## 5 2D Modelling  
A 2D gravity model was generated using the computer software program Talwani 2D gravity modelling (TWGRAV), as reported in [32]. The 2D gravity forward modelling of this study was performed according to the methods described in [32], which incorporates 2D formulations from [33]. For the 2D gravity modelling, the free-air gravity anomalies were applied where the Bouguer gravity data may have encompassed further inaccuracy. On behalf of its design, the Bouguer gravity field in deep water is considerable. Bathymetry laterally profiles the model regions, which are not sufficiently fitted, and the Bouguer gravity field may cover this incorrectness. Generally, several geological structures are somewhat stringy, and the difficulties associated with them can be explained with 2D modelling procedures. Several approaches intended for the calculation of the gravitational attraction instigated by occasionally formed 2D modelling bodies have been introduced [34; 32; 37; 35; 36; 27]. These approaches use a 2D modelling system procedure based on a geological cross unit, wherein the forms of the effects of gravity are planned to shown by a polygon. The 2D modelling is split into numerous small bodies of dissimilar sizes, followed by similar forms [32]. In this technique, the 2D modelling is estimated using a polygon with a sufficiently large number of borders. Together, the vertical-horizontal constituents of the gravitational attraction caused by this polygon can be calculated at some specified point. In addition, the densities of 2D modelling were controlled by the Vp velocities in [38] and Birch empirical functions in [39; 40]. These studies established an experimental correlation among seismic velocities and densities. This correlation was initially created between shelf and deep-sea deposits;however, it was stretched to a broader variety of rocks with greater velocities. In a Birch relation was applied to adapt the Vp velocity into the density (\(p\)). Table 1 summarizes the density values that were useful in the designs [38,39]. The 2D modelling body was designed lengthsways with three seismic profiles (P1-P1\({}^{\prime\prime}\), P2-P2\({}^{\prime\prime}\), and P3-P3\({}^{\prime\prime}\)). These profiles intersected the bathymetric-topographic features of the area under investigation (Figure 1b). These seismic outcomes can be used to make an early density model. Free-air anomaly standards were tested every half kilometre along the seismic profiles to achieve an even 2D (Figure 2b). The 2D modelling procedures carried out on the three profiles are presented in Figures 4-6. Figure 4 shows the 2D gravity modelling alongside the profiles P1-P1\({}^{\prime\prime}\) in portion (C). The model was about 285 km long. The bathymetric value of the profile is similarly displayed in Figure 4A for assessment. In addition, the free-air gravity anomalies designed from the 2D model and the detected anomalies are shown in Figure 4B. In the lateral profile, the gravity values exhibited significant dissimilarities, particularly near the left brink of the profile. A \(-\)Ve gravity anomaly was observed through the thickening of the deposited strata. The gravity values declined sharply near the Pliny trench area due to major crustal thickening and the marine geological features gradient. The basement deepness differed from approximately 9 km at the Egyptian coastline to around 13 km in the middle portion of the study area. The Moho depth next to the Egyptian coastline was approximately 23 km. The depth ranged between 20 and 24 km underneath the East Mediterranean Ridge and the Herodotus abyssal plain. These results agree with the seismic outcomes reported in [41]. The transition from the continental to oceanic crust inside the African plate was observed as an expanse around 40-km offshore from the Egyptian coast (Figure 4), agreeing with drilling evidence of sedimentary structures at the Egyptian coastline [3,6,9,14,42]. Figure 5C displays the 2D gravity modelling alongside profile P2-P2\({}^{\prime\prime}\).