## 5 2D Modelling
The profile was 240 km long, generally trending in the WNW-ESE direction and ranging from the Eratosthenes Seamount to the Levant Basin. The gravity anomalies designed from the 2D model and the observed field are shown in Figure 5B. The bathymetry along this profile is accessible as shown in Figure 5A. Moreover, at the profile's limits, the \(-\)Ve values ranged from \(-\)0.5 to \(-\)60 mGal and displayed a rapid reduction, as shown in the free-air anomaly alongside profile P2-P2\({}^{\prime\prime}\). This is indicative of a severe devordrop of the basement and the growth of the sedimentary layer; in this case, there was an abundant deposit cover located underneath the Plio Quaternary sediment in the Levant Basin. The movement of the oceanic-continental crust happens at a distance of approximately 60 km from the Arabian plate, as determined by the seismic results (Figure 5). The depth of the basement extends from around 4 km underneath the Eratosthenes Seamount to around 13 km beneath the Levant Basin, and decreases to approximately 6 km near the Arabian plate. The Moho depth varies from approximately 26 km underneath the Eratosthenes Seamount to around 23 km below the Levant Basin, and to approximately 24 km towards the Arabian plate. Figure 6C displays the 2D gravity modelling alongside profile P3-P3\({}^{\prime\prime}\). The bathymetric rate of the profile was too accessible in Figure 6A. The gravity anomaly calculated by the 2D model, which resulted from the seismic model, is presented in Figure 6B. The profile was 400 km long, and the free-air anomaly had \(-\)Ve values ranging from \(-\)2 mGal to \(-\)140 mGal below the East Mediterranean Ridge. The Moho depth values were significantly \begin{table}
\begin{tabular}{c c c} \hline \hline
**Layer** & **Density (\(p\)) Model (g/cm\({}^{3}\))** & **Velocity Relationship (Vp) (km/sec)** \\ \hline Water & \(p=1.04\) & \(\mathrm{Vp}=1.4\)-1.5 \\ Sediments & \(p=2.35\)–2.5 & \(\mathrm{Vp}=1.5\)-4.5 \\ Upper crust & \(p=2.75\)–2.82 & \(\mathrm{Vp}=6.0\) \\ Lower crust & \(p=2.90\) & \(\mathrm{Vp}=6.5\) \\ Oceanic crust & \(p=2.92\)–2.95 & \(\mathrm{Vp}=7.0\) \\ Moho & \(p=3.30\) & \(\mathrm{Vp}=8.0\) \\ \hline \hline \end{tabular}
\end{table} 
Table 1: Density and velocity relationship in g/cm\({}^{3}\) unit and (km/s), respectively. Adapted from [PERSON] empirical functions [38,39]. associated with the dissimilarities in the gravity values alongside the profile. The Moho site had a depth of around 27 km near the Egyptian coastline, which increased as a slightest depth of around 19 km below the Herodotus abyssal plain. The Moho depth increased again around 26 km under the East Mediterranean Ridge. The rise in the \(-\)Ve gravity value resembles the comparatively great depth of the sedimentary deposit. The evolution of the continental and oceanic crust inside the African plate was modelled at an extant beyond around 40 km from the Egyptian coastline ([PERSON], 2018). The basement depth of approximately 8 km under the Egyptian coastline agreed with the borehole outcomes presented by ([PERSON], 2018). The depth ranged from about 10 to 13 km at the Herodotus abyssal plain and increased to 14.5 km below the East Mediterranean Ridge. The major part of the seismic section data in 2D gravity modelling along profiles P1-P1\({}^{\prime\prime}\), P2-P2\({}^{\prime\prime}\), and P3-P3\({}^{\prime\prime}\) as shown in (Figures 4-6) are controlled as described in ([PERSON], 2018; [PERSON], 2018). Figure 4: 2D modelling gravity along profile P1–P1\({}^{\prime\prime}\). Figure 5: 2D modelling gravity along profile P2–P2\({}^{\prime\prime}\). According to the main results achieved in the current study, a drawing model of the study area and its adjacent areas showing a simplified geological tectonic model of the major geological structure was produced and is presented in Figure 7a. A sketch model is additionally based on the results of previous various geological studies inside the study area [8, 18, 19, 20, 21, 22].