## 5 Discussion  
Interpretation of cross-section P1 was performed by comparing this section with the Banda Aceh geological map, as shown in Figure 1, starting from station ACH01 and going through to ACH11 sequentially. This method identified that the low-resistivity area C1 consists of sedimentary and metasedimentary rocks (marine/continental sediment) in the form of alluvium, with resistivity values ranging from 10 to 800 \(\Omega\)m [61], corresponding to the resistivity depicted in the MT cross-section of P1. The high-resistivity area R1 was identified as igneous rock, consisting of limestone formations with a resistivity range of \(2\times 10^{4}\) to \(2\times 10^{6}\)\(\Omega\)m [62], from the Lamno Formation, limestone from the Raba Formation, and metamorphic rocks consisting of agglomerates (Quartz rocks) from the Bentaro Volcanic Formation, which matches with the depicted resistivity in the MT cross-section of P1. According to the geological map in Figure 1, Miocene and Quaternary volcanic rocks and sedimentary rocks were identified in Figure 16 as C2. The resistivity contrast between R1, C1, and C2 is not identified as a fault because, based on the references, this area records low seismic activity [25]. Then, between stations ACH04 and ACH05, based on the MT cross-section of P1 in Figure 15, there is a resistivity contrast from a distance of 20-30 km, as shown in the MT cross-section of P1 in Figure 15, which is interpreted as the Aceh Segment, a part of the Sumataran Fault, and confirmed by the geological map in Figure 1; this is further supported by gravity anomaly analysis references [25]. This analysis indicates a difference in vertical block densities, with high densities (2.4-2.55 g/cm\({}^{3}\)) and low densities (2.2-2.4 g/cm\({}^{3}\)) over a distance of 25-50 km, which aligns with the MT cross-section results at a distance of 20-30 km and a dip angle of 90\({}^{\circ}\), as per reference [25]. Based on the MT section in Figure 16, a creep zone (C3) characterized by a conductive zone is visible at a depth of 2 km, confirmed by the existence of the creeping zone in the Aceh Segment along \(\sim\)100 km [55]. Characterizing the creeping zone corresponds to the presence of the fluids related to the old terrace deposits of the Indrapuri Formation characteristics. The Indrapuri Formation is characterized by volcanic rocks, including tufufaceous and calcareous sandstones, which can contain fluids such as water and contribute to low-resistivity zones. The high-resistivity zone with a range of 150-1000 \(\Omega\)m (R2) is characterized as basement rock, specifically metamorphic rocks from the Triassic-Cretaceous age, as confirmed by the geological map in Figure 1. The low-resistivity zone with resistivity values of 1-15 \(\Omega\)m (C3) is characterized as volcanic rock from the Lam Teuba Volcanic Formation and the Indrapuri Formation, consisting of old terrace deposits and volcanic gravels, which  
Figure 18: Profile 3 (P3) of the 3D resistivity model. The black question mark symbol (?) depicts the unknown fault. tend to have low resistivity [63], as confirmed by the geological map in Figure 1, consistent with the MT cross-section in Figure 16. Further, between 55 and 60 km, the Seulimeum Fault Segment is not visible on the MT cross-section of P1.