## 2 Geological Setting  
The SP is located along the boundary between Calabrian Arc and Southern Apennines (Figure 1), with the Pollino massif to the north and Sila massif to the south. The Calabrian Arc represents a fault-bounded continental fragment within the western Mediterranean orogen. The tectonic evolution is related to the subduction and rollback of Ionian oceanic lithosphere and the slow convergence between the Eurasian and African-Adriatic continental plates [30, 31, 32]. The Southern Apennines are a NW-SE oriented segment of the Apennines thrust belt. It is characterized by a duplex structure, which consists of two thrusts belts overlapping the Apulian platform [33, 34, 35, 36]. In the SP, the chain is prevalently composed by Apenninic terranes overlapped by thin Calabrian Arc units [37]. The first ones, outcropping along the northwestern side of the SP, are made by Mesozoic-Tertiary carbonate succession and \"flyschiod\" deposits overlapped by Plio-Pleistocene siliciclastic succession [38, 39, 40]. Instead, the Calabrian Arc terranes, cropping out along the southern margin, consist of igneous and metamorphic rocks [41] (Figure 1). In the central sector of the SP, the basement is overlapped by a thick Miocene-Holocene succession; the mio-pliocene deposits represent the infilling of the Sibari-Corigliano Basin, which evolution is strictly connected with the Sangineto Line activity [42, 43], and they are deformed by fault activity with formation of morphological/structural high \begin{table}
\begin{tabular}{c c c c c c c c} \hline \hline
**Satellite** & **Orbit Type** & **Track/Beam** & \begin{tabular}{c} **No. of Used** \\ **Images** \\ \end{tabular} & \begin{tabular}{c} **No. of** \\ **Pairs** \\ \end{tabular} & \begin{tabular}{c} **Temporal Span** \\ **Pairs** \\ \end{tabular} & \
\begin{tabular}{c} **Ground** \\ **Resolution (m)** \\ \end{tabular} &
\begin{tabular}{c} **Incidence** \\ **Angle** \\ \end{tabular} \\ \hline Envisat & Ascending & 86 & 38 & 137 & 4 May 2003 to & 90 & 23 \\ Envisat & Descending & 222 & 33 & 115 & 27 August 2003 to & 90 & 23 \\ COSMO-SkyMed & Ascending & B12 & 12 & 25 & 5 December 2012 to & & \\ COSMO-SkyMed & Descending & B03 & 33 & 60 & 29 October 2009 to & 25 & 29.3 \\ \hline \hline \end{tabular}
\end{table} 
Table 1: Used image datasets. Ground resolution values are obtained after a multi-looked operation. suggest the existence of WNW-ESE trending shallow-crustal folds, developed within a recent and still active transpressional field. The boundaries between the SP and Pollino and Sila massirs are marked by dislocations produced along plio-holocenic high angle faults. The latter is represented in the NW sector by the NW-SE normal fault of the Sangineto Line [48, 49], while in correspondence of the Sila Massif it consists of the WNW-ESE Rossano-Corigliano fault (Figure 1). The recent activity of these faults is still debated [49, 50, 51, 52, 53]. The existence of NE-SW trending normal fault in the area of the CPati Delta is suggested by [48]; recentoseismic evidences related to a NE-SW structural lineament, maybe active during the period between the II and the VII-IX century A.D., are observed in Parco del Cavallo and Casa Bianca archaeological sites [47]. Five to eleven different order of marine terraces are recognized along the outer limit of the plain and uplift rates greater than 3.5 mm/yr are estimated [50, 54, 55]. Holocene deposits are the result of the post Last Glacial Maximum (LGM) transgression and the following (started about 6 ka B.P.) normal regression related to the CPati Delta degradation [56, 57]. The Holocene evolution occurred in a tectonic-controlled setting, which drives the thickness and the facies association lateral variability of the deposits [57]. The post LGM succession consists of marine clayey-silty deposits, overlapping a late Pleistocene coarse-grained unit, passing upward to costal, deltaic and continental ones [57, 58, 59].