## 5 Discussion  
In order to discuss the various tectonic activity signals of the Wadi Araba basin, we examined and analyzed the results of all calculated morpho-tectonic indices. The results of the S\({}_{\rm mf}\) and V\({}_{\rm f}\) indices show a well-correlated relationship for all mountain front segments, with the exception of segments N6, N10, S7, S17, and S18 (Figure 9). These segments have similar S\({}_{\rm mf}\) values regarding the other segments, but they indicate a very high V\({}_{\rm f}\) index value. These inconsistent values indicate anomalies in the signals that give rise to very high mean values with relatively low S\({}_{\rm mf}\) values. This case was recorded by the author of Ref. [1]. Therefore, we agree with his conclusion, which states that the S\({}_{\rm mf}\) index values are more significant than the mean V\({}_{\rm f}\) values in terms of recognizing the activity of the front segments. The authors of Ref. [2] applied a method that used S\({}_{\rm mf}\) and V\({}_{\rm f}\) results to define the tectonic activity classes. Mountain fronts indicated by active signatures have low S\({}_{\rm mf}\) values (1.00:1.50), whereas higher values of S\({}_{\rm mf}\) (>3.00) indicate fronts that are strongly affected by erosion processes. Many authors concluded that high S\({}_{\rm mf}\) values may explain that the range-bounding fault segment responsible for the front formation could be some distance away from the erosion-affected mountain front [1; 2; 11; 42]. When mountain fronts' values are plotted against V\({}_{\rm f}\) values, it reveals that most segments fall within the limits of Class 2 (moderate tectonic activity), which indicates uplift rates between 0.05 and 0.5 mm/yr [3]. Accordingly, the morpho-tectonic analysis shows that the Northern and Southern Galala Plateaus mostly reflect moderate signals of active tectonics. The role of rock and material resistance in streams is applied to understand the development of the topography results due to erosion actions and the stream flow over the underlying rocks and soils of different strengths. The significance of this index confirms that the S\({}_{\rm L}\) values provide higher results when streams flow over resistant rocks or materials or uplifting regions and record lower values when rivers run over less resistant rocks or weakly uplifting areas. In this study, some of the S\({}_{\rm L}\) values abruptly changed over the same rock units. This situation could be recorded as an anomaly, as the S\({}_{\rm L}\) index should reflect the same values over the same rock resistance. Based on the S\({}_{\rm L}\) index values, and due to the mountain fronts having rocks with very low and low resistance, the S\({}_{\rm L}\) index value confirms that most mountain front segments reflect moderately active tectonic signatures. Figure 8: Location of the V\({}_{\rm f}\) index along the stream crossing Northern and Southern Galala Plateaus. Regarding regional seismic hazards, most of the seismic risk studies have concentrated on long-term deformation and high-strain regions that are affected by major earthquakes and significant slip rates [1,18]. Moreover, high-intensity earthquakes in continental low-strain regions produce slow slip rates (e.g., Cairo earthquake and Gulf of Suez earthquakes in Egypt in 1992 and 2012, respectively [25,26; 43]; the Van earthquake in Turkey, 2011 [44]), reflecting the need for similar studies in the Gulf of Suez. Most of the Egyptian seismic signals were recorded in the northern Red Sea, including the Gulf of Suez, with some seismic activity coming from the middle and southern parts of Egypt [43,45,46]. The average magnitude of these seismic activities was recorded as (4-7). Although regional GPS observations [46] indicate that the modern strain rate along the Gulf of Suez is low, the results of this work indicate that this situation has been similar over medium and longer timescales.