GNGTS 2014 - Atti del 33° Convegno Nazionale

GNGTS 2014 S essione 1.1 107 Merlini S., Cantarella G., Doglioni C.; 2000: On the seismic profile Crop M5 in the Ionian Sea . ����� ���� ����� ����� Boll. Soc. Geol. Ital. 119, 227–236. Michetti A.M., Esposito E., Guerrieri L., Porfido S., Serva L., Tatevossian R., Vittori E., Audemard F., Azuma T., Clague J., Comerci V., Gurpinar A., Mccalpin J., Mohammadioun B., Mörner N.A, Ota Y., Roghozin E.; 2007: Intensity Scale ESI 2007 . ������� ����������� ����� ����� ��������� ��������� ����� ��� �� ��� Memorie Descrittive della Carta Geologica d’Italia, Roma, 74, 53 pp. Moretti I. and Royden L.; 1988: Deflection, gravity anomalies and tectonics of doubly subducted continental lithosphere: Adriatic and lonian Sea . ��������� Tectonics , 4, 675-693. Porfido S., Esposito E., Vittori E., Tranfaglia G., Michetti A.M., Blumetti M., Ferreli L., Guerrieri L.,. ����� ��� ����� Serva L.; 2002: Areal distribution of ground effects induced by strong earthquakes in the Southern Apennines (Italy) . Surveys in Geophysics 23,6, 529-562. Porfido S. Esposito E., Vittori E., Tranfaglia G., Guerrieri L. Pece, R; 2007: Seismically induced ground effects of the 1805, 1930 and 1980 earthquakes in the Southern Apennines (Italy) . Boll.Soc.Geol.It. (Ital .J. Geosci.), 126, 2 , pp. 333-346. Rovida A., Camassi R., Gasperini P., Stucchi M.; 2011: CPTI11, la versione 2011 del Catalogo Parametrico dei Terremoti Italiani. Milano, Bologna, http://emidius.mi.ingv.it/CPTI. DOI:10.6092 /INGV.IT -CPTI11. Serva L., Esposito E., Guerrieri L., Porfido S., Vittori E., Comerci V.; 2007: Environmental effects from five hystorical earthquakes in Southern Apennines (Italy) and macroseismic intensity assessment . ������������ �� ����� ��� Contribution to INQUA EEE Scale Project. Quaternary Int., 173-174, 30-44. Serva L., Michetti A.M.; 2010: Shakeistics: l’eredità degli studi nucleari in Italia per la valutazione del terremoto di riferimento per la progettazione degli impianti , 48 p., Insubria University Press, Fotoincisione Varesina, Varese. Slejko D., Camassi R., Cecic I., Herak D., Herak M., Kociu S., Kouskouna V., Lapajne J.,Makropoulos K.,Meletti C., Muco B., Papaioannou C., Peruzza L., Rebez A., Scandone P., Sulstarova E., Voulgaris N., Zivcic M., Zupancic P.; 1999: Seismic hazard assessment for Adria . Ann. Geofis. 42, 1085–1107. Stucchi M.,. Rovida A, Gomez Capera A. A., Alexandre O., Camelbeeck T., Demircioglu M. B., Kouskouna V., Gasperini P., Musson R. M. W., Radulian M., Sesetyan K., Vilanova S., Baumont, Fäh D., Lenhardt W., Martinez Solares J. M., Scotti O., Zivcic M., Albini P., Battlo J., Papaioannou C., Tatevossian R., Locati M., Meletti C., Vigano D., Giardini D.; 2013: The European Earthquake Catalogue (SHEEC) 1000-1899 . J. of Seismol., doi:10.1007/s10950-012-9335-2. Seismic cycle measurements from SAR interferometry: inter-, co- and post-seismic deformation associated to the 2012 Emilia seismic sequence G. Pezzo, C. Tolomei, S. Atzori, S. Salvi, J.P. Merryman Boncori Istituto Nazionale di Geofisica e Vulcanologia, CNT, Roma, Italy Introduction. In this study we present some preliminary results concerning the measurement and modeling of the earthquake cycle from SAR interferometry, in a portion of the Po Plain affected by a seismic sequence during 2012. The SARdata availability for the study area spanning from 1992 to 2013 offers a precious opportunity to measure the surface deformation related to different phases of the seismic cycle. In fact the ground deformation due to the tectonic activity are one of the most important tools to improve the knowledge of the deep mechanisms governing the cycle. This can be subdivided in three main different phases: interseismic, coseismic and postseismic (e.g. Scholz and Kato, 1978). The interseismic phase can be again subdivided into a purely interseismic step and a preseismic one, but the state of knowledge concerning the latter is still vague (e.g. Deng et al. ,1998). Soon after the seismic event the post-seismic deformation occurs; two phases can be discriminated: short and long-term deformation. The first one is related to afterslip and/or pore pressure readjustments, which take place over periods ranging from a few hours to a few months after the earthquake and can be observed by using SAR methods; in contrast, the second one is related to the viscoelastic relaxation occurring in the lower crust and upper mantle, ranging from months to years after the earthquake (e.g. Segall, 2002), and it is difficult to measure with SAR methods. Moreover, due to the very low velocity