The region under study goes from longitudes 9˚00'E to 10˚00'E and latitudes 3˚03'N to 4˚06'N (Figure 1). It constitutes the Douala sedimentary sub-basin
Figure 1. Location map of Cameroon (West Africa) and outlines of the Douala and Kribi/Campo sedimentary sub-basins. (Modified from SNH (1999) in:  ).
which together with the Kribi-Campo sub-basin makes up the Douala/Kribi- Campo sedimentary basin, one of the major basins of the Cameroon Atlantic basin. The Douala/Kribi-Campo basin is also part of the broader Aptian salt basin of Equatorial West Africa  . To the North of the Douala sub-basin is the Cameroon Volcanic Line (CVL)    while the Kribi-Campo sub-basin is located to the south. The Douala/Kribi-Campo basin has been shown to have the shape of a half-graben  . Some other studies have identified a zone with isogals oriented NNW-SSE to N-S, zones of positive anomalies reaching maximums of 30 mgal which are ring-like and present E-W gradient of approximately 2.2 mgal/km   ; which could be as a result of an uplift of dense material that forms a dome with small material  . In another study along Bouguer gravity profiles  , two major structures were located: one being a half-dome of mantle material and the other a pillar of high density rocks. The work of Ndikum et al.  along a NW-SE profile brought to light an anomalous body below this basin which was shown to be probably an intrusive igneous block with density 2.77 g/cm3.
In this study, 2.5D gravity modelling will be carried out along a WWS-EEN oriented profile with the aim of obtaining more information on the existing structures found in the sub-surface region of the Douala sub-basin.
2. Geological & Tectonic Settings
The Douala sub-basin lies between latitudes 3˚03'N and 4˚06'N and longitudes 9˚00'E and 10˚00'E, covering a total surface area of 12,805 km2 (Figure 1). It has a crescent shape which starts from the south-eastern border of Mount Cameroon with the onshore part of about 70 km wide (in the N20E direction) and extends throughout the Atlantic coast showing a gradual decrease in width of the onshore part towards the South up to Londji (located to the North of Kribi). The eastern limit of the sub-basin is the late Proterozoic Pan-African belt. The gradual North-South opening of the South Atlantic is linked to the formation of the Douala sub-basin, which resulted in the diachronism of deposits from South to North and a temporal and spatial variation of sedimentary environments along the West African coast  . According to Reyre  , Hoffman  & Njike  , an explanation to the half-graben form of the Douala sub-basin is in its creation which could have been controlled by an E-W distension that could have provoked the complete rupture between the African & South American continents giving rise to the opening of the South Atlantic.
The basic stratigraphy of the Douala sub-basin is interpreted to comprise of pre-rift, rift, transition and drift megasequences related to the tectonic evolution over African cratonic basement and associated Atlantic margin. On the other hand, the regional stratigraphy and tectonics can be summarized in four main phases of evolution related to pre, syn and post-rift separation of Africa from South America  . Its lithostratigraphy consists of seven major Formations related to its geodynamic and sedimentary evolution    which include: 1) the Mundeck Formation (Aptian-Cenomanian) which represents the syn-rift period; 2) the Logbadjeck Formation (Cenomanian-Campanian), discordant onto the Mundeck Formation; 3) the Logbaba Formation (Maastrichtian); 4) the N’kapa Formation (Paleocene-Eocene); 5) the Souellaba Formation (Oligocene) lying unconformably on N’kapa deposits; 6) the Matanda Formation (Miocene); and 7) the Wouri Formation (Plio-Pleistocene); all these last six formations make up the postrift sequence  .
The Douala sub-basin contains a more continuous stratigraphic section, and is larger than the Rio del Rey basin. Shallow marine limestones, sandstones and shales overlay late Cretaceous, Palaeogene and Neogene ages Continental basal Cretaceous sands. At the western margin of the basin these formations are overlain by basaltic lavas from the Cameroon volcanic centre. When traced offshore, the sedimentary formations thicken markedly, with evidence for over 7 km of subsidence since the middle of the Cretaceous Period. There are more sands and fewer shales than in the Rio del Rey basin, and growth in faulting and diapirism due to overpressured shales are largely absent  .
From its tectonic platform, the Douala sub-basin was given rise to by the Cretaceous break-up of Gondwana and the separation of Africa from South America. Though the initial rifting phase may have started during very Early Cretaceous time (Berriasian-Hauterivian), the principal rifting episode in these areas occurred from late Barremian-Aptian time. It is believed that the initial formation of oceanic crust began during the late Aptian-late Albian interval, as the continents separated. During the passive “drift” phase of the continental margin evolution, several additional tectonic events occurred at 84 Ma (Santonian), 65 Ma (Cretaceous/Tertiary boundary) and 37 Ma (late Eocene). The final uplift event relates to the growth of the Cameroon Volcanic Line (CVL) and effectively lasts from 37 Ma through to present day on the northwest margin of the basin  .
3. Data Processing & Interpretation
3.1. Residual Field
Gravity data constituted of 116 data points with positions located between latitudes 3˚03'N and 4˚06'N and longitudes 9˚00'E and 10˚00'E were used for this study. Upon interpolation on a 100 by 100 square grid with spacings of 0.0285 in longitude axis and 0.0250 in latitude axis, a Bouguer anomaly map having contour interval of 12 mGal was generated (Figure 2). Very high positive anomaly values attaining a peak of 104.1 mGal was observed toward the NW section of the study area.
The residual field produced from more localised sources with short wavelengths, which usually are found at shallow depths was obtained by separation of the regional & residual fields in the Bouguer data by employing the Upward continuation method & Analytical method by least squares.
The upward continuation method is similar to low-pass filtering for it is used to remove high frequency contents from data. Upward continuation was carried out by using the program Fourpot, version 1.3 by Markku Pirttijärvi  . In order to carry out upward continuation on gravity data, the maximum height, h0,
Figure 2. Bouguer anomaly map with study area indicated by black rectangle.
to be used has to be determined. This height is known as the optimum upward continuation height. This optimum height was obtained using the empirical method  to be equal to 30 km.
The analytical method by least squares practically likens a regional field of order n to a polynomial of degree n. Regional fields of different orders are therefore generated and the one that best fits the data is retained. In this study, correlation between regional fields that were generated for polynomial orders from n = 1 to n = 10 and the regional field obtained at the optimum continued height of 30 km was carried out in order to determine the highest correlation factor. The maximum correlation factor of 0.99 was obtained for a polynomial order of n = 4.
The residual field thus obtained under these conditions was interpolated using the Kriging method to yield a 100 × 100 square grid with longitude and latitude spacings of 0.0285 and 0.0250 plotted with a contour interval of 5 mGal  . These residual fields are characterised by many ring-like positive gravity anomaly contour lines in the study region.
Gradients were analysed for this residual field using the Multi-Scale Horizontal Derivative of the Vertical Derivative (MSHDVD) method  which did not contain any emphasis of quasi-linear contacts or quasi-circular contacts thus excluding the existence of fault lines across this region.
When spectral analysis for source-depth estimation was carried out using the program Fourpot version 1.3, the result obtained on the residual field at the upward continuation height of 30 km suggest that the depth of the potential field source is about 4.8 km.
3.2. Ideal Body Solution
The ideal body theory which characterizes the extremal solution with the smallest possible maximum density was originally developed by Parker   . This theory is of much assistance in the fundamental problem of non-unique- ness encountered in the interpretation of gravity anomaly data. This is even the case when the solution set is bounded by physical or geologic constraints.
The ideal body theory is based on the basic philosophy that when a data set admits an infinite solution set, as is the case with potential fields, like the gravity field, properties common to all solutions are sought and as such definite information about the unknown true solution is derived.
In the specific case of gravity data, the maximum absolute value of the density contrast of the source constituting bounds on the uniform norm was treated by Parker. There exists a unique solution with the smallest possible uniform bound when a data set and a region in which a source is confined are considered. For all possible sources in that region of confinement, this source is attributed the term “ideal body” and its norm is the greatest bound on the maximum absolute value of all sources fitting the data. Consequently, any solution (as well as true one) must somewhere reach or exceed this bound  .
Because the analysis of gravity ideal-body is especially well suited for handling sparse data contaminated with noise, for finding useful, rigorous bounds on the infinite solution set, and for predicting accurately what data need to be collected in order to tighten those bounds, it is an excellent reconnaissance exploration tool  .
The program, IDB2, developed by Huestis and Ander  was used to obtain the ideal body solution in this study. The ideal body solution was obtained along a 50.2 km WWS-EEN profile (QQ') (Figure 3) using the following six (6) sets of distance (in km) and gravity anomaly (in mGal) points: (0.87, 46.10), (7.26, 56.02), (13.65, 66.00), (20.05, 75.05), (27.43, 88.83) & (41.52, 55.82).
The initial run of the program such that the ideal body touches the bottom of the volume indicated that the greatest lower bound on the density contrast of the source is equal to 0.266 g/cm3 (see Figure 4). Using this value, this method suggests through other runs & analysis that the minimum thickness of the ideal body should be 5.1 km while the maximum depth to the top of the ideal body is estimated at 11.5 km. This value & the shape of the ideal body plot (Figure 4) are very useful as they will serve as constraints for modelling.
3.3. 2.5D Modelling
2.5D modelling has been carried out on the residual field using the program
Figure 3. Residual field plot in the study area showing WWS-EEN profile (QQ') and another profile (PP') used in previous studies  .
GRAV2DC  . This program offers the possibility to interactively design a geological model in the form of a polygon whose gravity signature correlates with the observed anomalies. 2.5D modelling was carried out with this program using as constraints the value of the density contrast (0.266 g/cm3) obtained from the ideal body solution; the result of spectral analysis and the result of
Figure 4. Ideal body plot when it is touching both the surface and bottom of the region of confinement. The greatest lower bound on the density contrast of the source is given to be equal to 0.26 g/cm3. (Horizontal axis is distance in km along profile, vertical axis is depth in km with negative sign signifying depth increases downward, the scale takes values in g/cm3).
multi-scale analysis of the maxima of gradients. The model obtained presented two major bodies both having a density contrast of 0.266 g/cm3. The first body, step-like in shape, is located down to a depth of about 4.25 km with lateral extensions of 33 km in perpendicular directions to the profile QQ' and whose base is found at a depth of about 30.25 km. The second body, found to the left of the first body and in form of a pillar, is down to a depth of about 10.77 km with lateral extensions of 30 km in perpendicular directions to the profile QQ' and has a base that appears to go deep beyond the crust-mantle boundary into the mantle (Figure 5).
Some very thin elongated blocks also appear in the model somewhere between the two major blocks: a first one with density contrast 0.266 g/cm3 at a depth of about 3.6 km overlying two blocks of densities 0.059 g/cm3 & 0.114 g/cm3 at depths of 5.63 km & 4.73 km respectively; another of density contrast 0.266 g/cm3 at a depth of 10.77 km, and a last block (to the bottom left of the step-like block) of density 0.0685 g/cm3 at a depth of 27.78 km.
Figure 5. 2.5D model from the WWS-EEN Profile QQ' showing (in the lower section) two major blocks with density contrast = 0.26 g/cm3 and other minor blocks (in the upper section, asterisks represent observed field while smooth line represents calculated field).
The 2.5D model derived from the high gravity values found in the region of study as contained on the bouguer anomaly and the residual anomaly maps (Figure 2 and Figure 3) showed a considerable good match between the observed field and the calculated field (Figure 5).
Of the two major bodies present on this model, the step-like shaped block with density contrast of 0.266 g/cm3 is very probably an intrusive body whose top lies at a depth of about 4.25 km which is approximately equal to the value of 4.8 km suggested by spectral analysis and considerably lesser than the maximum value of 11.5 km suggested by the ideal body solution. The body also has an average thickness of about 26 km (with its base lying at about 30.25 km) which is in agreement with the suggestion by the ideal body solution that the minimum thickness of the body is 5.1 km. This intrusive body with density contrast of 0.266 g/cm3 which in its alignment is not completely vertical, but elongates and varies in steps horizontally will have a density of about 2.77 g/cm3 considering the sedimentary background with average density of 2.5 g/cm3  . This implies that the intrusive body is of igneous origin. This totally agrees with the results of Ndikum et al. 2014  which located an igneous intrusive body with similar characteristics along a NW-SE profile. Along the NW-SE profile, the body was found to have a thickness of about 26.9 km with its base at a depth of about 32.8 and its top at depth of about 5.9 km.
Concerning the body with the shape of a pillar and having a density contrast of 0.266 g/cm3, a similar analysis will suggest a density of about 2.77 g/cm3. This body, along the QQ' profile, had an estimated length of 6 km moving from (9˚45.6'E, 4˚57.2'N) to (9˚48.5'E, 4˚58.6'N) at a depth of about 10.77 km. This is in great agreement with the results of the study of Koumetio et al.  which identified a pillar of upper mantle formation with depth of about 14 km. This pillar according to this result was located approximately between longitudes 9˚46'E to 9˚56'E and had its basement merges with the limit between mantle and crust of the Congo Craton. This surely explains why the pillar shaped body in this work has a base which goes beyond the crust-mantle boundary.
Furthermore, the many ring-like positive gravity anomaly contour lines seen in the study area on the Bouguer anomaly map (Figure 2) do agree with the results of Roussel and Lecorche  and Koumetio et al.  whose similarities suggested a more extensive movement that would have affected the whole of West African coast.
Bouguer anomaly fields have been extracted from a set of 116 gravity data points located between latitudes 3˚03'N and 4˚06'N and longitudes 9˚00'E and 10˚00'E. These Bouguer fields were then processed at an upward continuation height of 30 km to obtain Residual fields which were characterised by high positive values. 2.5 D modelling was carried out on the residual fields along a 50.2 km WWS- EEN profile using as constraints the results from spectral analysis, the multi- scale analysis of the maxima of gradients, and the inverse method of the ideal body solution. This model suggested the existence of two major blocks with density contrast of 0.266 g/cm3 below this area of study. The first block was shown to be probably an intrusive igneous body with a density of about 2.77 g/cm3 and it has an average thickness of about 26 km with its top and base lying at depths of about 4.25 km and 30.25 km respectively. The second block located at a depth of about 10.77 km was seen to be most likely a pillar of igneous material with a density of about 2.77 g/cm3 whose base goes deep down beyond the crust-mantle boundary. The results obtained in this study also support the fact that there are similarities between the Douala sedimentary sub-basin and the coastal sedimentary basin of Mauritania-Senegal and so foster the suggestions of a more extensive movement that would have affected the whole of the West African coast.
 Brownfield, M.E. and Charpentier, R.R. (2006) Geology and Total Petroleum Systems of the West-Central Coastal Province (7203), West Africa. U.S. Geological Survey Bulletin 2207-B.
 Tokam, K.A.P., Tabod, C.T., Nyblade, A.A., Julia, J., Wiens, D.A. and Pasyanos, M. (2010) Structure of the Crust beneath Cameroon, West Africa, from the Join Inversion of Rayleigh Wave Group Velocities and Receiver Functions. Geophysical Journal International, 183, 1061-1076.
 Ndikum, E.N., Tabod, C.T. and Tokam, A.-P.K. (2014) Frequency Time Analysis (FTAN) and Moment Tensor Inversion Solutions from Short Period Surface Waves in Cameroon (Central Africa). Open Journal of Geology, 4, 33-43.
 Ndikum, E.N., Tabod, C.T., Tokam, A.-P.K. and Essimbi, B.Z. (2014) Fault-Plane Solution of the Earthquake of 19 March 2005 in Monatele (Cameroon). Open Journal of Geology, 4, 289-293.
 Njike, P.R.N. (1984) Contribution à l’étude Géologique Stratigraphique et Structurale de la Bordure du Basin Atlantique du Cameroun. Thèse de Doctorat 3e Cycle, Université de Yaoundé I, Faculté des Sciences, Cameroun.
 Koumetio, F., Tabod, C.T. and Manguelle-Dicoum, E. (2009) Evidence for Upper Mantle Intrusion in the West African Coastal Sedimentary Basins from Gravity Data: The Case of the Southern Part of the Douala Basin, Cameroon. Global Journal of Geological Sciences, 7, 181-187.
 Ndikum, E.N., Tabod, C.T., Essimbi, B.Z., Koumetio, F. and Noutchogwe, C.T. (2014) Gravity Model for an Anomalous Body Located in the NW Protion of the Douala Sedimentary Sub-Basin, Cameroon (Central Africa). Open Journal of Geology, 4, 524-541.
 Kenfack, P.L., Ngaha, P.R.N., Ekodeck, G.E. and Ngueutchoua, G. (2012) Mineralogic Characterization and Petroleum Potential of Clays (Shales) of the N’Kapa Formation (Paleocene-Eocene) in the Douala Sedimentary Sub-basin (South-West Cameroon). International Journal of Geosciences, 3, 696-709.
 Kenfack, P.L., Njike, P.R.N., Ekodeck, G.E. and Ngueutchoua, G. (2012) Fossils Dinoflagellates from the Northern Border of the Douala Sedimentary Sub-Basin (South-West Cameroon): Age Assessment and Paleoecological Interpretations. Geosciences, 2, 117-124.
 Nguene, F.R., Tamfu, S., Loule, J.P. and Ngassa, C. (1992) Paleoenvironnements of the Douala and Kribi/Campo Subbasins in Cameroon, West African. Géologie Africaine: Colloque de Géologie Africaine, Libreville, Recueil des Communications, 6-8 May 1991, 129-139.
 Ngon, G.F.N., Etame, J., Ntamak-Nida, M.J., Mbog, M.B., Mpondo, A.M.M., Martine, G., Yongue-Fouateu, R. and Bilong, P. (2012) Geological Study of Sedimentary Clayey Materials of the Bomkoul Area in the Douala Region (Douala Sub-Basin, Cameroon) for the Ceramic Industry. Comptes Rendus Geoscience, 344, 366-376.
 Pirttijarvi, M. (2009) FOURPOT, University of Oulu, Department of Physics, Geophysics.
 Zeng, H., Xu, D. and Tan, H. (2007) A Model Study for Estimating Optimum upward Continuation Height for Gravity Separation with Application to a Bouguer Gravity Anomaly over a Mineral Deposit, Jilin Province, Northeast China. Geophysics, 72, 145-150.
 Koumetio, F., Njomo, D., Tabod, C.T., Noutchogwe T.C. and Manguelle-Dicoum, E. (2012) Structural Interpretation of Gravity Anomalies from the Kribi-Edea Zone, South Cameroon: A Case Study. Journal of Geophysics and Engineering, 9, 664-673.
 Roussel, J. and Lecorce, J.P. (1983) Regional Gravity Trends Associated with the Mauritanides Orogen (West Africa). Reidel Publishing Company, 116, 63-71.