## 2 Geological and Seismotectonic Setting  
The geological structure of Cephalonia comprises alpine formations that belong to the Paxi and Ionian geootectonic units and post-alpine deposits of Pliocene to Quaternary lying uncomformably on the alpine basement [25; 26; 27; 28; 29; 30; 31; 32; 33] (Figure 3). The Paxi unit occurs in the largest part of Cephalonia (Figure 3) and includes mainly carbonate rocks from Triassic to Middle Miocene and a Middle Miocene-Early Pliocene clay-clastic sequence, which includes marls, clays and limestones [32; 33] (Figure 3). Figure 2: Flow chart showing the approach followed for the compilation of the ETL inventory and the respective landslide susceptibility assessment in Cephalonia. The Ionian unit is the allochthon tectonic nappe, which crops out in the eastern part of Cephalonia emplaced on top of the Paxi unit (Figure 3). It includes a sequence of Triassic evaporites and limestone breccia as well as Jurassic-Cretaceous fine-grained limestones, red nodular limestones, and shales with the Upper Eocene-Lower Miocene flysch at the top of the sequence [32,33]. The western boundary of the Ionian unit is defined by the Ionian thrust (IT, Figure 3), which is the most external tectonic structure of the Hellenides. The Paxi and Ionian geotectonic units are affected by major reverse faults [31] (Figure 3). The Pliocene-Quaternary deposits include the Pliocene-Calabrian sequence and the Pleistocene-Holocene formations [32,33]. The Pliocene-Calabrian sequence is a marine sequence, observed in an elevated coastal area with width ranging from 2 to 10 km, especially  
Figure 3: The neoetectonic map of Cephalonia along with epicenters of historical and recent earthquakes that triggered landslides in the island. Fault blocks are also noted (EP: Erissos peninsula, AM: Aenos Mt fault block, AP: Argostoli peninsula, PP: Paliki Peninsula) along with their marginal faults (AEF: Ayia Efimia Fault, KAF: Kontogourata–Agonas Fault, CTFZ: Cephalonia Transform Fault Zone) and other major structures (IT: Ionian Thrust). in the largest part of the Argostoli peninsula (AP) and in the eastern and western part of the Paliki peninsula (PP) (Figure 3). It has developed over Paxoi formations, with thickness ranging from 200 to 500 m. The lower part of the sequence is composed of conglomerates, breccia, calcarenites and limestones of the Lower Pliocene. The intermediate part includes yellowish marks with siltstones, sandstone intercalations, sands and conglomerates of the Middle-Upper Pliocene. The upper part consists of marks with intercalations of sands and coarse-grained calcarenites [29; 32; 33]. The Middle-Upper Pleistocene-Holocene formations occur in several places, mainly in the Argostoli peninsula (Figure 3). These are continental deposits and are classified into scree, marine calcarenites of the Middle Pleistocene, Pleistocene interglacial deposits, Pleistocene scree and Holocene deposits [32; 33]. Recent deposits also occur in many sites. Red terrestrial clay sands and coastal conglomerates as well as red calcareous crusts are found in the southwestern part of AP and in the area located WSW of Skala (Figure 3). Scree and alluvial fans cover the Pliocene formations along the foothills of Aenos Mt. These formations cover many limestone slopes. Loose fine-grained and coarse-grained alluvial deposits consist of sands, cobbles and clays on narrow beaches and wide valleys of Cephalonia. Regarding its neotectonic structure, the island is composed of the following fault blocks with different kinematic evolution [33] (Figure 2). The fault block of Aenos Mt (AM) is located in the central and eastern part of Cephalonia. It is bounded to the southwest by the eponymous fault (AFZ--Aenos fault in Figure 3), to the northwest by the Kontogourata-Agon fault (KAF--Kontogourata-Agon fault in Figure 3), to the northeast by the Ayia Efimia fault (AEF--Ayia Efimia Fault in Figure 3) and to the southeast by the Palaeokastro fault (PF--Palaeokastro fault in Figure 3).