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The Sokoto Basin (Nigerian Sector of the Iullemmeden Basin)

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The Sokoto Basin (Nigerian Sector of the Iullemmeden Basin) Chapter 6 The Sokoto Basin (Nigerian Sector of the Iullemmeden Basin) The Iullemmeden Basin in north-western Nigeria is known locally as the “Sokoto Basin”. It consists predominantly of a gently undulating plain with an average ele- vation varying from 250 to 400 m above sea-level. This plain is occasionally inter- rupted by low mesas. A low escarpment, known as the “Dange Scarp” is the most prominent feature in the basin and it is closely related to the geology. The sediments of the Iullemmeden Basin were accumulated during four main phases of deposition. Overlying the Pre-Cambrian Basement unconformably, the Illo and Gundumi Formations, made up of grits and clays, constitute the Pre- Maastrichtian “Continental Intercalaire” of West Africa. They are overlain uncon- formably by the Maastrichtian Rima Group, consisting of mudstones and friable sandstones (Taloka and Wurno Formations), separated by the fossiliferous, shelly Dukamaje Formation. The Dange and Gamba Formations (mainly shales) separated by the calcareous Kalambaina Formation constitute the Paleocene Sokoto Group. The overlying continental Gwandu Formation forms the Post-Paleocene Continental Terminal. These sediments dip gently and thicken gradually towards the northwest, with a maximum thickness of over 1,200 m near the frontier with Niger Repub- lic. The geological map of the Sokoto Basin of northwestern Nigeria is shown on Fig. 6.1 while Fig. 6.2 summarizes the geological sequence in the basin. Pre-Maastrichtian Deposits (The Continental Intercalaire) In the Sokoto Basin, the pre-Maastrichtian sediments are of fluviatile and lacustrine origin. They belong to the Illo and Gundumi Formations which extend northwards into Niger Republic. These deposits belong to the upper part of the “Continental Intercalaire” which comprises a group of poorly fossiliferous sediments covering a very extensive area, bounded on the west by the crystalline basement rocks of Niger Republic, and on the east by the Quaternary sands of the Chad Basin. The Gundumi Formation lies unconformably on the basement and consists of basal conglomer- ates, and gravels with sand and variegated clays increasing upwards; the maximum thickness is about 350 m. The Illo Formation includes interbedded clays and grits, with an intermediate pisolitic and nodular clay member, and attains over 240 m N.G. Obaje, Geology and Mineral Resources of Nigeria, Lecture Notes 77 in Earth Sciences 120, DOI 10.1007/978-3-540-92685-6 7, C Springer-Verlag Berlin Heidelberg 2009 78 6 The Sokoto Basin (Nigerian Sector of the Iullemmeden Basin) Fig. 6.1 Geological sketch map of the southeastern sector of the lullemmeden Basin (Sokoto Basin) (After Kogbe, 1981b) in thickness. The continental period represented by the Gundumi and Illo Forma- tions was terminated by a Maastrichtian marine transgression. The sea penetrated the interior of the continent both from the north (the Tethys), and from the south (Gulf of Guinea), through the mid-Niger Basin. The type section and type locality of the Gundumi Formation are at Dutsin Dambo. The contact of the Gundumi Formation with the basement is conglomeratic. At Kona Rolga, on the Sokoto-Gusau road, a good exposure of the basal conglomer- ates occurs at about 11 km north of Talata Mafara where the basement outcrops. These conglomerates outcrop for hundreds of square kilometres, with large, well- rounded pebbles in a massive clayey feldspathic and ferruginous matrix. The pebble conglomerates occur also abundantly around Tureta. The Illo Formation is a lateral equivalent of the Gundumi Formation. Like the Gundumi sediments, the Illo Formation overlies the basement unconformably. The deposits are continental, fluviatile to fluvio-lacustrine in origin. They dip gently north-westwards with a NE–SW direction of strike. The Illo Formation consists Pre-Maastrichtian Deposits (The Continental Intercalaire) 79 Eocene Gwandu Formation Continental Continental Termaire p Gamba Formation u Marine o r G Kalambaina Formation o Marine t Paleocene o k o Dange Formation Marine S Continental p Wurno Formation u o r Dukamaje Formation G Marine a m Maastrichtian i R Taloka Formation Continental Continental Continental Pre- Gundumi – Illo Formation Intercalaire Maastrichtian Fig. 6.2 Stratigraphic successions in the Nigerian sector of the lullummeden Basin (Sokoto Basin) predominantly of cross-bedded grits with a major intercalation of pisolitic and nodu- lar clay. Laterites and lateritic ironstones form a resistant capping on top of the grits and thin layers of multicoloured ferruginous deposits occur randomly within the grits. The type section of the Illo Formation is on the hill east of Gore village about 3.5 km north of Giro. Correlation has been made with the Bima Sandstone of north-eastern Nigeria, based on structures and contacts with the basement. An outstanding characteristic in the Bima Sandstone is current bedding, which is also a widespread feature in the Illo and Gundumi Formations. In addition, wherever their lower contact could be observed, the Bima Sandstone rests directly on the basement (Murat, 1972). The same observation is true for the Gundumi and Illo Formations which are underlain by basal conglomerates that become hardened towards the contact with the base- ment. It has also been suggested that the Bima Sandstone was deposited by fluviatile currents flowing from the north-west, repeatedly interrupted by minor disturbances, a fact confirmed by the direction of cross-beds in the area. The “Continental Intercalaire” is important in Africa. It is remarkable for the unity of facies, flora and fauna, implying that there was a uniform climate over large parts of the continent, and a continuous transition from the Jurassic to Creta- ceous. The Karoo Series of South Africa can be correlated with the upper beds of the lower portion of the “Continental Intercalaire” (Furon, 1960). The “Continental Intercalaire” corresponds to the upper part of the Nubian Sandstone, which, in the Arabo-Nubian shield, begins at the base of the Palaeozoic. The Iullemmeden Basin, as well as many other parts of North and South Africa, experienced extensive peri- ods of continental sedimentation with the accumulation of fluvio-lacustrine nature 80 6 The Sokoto Basin (Nigerian Sector of the Iullemmeden Basin) in pre-Cenomanian times. The northern limits of the continental deposition coin- cides with the Algeria- Moroccan Sahara and extends eastward into Egypt and the Sudan. The southern limits extend as far as South Africa. Maastrichtian Deposits (The Rima Group) The second phase in the depositional history of the sediments of the Sokoto Basin began during the Maastrichtian, when the Rima Group was deposited uncon- formably on pre-Maastrichtian continental beds. The type sections of the three Maastrichtian formations are at Taloka, Dukamaje and Wurno. The unconformity is well exposed at Wurno. The lower sandstones and mudstones of the Rima Group belong to the Taloka Formation; with a maximum thickness of about 100 m. Excel- lent exposures of the upper portion of the formation can be observed at Goronyo, Taloka and Shinaka. The basal beds are exposed further to the east near Takarau and Gidan Mata. The formation consists essentially of white, fine-grained, friable sand- stones and siltstones, with thin intercalated mudstones and carbonaceous mudstones or shales. In the Gilbedi district, on the northern side of the Rima valley, the Taloka Formation occupies the base of a high scarp feature which is the northern termi- nal of the “Dange Scarp”, a prominent topographic feature which runs southwards towards Dange. The upper levels of the escarpment are occupied by younger for- mations. The hills near Goronyo on the southern side of the Rima valley are lower. The greater part of the hill is made up of sediments of the Taloka Formation, with the overlying Dukamaje Formation poorly developed. The Wurno Formation is only represented at the summit where it is preserved by laterite. The Taloka Formation The type locality of the Taloka Formation is at Taloka village, about 2 km east of Goronyo. The type section is on a hill that forms part of a continuous exposed ridge between Shinaka, through Taloka to Goronyo. These beds disintegrate rapidly on exposure, and the base of the ridge is covered by a layer of overburden. Four major lithofacies can be recognized. (i) The lowest siltstone layer is reddish-purple to brown in colour. The siltstone is clayey and poorly consolidated. The total thickness is about 6 m. (ii) Whitish-grey, light-brown siltstone with thin beds of carbonaceous shale; semi- consolidated with intercalations of grey siltstone with black lignitic siltstone. The total thickness is about 5 m. (iii) Well-bedded light b rown, friable siltstone with alternate bands of yellowish brown clay-stone and carbonaceous shale with a total thickness of about 18 m. (iv) White poorly-consolidated siltstone, alternating with brown layers attaining a maximum thickness of 13 m. The topmost beds are in contact with the Maastrichtian Deposits (The Rima Group) 81 “Callianassa-burrowed” horizon of the overlying Dukamaje Formation. The siltstones are generally finely bedded often varicoloured as a result of chemi- cal alteration. The thin-beds or “laminae” are typical of tidal flat environments and each lamina represents an individual tidal cycle. Small load casts and bio- turbation structures are abundant. These are indicative of low energy marine environments (e.g. bays), lenticular bedding (“Flaser bedding”) and wavy bed- ding are also common. These point to a tidal-flat environment. The Dukamaje Formation The Dukamaje Formation consists predominantly of shales with some limestones and mudstones. The type section of the formation is exposed on the hill south-west of the village of Dukamaje. The base of the section is well exposed and the sharp contact with the underlying Taloka Formation can be observed in several sections on the foot of the hill south-west of the village The formation varies from about 12 m at the type area to less than 0.5 m, 50 km further south.
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