains. This is because they are composed of much softer rocks than the Peninsula Formation Sandstone, and were thus soon eroded into
2520-418: The bare rocky surfaces of the quartzites above and below. In several locations the quartzites below the glacial horizon have been rucked into a series of folds. This is believed to have been caused by the movement of ice ploughing into the underlying unconsolidated sands. A good example of this can be seen on a ridge of rocks near Maclear 's Beacon on Table Mountain, close to the edge of the plateau overlooking
2590-446: The bottom, through which rivers flow from the inland Great Escarpment to the sea. It is from within these narrow defiles, many of which can be traveled by road, that one is afforded a cross sectional view of the mountains, and can appreciate their intense folding and distortion (see the photographs on the top right above). Their origin is as follows: After the fold mountains had been formed they became buried under sediments derived from
2660-613: The depression that had been the Agulhas Sea, and rucking the Cape Supergroup sediments into folds running roughly parallel to what would ultimately become the south-western and southern coastlines of South Africa. This mountain building continued into the next phase of the Karoo sedimentation, which began about 260 million years ago, after the ice sheets had melted, leaving a large lake (the Karoo Sea) extending over much of South Africa. The resulting marine or lacustrine deposits form
2730-586: The early Devonian Period) there was further subsidence of the rift valley floor. This brought about the deposition of deeper-water, fine grained sediments of the Bokkeveld Group . This is in marked contrast to the predominantly sandy sediments of the Table Mountain Group. The Bokkeveld Group consists predominantly mudstones. After the Cape Supergroup had been folded into the Cape Fold Mountains, these soft mudstones readily washed away from
2800-503: The east. These formations contain no fossils. Today the Klipheuwel Group is exposed in several small patches near Lamberts Bay, Piketberg, and to the south-west of Paarl Rock . The Natal Group, which is similar to the Table Mountain Group (see below), is found in several elongated patches near the coast of the northern Eastern Cape and KwaZulu-Natal . It forms the impressive cliffs of Oribi Gorge , and can also be seen in
2870-501: The east. Sir Lowry's Pass is the only crossing, in the form of the N2 motorway. The Steenbras Dam , one of Cape Town 's main supply dams, is located in the Elgin valley south of the town of Grabouw due to the abundant rainfall normally experienced in the uplands of the catchment area. The Gantouw (Eland Pass) ceased to be used by wagons on 6 July 1830, when the new Sir Lowry's Pass road
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2940-518: The ebb and flow of tidal currents, as well as polygonal sand-filled mud cracks that indicate occasional exposure to desiccation. This layer, known as the Graafwater Formation , reaches a maximum thickness of 400 m, but on the Cape Peninsula it is only 60–70 m thick. No fossils have been found in the Graafwater rocks, but shallow-water animal tracks have been found. A particularly good example of these tracks can be viewed in
3010-428: The eroding African landscape to form the parallel ranges of mountains that run for 800 km along the southern and south-western Cape coastline today. In fact, they form the coastline, either sloping steeply directly into the sea, or are separated from it by a relatively narrow coastal plain. The Falkland Mountain range had probably eroded into relative insignificance by the mid-Jurassic Period, and started drifting to
3080-417: The flat plains of the "Lower Karoo" , except where they were protected by hard, erosion resistant dolerite or turbidite caps, to form isolated mountains that stand out from the plain. The mountains are not particularly ancient, despite their old-looking appearance. They are considered middle-aged in geologic terms. They were created when the Falkland Plateau collided with Southern Africa, when Pangaea ,
3150-612: The foyer of Geology Department of the University of Stellenbosch, where a slab of Graafwater rock from the Cederberg mountains has been built into the wall. The cutting for Chapman's Peak Drive, on the Cape Peninsula, is carved into the Graafwater Formation which overlays the Cape Granite basement rock below the road. The Graafwater Formation can also be clearly seen in the cutting on the second hairpin bend as
3220-440: The granite weathers is clearly displayed. With further subsidence of the rift valley floor, and possibly breaking through to the ocean, the sediments abruptly become more sandy, indicative of a sudden increase in the depth of the Agulhas Sea (see photograph on the right). A deposit, known as the Peninsula Formation (also often referred to as Table Mountain Sandstone ), consisting of thickly layered quartzitic sandstone , with
3290-433: The massive Himalaya-sized Falkland Mountains to the south of the Cape Fold Belt. Sediments eroded from these mountains provided the bulk of the 6 km thick Beaufort sediments in the Karoo Basin, but they also covered the Cape Fold Belt, thereby protecting them from erosion. At the end of the Karoo Period about 180 million years ago, the subcontinent was covered by a thick layer of Drakensberg lavas , an event that
3360-473: The mountain tops, and only remain in the valleys. Here they form the fertile soils on which the vineyards and fruit orchards of the Western Cape flourish with the help of irrigation from the rivers that have their sources in the surrounding mountains. The Bokkeveld Group does not extend on to the Cape Peninsula or its isthmus (the Cape Flats). Here the Stellenbosch , Franschhoek , Paarl , Durbanville , Tulbagh and Constantia vineyards have been planted on
3430-422: The mountains comprise two distinct ranges, the US-ACAN restricted the application of Sentinel Range to the high northern one and gave the name Heritage Range to the southern one; the Committee recommended the name of the discoverer for this entire group of mountains. Geologically, the Ellsworth Mountains occupy a discrete block of continental crust known as the Ellsworth-Whitmore Mountain terrane. This terrane
3500-401: The new Sir Lowry's Pass, and are a national monument. This route still serves as the primary route out of the Cape Town area for travellers heading east along the coast of South Africa. The climate is typically Mediterranean ; however, it is generally much cooler and more verdant than other areas in the Western Cape , with annual precipitation exceeding 1500 mm (as high as 3300 mm on
3570-444: The north and east, so that the oldest rocks are exposed in the south and west, while the youngest members of the Supergroup are exposed in the north, where the entire Cape Supergroup dives beneath the Karoo rocks . Drilling in the Karoo has established that Cape Supergroup rocks are found below the surface up to approximately 150 km north of their northernmost exposure on the surface. The Cape Supergroup extends eastwards beyond
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#17327800993613640-489: The north-eastern Eastern Cape and KwaZulu-Natal , where the Cape Supergroup is represent only by the Natal Group and a trace of the Peninsula Formation (without the intervening Graafwater Formation). The Witteberg sediments were laid down in what remained of the Agulhas Sea – a shallow, much reduced expanse of water compared to its size during the Bokkeveld period. Immediately following the Witteberg period (about 330 million years ago) much of Gondwana (particularly what
3710-412: The protective layer over the Cape Fold Belt eroded away, exposing their mountain tops. The rivers breached these ridges, after possibly being dammed back for a short period, creating a narrow passage through the low rocky barrier. Continued erosion exposed more and more of these quartzitic mountain ranges, but the rivers, now confined to narrow, fast flowing gorges, continued breaking through each barrier as
3780-458: The reserve varies from 500m to 1590m. Weather conditions can be unpredictable, and bad weather can make conditions dangerous. The entrance to the reserve is at Nuweberg, in Viljoen's Pass (R321) between Villiersdorp and Grabouw. An additional 7000 hectares of state and privale land adjacent to the reserve is co-managed by the Theewaterskloof Conservancy , which includes CapeNature and private landowners. Cape Fold Belt The Cape Fold Belt
3850-446: The shales ( Bokkeveld Group ) persisting in the valley floors while the erosion resistant sandstones (of the Peninsula Formation) form the parallel ranges, the Cape Fold Mountains, which reach a maximum height of 2325 m at Seweweekspoortpiek ('Seven Weeks Defile Peak' in Afrikaans). The Cape Fold Mountains form a series of parallel ranges that run along the south-western and southern coastlines of South Africa for 850 km from
3920-422: The south-west soon after Gondwana began to break up 150 million years ago, leaving the Cape Fold Belt to edge the southern portion of the newly formed African continent. Even though the mountains are very old by Andean and Alpine standards, they remain steep and rugged due to their quartzitic sandstone geology (see below) making them very resistant to weathering . The famous Table Mountain forms part of
3990-464: The southern Karoo . These rocks were laid down 370 – 330 million years ago in the silted up, and therefore shallow marine conditions of what remained of the Agulhas Sea. The group contains fewer fossils than the Bokkeveld Group, but the assemblage that is preserved includes primitive fish, an extinct species of shark, brachiopods, bivalves , and a meter long sea scorpion . There are also plant fossils and numerous animal tracks. The Witteberg Group
4060-405: The southern coastline of Africa. The Cape Fold Mountains possibly survived erosional obliteration, firstly because of the extremely hard rocks (the Peninsula Formation Sandstone) that form the backbone of the mountain chains, but also possibly because they had become buried under the Karoo deposits which originated in the Falkland Mountains. Thus traces of Karoo deposits can, for instance, be found in
4130-400: The subcontinent, about 180 million years ago, and again 20 million years ago, started an episode of continuous erosion that was to remove many kilometers of surface deposits from Southern Africa. Although the tops of the original Cape Fold Mountains were eroded away, they eroded much slower than the considerably softer Karoo deposits to the north. Thus the Cape Fold Belt "erupted" from
4200-407: The supercontinent formed during the Cambrian - Ordovician periods (from 510 to about 330–350 million years ago),. Their stature, with heights varying from 1000m to 2300m, is mostly due to the weather-resistant rocks of quartzitic sandstone of the Peninsula Group (see above). They occur in long parallel ranges each not much more than 10 km wide, separated by equally long valleys with
4270-479: The surrounding landscape eroded to lower and lower levels, particularly during the past 20 million years. These 150‑million-year-old rivers therefore cut the defile, starting by flowing over, and then through the gradually erupting Cape Fold Mountains, to form the spectacular "poorte" and "klowe" (plural of "poort" and "kloof", the Afrikaans for defile or chasm) that characterize these mountains today. The best known defiles are: Meiringspoort , Seweweekspoort ,
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#17327800993614340-451: The surrounding sediments have been eroded away (see, for instance, Oribi Gorge in KwaZulu-Natal ). The mountains, although only of moderate height, are majestic and dramatic. This is due in part to numerous geological factors; The ranges usually have few to no foothills and rise directly from valley floors. The bases of the mountains are usually at or near sea level. The mountains of the Cape Fold Belt are composed of rocks belonging to
4410-441: The time. The Upper Peninsula Formation, above the Pakhuis and Cederberg Formations, consists of much softer sandstone than the Lower Peninsula Formation, and is often referred to as the Nardouw Formation . In the Cederberg this formation has been eroded by the wind into a wide variety of "sculptures", caves, and other fascinating structures for which these mountains have become well-known. About 400 million years ago (in
4480-400: The weathered Cape Granite and Malmesbury shale soils, which form the basement rocks on which the Cape Supergroup rocks in this region rest. The Bokkeveld Group extends eastwards to Port Alfred (near Grahamstown ), approximately 120 km beyond the eastern extent of the Cape Fold Belt. The bulk of the fossils found in the Cape Supergroup occur in the Bokkeveld mudstones. They include
4550-579: The west to East London in the east, plus the KwaZulu-Natal coastline, became flooded, leading to a seaway across the southern and eastern parts of the country, called the Agulhas Sea. The sea floor consisted of the Klipheuwel Group in the west, the Natal Group in the east, and eroded pre-Cambrian rocks in between. The first sediments into the initially still shallow, possibly inland, sea were alternating layers of maroon-colored mudstones and buff-colored sandstones, each mostly between 10 and 30 cm thick. The mudstone units commonly display ripple marks from
4620-446: The yellow block labeled C on the Earth's geological timeline diagram on the right.) An 8-km-thick layer of sediment, known as the Cape Supergroup (see below), accumulated on the floor of this rift valley. Closure of the rift valley, starting 330 million years ago, resulted from the development of a subduction zone along the southern margin of Gondwana , and the consequent drift of the Falkland Plateau back towards Africa, during
4690-403: Was accompanied by upliftment or bulging of Southern Africa, ushering in an almost uninterrupted period, continuing to the present, of erosion removing many kilometers of surface rocks from the entire subcontinent. Rivers running off this bulging interior into the seas that were forming around South Africa as Gondwana was breaking up 150 million years ago, eventually encountered rocky ridges as
4760-401: Was opened. Wagons of the Great Trek beginning 1835, did not actually use the old pass, instead they used the new road. When previous migrants decided to leave the Cape Town area, or Cape Colony as it was then known, this was the first mountain range they crossed. Cuts and wheel markings from their ox wagons can still be seen in rock formations of the old Gantouw pass which lies slightly north of
4830-417: Was part of the early Paleozoic amalgamation of Gondwana and consists of a 13,000 meters (43,000 ft) thick section of folded Cambrian – Permian strata , which accumulated on Grenville -age continental crust. It was likely once part of the Cape Fold Belt that was detached from southern Africa during the breakup of Gondwana and later incorporated into Antarctica. The stratigraphy consists of
4900-433: Was to become Africa and Antarctica, but also parts of South America and India) became covered in a kilometers thick layer of ice as the super-continent drifted over the South Pole. The diamictite deposits left by these glaciers form the first layer of the Karoo Supergroup , called the Dwyka Group . During the glaciation period the Falkland Plateau started to move northwards into what was to become southern Africa, closing
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