## 2 Study Area  
The study area in Calabria Region, southern Italy, extends 300 km\({}^{2}\) across the Crotone Basin (Figure 1), which lies on the Ionian side of the Calabrian Arc, i.e., one of the highly active Mediterranean tectonic regions. From a geological point of view, the basin is generally considered a fore-arc basin [31]. It started opening between Serravallian and Tortonian, on top of the SE verging Calabrian accretionary wedge, the latter being grown along the Neogene subduction zone between the sinking Ionian lithosphere and the overriding European plate [32]. Two NW-trending sinist shear zones laterally bound the basin [31]. According to the model proposed by [PERSON] [33], such basement wrench faults caused the partitioning of the basin into separate sub-basins subject to differential subsidence and mutual displacements [34]. Along the coasts of the Crotone province, several marine terraces nowadays provide the evidence of the strong uplift that affected the Calabrian Arc since the Middle Pleistocene. At these terraces, a transgressive erosional surface can be recognized, above which shallow-marine sediments unconformably overlie a Plio-Pleistocene slope succession known as the Cutro Clay [31]. In absence of a general consensus on their number and identification [31], and following the identification made by [PERSON] et al. [35], these marine terraces are referred to as (Figure 1c): the older Cutro terrace (1 st order, Middle Pleistocene) and the Late Pleistocene Campolongo (2 nd order), Capo Cimiti (3 rd order), Capo Rizzuto (4 th  
Figure 1: (a) Location of the study area of Crotone and Capo Colonna in southern Italy with indication of Sentinel-1 data coverage; (b) topography from NASA’s SRTM digital surface model, with indication of hydrocarbon-production infrastructure and concession areas (data source: [29]); and (c) simplified geology (modified after [30]). D.C 1.AG, D.C 2.AG, D.C 4.AG, and F.C 1.AG are the unique identifiers of the concession areas. order) and Le Castella (5 th order) terraces [30; 36]. Being placed at progressively lower elevations (around 180-200 m a.s.l.) and dislocated by Quaternary faults [31], these terraces are a distinctive feature of the local topography (Figure 1b). Of these, it is worth focusing on the terrace a few kilometers SE from Crotone that occupies the 3 km EW-elongated promontory of Capo Colonna (Figure 1b), i.e., the easternmost piece of land in the study area, projecting into the Ionian Sea with an eastward dip of \(\sim\)1\({}^{\circ}\)[31]. A topographic gradient characterizes the promontory, from \(\sim\)50 m a.s.l. elevation at the N-trending landward border representing a paleo-coastline, up to 10-15 m a.s.l. at the coastal cliffs [31]. The internal margin of the terrace is covered by a colluvial layer, while seaward up to 10 m thick carbonate and siliciclastic sediments are found. This complex sedimentary body exhibits a non-homogeneous behavior, from both hydrogeological and mechanical points of view [37]. While in other terraces the steep cliffs are carved in terrace deposits, at Capo Colonna they are carved directly into older units [38] and are subject to severe marine erosion due to strong wind-driven waves undercutting the newly exposed base of the cliffs. Large slabs of Pleistocene fossiliferous calcarenite consequentially fall down [27], thus contributing to severe scarp retreat that threatens the structural stability of properties and the preservation of renown archaeological monuments located close to the cliff edge [27; 37; 39]. Coastal erosion has been affecting this area for centuries, together with subsidence and tectonic-induced submergence of sites that were once sub-aerially exposed along the coast. [PERSON] [40] has demonstrated the relationship between such fault-controlled subsidence and preservation of shallow-marine small-scale cycles visible in the northern Crotone Basin.