GNGTS 2013 - Atti del 32° Convegno Nazionale

June, 2012: preliminary data and results” edited by Marco Anzidei, Alessandra Maramai and Paola Montone, 55 , 4, 647-654, doi:10.4401/ag-6134. Serpelloni E., and 21 more authors; 2012: GPS observations of coseismic deformation following the May 20 and 29, 2012, Emilia seismic events (northern Italy): data, analysis and preliminary models . Annals of Geoph . , spec. issue “The Emilia (northern Italy) seismic sequence of May-June, 2012: preliminary data and results” edited by Marco Anzidei, Alessandra Maramai and Paola Montone, 55 , 4, 759-766, doi:10.4401/ag-6168. Sirovich L. and Pettenati F.; 2004: A new Automatic Source Inversion Technique of Intensity Patterns of Earthquakes; Validation on a Destructive Shock of 1936 in NE Italy . Journal of Geophysical Research, 109 , B10309, doi: 10.1029/2003JB002919, 2004, pp. 16. Sirovich, L., Pettenati, F., and Cavallini, F.; 2013: Intensity-Based Source Inversion of the Destructive Earthquake of 1694 in the Southern Apennines, Italy . J. Geophis. Res. In stampa SEISMIC ANALYSIS OF THE WESTERN MARGIN OF THE EASTERN SOUTHERN ALPS FOREDEEP M. Pola 1 , A. Ricciato 2 , R. Fantoni 3 , P. Fabbri 1 , D. Zampieri 1 1 Dipartimento di Geoscienze, Università degli Studi di Padova, Italy 2 GEPlan consulting, Ferrara, Italy 3 Eni E&P, San Donato Milanese, Italy Introduction. The Veneto-Friuli area (NE Italy) represents the foreland of three orogenic belts, which are currently active although at different rates: the Dinarides to the E, the Eastern Southern Alps to the N and the Apennines to the SW (Massari et al ., 1986; Fantoni et al ., 2002). Since the Mesozoic time this area has been affected by several phases of tectonic deformation (Mesozoic extensional cycle and Cenozoic compressional cycle; Fantoni and Franciosi, 2009, 2010) resulting in a fragmented architecture buried beneath the Quaternary Veneto-Friuli alluvial plain. With the aim of unravelling the architecture and the evolution of the western margin of the Veneto-Friuli foredeep, marked by the Schio-Vicenza Fault, about 1000 km of 2D seismic sections and more than 10 deep wells acquired by ENI for hydrocarbon exploration were interpreted. The Schio-Vicenza fault marks also the eastern boundary of the structural high of the Lessini and Berici mountains and Euganei hills (LBE), which constitutes a foreland block only weakly affected by the Alpine shortening separating the Western from the Eastern Southern Alps and their forelands (Bigi et al. , 1990; Laubscher, 1996). The northern part of the Schio- Vicenza fault is well exposed in the Veneto Pre-Alps to the north of Schio (Fig. 1) and has been the subject of many studies ( e.g ., De Boer, 1963; Semenza, 1974; Zanferrari et al., 1982; Zampieri, 1995; Castellarin and Cantelli 2000; Zampieri and Massironi, 2007; Fondriest et al. , 2012). In contrast, the southern part of the fault is buried beneath the Veneto alluvial plain and its occurrence is only highlighted to the south of the Euganei Hills near Conselve (Finetti, 1972; Fig. 1). TheVeneto-Friuli forelandwas affected by different flexural cycles related to the diachronous build up of the three surrounding chains (Fantoni et al. , 2002). The flexuring started during the Paleocene-Eocene with an eastward faint inflection affecting mainly its eastern sector (Friuli Plain) and linked to the build up of SW-vergent Dinaric thrust belt (Doglioni and Bosellini, 1987; Fantoni et al ., 2002). After the Lower Oligocene regional emersion, two main depositional/ flexuring cycles occurred in the foredeep (Fantoni et al., 2002): i) the Chattian-Langhian cycle, characterised by a weak north-ward inflection (bending angle below 1°) and producing an accommodation space filled by clastic supply mainly from the uplifted sector of the South Alpine chain; ii) the Serravallian-Lower Messinian cycle, affected by a prominent bending towards NNW due to the quick uplift of the Southern Alps belt (Zattin et al. , 2006). The end of the Serravallian-Lower Messinian cycle is attested by a prominent sub-aerial erosion (intra- Messinian Unconformity) controlled by a combination of factors like dropdown of the eustatic level, differential subsidence and regional uplift (Ghielmi et al ., 2013). During the Pliocene- 186 GNGTS 2013 S essione 1.2