Archaeoseismology and Palaeoseismology in the Alpine ... - Tierra

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For these reasons, the added value provided by the EEE catalogue is evident. Therefore it will be very helpful, not only for scientific purposes but also for a correct definition of most vulnerable areas and consequent measures to be adopted for the mitigation of seismic risk. Acknowledgments: Sincere thanks are due to the Organizing Committee of the International Workshop on Earthquake Archaeology and Palaeoseismology for their technical support. References Blumetti, A.M., Esposito, E., Ferreli, L., Michetti, A.M., Porfido, S., Serva, L., Vittori, E., 2002. New data and reinterpretation of the November 23, 1980, M 6.9, Irpinia‐Lucania earthquake (Southern Apennine) coseismic surface effects. International Workshop ‘‘Largescale vertical movements and related gravitational processes’’. Studi Geologici Camerti 2002, 19–27. Esposito, E., Luongo, G., Marturano, A., Porfido, S., 1987. Il terremoto di S.Anna del 26 Luglio1805. Memorie della Societa` Geologica Italiana,vol. 37, 171‐191, Roma. Esposito, E., Gargiulo, A., Iaccarino, G., Porfido, S., 1998. Distribuzione dei fenomeni franosi riattivati dai terremoti dell’Appennino meridionale.Censimento delle frane del terremoto del 1980. Proceedings of the International Convention on Prevention of Hydrogeological Hazards. C.N.R‐ IRPI , vol. I, 409‐429,Torino. Esposito, E., Pece, R., Porfido, S., and Tranfaglia, G.: Ground effects and hydrological changes in the Southern Apennines (Italy) in response to the 23 July 1930 earthquake (MS=6.7), Nat. Hazards Earth Syst. Sci., 9, 539‐550. Guerrieri L., Tatevossian R., Vittori E., Comerci V., Esposito E., Michetti A.M., Porfido S. and Serva L. (2007). Earthquake environmental effects (EEE) and intensity assessment: the INQUA scale project. Boll. Soc. Geol. It. (Ital. J. Geosci.), Vol. 126, No. 2, 375‐386, Roma. Keefer, D. K.,(1984). Landslides caused by earthquakes. Bull. Geol. Soc. of America, 95,406‐421. 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., Mc Calpin J., Mohammadioun B., Morner N.A., Ota Y. & Roghozin E. (2007). Intensity Scale ESI 2007. In. Guerrieri L. & Vittori E. (Eds.): Memorie Descrittive 1 st INQUA‐IGCP‐567 International Workshop on Earthquake Archaeology and Palaeoseismology 42 Carta Geologica. d’Italia., vol. 74, Servizio Geologico d’Italia – Dipartimento Difesa del Suolo, APAT, Roma, 53 pp. Oddone, E. (1932). Studio sul terremoto avvenuto il 23 luglio 1930 nell’Irpinia. Relazione a S. E. il Ministro dell’Agricoltura e Foresta. La meteorologia pratica 13, 16–26, (77–84, 116–125, 171–176). 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.), Vol. 126, No. 2, 333‐346, Roma. Porfido, S., Esposito, E., Michetti, A.M.,Blumetti,A.M.,Vittori, E.,Tranfaglia, G., Guerrieri, L., Ferreli, L., Serva, L.( 2000).. The geological evidence for earthquakes induced effects in the Southern pennines (Italy). Surveys in Geophysics 23, 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.), Vol. 126, No. 2, 333‐346, Roma. Reicherter, K., Michetti. A., P.G. Silva (eds.). (2009). Palaeoseismology: Historical and Prehistorical Records of Earthquake Ground Effects for Seismic Hazard Assessment. Geological Society of London, Special Publications, 316. London, U.K. Serva, L., (1985a) The earthquake of June 5, 1688 in Campania. In:Postpischl, D. (Ed.), Atlas of Isoseismal Maps of Italian Earthquakes,vol. 114(2A). CNR‐PFGRoma, pp. 44–45. Serva, L., (1985b). The earthquake of September 8, 1694 in Campania‐Lucania. In: Postpischl, D. (Ed.), Atlas of Isoseismal Maps of Italian Earthquakes, vol. 114(2A). CNR‐PFG, Roma, pp. 50–51. Serva L., Esposito E., Guerrieri L., Porfido S., Vittori E. & Comerci V. (2007). Environmental Effects from some historical earthquakes in Southern Apennines (Italy) and macroseismic intensity asseessment. Contribution to INQUA EEE scale project. Quaternary International, Volumes 173‐174, pp. 30‐44 Silva, P. G., Rodríguez Pascua, M. A., Pérez‐López, R., Bardaji, T., Lario, J., Alfaro, P., Martínez‐Díaz, J.J., Reicherter, K., Giménez García, J., Giner, J., Azañón, J.M., Goy, J.L., Zazo C. (2008). Catalogacion de los efectos geologicos y ambientales de los terremotos en Espana en la Escala ESI 2007 y su aplicacion a los estudions paleosismologicos. Geotemas, 6, 1063‐1066.
1 st INQUA‐IGCP‐567 International Workshop on Earthquake Archaeology and Palaeoseismology THE RÍO GRÍO DEPRESSION (IBERIAN RANGE, NE SPAIN). NEOTECTONIC GRABEN VS. FLUVIAL VALLEY F. Gutiérrez (1), P. Lucha (1) and L. Jordá (2) (1) Dpto. Ciencias de la Tierra, Univ. de Zaragoza, C/. Pedro Cerbuna 12, 50009 Zaragoza, SPAIN. fgutier@unizar.es (2) Calle de La Cañada 5, Portal A, 2º Izq, 28720 Bustarviejo, Madrid, SPAIN. Abstract: This contribution presents a geomorphological map of the Río Grío depression, located in the central sector of the Iberian Range, NE Spain. In previous geological maps this depression, ca. 30 km long, has been interpreted as an erosional fluvial valley. Geomorphological mapping reveals that it corresponds to a neotectonic graben filled by alluvial fan deposits and subsequently dissected by the axial Grío River and its tributaries. The length of the normal faults indicates that some of the mapped neotectonic structures have the potential to generate earthquakes with moment magnitudes as high as 6.8. This work suggests that there may be a limited knowledge on the distribution recent faults in some sectors of Spain and that a higher input on the geomorphology and Quaternary geology in the geological maps would help to overcome this weakness. Key words: neotectonic graben, fluvial incision, geomorphological mapping, seismic hazard. INTRODUCTION The Iberian Range, with a prevalent NW‐SE structural trend, is located in the NE of the Iberian Peninsula. This intraplate orogene results from the tectonic inversion of Mesozoic basins occurred from late Cretaceous to Early‐ Middle Miocene times (orogenic stage). During the postorogenic stage extensional tectonics generated grabens superimposed on the previous contractional structures. Although an extensional stress field has prevailed in the central sector of the Iberian Range from the Middle Miocene up to the present‐day, two main phases of graben development can be differentiated (Capote et al., 2002; Gutiérrez et al., 2008). The first extensional phase produced the Calatayud and Teruel Grabens, both around 100 km long and filled with Mio‐ Pliocene terrestrial sediments. The second extensional phase started in the Late Pliocene and generated new tectonic depressions like the Daroca Half‐graben and the Jiloca Polje‐graben (Fig. 1). Recently, new Plio‐Quaternary grabens have been discovered through the elaboration of geomorphological maps, like the Munébrega Half‐graben, which is superimposed on the SW margin of the Calatayud Neogene Graben (Gutiérrez, 1996). Three faulting events younger than 72 ka have been inferred from a trench dug across the master fault of this fault‐angle depression (Gutiérrez et al., 2009). In this work we interpret for the first time the Río Grío valley, located to the NE of the Calatayud Neogene Graben, as a dissected neotectonic graben (Fig. 1). GEOLOGICAL SETTING The NW‐SE‐trending Río Grío morphostructural depression is located within the so‐called Calatayud‐ Montalbán Massif, one of the main Paleozoic outcrops of the Iberian Range. The massif is primarily composed of strongly indurated sandstones and argillites of Precambrian and Paleozoic age. These formations are divided into two main structural units bounded by a major Variscan thrust known as the Datos Thrust (Álvaro, 1991). 43 This structure runs along the Río Grío depression (Gozalo and Liñán, 1988) and is largely concealed by the graben fill alluvium (Fig. 1). In the studied area the SW‐dipping Datos Thrust shows a linear trace indicating a high angle (Álvaro, 1991), probably caused by subsequent Variscan and/or Alpine folding. The hanging wall of the Datos Thrust, designated as the Badules Unit, is composed of Precambrian, Cambrian and Ordovician formations. The footwall is named the Herrera Unit and in the mapped sector the outcropping rocks include Ordovician and Silurian formations. The structure of the Precambrian and Paleozoic rocks is dominated by NW‐SE‐trending and NE‐ verging folds and reverse faults. The Badules Unit is affected by the NW‐SE trending and SW dipping Jarque Thrust. North of La Aldehuela, this thrust, called Inogés Fault by Aragonés et al. (1980), is situated along the foot of the Vicort Range front at the southwestern edge of the Río Grío structural depression (Fig. 1). In the northern sector of the Río Grío structural depression the Paleozoic rocks of the Herrera Unit are overlain unconformably by two outcrops of Mesozoic and Paleogene formations affected by Alpine compressional structures (Fig. 1). The Paleogene sediments correspond to folded alluvial fan conglomerates. Locally, subjacent dissolution of the gypsum‐bearing Keuper facies, Late Triassic in age, has produced recent deformational structures of gravitational origin with a restricted spatial distribution (Fig. 1). DESCRIPTION OF THE RÍO GRÍO GRABEN The 27 km long and NW‐SE trending Río Grío Graben is flanked by prominent ranges made up of resistant Paleozoic rocks, the Vicort‐Modorra Range to the SW and the Algairén Range to the NE. The Vicort‐Modorra Range constitutes an uplifted horst that separates the Calatayud Graben and the Río Grío Graben. The Río Grío morphostrutural depression is filled with alluvial fan deposits that have been deeply dissected by the longitudinal Grío River and its tributaries.
Page 1: Abstracts Volume Archaeoseismology
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Page 13 and 14: DISCUSSION Based on detailed field
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Page 31 and 32: Nevertheless the lack of research,
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Page 57 and 58: RISK ANALYSIS The created hazard ma
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1 st INQUA‐IGCP‐567 Internation
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Fig. 8: Seismic ground shaking may
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elevant qualitative criteria are po
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CONCLUDING REMARKS The exposed exam
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produced by significantly different
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It is possible that a portion of th
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In addition, the Database of histor
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were published by IGME (1983) and E
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The city collapsed and it was aband
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Fig. 4: Slipped lintel in a window
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to overcome shear resistance and in
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Newmark, N.M. (1965). Effects of ea
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associated with various tsunamis (<
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this method, the magnitude of the e
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etween pieces. Fragments have not f
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on the exact date of the earthquake
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THE ARCHAEOLOGICAL ZONE COLOGNE Aft
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affecting the Alcázar was about 50
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archaeoseismology could instead bec
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In the area later occupied by Vilni
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Fig. 2: Assemblage of landforms ass
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Fig. 8: Data and regression for mag
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Fig. 3: Relationships among magnitu
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CONCLUSIONS 1. Spatial distribution
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The stratigraphic sequence (Fig. 4)
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especially in the zones of hanging
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interpretations are based on relati
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Fig. 5: Gray‐scale value laser im
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(~40 cm), F‐ rotated building str
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Index 1 st INQUA‐IGCP‐567 Inter
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