## 6 Conclusions  
This investigation incorporated geomorphological images of the depositional systems from the 3D seismic volume (time slices) with detailed seismic facies classification of the fluvial point bar sediments. The sequence stratigraphy of 3\({}^{\text{rd}}\), 4\({}^{\text{th}}\), and 5\({}^{\text{th}}\) orderswith systems tract detail analysis from the high-resolution 2D seismic sections has been conducted as well. The approach allowed us to accurately interpret such lateral and vertical heterogeneous deposits with different geomorphological elements that were observed within time slices and 2D seismic sections. A chronological framework was established by describing high-resolution sequence stratigraphic discontinuities using high-resolution 2D seismic sections for roughly \(-507\) ms (522 m) thick succession. The utilized approach led to an accurate correlation of the geomorphological features encountered on time slices with certain sequence surfaces in the seismic sections. Furthermore, the identification in the surfaces' section views explained the spatial relation between channel belts and channels detected in the same 3D time slices. Therefore, we can conclude that these channel belts exist in several sequences and are not simply mounds of auto-cyclic rapid abandonment of a fluvial channel system. The predominant sediment types in these fields are high stand of the distal shelf, shallow marine deltaic deposits, and fluvial low stand incised valley deposits. Small quantities of estuarine sediment were found overlying the incised valleys. The production of new sheet accommodation generally takes place throughout the transgressions and subsequent high stand phase, where minimum accommodation is confined to mostly incised valleys in the low stand phase. The geomorphological elements observed are comprised of fluvial point bars, tide-influenced point bars, plugs of the abandonment mud, mouth bar clinoforms, estuarine valley fills, channels, and channel belts. The reflection terminations' geometry can distinguish the reflection configuration of the distinct clinoform and point bars. Thus, convex-up geometries characterize the point bars, while concave-up geometries distinguish the clinoform mouth bars. Besides, point-bar horizontal accumulation surfaces are likely to have preserved the down-laps, whereas the mouth bar's clinoform seems to exhibit a long extension of reflection terminations of top laps and onlaps. Incised valleys in this section of the basin are common features. A comprehensive channel belt analysis observed at \(-96\) ms shows that the channel belt is a single-story system situated in a shallow valley (Figure 5). The features used to identify the incised valleys included the existence of carved-out branched tributary valleys, non-existent levees, and related over-bank sediments. The occurrence of the point bar top deposits at the middle of the interflue level, the valley fills presence, which contains the fluvial phase, and estuarine deposits with a regional tendency of interfluves to the incised valley direction. The increase of fluvial discharge associated with climate changes was perhaps the most probable influence for valley formation. Such differences are overlaid on the accretion of sequences consisting of continental cycles to marine successions related to changes in high amplitude and high frequencies of the sea level. Two primary control factors include the amount of erosion along the boundaries of the sequence and the different accommodation styles developed at different times. These impact the degree of systems tract (TSTs, LSTs, and HSTs) for all depositional sequences. Despite the apparent evidence of the fluvial and distal marine deposition, marine sediments' nearshore evidence was not observed. That may be related to the rapid shoreline movement recorded over the study area, which rarely existed long enough to allow for significant deposits.