The Cameroonian continental shelf, located in the central part of the Gulf of Guinea, extends between latitudes 2˚20'N and 4˚30'N and longitudes 8˚20'E and 9˚55'E.

From the north-south coastline, the 200-metre isobath is quickly reached, with a slope that reaches almost 20% above 100 metres depth.

The tectonics of the basin, characterized by horsts and grabens, are associated with the N60 faults resulting from the opening of the South Atlantic from the Albian. Four major lithostratigraphic ensembles are identifiable, including formations dating from the Albian to the Cenomanian, Paleogene facies, middle to late Miocene facies, and Pleistocene facies [16] .

This plateau belongs to two basins: the northern basin (Douala-Rio Del Rey) and the southern basin (Campo), separated by the advance of the Precambrian basement at the level of Kribi. In the northern part of the plateau, the sedimentary cover is dominated by loose deltaic complexes from the Sanaga and Niger rivers, incised by channels filled with Pleistocene deposits. In the southern part, where the waters are calm and sedimentation is more limited, there are relict deposits of the last eustatic cycle composed of muddy sands rich in glauconia and bioclastic calcareous sands [7] [14] .

The displacement in latitude of the Inter-Tropical Convergence Zone (Z.C.I.T.) of the air masses is the cause of the monsoon circulating towards the continent and the Harmattan winds of the NE direction blowing towards the ocean [17] - [19] . The marine hydrodynamism of the Gulf of Guinea ( Figure 1 ) are determined mainly by the general regime of the oceanic circulation which is expressed near the coast by the action of the waves and tidal currents that affect the Bay of Biafra; a coastal drift current towards the north. Offshore, the deep Guinea Current flows parallel to the coast to the south, carrying part of Nigerien waters [20] - [22] .

Terrigenous inputs to the Cameroonian continental shelf are mainly of fluvial origin, with coastal rivers such as the Sanaga, which carries about 6,000,000 tons of sediments per year, mainly composed of clay and silt [23] [24] and pollens and spores [25] [26] .

Available oceanographic data confirm the presence of a northwestward coastal drift, with nearshore current velocities ranging from 0.2 to 0.5 m/s, and a southward-flowing Guinea Current offshore, with mean velocities of 0.1 to 0.3 m/s [20] [22] . These values support the inferred role of both currents in transporting sediments and pollen along the shelf.

The cycle of the seasons, the annual distribution of precipitation and temperatures act on the vegetation that develops on essentially ferralitic soils linked to the quality of the bedrock [27] - [30] . Plant ecosystems are mainly made up of dense humid forests in the south and savannahs in the north [31] - [33] . Other plant associations characterized by specific taxa linked to specific edaphic or climatic conditions are present, such as along the coast with mangroves with Rhizophora mangle, Avicennia africana, Langucularia racemosa [34] [35] ; and at higher altitudes, the mountain formations with Podocarpus, Olea, Rapanea [36] . The distribution of sediment types along the coast, particularly the concentration of fine-grained pélites in estuarine zones and near river mouths [14] , also influences vegetation development and pollen preservation. These pélitic zones, rich in clay minerals such as kaolinite, illite, and smectite, and higher in organic matter, create favorable conditions for the accumulation and conservation of pollen grains in marine sediments. This sedimentological context reinforces the connection between coastal vegetation types such as mangroves and the palynological signal recovered offshore.

The samples were collected during three oceanographic missions aboard the N.O. André Nizery, as part of the CAMPUS-Cameroon [12] and CHRIS-Elf [13] programs. A total of 472 dredging samples were collected from the Cameroonian continental shelf. Among these, 71 samples were selected for palynological analysis based on their geographical distribution, depth range (from nearshore to ~200 m), distance from the coast, and sediment texture, with a preference for fine-grained sediments (clay and silt) that favor pollen preservation [25] [37] [38] .

After laboratory processing, 66 samples retained for the analysis. This final dataset provides a representative coverage of the main hydrodynamic and sedimentological gradients across the shelf, allowing for a robust assessment of pollen and spore dispersal patterns in relation to terrigenous inputs and oceanic circulation, as illustrated in Figure 2 .

The samples were prepared according to classical palynological methods (Cour, 1974; Faegri and Iversen, 1975). Pollen identification was carried out using regional monographs [39] - [42] and slides from the Reference Collection of Current Pollens of the Montpellier Laboratory. The data obtained were organized in the form of contingency matrices [43] [44] and analysed using a correspondence factor analysis (FCA).

Two series of analyses were carried out:

Data processing and graphical representation were carried out using the PAST software [45] .

Isopollen maps have been generated to visualize the dispersal of pollen on the continental shelf, according to the same principle as topographic or sedimentological maps. These isopollen curves connect the points where pollen concentrations are similar, thus illustrating the areas of accumulation and dispersal of pollen as a function of the physico-chemical and hydrodynamic conditions of the basin. This method has been used previously by [8] and [9] on the South Atlantic coasts of Africa.

The palynological analysis of the 66 samples collected across the Cameroonian continental shelf revealed a diverse assemblage of taxa representative of the surrounding vegetation cover. From the 66 valid samples, a total of 43,131 pollen grains were counted, of which 42,241 were confidently identified, corresponding

Axis 1 has an ecological significance, showing a cloud formed by groupings of distinct samples, one located in the northern basin containing abundant mangrove pollen, particularly Rhizophora, as well as taxa from various plant ecosystems traversed by the Sanaga River, and carried northwards by coastal drift; and the other in the southern basin receiving rivers that pass only through forested areas and rarely transporting taxa from open formations such as Grasses. Furthermore, this southern basin is influenced by nutrient-rich upwellings where dinocysts develop. The second axis is a factor related to marine hydrodynamics, which would influence pollen dispersion according to their size and shape.

Some maps of the distribution of certain pollens or spores have been chosen in order to illustrate certain apparent phenomena on the Cameroonian continental shelf.

On the various pollen distribution maps ( Figures 5-10 ), it can be seen that the high concentrations of pollen are located at the front of the mouths of coastal rivers, they decrease regressively as they move away from the mouth. This confirms that the terrigenous inputs of the Cameroonian Continental Shelf are essentially of fluvial origin, particularly drained by the Sanaga River [26] . However, northern wind inputs (Sahel, Sahara) cannot be neglected, since various data show that pollen has been observed on gauze filters installed on ships cruising far off the Gulf of Guinea [46] and in aerosols off NW Africa [47] .

The identification of pollens revealed a significant presence of botanical families and a notable diversity among taxa at the generic and specific level. Rhizophora pollens are the most abundant because these plants produce a lot of pollen and the sources of production that are mangroves develop near the coast. However, most of the taxa of the ecosystems crossed by the main Sanaga River are observed on the continental shelf, even the pollen of Graminae ( Figure 7 ) and Compositae ( Figure 8 ) that grows in savannahs far from the coast [26] . The pollen diversity observed in different samples distributed throughout the continental shelf reflects the picture of the botanical diversity of the adjacent continent. These results corroborate previous work on terrestrial samples [10] [48] [49] . However, it is important to point out that pollens from more distant ecosystems may be absent or underestimated in marine areas, due to the long distance travelled by these pollens to the ocean. This could thus limit the accuracy of paleoenvironmental reconstructions based solely on marine samples [9] . This spatial distribution faithfully reflects the ecotones between the different vegetation types adjacent to the Cameroonian coast, including mangroves, dense humid forests, and savannahs further inland.

Factor Correspondence Analysis (FCA) made it possible to distinguish two groups of samples, one located in the northern basin; and the other on the southern basin of the continental shelf. The samples from the southern sector are mainly characterized by forest taxa and the virtual absence of mangrove taxa and savannah taxa, in particular the Graminae. The coastal rivers in this sector drain only the forest areas; on the coast, their flows drown in the calm and cold waters where dinocysts are concentrated, at the same time as fish and organisms that proliferate thanks to nutrient-rich upwellings [50] [51] , up the coast at the upper limit of the southern sector basin.

The samples from the northern sector are much more characterized by pollen from mangroves (Rhizophora, Avicennia, Nypa) and inputs from the Sanaga (Graminae, Alchornea, Cyperaceae, Irvingia) crossing various plant ecosystems. The pollen carried by the Sanaga is absent in the southern sector because the flows of the river are deported to the northwest by the coastal drift.

By juxtaposing the distributions of spores ( Figure 5 ) and Rhizophora ( Figure 6 ), we can see that near the coast, the flows are gradually oriented towards the NW, while offshore the concentrations of Rhizophora decrease as they go southwards. In addition, the pollens of Poaceae and Asteraceae, which are known to come from the savannahs and end up on the continental shelf via the Sanaga, are more concentrated in the northern sector. Indeed, in this area, the trade winds blowing towards the mainland reinforce the swells at the origin of coastal currents [22] . Near the coast, these coastal currents constitute the coastal drift that brings up the flows of the coastal rivers to the NW, in particular that of the Sanaga made up in part of the spores. This phenomenon has also been observed on the Cabindan and Congolese plateau, where a large part of the waters of the Congo River are recovered from the open sea by the drift of the N-NE trade winds which brings them back to the coasts of Pointe-Noire and Mayumba [52] [53] .

In the northern sector, the mangroves growing abundantly near the coast at the level of the Cross-River, the Rio Del Rey complex and the Bay of Douala discharge pollen directly into the basin, and for this, the percentages of Rhizophora reach up to more than 80% in the samples. In these places in the Gulf, marine hydrodynamics can be summed up by the confluence of the flows of the rivers that flow into them, the Nigerien waters, and the waters of the coastal drift coming from the south; this flow is brought out to sea by the tides, and then taken up offshore by the deep Guinea Current which circulates southwards. This is how the pollen content of Rhizophora decreases from north to south ( Figure 6 ); and moreover and far from the production areas, the proportions of Rhizophora are more significant offshore than near the coast.

The deep waters of the Guinea Current are brought back to the coast by the Equatorial Counter Current (ECC) and taken up by the coastal drift, representing a closed circuit marine circulation. A mixing of pollens is carried out that mixes marine pollen flows by providing a pollen spectrum that reflects the instantaneous image of the adjacent continental vegetation, and would be a reference when reconstituting paleoenvironments and paleoclimates; but also reassuring in sequential stratigraphy, when one wants to correlate distant drilling on the same platform during oil prospecting [13] .

The difference in distribution between large or flattened pollens, observed near the coast, and small pollens, transported further offshore, can be explained by the various hydrodynamic forces. Large pollens, which are less likely to be trapped in ocean currents, are deposited more quickly, while small pollens, often trapped in the colloids of suspensions, are transported over greater distances. These observations confirm that pollen size and shape play a key role in their dispersal, as described by [11] and [51] .

Irvingia pollens ( Figure 7 ), which resemble trilete spores, are flattened and triangular in shape, and are preferentially deposited near the coasts and at the front of the mouths. Indeed, the sediments found there are pelites [14] , it seems that these relatively large and irregularly shaped pollens are not sufficient to insert themselves into the interstices, they are not transported and are the first to sediment when the flow of the river weakens in contact with marine water at the mouths. On the other hand, the pollens of Alchornea ( Figure 8 ), which are small in size and round or regular in shape, trapped in the colloids of the suspensions, or clinging to the interstices of the fine particles of the pelites, are carried away from the mouth in the direction of the prevailing currents. Such a result was obtained from the laboratory experiment and field study at Silwood Lake in England of the influence of size on differential sorting in pollen and spore sedimentation processes [11] .

While this study acknowledges the key role of marine currents—particularly the northwestward coastal drift and the southward Guinea Current—in pollen dispersal, it does not fully account for the complex interactions between these currents, tidal regimes, secondary countercurrents, and other hydrodynamic factors (e.g., eddies, seasonal changes in salinity or temperature) that may influence pollen transport. A more detailed hydrodynamic model or in situ measurements (e.g., current velocity, turbidity profiles) would help refine the interpretation and better quantify the respective influence of these dynamic processes.