GNGTS 2015 - Atti del 34° Convegno Nazionale

108 GNGTS 2015 S essione 1.2 More specifically, the analysis consisted of the following main steps: (a) collection and acquisition of aerial photos, numeric cartography, Digital Terrain Model (DTM) data, geological and geophysical data; (b) generation of the vector cartographic database and alpha-numerical data; c) image processing and features classification; d) cartographic restitution and multi- layers representation. Three thematic data sets have been generated: “faults”, “earthquakes” and “gravimetric” data. The fault dataset was built by merging all Plio- Quaternary structural data extracted from the available structural and geological maps, and many geological studies (Boncio et al. , 2004; Galadini et al., 2000, 2003; Falcucci et al. , 2011; Moro et al. , 2013). The earthquake data set consists of seismic data collected in the available historical and instrumental Catalogues (Gruppo di lavoro CPTI, 2004); CPTI11, Rovida et al. , 2011; ISIDE, INGV database). Seismic data have been standardized in the same format and merged in a single data set. As regards the gravimetric data set, we performed a Multiscale Derivative Analysis (MDA) of the gravity field, based on the good resolution properties of the Enhanced Horizontal Derivative (EHD) signal (Fedi et al. , 2005). The main results of our integrated analysis show a good correlation among faults, epicentral location of earthquakes and MDA lineaments from gravity data. Furthermore, 2D seismic hypocentral locations were correlated with the information yielded by the application of the DEXP method to gravity data (Fedi and Pilkington, 2012), to estimate strike, dip direction and dip angle of some faults of the areas. Seismotectonic framework of the area. The central Apennines consists of a Mio-Pliocene thrust-and-fold belt that developed as the result of the convergence between the Hercynian European plate and the westward subducted Paleozoic Adriatic lithosphere (Patacca and Scandone, 2004). The opening of the Tyrrhenian basin and the flexural retreat of the lithospheric plate dipping below the Italian peninsula (Malinverno and Ryan, 1986; Royden et al. , 1987; Patacca et al ., 1990; Doglioni, 1991; Doglioni et al ., 1994) caused the E-W migration of the compressive front and, since the Mio-Pliocene, contemporary extentional tectonics affected the innermost portion of the Apennines chain previously controlled by compressive tectonics. The intra Apennine extension has also been characterized by a progressive northeastward migration determining an age of the extensional tectonic structures, progressively younger heading eastwards (Lavecchia et al. ,1994; Bartole, 1995; Calamita et al., 1999; Galadini and Messina, 2004). Since Pliocene, and during the entire Quaternary NW–SE trending faults have been responsible for the formation of several half-graben structures that currently match intermountain basins in which Plio-Quaternary continental sediments (up to 1,200 m thick in the case of the Fucino Plain) (Galadini and Messina, 1994) have been deposited. ����� ������� These include the Fucino, L’Aquila, Sulmona, Rieti, Leonessa and Norcia basins. Normal and normal-oblique faults generally bound these depressions to the northeast. Changes during the Quaternary, however, affected the kinematic evolution of the (Patacca et al. , 1990; Cinque et al. , 1993; Pantosti et al. , 1993) central Apennines and are represented by the end of the activity of some normal faults, and by evidence of oblique-slip kinematics on faults previously characterised by normal movements (Galadini, 1999).To the west and northwest the boundary of the Abruzzi Apennines is represented by the contact between units overlain onto the Latium-Abruzzi carbonate and those belonging to the Umbro-Marchean Apennines; the surface trace of such contact is marked by the Olevano-Antrodoco- Sibillini Line (Patacca et al. , 1990; Bigi et al. , 1991a; Galadini, 1999; Pizzi and Scisciani, 2000; Centamore and Rossi, 2009; Pizzi and Galadini, 2009; Calamita et al. , 2011). East and SE of the Abruzzi Apennines, Oligo-Miocene flysch units of the Molise domain are separated from Latium-Abruzzi units by the Ortona-Roccamonfina Line, (Locardi, 1988; Di Bucci and Tozzi, 1991; Centamore and Rossi, 2009; Pizzi and Galadini, 2009). The persistence of the extensional activity during the Late Pleistocene–Holocene is demonstrated by the present seismicity with earthquakes of magnitudes up to 7.0 in past centuries (Working Group CPTI 2004) and by the numerous studies dealing with active tectonics and paleoseismology. The present tectonic regime shows that the