## 2 Geological Setting
In the western Betic Cordillera,the slab is dipping eastward to south-eastward [84; 85; 86], while in the central and eastern Betic Cordillera, it is detached due to slab tearing [81]. In this view, the Alboran Basin was formed due to the back-arc extension [87]. Some hypotheses suggest that subduction with rollback continues to be active today in the western Betic Cordillera [34; 80; 88; 89]. In addition, [PERSON] et al. [90; 91] proposed that the delamination of the continental Alboran lithosphere was driven by the subduction of the oceanic lithosphere. This model is consistent with a slab rollback of an east-dipping slab beneath the Alboran Sea [92], resulting in the delamination of the Alboran lithosphere during the Late Miocene and its replacement by an asthenospheric plume. The current evolution of the Betic Cordillera is driven by a 3-5.6 mm/year westward migration [34; 93] and clockwise rotation [30] of the northern branch of the Gibraltar Arc with respect to Eurasia and a simultaneous NW-SE convergence of 4-6 mm/year along the Eurasia-Nubia plate boundary, oblique to its E-W regional trend [28], affecting the region heterogeneously (Figure 1b). In the western Betic Cordillera, the westward migration of the arc is accommodated by active folding [94] and faulting [95], as observed in regional geodetic studies [30; 34; 93]. In the eastern Betic Cordillera, the convergence is transferred through the Trans-Alboran Shear Zone [96; 97], a transprestive tectonic corridor that continues onshore as the Eastern Betic Shear Zone (Figure 1b) [98]. This is a consequence of the movement towards the NW of a tectonic indenter located in the Gulf of Vera (Figure 1) [99; 100]. In the central Alboran Sea, the NW-SE compression is due to the north-westward movement of another tectonic indenter (Figure 1b) [36], generating strike-slip faulting and affecting the coastal areas to the south of Sierra Nevada [101]. On the contrary, the Alboran Domain in the central Betic Cordillera is affected by a NE-SW to ENE-WSW extension of nearly 2 mm/year (Figure 1b) [29]. Finally, the South Iberian Domain in the central Betics presents a 1 mm/year westward displacement with respect to the stable Iberia [31], but no extension has been registered [30]. The ENE-WSW extension in the central Betic Cordillera (Figures 1 and 2) is mainly accommodated by NW-SE extensional fault zones, primarily affecting the Alboran Domain [35]. The main ones include the Baza Fault zone in the northeast [102], the Almeria-Tabernas Fault zone in the east [103], the Balangerra Fault in the south [101], and the extensional system of the Granada Basin in the west (Figure 1b) [104]. The extensional system of the Granada Basin (Figures 1 and 2) accommodates the extension of the central Betic Cordillera [30; 105] and affects the upper crust of the Alboran Domain as well as the South Iberian Domain, rooting into a detachment zone at a depth of approximately 10-15 km [104]. The active detachment has been considered the western continuation in the depth of the Mecina detachment [20; 106]. The western boundary of the Granada Basin is subject to both compressional and strike-slip faulting (Figure 2) [107; 108; 109; 37]. The Campo de Dalias and the adjacent Alboran Sea are affected by NW-SE normal dextral faults, such as the Balanegra Fault, and ENE-WSW folds (Figure 2) [101; 102; 38; 101; 110; 111; 112]. The connection zone between the seismogenic areas of the Granada Basin and the Campo de Dalias is hardly affected by seismicity (Figure 1b). There, the synformal area called the Alpujarras Corridor has been interpreted as a dextral fault zone with related normal and reverse faulting (Figure 2) [101; 64; 31].