In the field, a canoe was used as a means of transportation on the water surface, and a steel Van Veen grab equipped with a rope was employed for sediment sampling. A cooler was used to preserve the collected sediment samples ( Figure 2 ).

In the laboratory, grain-size analyses were conducted using a set of equipment that included a drying oven ( Figure 3(a) ) and a mechanical vibrating sieve ( Figure 3(b) ). The vibrating sieve consisted of sixteen (16) sieves from the AFNOR series. An X-ray fluorescence (XRF) spectrometer connected to a computer was used for geochemical analyses ( Figure 3(c) ).

In the field, twenty (20) sediment sampling points were selected, taking into account the size of the study area and zones inaccessible by canoe. Sediments were collected at each station using a Van Veen grab. The grab was lowered in an open position through the water column until it reached the sediment surface ( Figure 4 ). Upon contact with the bottom, the traction applied to the rope activated the grab arms, immediately enclosing the sediments. The collected sediments were then retrieved, transferred into pre-labeled plastic bags, and stored in a cooler at approximately 4˚C. All samples were subsequently transported to the laboratory for further analyses.

In the laboratory, the samples were divided into two sets: one for grain-size analysis and the other for geochemical analysis and carbonate determination. Prior to grain-size analysis, the samples were washed with dichloromethane to remove metallic pollutants and organic matter. They were then placed in an oven at 50˚C for 12 hours to ensure complete moisture removal.

For the geochemical analysis, the sample preparation and X-ray fluorescence (XRF) analysis followed the protocol described below. After oven-drying at 70˚C for 24 hours, the samples were ground to obtain a very fine particle size (powdered samples). Five grams of powdered sample were mixed with 1 g of binder powder and thoroughly homogenized. The resulting mixture was then pressed into pellets using a hydraulic press.

A 100 g sandy fraction of each treated sample was sieved using a stack of sixteen (16) sieves with decreasing mesh sizes ranging from 5 mm to 63 µm. The material retained on each sieve after agitation (20 minutes of vibration) was collected and weighed, allowing the determination of the weight percentage retained on each sieve.

This analysis aims to quantify the carbonate (CaCO₃) content in each sediment sample. The carbonate percentage was determined by weight loss. One gram (1 g) of dry sediment was placed in an Erlenmeyer flask and treated with 10 ml of hydrochloric acid (HCl) diluted to 50%. This reaction released carbon dioxide (CO₂) gas. The calcium carbonate content was calculated based on the volume of gas evolved according to the following formula:

${\text{CaCO}}_3\left(\%\right)=\frac{\left(P_i-P_f\right)\times 100}{P_i}$

(where P_i represents the initial weight of the dry sample, P_f represents the final weight of the sample after calcination).

The pelletized sample was placed under the X-ray beam of the fluorescence spectrometer. Sample information was entered into the XRF analysis software. XRF is an elemental chemical analysis method that exploits a physical property of matter, namely X-ray fluorescence.

XRF analysis involves bombarding the sample with X-rays, causing it to emit energy in the form of X-ray photons. Each atom emits photons with specific energies and wavelengths, a phenomenon known as X-ray fluorescence or secondary X-ray emission, which is characteristic of the atoms present in the sample [7] . From the emitted secondary radiation, an X-ray spectrum is obtained, which is characteristic of the sample’s chemical composition. Mass concentrations of the elements are then determined by analyzing this spectrum.

The preparation of thin sections involved three main steps:

Observation of the polished sections using Scanning Electron Microscopy (SEM) provided lectron images. All particles present in the sample were automatically detected after image processing. Spectra of the polished sections were acquired using Energy-Dispersive Spectroscopy (EDS) coupled with SEM.

The creation of spatial distribution maps for sediments and rare earth element concentrations required the input of geographic coordinates of the study area into the coordinate bar of ArcGIS software (version 10.2.2). The study area map was first georeferenced and then digitized. Georeferencing is the process of assigning real-world geographic coordinates to the study map image. For this work, the WGS 84-UTM-29N coordinate system was used. Digitizing the map creates a data layer.

Subsequently, the database was mapped using the Inverse Distance Weighting (IDW) method, which interpolates data within a grid of regularly spaced points. Each point in the grid was assigned a variable value calculated from the original data file values. This procedure allowed the generation of various maps representing the spatial distribution of the studied parameters.

The bottom of the Sassandra River estuary is covered by unconsolidated detrital sediment deposits. This superficial sedimentary layer is characterized by the presence of very coarse sands, coarse sands, medium sands, fine sands, and muds.

These sands are composed of bioclastic fragments and exhibit minor color variations, ranging from yellow to reddish. They occupy the western (upstream) part of the estuary and extend along the southern channel until merging with medium sands. Small patches of coarse sediments are also observed near the large island and within areas of medium sands ( Figure 5 ). The mean grain size (MZ) ranges from −0.49 to 0.90 Φ ( Table 1 ). The sediments are very poorly to moderately sorted, with fine-skewed asymmetry for coarse sands and strongly fine-skewed asymmetry for very coarse sands.

These sands, ranging in color from yellow to reddish-brown and brownish-yellow, constitute the largest part of the superficial sedimentary cover. They show maximum spatial extent ( Figure 5 ), covering almost the entire estuary, including large portions of the channels, the river mouth area, and the eastern side. Around the large island and in the eastern channel, a mixture of medium and fine sands is observed. The mean grain size (MZ) varies from 1.07 to 1.92 Φ ( Table 1 ). Standard deviation (Σ) values range between 0.37 and 0.79 Φ, indicating well-to moderately sorted sands. Skewness (Ski) ranges from 0.21 to 0.37 Φ, reflecting a fine-skewed distribution.

Fine sands, ranging in color from yellow to brown, and dark to dark-greenish muds are concentrated around the large island. They form the dominant sedimentary cover in the northern branch of the estuary ( Figure 5 ). Fine sands exhibit minor color variations.

Carbonate contents range from 0.99% to 4.58%, with a mean value of 2.29% ( Table 1 ), indicating undersaturated carbonate sedimentation. In coarse to very coarse sands, carbonate contents are higher compared to muds, medium sands, and fine sands.

Ech: Echantillon. Long: longitude. Lat: latitude.

Figure 6 shows sand grains with angular to sub-angular shapes. Many of these grains exhibit numerous cracks and fractures with black coatings. Spectral analysis of these coatings reveals the presence of chemical elements such as iron, magnesium, phosphorus, silicon, aluminum, sodium, calcium, and potassium (Spectrum 3, Spectrum 1, Figure 7 ). Semi-quantitative compositions of the black coatings observed on the grain surfaces and within the cracks are presented in Table 2 and Table 3 . Iron, potassium, and phosphorus are the most dominant chemical elements.

The rare earth elements (REEs) present in the sediments, along with their concentrations, are listed in Table 4 . The analyzed REEs include lanthanum (La), cerium (Ce), thulium (Tm), and yttrium (Y). Their concentrations range from 0.0 to 39.90 ppm for La, 0.0 to 20.50 ppm for Ce, 2.40 to 10.50 ppm for Tm, and 2.50 to 9.00 ppm for Y.

Their spatial distributions in the surface sediments generally indicate higher concentrations upstream. Lanthanum and yttrium exhibit elevated concentrations both upstream and at the river mouth ( Figure 8 and Figure 9 ). Thulium and cerium are more concentrated upstream and in the extreme southwestern part of the estuary ( Figure 10 and Figure 11 ). In contrast, the remainder of the estuary is characterized by very low concentrations.

The sedimentary fill of the estuarine bottom comprises all grain-size classes, ranging from sands to muds. The distribution of these surface sediments shows little difference from that reported by [8] [9] , with the same sediment types observed. According to the map by [9] , coarse sands cover almost the entire estuarine bottom, while muds accumulate mainly along the margins. This comparison highlights the instability of sediment deposits, which may be attributed to seasonal variations in energy and hydrodynamic conditions. During their studies, energy levels in the main channel were high [9] , which likely transported fine particles while leaving coarser grains in place. The accumulation of mud around the island may result from the deposition and decomposition of plant debris originating from the island. Their dark color could partly reflect the transformation of organic matter derived from this debris, a phenomenon also noted by [10] for the superficial sediments at the mouth of the Comoe River. Sands in the main channel are generally coarse to medium. The mixed characteristics observed, with coarser and finer sediments combined, are consistent with a transitional environment [11] .

The relatively low carbonate content (mean 2.29%) can be attributed to the silico-bioclastic nature of the sediments, dominated by detrital materials with a siliceous composition. In contrast, these values are considerably lower than those reported by [12] for sediments of the Moulouya estuary, where carbonate contents approach 40%. This difference is mainly explained by the predominance of shell debris in the sediments of the Moulouya estuary [12] .

Sand grains from the Sassandra River estuary are characterized by numerous fractures and cracks with black coatings, which often leave reddish-brown stains. Several factors may explain the formation of these fractures and cracks. They may result from aquatic impacts or from violent collisions between grains, particularly when some grains are considerably coarse. During water flow, coarse sediments collide while rolling or sliding, generating shear stresses that induce cracks and fractures [13] .

The black coatings observed on the grain surfaces may consist of iron oxides, which would explain the yellowish-red to brown coloration of the sands. Rare earth element (REE) contents are very low and are more frequently detected in sediments exhibiting these black coatings. Indeed, Carpentier [14] reports that in the sediments of the Lesser Antilles, iron oxides can trap rare earth elements. Similarly, Matias [15] notes that REEs are generally associated with amorphous or crystalline iron oxides.

Chemical elements such as phosphorus, calcium, sodium, and potassium trapped in the sediments are likely related to human activities. Their presence may result from urban effluents or agricultural practices, such as the application of phosphate fertilizers [16] . Through erosion and leaching from fertilized agricultural lands, these agrochemicals can enter the aquatic system and become incorporated into the structure of the sand grains. This is consistent with findings by [17] , who reported that agriculture in southwestern Côte d’Ivoire is primarily extensive, with significant soil leaching.

Mapping of sediments and determination of their chemical composition constitute fundamental tools in coastal engineering. However, estimating the volume of detrital sediments over multiple years is necessary to fully understand the dynamics of sedimentary infilling.