SEDIMENTARY FACIES AND DEPOSITIONAL ENVIRONMENTS OF CENOZOIC SEDIMENTARY FORMATIONS CROPPING OUT AT THE CENTRAL PART OF THE DOUALA BASIN

The Douala Basin is one of three units of the Cameroonian coastal basin in the Gulf of Guinea, formed from the east-west extension between African and South American plates generated during the opening of South Atlantic in the Early Cretaceous. This basin contains sediments from Lower Cretaceous to present. The Cretaceous depositional environments are well understood whereas there is very little information concerning Cenozoic depositional environments. Facies and their stratigraphical distribution analyses were conducted on Cenozoic formations exposed at the E-W central part of the Douala Basin in the Missole II, Piti, Missole I and Dibamba localities, with an objective to provide details on the depositional environments and to reconstruct the depositional model and their evolution over time. Seventeen (17) lithofacies were identified on the basis of lithology, grain size and sedimentary structures. The facies constitute three (3) main facies associations; the gravelly dominated, the sandy dominated and the fine grained dominated. These facies and facies associations were interpreted and five depositional environments successions were recognized; the fluvial-braided and meandered channel, the delta plain, the continental shelf and the marginal-littoral. The facies distribution shows a progradational succession from a fluvial to delta plain at the axial part of the basin and a storm dominated continental shelf to marginal-littoral at the central part of the basin. The facies stacking patterns depict sedimentation mainly controlled by sag subsidence and probably by climate.


INTRODUCTION
The Douala Basin is a part of West African basins formed during the opening of the South Atlantic and located in the Gulf of Guinea (Fig. 1a). This basin records sediment from early Cretaceous to recent. Knowing about the environments of the Douala Basin is crucial to better understand the evolution of the West African margin. Discovery of petroleum from Cretaceous sediments have been focused many studies on this period in the Douala Basin and some studies have been carried out on specific aspect of the basin since the mid-1960s by (Reyre, 1966;Belmonte, 1966;Dumort, 1968;Regnoult, 1986).
These studies concern the structure and the stratigraphy of Douala Basin. Salard (1977;1979;1981) also detailed the Late Cretaceous and Cenozoic palynoflora and biostratigraphy of the basin based on data from Kwa-Kwa well. As part of petroleum research, Nguene et al. (1992;Loule et al., 1997) used data synthesis from eight oil wells to describe the paleoenvironmental evolution of the Douala and Kribi/Campo Basin and Mbesse et al. (2012) established a Palaeocene-Eocene boundary of the Science Publications AJG Douala Basin based on palynostratigraphic analysis performed on four wells core samples.
However, outcrops have rarely been studied with the exception of the Cretaceous and Early Palaeocene characterized by (Njike Ngaha, 1984;2005;Njike Ngaha and Eno Belinga, 1987;Ntamak et al., 2003;Kenfack et al., 2012;Oliver and Petters, 2013). The application of sedimentological analysis has, in the past, been very limited in the Douala Basin, especially on Cenozoic outcrops and studies to date devoted only to very briefly different sedimentological processes during this period. On the other hand, these outcrops are generally scarce, occur as small sections and are sometimes weathered in places. This may explain why geological information from this period in the Douala Basin, especially evolution of its depositional environment, is still very scanty.
The main objective of this study was to provide details on lithofacies evolution, the depositional environments of Douala Basin during the Cenozoic and their depositional model evolution over time by presenting field observation data and interpretation. Our study will consist in the description of facies association and their depositional process and facies succession cropping out in the E-W central part of the Douala Basin. These preliminary studies are important for palaeogeographic understanding of Cenozoic sedimentation in the Douala Basin in its relation to similar formations within the West African margin.

GEOLOGICAL AND TECTONOSEDIMENTARY SETTING
The Douala Basin is a large epicontinental and structural depression found in the Gulf of Guinea (Fig. 1a). It has a roughly triangular shape; its maximum width occurs around the vicinity of the Mount Cameroon volcanic massif, which limits it to the northwest. In the east, it is limited by Precambrian basement and to the west it extends under the Gulf of Guinea Sea. Hedberg (1969;Delteil et al. (1975) estimate that there are links between the tectonic evolution and sedimentary sequences in the basins of the West African coast from Angola to Cameroon. Regarding the Cameroonian coastal basins, Benkhelil et al. (2002) differentiated three major tectonic episodes driving sediment dynamics. This is the syn-rift phase, the drift I and II phases. These conclusions have been later confirmed in the Douala Basin by Manga (2008).
The syn-rift phase (Barremian-Aptian): This phase begins before the effective separation of the two continents, with morphology comparable to that currently observed in the East African rift valleys (Logar, 1983;Rosendahl and Scott, 1989). This phase begins in the Douala basin in the Aptian to Albian by narrow tectonic trough. The majority of the sediments encountered and described by (Reyre, 1966;Dumort, 1968;Njike Ngaha, 1984;Regnoult, 1986) are of continental fluvial or lacustrine origin and consist essentially of polygenic and polymictic conglomerates with some interbedded sandstones and shales (Fig. 2). These deposits are named "basal sandstones" or Mundeck formations by (Nguene et al., 1992;Pauken, 1992;Meyers et al., 1996;Ntamak et al., 2010) and are characterized by syntectonic deformations.
The drift I phase (Aptian-Eocene): It is characterized by several tectono-sedimentary events including the E-W extension and faulted subsidence. This phase corresponds to open ocean accompanied by evaporite deposits (absent in Douala Basin) whose cycle end is marked by marine sediments which testify to the opening of the South Atlantic.
During this phase, the Douala Basin recorded marl, clay and limestone deposits subsequent to the global Cenomanian-Turonian transgression demonstrated by (Reyre, 1966;Dumort, 1968;Regnoult, 1986;Njike Ngaha, 1984;2005). The drift I phase is also marked in the basin by a regressive period, due to falling sea level. This regressive episode created an erosional unconformity surface at the base of the Upper Cretaceous (Fig. 2) which was later succeeded by lacustrine deposits of the Logbadjeck (Cenomanian-Campanian) and Logbaba (Maastrichtian) formations and marine deposits of the N'kapa (Palaeocene-Eocene) formations highlighted by (Nguene et al., 1992;Coward et al., 1999).
The drift II phase (Eocene to Recent): The Douala Basin during Eocene was marked by a regressive tendency with flexure and resumption of erosion on the emerged margin. This intensive erosion on the margin created an unconformity on which were deposited formations consisting of black or brown clay with some small sandy bars, clayey sands interbedded with thin limestone, sand and gravel alternating with plastic clays (Fig. 2). These deposits are named Souellaba (Oligocene) and Matanda (Miocene) formations by Nguene et al. (1992). During the Late Miocene to Recent, there has been a general regression, followed by the establishment of new deltaic units of detrital materials, most of which contain volcanic elements.  Regnoult, 1986;Nguene et al., 1992;Manga, 2008) Science Publications

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These sediments consists of coarse-grained sands interbedded with plastic clays belong to the Wouri formation indicate by Nguene et al. (1992).

BASIC DATA AND METHODS
The studied outcrops are located in the E-W central part of the Douala Basin, along the Yaoundé-Douala No 3 National Highway and the Yaoundé-Douala railway (Fig. 1b). These outcrops were investigated for about 20 km moving towards Douala. Outcrops described have been identified in the localities of Missolé II, Piti, Missolé I and Dibamba (Fig. 1b). About 300 m of sedimentary deposits have been described and analyzed on the basis of lithology, grain size and sedimentary structures. The facies description, their interpretation and their stratigraphic evolution were carried out. The facies codes used were modified according to (Miall, 1978;1985;Mclean and Jerzykiewicz, 1978;Postma, 1990;Walker and Plint, 1992;Allen, 1996;Reading and Collinson, 1996).

FACIES AND FACIES ASSOCIATIONS
In this study, seventeen facies were identified and a summary of each facies description is given in Table 1. These facies were grouped into three major facies associations and will be described and interpreted below. The detailed facies logs are provided in Fig. 4.

Facies Association A: Gravelly-Dominated
This facies association consists of the four lithofacies (Gms, Gmg, Ghi and Gt) as described below.

Description
The Gms facies is a heterolithic conglomerate with a sandstone-clay matrix. The lithic elements of this conglomerate are 4-5 cm in diameter. These elements are rounded to subangular with quartz fragments being dominant. The unconsolidated matrix consists of coarse to medium-grained sandstones which is poorly sorted, mixed with clay and varies from grey to red, depending on the clay content (Fig. 3a). There is no graded bedding or other sedimentary structures and the bed varies from 1-12 m in thickness. The Gmg facies with 5 m thick is constituted by cm-scale rounded to subangular quartz grains (Fig. 3b). It is associated locally to Ghi facies. The matrix consists of medium to coarse-grained sands. It presents graded bedding and its basal surface is erosive. The Ghi facies is coarsegrained sandstones with quartz pebbles 3-4 cm in diameter in a clayey sandstone matrix (Fig. 3c). At the basal boundary of this facies, rounded quartz pebbles are slightly imbricated. This coarse-grained sandstone is poorly sorted and rests on an erosive surface. The bed has thickness of about 4-6 m. The Gt facies is ferruginous coarse-grained sandstone, with rounded quartz pebbles 4-5 cm in diameter ( Fig. 3d and e). These pebbles occur in a sandstone matrix poorly sorted and are associated to Sg facies. In some places, Gt facies shows cross bedding rarely multistorey with pebbles lag at set base. The set has lowangle and oriented generally westward.

Interpretation
The Gms facies records deposition by debris flows, accompanied with sliding by gravity (Nilsen, 1982) on a slope. The predominance of the matrix composed of coarse to medium poorly sorted sands, mixed with clay indicates that the flow remained highly concentrated during transport and that the clasts remained closely packed during deposition (Fisher, 1971). This process was followed by a pseudoplastic grain flow (Nemec and Steel, 1984) that allowed facies Gmg to be put in place by gravity. Ghi facies shows a combination of characteristics that is usually associated with debris-flow deposits (poor sorting, erosive base) as well as features of stream-flow deposits (e.g., clast subrounding and clast imbrications). This facies is attributed to streamflow process resulting from a sediment transport by traction (Nilsen, 1982). This process was generated due to gravity by very high-energy water current on a moderate shelf slope (Nemec and Steel, 1984;Miall, 1996). The process was followed by mass-flow from turbulent currents. The cross-bedded ferruginous coarse-grained sandstones with rounded quartz pebbles (facies Gt), suggests relatively rapid sedimentation from a high-energy flow. The characteristics of these facies are consistent with deposition in fluvial channels from high-velocity flow in the deepest part of the stream (Allen, 1980;Miall, 1996;Collinson, 1996) or gravity flow produced by density-current (Gugliotta et al., 2013). The Gt facies is also interpreted to have been deposited as a channel lag under conditions of lower flow regime, with sediment transport occurring via tractional currents (Ghazi and Mountney, 2009).

Facies Association B: Sandy-Dominated
This facies association is composed of fine to medium and coarse-grained sandstones containing sometimes pebbles. It consist of six lithofacies includes the cross-bedded Sandstone (St), the coarse to mediumgrained sandstone (Sm), the horizontally bedded Sandstone (Sh), fine to medium-grained Sandstone (Sg), medium to coarse-grained cross-stratified sandstone (Ss) and the convoluted Sandstone (Sc).

Description
The Sm facies is a homogeneous coarse to mediumgrained sandstones organized in bars of several meters. The grains are mostly mm-size consisting of angular immature mainly quartz and feldspar grains (Fig. 3f).

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Interpretation
The Sm facies is interpreted as a sand deposit coming directly from a turbulent suspension of hyperconcentred mass flow or a high-density subaqueous turbidity current (Ghibaudo, 1992). The convoluted fine-grained Sandstone (Sc) probably results from sediment liquefaction initiated by excess pure waters pressure suggested by Cojan and Thiry (1992). The Sg facies is interpreted as mass flow deposits from turbulent suspension. Deceleration of these turbulent suspensions would have produced most of the deposits of the Sg facies (Lowe, 1982). The loads casts observed at the basal boundary of this facies probably generated by pressure balance within sediment with interface sand/clay deformations. The moderate to poor sediment sorting, the low-angle of trough cross-stratification favours a fluvial bedform interpretation of St facies (Collinson, 1996;Miall, 1996;Eriksson et al., 1998). This deposit may be the result of migration of 3-D megaripples responding to changes in the speed and direction of currents (Chamley, 1999). This facies may also have been deposited during successive filling phases of channels or during progradation of meandering bars (Cojan and Renard, 2006). The Sh facies is interpreted as plane bed sand of upper flow regime deposited in section of river valley as channel fill developed on top of sand bars (Miall, 1978;Harms et al., 1995). The Ss facies is interpreted as deposit by oscillatory flow in storm dominated shoreface environment (Allen, 1996).

Description
The Fl facies forms clayey siltstone and occurs in the form of an individual bar with a thickness of several meters and associated with horizontally bedded Sandstone facies (Sh), kaolinic claystone (Fm) and shale/mudstone Facies (Fml). It shows parallel laminations and weathered surfaces show traces of rubefaction, whereas fresh surfaces are white or lightpink. A few fragments of lignite were observed, bioturbation and plant root traces are common (Fig. 3l). This facies presented on the top rounded-sharp flute marks (Fig. 3m). The grey argillaceous Facies (Fr) with 2 m thick has massive structure and grey spotted with purple. Traces of bioturbation are frequently observed in this facies ( Fig. 3n and o). It is associated with horizontally bedded Sandstone (Sh). The multicoloured kaolinic clays Facies (Fm) has a thickness of several meters and associated with clayey siltstone (Fl), trough cross bedded Sandstone (St). This facies is massive and shows locally desiccation-cracks (Fig. 3p). Bioturbation, microorganism activity and plant root traces are also common (Fig. 3q). The black clay Facies (Fsf) is massive claystone with fossils content as moulds of bivalves and gastropod shells. There is also the presence of some coal debris. This facies is associated with clayey siltstone Facies (Fl) and fine to medium-grained Sandstone facies (Sg). The individual bed has thickness of about 15 m ( Fig. 3r and s). The Fml facies consists of compacted, fissile black shale (Fig. 3t). These clays may be bioturbated in some areas. Many animal fossils are observed including shell moulds of molluscs (bivalves, gastropods), as well as Nautilus debris. Its thickness is estimated at more than ten meters. Towards the top of the bed, this facies is associated with clayey siltstone Facies (Fl). The massive or laminated black claystone Facies (Fmlc) shares the same features as Fml facies but contains some carbonaceous plant debris (Fig. 3u). It is associated with medium to coarse-grained Sandstone facies (Sm) and limestone Facies (Fc). The individual bed is about 40 m thick and presents at the top, some ferruginous nodules parallel to the stratification. The presence of parallel laminations is also noted at the bottom of the bed. The limestone Facies (Fc) occurs as a lenticular bed with thickness of about 0, 65 m thick. It is associated with Fmlc facies and in addition to numerous fragments of bivalves and gastropods; it also has siliciclastic elements such as subrounded to rounded quartz pebbles which sometimes show a ferruginous coating (Fig. 3v).

Interpretation
The Fl facies is interpreted as deposition from suspension settling and from weak traction currents during flood events commonly observed during overbank sedimentation on the floodplain. Similar facies were interpreted as deposition in shallow water over washing or represent the deposits of waning stage flood deposition, chiefly in overbank areas with the majority of deposition occurring from suspension settling and with only limited bedload transport via weak currents (Walker and Cant, 1984;Reading, 2009;Hjellbakk, 1997;Chamley, 1999). Miall (1978) interpreted the Fr facies as a levee or overbank deposit formed during flood events. The Fm facies is interpreted as representing deposition by suspended fine particles during overflow periods. Similar facies is interpreted as overbank or drape deposits, thus it may represent the most distal floodplain (Miall, 1978;1985).

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The presence of desiccation cracks in this facies is also typical of most of floodplain deposits in a semi-arid and arid climate (Turner, 1980;Bridge, 2006;Cain and Mountney, 2009). The Fsf facies is interpreted as suspension deposit settling from weak currents or shallow lacustrine deposit (Miall, 1996;Nichols, 2013). The dark colour of this facies may suggest a relatively anoxic confined or closed environment, which can favoured the preservation of organic matter. The Fml facies result from suspension settling in a calm environment. Similar facies is interpreted as suspension settling deposit far away from wave action in a marine environment (Reading and Collinson, 1996). The Fmlc facies is interpreted as suspension settling deposit in a calm marine environment with a large portion of marine water (Johnson and Baldwin, 1996). The limestone facies Fc represent accumulation in a carbonate-rich shallow marine environment subjected to sediment input from the neighbouring terrestrial environment (Wakefield and Mountney, 2013).

FACIES SUCCESSIONS
According to (Dalrymple, 2010), vertical facies successions represent genetically related lithofacies that occur in combination and typically represent individual depositional environments. Five types of facies successions are identified from the description and associations of facies of the formations cropping out in the E-W central part of the Douala Basin: Braided river, meandered river, delta plain, continental shelf and marginal-littoral facies succession.

Braided River Facies Succession
This facies succession consists at the bottom of the gravelly dominated facies association, Gms and Gmg facies with a thickness of about 16-18 m. This facies is poorly sorted with outsized clast and without sedimentary structures. This suggests that deposition of this facies was controlled by debris flow process accompanied with sliding by gravity on a slope, mainly associated with a pseudoplastic grain flow (Nilsen, 1982;Nemec and Steel, 1984). The gravelly dominated facies association exhibit vertical and lateral evolution towards the sandy dominated facies Association (Sm, Sg, Sc and Sh) composed of coarse to medium-grained, medium to finegrained sandstones, horizontally sandstone and the argillaceous Facies (Fr) from the fine dominated facies association with thickness of about 30-32 m. This facies succession shows general fining-upward package (Fig. 4a). This suggests progressive decreasing of the flow process while argillaceous facies represent overbank or levee deposits. However it is inferred that convolute bedded sandstones are indication of sediment liquefaction initiated by excess pure water pressure (Cojan and Thiry, 1992).

Meandering River Facies Succession
This facies succession is made up at the bottom of gravelly dominated facies association (Ghi) composed of the pebbly very coarse-grained sandstones with thickness of about 4-6 m. This facies is poorly sorted and pebbles clast are rounded and slightly imbricated. This suggests deposition by stream-flow process or transport by traction due to gravity on a moderate shelf slope (Nemec and Steel, 1984;Miall, 1996). The gravelly dominated facies association show vertical and lateral evolution towards the sandy dominated facies association (Sg and Sh) consists of medium to fine-grained sandstones and Fl and Fm facies from fine dominated facies association. This facies succession has overall thickness of about 30 m and show fining-upward package (Fig. 4b). The sandy dominated facies association is interpreted as meandering river channel deposits while the silts and mud facies represent floodplain deposits (overbank).

Delta Plain Facies Succession
This facies succession indicates at the bottom sandy dominated facies association (Sm) consists of medium to fine-grained sandstones with clay matrix. This facies is interpreted as a sand deposit coming directly from a turbulent suspension of hyperconcentred mass flow or a high-density subaqueous turbidity current (Ghibaudo, 1992). The vertical evolution of this facies succession exhibits coarsening-upward motif (45-50 m thick) composed of fine dominated facies association, Fl and Fsf facies and finally fine to medium Sandstone (Sg) from sandy dominated facies association and cross bedded coarse-Grained sandstone (Gt) from gravelly dominated facies association. The Fl and Fsf facies are interpreted as suspension settling deposits in a calm and confined or closed environment which could be a brackish environment that characterizes a pro-delta (Mutti et al., 2000) or a tidal deposits of a flooding continental margin, observed in estuarine environments (Shanmugam et al., 2000). The Sg facies is interpreted as mass flow deposits from turbulent suspension while the Gt facies suggest relatively rapid sedimentation from a high-energy flow. The characteristics of these facies are consistent with deposition in fluvial channels from high-velocity flow in the deepest part of the stream (Allen, 1980;Miall, 1996;Collinson, 1996) or gravity flow produced by density-current (Gugliotta et al., 2013). This facies succession is interpreted to represent shallow marine to delta plain depositional system based on its coarsening-upward nature (Fig. 4c).

Continental Shelf Facies Succession
This succession is made up of fine grain dominated facies association (Fl, Flm, Flmc and Fc) composed of silt, compacted, fissile black shale, massive or laminated black claystone, limestone and medium to coarse-grained sandstones from sandy dominated facies association. This succession exhibits coarsening-upward motif with thickness of about 100 m. The depositional processes indicate by sandstone facies characterized by the presence of shells fragments of bivalve, cross stratification and bioturbation, provide evidence of storm currents and deposit by oscillatory flow in storm dominated shoreface environment reported for similar facies by Allen (1996); Hamberg and Nilsen (2000). The fine grain dominated facies association is interpreted as suspension settling deposits in a shallow marine depositional environment. However, fluctuation of sea level and thermal subsidence have favoured deposition of thick black clays bed with a level of ferruginous nodules which indicates period of oxidizing of depositional environment. The coarseningupward nature of this facies succession is interpreted to repres-ent storm-dominated continental shelf depositional system (Fig. 4d).

Marginal-Littoral Facies Succession
The succession is composed of sandy dominated facies association (St) consist of medium to coarse-grained cross bedded sandstones and the massive kaolinic clays Facies (Fm) from fine grain dominated facies association. The St facies is interpreted as fluvial bedform deposit outcome of migration of 3-D megaripples responding to changes in the speed and direction of currents (Chamley, 1999). The Fm facies is interpreted as floodplain deposit (overbank). The coarsening-upward packages of this facies succession can be interpreted as a result of sea level fall and resumption of fluvial activities (Fig. 4e). This is marked by an influx of greater clastic sediments resulting from erosion of the edges of the basin.

FACIES SUCCESSION STRATIGRAPHIC EVOLUTION AND DEPOSITIONAL MODEL
The studied outcrops exposed at the E-W central part of the Douala Basin comprise about 300 m thick of sediments consists of conglomerates, pebbly coarse, medium and fine-grained sandstones with siltstones, mudstone, shale and limestone. The five facies successions described herein are closely related and their inter-relationship supports their spatial and temporal evolution from fluvial to delta plain overlain progradationally by continental shelf and then marginallittoral deposits. The depositional model suggest for the formations cropping out at the Missole II, Piti, Missole I and Dibamba localities in the Douala Basin was developed from the lithofacies, lithofacies association studies and facies succession stratigraphic connection (Fig. 5). The model involves major depositional systems of fluvial to delta plain, continental shelf and marginal-littoral. The fluvial systems with braided and meandering channel are inferred to have fed delta plain, continental shelf and marginal-littoral system with sediment. The marine facies assemblage shows a large terrigenous influence.

DISCUSSION
The spatial and temporal evolution of the depositional environment of studied formations is proposed and was probably controlled by tectonics influencing transgressive and regressive movements of marine water as well as the sea levels change. In the Douala Basin as in the other basins of West African margin, the initial extension movement created a series of normal faults in the basement of the basin. The replay of these faults was created frequent subsidence movements in the basin. All of these have been at the base of the changes in the nature of the depositional environment. The facies analysis, facies association interpretation and vertical and lateral facies successions have permitted the generalized evolution of depositional patterns as progradational successions. Continental depositional processes of fluvial, marginal-littoral and delta plain and marine depositional processes of continental shelf were responsible for the deposition of formations of Missole II, Piti, Missole I and Dibamba localities in the central part of the Douala Basin. According to Robertson (1992), the equatorial portion of the South Atlantic continues to experience rapid extension during the Early Palaeocene and sedimentary basins in this surrounding area will undergo rapid subsidence. Cenozoic deposition in the Douala Basin started within this context with gravity driven and mud flow sedimentation in a fluvial environment with braided and meandering channel (Fig. 5a). Towards the basin axis, textural changes occur from very coarse-medium grained to fine-grained sandstone, siltstone and black claystone of the delta plain environment, due to a relative transgression of the sea in the Douala Basin. This marine transgression was demonstrated by Regnoult (1986) and would have attained its maximum in the Ypresian. However, the subsidence phase which has favoured the deposit of marine facies would have broken up during the late Eocene by an uplifting episode reported by (Nguene et al., 1992;Benkhelil et al., 2002;Dickson et al., Science Publications AJG 2003). This uplift has contributed to a regression of the sea followed by erosion of a part of the emerged margin (Fig. 5b). This period of regression was evidenced by the presence of a small coarseningupward motif of the delta plain facies succession. This erosive period coincides with the relative global decline in sea level and has contributed to build a regional unconformity surface called "surface africaine I" reported by Reyre (1966) as well as in the Gabon, Dahomey and Ivory Coast basins and would have significantly contributed to the building of the current continental shelf. At the central part of the basin, fine to medium-grained sandstone, siltstone, shale, massive or laminated black claystone and limestone facies have been reported and formed the stormdominated continental shelf deposits. Deposition of these facies was made probably during the Oligocene to Early Miocene thermal subsidence of the Douala Basin, renewed after uplift and erosion episode of the emerged margin during the Late Eocene indicate by Nguene et al. (1992). In addition this thermal subsidence coincides with the relative sea level rise on the continental shelf completely builds in the Douala Basin (Fig. 5c). This marine transgression was also carried out in the Kwanza and Congo Basins by Logar (1983); Reyre (1984), but has not yet been confirmed in the Gabon basin. During the Middle Miocene, the edification of the Cameroon Volcanic Line reported by (Nguene et al., 1992;Benkhelil et al., 2002) was probably responsible for the uplift of the margin of the basin and the regression of marine waters westward. Marginal-littoral environment was developed within this context and sedimentation was marked by a large influx of clastic sediments resulting from erosion of the edges of the basin (Fig. 5d).
However, despite a few manifestations of faulting subsidence observed at the bottom of the studied series through the presence of conglomerates and some soft sediment deformations, it is noted that any manifestation of the faulted subsidence has been identified in the upper part of the studied series. This allows agreeing upon the hypothesis of thermal subsidence which characterizes the Douala Basin during the Cenozoic suggested by Nguene et al. (1992) and seems to be accepted in almost all basins in the West African margin by Logar (1983;Reyre, 1984).

CONCLUSION
Facies analysis of the Cenozoic formations cropping out at the E-W central part of the Douala Basin allows identification of depositional environments and made possible suggestion on the evolution of the depositional model for the successions. The five facies successions exhibit vertical and lateral facies evolution from braided and meandered channel of fluvial environment at the base to delta plain environment along the basin axis and the continental shelf to marginal-littoral environment at the central part of the basin. Debris flow processes dominated deposition of gravelly dominated facies associations, the poor sorting and subangularity of most of the coarse detritic clasts indicate source from nearby area. The proposed depositional model has evolved over time. This evolution was probably controlled by sag subsidence influencing transgressive and regressive movements of marine waters as well as the changes in sea level, climatic changes or combination of both in the Douala basin. This condition is similar to that for the most part of the other basins of West African margin.