## 7 Depositional and Structural Evolutionary Model
Extensional deformation during the syn-rift stage [69; 72] has resulted in the weakening of roof strength, forming outer-arc bending on top of the diapiric structures, while the wedge-shaped geometry introduced anisotropic conditions. Additionally, the accumulation of sediments in the basin differentially increased the average density and thickness of the overburden. Evaporitic intrusions started to pierce the overburden, bending the roof and affecting the depositional patterns. At this stage, an active diapiric phase of halokines [2] was established in the area, controlled by sediment accumulation rates and the degree of anisotropic conditions of the roof [114]. Intervals of thick- to massive-bedded limestones started to form in the stratigraphic record, characterized by sedimentary features (e.g., erosional surfaces, planar and ripple cross-lamination), which indicates deposition by turbidity currents. Syn-sedimentary slump events also occurred, suggesting a depositional environment of unstable conditions originating mainly from the salt rise (Figure 13e). Figure 14: Simplified chronostrigraphic correlation of available interpretations for the Ionian zone, regarding the tectono-stratigraphic and salt tectonics processes, suggested by various researchers and this study. Data derived from key references are listed in the figure [69; 71; 72; 82; 83] (* represents diapiric movement in Albania region). The effect of the salt uprise in the study area is imprinted in the whole Cretaceous carbonate succession with intervals of calciturbidites and calcidebrites (Figure 13f). Internal unconformities and onlap structures, observed in the studied sections, suggest the folding of the roof due to a halokinetic uprise, as is also evidenced in the Vigla section by the detailed 3D photogrammetric model (Figure 11). This fact, supported also by the available seismic profile, the surface cross sections and structural measurements, enabled us to identify a basal megaflag [6,115], consisting mainly of Late Triassic carbonates and Jurassic shales, in the studied area. Salt uprise is inferred to have slowed down and ceased gradually during the Early Eocene (Figure 13g), where the final occurrences of the fine-grained calciturbidites were found in the stratigraphic record (Figure 14). Monotonous, pelagic thin- to medium-bedded mudstones overlie the aforementioned calciturbidites, followed by the deposition of the Oligocene flysch sediments. The active diapiric phase ceased probably due to the increase in the overburden thickness that exceeded the threshold thickness for salt mobilization [2] or a reduction in the triggering external tectonic forces. As salt rise ceased, contractional deformation started to affect the basin configuration, introducing a phase of tectonic inversion, where the previously extensional structures that favored reactive and active diapiric phases were then reactivated as thrust faults. Uprising salts enhanced block movements across the pre-existing fault surfaces, acting as local declollement horizons (Figure 13h,i). A typical fold-and-thrust belt regime was established in the area, developing asymmetric synclinal and salt-cored anticlinal structures. The salt intrusion of the previous stages had already formed upturned flaps flanking the diapiric body to an almost sub-vertical inclination of the strata. Compressional deformation increased further from the dips, resulting in the complete overturning of fold limbs (Figure 13j,k). The combination of salt-driven inversion tectonics provided favorable conditions for the formation of structural traps.