GNGTS 2018 - 37° Convegno Nazionale

232 GNGTS 2018 S essione 1.2 GKHR; 2009: Geološka karta Republike Hrvatske ( Geological Map of the Republic of Croatia ) scale 1:300.000 . Hrvatski geološki institut (Croatian Geological Survey), 1 sheet. <www.hgi-cgs.hr/ogk300/ogk300.html >. Grandić, S., Boromisa-Balaš, E., Šušterčić, M., Kolbah, S.; 1999: Hydrocarbon possibilities in the Eastern Adriatic Slope zone of Croatian offshore area . Nafta, 50/2, 51-73. Grandić, S., Biancone, M., Samaržija, J.; 2001: Geophysical and stratigraphic evidence of the Triassic rift structuration in the Adriatic offshore area . Nafta, 52/12, 383-396. Grandić, S., Kratković, I., Rusan, I.; 2010: Hydrocarbon potential assessment of the slope deposits along the SW Dinarides carbonate platform edge . Nafta, 61 (7-8), 325-338. Đurasek, N., Frank, G., Jenko, K., Kužina, A., Tončić-Gregl, R.; 1981: Prilog poznavanju naftno-geoloških odnosa u sjeverozapadnom dijelu jadranskog podmorja . ( Contribution to the understanding of oil-geological relations in NW Adriatic area ). In: Šolc, A. (Ed.), Kompleksna naftno-geološka problematika podmorja i priobalnih dijelova Jadranskog mora, (Complex Oil-geological Aspects for Offshore and Coastal Adriatic Areas), Split, Zbornik radova (Proceedings), I, 201-213. Korbar, T.; 2009: Orogenic evolution of the External Dinarides in the NE Adriatic region: a model constrained by tectonostratigraphy of Upper Cretaceous to Paleogene carbonates . Earth-Science Reviews, 96, 296-312, DOI 10.1016/j.earscirev.2009.07.004. Placer, L., Vrabec, M., Celarc, B.; 2010: The bases for understanding of the NW Dinarides and Istria Peninsula tectonics . Geologija, 53/1, 55-86, DOI 10.5474/geologija.2010.005. Prelogović, E., Kuk, V., Jamičić, D., Aljinović, B., Marić, K.; 1995: Seizmotektonska aktivnost Kvarnerskog područja . In: Vlahović, I., Velić, I.,Šparica, M. (Eds.) Proceedings of the First Croatian Geological Congress, Opatija, vol. 2, Croatian geological society and Institute of geology, 487- 49. Prtoljan B., Jamičić, D., Cvetko-Tešković, B., Kratković, I., Markulin, Ž.; 2007: The influence of Late Cretaceous synsedimentary deformation on the Cenozoic structuration of the middle Adriatic, Croatia . Geodinamica Acta, 20/5, 287-300, DOI 10.3166/ga.20.287-300. Salopek, M.; 1954: Prilozi poznavanju geološke građe Labinskog i Pićanskog basena Istre. JAZU, 60. Soto, I. J., Flinch, J., Tari, G.; 2017: Permo-Triassic Salt Provinces of Europe, North Africa and the Atlantic Margins 1st Edition, Tectonics and Hydrocarbon Potential . Elsevier, 632, DOI 10.1016/C2015-0-05796-3. Vlahović I., Tišljar, J., Velić, I., Matičec D.; 2005: Evolution of Adriatic Carbonate Platform: paleogeography, main events and depositional dynamics . Paleogeography, Paleoclimatology, Paleoecology, 220/3-4, 333-360, DOI 10.1016/j.palaeo.2005.01.011. Wrigley, R., Marszalek A., Rodriguez, K., Hodgson, N.; 2014: Offshore Croatia – Hunting ‘Big Oil’ in the centre of Europe . First Break, 32, 61-68. LATE QUATERNARY FAULTING IN THE NE MARGIN OF THE SARNO PLAIN (SOUTHERN APENNINES, ITALY) E. Valente 1 , A. Ascione 1 , N. Santangelo 1 , A. Santo 2 1 Dipartimento di Scienze della Terra, dell’Ambiente e delle Risorse, Università degli Studi di Napoli Federico II, Napoli, Italy 2 Dipartimento di Ingegneria Civile, Edile e Ambientale, Università degli Studi di Napoli Federico II, Napoli, Italy Introduction. The Sarno plain is placed along the Tyrrhenian flank of the southern Apennines. The southern Apennines has been affected, since the late Tortonian, by extensional tectonics related to the opening of the Tyrrhenian back-arc basin (Patacca et al. , 1990). This process caused the formation, since the Lower Pleistocene, of large peri-Tyrrhenian grabens and half-grabens filled up by a several thousands of meter thick sequences of marine and continental deposits interbedded with volcanoclastic units (Santangelo et al. , 2017). The Sarno plain is located in the southern part of the large Campana plain peri-Tyrrhenian graben, which includes the volcanic districts of the Phlegrean Fields and the Somma-Vesuvius. The latter volcanic edifice bounds the Sarno plain to the N, whereas the carbonate ridges the Sarno Mts. and Lattari Mts. bound the plain towards NE and SE, respectively. Cinque et al. (1987) point to tectonic subsidence of the Sarno plain of about 30 m in the last 130 ka. Holocene fault activity has been proved for both the Sebeto plain (located N of the