Eze, C. L., Institute of Geosciences and Space Technology, Rivers State University of Science and Technology, P.M.B. 5080, Port Harcourt, Nigeira, email@example.com
Sunday, V.N., Department of Geography/Environmental Management, University of Portharcourt, Nigeria, vn.Sunday@uniport.edu.ng.
Ugwu, S. A., Department of Geology, University of Port Harcourt, Nigeria
Uko, E. D., Department of Physics, Rivers State University of Science and Technology, P.M.B. 5080, Port Harcourt, Nigeria
Ngah, S. A., Institute of Geosciences and Space Technology, Rivers State University of Science and Technology, P.M.B. 5080, Port Harcourt, Nigeira.
A total of 15 Earth tremors have been recorded in Nigeria. Possible mechanisms for these intraplate tremors were examined. A regional stress created by the West African Craton, and Congo Craton with an inferred principal stress acting West northwest-East southeast is seen as one of the possible causes of the intraplate tremors. Inhomogeneities and zones of weakness in the crust created by the various episodes of magmatic intrusions and other tectonic activities also were considered as sources of seismicity in the country. Possible fault systems were inferred based on the spatial distribution of the Earth tremors: Yola-Dambata, Akka-Jushi and Warri-Ijebu Remo systems. The spatial distribution of the tremors defined mostly northwest-southeast lines, contrary to earlier theories that the tremors occurred in the inland extension of the northeast-southwest oceanic faults.
Nigeria is not situated on any known seismic belt, yet between 1933 and 2000 Nigeria experienced 15 Earth tremors, three of which occurred in one year (Table 1). The first recorded Earth tremor in Nigeria occurred in Warri in 1933. This was followed three years later by the tremor that shook Lagos and its environs. In 1961, a tremor was reported around Ohafia area but some authors hold that this was a slope movement rather than an Earth tremor. The most severe of the tremors occurred in 1984 around Ijebu Ode (Ajakaiye, 1989). In 2000, another tremor occurred in the town of Jushi Kwari (Eze, 2007). These tremors show that Nigeria may not be as aseismic as previously thought. Major intraplate earthquakes are rare, and their occurrence is often unpredictable and can result in high consequences in terms of life-safety and economic loss. Consequently, the issue of intraplate seismic hazard is attracting increasing attention. The intensities of these events ranged from III to VI, based on the Modified Mercalli Intensity Scale. Of these events, only the 1984 tremor at Ijebu Ode, the 1990 at Ibadan, and 2000 at Jushi-Kwari were instrumentally recorded. They had body wave magnitudes ranging from 4.3 to 4.5, local magnitudes between 3.7 and 4.2, and surface wave magnitudes of 3.7 to 3.9 (Akpan and Yakubu, 2010). When these events occurred, there were no functional seismological observatories in Nigeria. Today, the country has seismographic network with four operational stations.
About two-thirds of NigeriaÛªs landmass is underlain by the Pre-cambrian basement complex consisting of gneisses, migmatites, schist, and various metamorphic rocks and granites (Figure 1). These are in places intruded and interspersed by the ÛÏOlder granitesÛ which originated in the Pan-Africa Orogeny (Olujide and Udoh, 1989). Basement Complex rocks outcrop in four main areas of the country: North of Rivers Niger and Benue, covering parts of Kaduna, Plateau, Bauchi, Kano and Sokoto States; southern Nigeria, covering the greater parts of Kwara, Oyo, Ogun; and Ondo States; southeast Nigeria, spanning the northern parts of Cross Rivers State and as far north as Yola; and north of Benue River in Gongola State. These crystalline basement rocks have been subjected to deformation of different intensities throughout the geological period. Consequently, North-South (N-S), Northeast-Southwest (NE-SW), Northwest-Southeast (NW-SE), North northeast-South southwest (NNE-SSW), North northwest-South southeast (NNW-SSE) and to a lesser extent, East-West (E-W) fractures have developed (Olujide and Udoh, 1989).
The Basement rocks are overlain by Cretaceous and Tertiary sediments of the seven major sedimentary basins, viz, the Calabar Flank, the Benue Trough, the Chad Basin, lullemmenden (Sokoto) Basin, the Dahomey Basin, and the Niger Delta Basin. Sedimentary successions in these basins are of middle Mesozoic to Recent age (Kogbe, 1989). The Niger valley is possibly a graben and the Benue a sinistral shear zone that may be part of a fracture zone within the Pelsium Megashear system (Sheidegger and Ajakaiye, 1985). The Benue trough has also been considered as a ÛÏfailedÛ rift since it contains no ophiolites (Nwachukwu, 1972).
In some cases, the Cretaceous sediments are cut by some major faults which may have been the result of the reactivation of post Pan-African fractures (Merki, 1970). It has been suggested that the Dahomeyan Basin is bounded by the Romanche Fracture zones to the west and the Chain fracture zone to the East (Wright, 1976; Hastings and Bacon, 1979; Ige et al., 1985). Both fracture zones trend approximately in the NE-SW direction.
Some of the important fault systems in Nigeria are the Ifewara, Zungeru, Anka and Kalangai fault systems. They are interpreted to have resulted from transcurrent movements (Garba, 2003). Adepelumia et al., (2008) conducted an integrated geophysical survey across a prominent zone of weakness clearly observable in Landsat
Multispectral Scanner (MSS) and Side-looking airborne radar (SLAR) images in the Precambrian basement complex of southwestern Nigeria and confirmed the existence of the supposed Ifewara shear zone formed by shearing activities during Late Precambrian times. They also identified a NNE-SSW trending fault system in the area. The 250 km-long, NE-SW trending Ifewara fault zone has been shown to be linked with the Atlantic fracture system (Adepelumia et al., 2008). Burke et al., (1977) and Hubbard (1975) believe that the pronounced age differences on both sides of the fault zone suggest that the zone may indeed be a suture of Kibaran age.
There are also many mid-Atlantic ridge transform fracture zones (St. Paul, Romanche, Charcot and Chain fracture zones) in the Gulf of Guinea which many believe form part of the Pelusium Megashear system that cuts across the continent of Africa from the West Africa Coast to the Nile basin in NE Africa (Neev and Hall, 1982; Ajakaiye et al., 1982). The compressional trough which follows the line has been ascribed to an obligue collision between a NW African plate and a central plate consisting of southern and eastern Africa, the Arabia Peninsula and the Levant (Neev and Hall, 1982).
Probable causes of Nigerian Earth tremors
The possible mechanism for the Nigerian Earth tremors has been attributed to the locations of Earth movements associated with NE-SW trending fracture and zones of weakness extending from the Atlantic Ocean into the country (Ajakaiye et al., 1986, Ajakaiye et al., 1987). Burke (1969) has also suggested possible relationship between the epicenters of some of the West African earthquakes and continent-ward extensions of oceanic fracture zones. Onuoha (1988) attributed the tremors to partial reactivation of fossil plate boundaries. The spatial alignment of the Earth tremors in Nigeria, however, defines a NW-SE trend (Figure 1) and these tremors are cannot be said to be associated with the NE-SW trending extension of the Atlantic Oceanic fractures into the landmass. The tremors have most likely been caused by regional stress and zones of weakness in the crust or transfer of stress from plate boundaries.
Nigerian Basement Complex rocks occur between the West African Craton, and Congo Craton. Murat (1988) inferred a principal stress acting WNW-ESE in the basement rocks. This is in concordance with the geographical location of the cratons as the sources of compression which are also in a WNW- ESE direction with respect to the Nigerian Basement Complex. Broad-scale uniform regional stress like this can generate intraplate earthquakes on low-strength pre-existing faults in the upper crust. This agrees with the regional stress models of Sykes, (1978); Iio and Kobayashi., (2002); Johnston and Kanter, (1990) and Zoback, (1992). The alignment of the tremors approximates to the direction of the principal stress. This is also one of the major fracture zones reported for the basement rocks of Nigeria (Olujide and Udoh, 1989).
Zones of Weakness
Cretaceous volcanics are recognized in sedimentary basins of Nigeria as pyroclastics, microdiorite sills and basalt dykes (Nwachukwu, 1972; Benkhelil, 1986). When a magmatic intrusion is present in stable rock the difference in geophysical properties can cause localized stress concentrations particularly when the intrusion is weaker than the surrounding rock. Initially, the mafic intrusion is more rigid than the surrounding rock. Over time, however, the intrusion can become much weaker than the surrounding rock. Campell (1978) has shown that inhomogeneities in the continental crust by this rock association can cause local stress concentrations. Kano, Bauchi and Yola have been intruded during the Proterozoic to Palaeozoic volcanic activity associated with the Pan-African orogeny. Rock intrusions in parts of the sedimentary basins of Nigeria may have created enough local stress concentration to initiate or predispose the areas to seismicity.
The zone of weakness model proposed by Sykes (1978) proposes that intraplate seismicity occurs where the crust has been weakened by previous tectonic activity. The Abakaliki and Benue Troughs are regarded as examples of failed rift arms following the opening of the South Atlantic. The troughs contain folded and unfolded mainly Cretaceous sediments which were deposited in two late Mesezoic rift troughs which formed the third arm of the Niger Delta Triple Junction (Merki, 1970). Extensional stress, due perhaps to upwelling magma beneath the region, must have deformed the crust and created faults. After the extensional sets ceased, the weakened crust was covered with sediment over millions of years. Over geologic time, these zones were incorporated into mid-plate structure and became subject to tectonic compressive stresses (Short and Stauble, 1967). Under stress, the previously fractured rock will fail before the pristine rock, leading to intraplate tremors. Johnston and Kanter (1990) have similarly found that 49% of all intraplate earthquakes occur near ancient failed rifts or passive margins, even though only one quarter of all stable continental crust is of this type.
Stress Transfer from Plate Boundaries
Stresses built up around plate boundaries could travel toward the centre of the plate triggering intraplate tremors especially in pre-existing faults. The coastal area of Nigeria lies in close proximity to the boundary between the African plate and South American plate. Some of the tremors that occurred in the coastal areas of Nigeria could have been possibly initiated by this process.
Nigeria is one of the stable continental crusts that have experienced some degree of seismicity. The Earth tremors in Nigeria are distributed among the basement complex and sedimentary basins (Figure 1). They are concentrated along the south western and north eastern to north central parts of the country. The tremors lie in the southeast- northwest orientation. Any future occurrences of Earth tremors in the country are likely going to occur along these inferred fault lines. Possible mechanisms for these intraplate tremors have been examined to include regional stresses created by NigeriaÛªs position between two cratons and zone of weakness resulting from magmatic intrusions and other tectonic activities in the sediments.
Adepelumia, A.A. Akoa,, B.D., Ajayia, T.R., Olorunfemia, A.O. Awoyemib, M.O. and Falebitaa, D.E. (2008). Integrated geophysical mapping of the Ifewara transcurrent fault system, Nigeria. Journal of African Earth Sciences 52(4-5), 161-166
Akpan, O. U. and Yakubu, A. Y. (2010). Earthquake Science, 23, p.289-294.
Ajakaiye, D. E. (1989). Earthquakes ÛÒ What are they? In Proceedings of the National Seminar on earthquakes in Nigeria (Ed.) Ajakaiye D. E; Ojo S. B. and Daniyan M. A..5-42
Ajakaiye, D.E Hall D.H., Millar, T.W.,Verheijen, P.J., Awad, M.B., and Ojo, S.B. (1986). Aeromagnetic Anomalies and Tectonic Trends in and around the Benue Trough, Nigeria. Nature, 319, 582-584.
Ajakaiye, D. E., Daniyan, M. A., Ojo, S. B. and Onuoha, K. M. (1987). The July 28, 1984 southwestern Nigeria earthquake and its implications for tectonics and evolution of Nigeria. Journal of Geodynamics, 7, 205-214
Benkhelil, J. (1982). Benue Trough and Benue Chain. Geological Magazine; 119 (2), 155-168
Burke, K. (1969). ÛÏSeismic Areas of the Guinea Coast where Atlantic Fracture Zones Reach AfricaÛ. Nature. 222 (5194), 655-657.
Burke, K., Dewey, J., and Kidd, W. S. F. (1977). World distribution of sutures ÛÒ the sites of former oceans. Tectonophysics, 40, 66-99
Campbell, D. L. (1978). Investigation of the stress-concentration mechanism for intraplate earthquakes, Geophys. Res. Lett., 5,.477ÛÒ479
Eze, C. L. (2007). Tsunami: Facts and Figures for Nigerian Coastal Dwellers and Tourists, Transparent Earth Nigeria Limited, Port Harcourt, 50pp
Garba, I. (2003). Geochemical characteristics of mesothermal gold mineralisation in the Pan-African (600 å± 150 Ma) basement of Nigeria. Applied Earth Science : IMM Transactions section B, 112(.3), 319-325
Hasting, D. A. and Bacon, M. (1979).Geologic structure and evolution of the Keta basin, West Africa. Geological Society of America Bulletin September, 90, 889-891
Hubbard, F. A. (1975). Precambrian crustal development in Western Nigeria: indications from the Iwo region. Bulletin of Geological Society of America. 86, 548-554
Ige, E.A., Ike, E.C and Woakes, M. (1985). Some Geological Aspects of Nigerian Seismicity: Paper presented at the National Seminar on Earthquakes in Nigeria, Ahmadu Bello University, Zaria Nigeria, Abstract Volume,.10.
Johnston, A. C. and Kanter L. R. (1990). Earthquakes in stable continental crust, Scientific American , 262(3), 68ÛÒ75.
Kogbe, C. A. (1989). Paleogeographic history of Nigeria from Albian times. In Geology of Nigeria (Ed.) Kogbe C. A. Rock View Nigeria Limited, Jos. 257-275.
Iio, Y. and Kobayashi, Y. 92002). A physical understanding of large intraplate earthquakes, Earth Planets Space, 54, 1001ÛÒ1004.
Merki, P.J. (1970). ÛÏStructural Geology of the Cenozoic Niger Delta. African GeologyÛ. Procceedings of Ibadan Conference on African Geology; Ibadan, Nigeria.
Murat A.V.C.I. (1988). Airphoto Interpretation As An Aid To Litho – Structural Mapping In Tropical Terrain – The New Federal Capital City Site, Abuja, Nigeria. Mineral Resources Exploration. Bulletin, 108, 65-75.
Neev, D., Hall, J. K., and Saul, J. M. (1982). The Pelusium Megashear System Accross African and Associated Lineament Swarms. Journal of Geophysical Research
Nwachukwu, S.O. (1972). The tectonic evolution of the southern portion of the Benue trough, Nigeria, Geological Magazine, 109, 411-419.
Olujide, P. O. and Udoh A. N. (1989). Preliminary comments on the fracture systems of Nigeria. In Proceedings of the National Seminar on earthquakes in Nigeria (Ed.) Ajakaiye D. E; Ojo S. B. and Daniyan M. A. 97-109
Onuoha, K. M. (1988). Earthquake hazard prevention and mitigation in the West African region. In: Natural and Man-Made Hazards. (ed) M. I. El-Sabh and T. S,. D. Reidel Pub. Co., Dordrecht, 787-797
Scheidegger, A.E. and Ajakaiye, D.E. (1985). Geodynamics of Nigerian shield areas. African Journal of Earth Sciences 3, 461-70
Short, K.C. and Stauble, A.J. (1967). Outline of the Geology of the Niger Delta. American. Association of Petroleum Geologists Bulletin. 51, 761-779.
Sykes, L. R. (1978), Intraplate seismicity, reactivation of preexisting zones of weakness, alkaline magmatism, and other tectonism postdating continental fragmentation, Rev. Geophys., 16, 621ÛÒ688.
Wright, J.B., 1976, Fracture systems in Nigeria and initiation of fracture zones in South Atlantic: Tectonophysics 34, 43-47.
Zoback, M. L (1992). Stress field constraints on intraplate seismicity in eastern North America, Journal of Geophysical Research 97(11), 761-782.