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Please use this identifier to cite or link to this item: http://hdl.handle.net/2122/4094
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dc.contributor.authorallPantosti, D.; Istituto Nazionale di Geofisica e Vulcanologia, Sezione Roma1, Roma, Italiaen
dc.contributor.authorallDe Martini, P. M.; Istituto Nazionale di Geofisica e Vulcanologia, Sezione Roma1, Roma, Italiaen
dc.contributor.authorallPapanastassiou, D.; National Observatory Athens, Institute of Geodynamics, P.O. Box 20048, Gr-11810, Greeceen
dc.contributor.authorallPalyvos, N.; University of Athens, Department of Geology, Panepistimiopolis Zografou, 157 84 Athens, Greeceen
dc.contributor.authorallLemeille, F.; Institut de Protection et de Sûreté Nucléaire, F-92265 Fontenay-aux-Roses Cedex, Franceen
dc.contributor.authorallStavrakakis, G.; National Observatory Athens, Institute of Geodynamics, P.O. Box 20048, Gr-11810, Greeceen
dc.date.accessioned2008-10-01T13:32:49Zen
dc.date.available2008-10-01T13:32:49Zen
dc.date.issued2001-08en
dc.identifier.urihttp://hdl.handle.net/2122/4094en
dc.description.abstractThis article presents the results of new field and aerial photo surveys of the Atalanti fault and of the mesoseismal area of the 20 and 27 April 1894 earthquakes. Coupled with a reanalysis of contemporary reports and previous investigations, these are used to gain a better understanding of the faults responsible for these events and their seismic behavior. The first shock was smaller and probably located inshore or offshore the Malessina peninsula. No resolving field evidence has been found to locate the seismogenic structure responsible for this shock. On the basis of the limited information available, we suggest the Malessina escarpment, a 12-km-long, ENE-trending, NW-dipping fault as a possible structure responsible for this event. On the other hand, the second and largest shock is definitely related to the Atalanti fault sensu stricto, a main WNW-trending, N-dipping active fault extending between the Platirema valley (a few km NW of the town of Atalanti) and Larymna. The total length of the rupture recognized in the field is about 32 km, but it can be extended further SE up to 40 km. No evidence for a longer rupture extending some other 20 km to the NW, between the Karagiozis river and Ag. Kostantinos, is found. The complex geometry of the fault with bends and step overs appears to be controlled by preexisting transverse structures. Minimum coseismic vertical throws, measured in the field after more than a century elapsed from the earthquake, are 30–80 cm, thus consistent with contemporary reports indicating 1-m average. Slip rates are not well constrained. The available estimates fall in the range 0.1–0.5 mm/yr confirming the smaller amount of crustal extension taking place in this area with respect to other nearby regions such as the Corinth gulf. No new data are available to define the average recurrence interval typical of the Atalanti fault. However, a reconsideration of the existing information induced us to rule out the possibility that the famous 426 B.C. earthquake occurred on the Atalanti fault. On the basis of the extent and size of the rupture recognized in the field, a M 6.8 is estimated for the second and largest shock.en
dc.language.isoEnglishen
dc.publisher.nameSeismological Society of Americaen
dc.relation.ispartofBulletin of the Seismological Society of Americaen
dc.relation.ispartofseries4 / 91 (2001)en
dc.subjectSurface ruptureen
dc.subject1894 Atalanti Earthquakeen
dc.subjectGreeceen
dc.titleA Reappraisal of the 1894 Atalanti Earthquake Surface Ruptures, Central Greeceen
dc.typearticleen
dc.description.statusPublisheden
dc.type.QualityControlPeer-revieweden
dc.description.pagenumber760-780en
dc.subject.INGV04. Solid Earth::04.04. Geology::04.04.01. Earthquake geology and paleoseismologyen
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dc.description.obiettivoSpecifico3.2. Tettonica attivaen
dc.description.journalTypeJCR Journalen
dc.description.fulltextreserveden
dc.contributor.authorPantosti, D.en
dc.contributor.authorDe Martini, P. M.en
dc.contributor.authorPapanastassiou, D.en
dc.contributor.authorPalyvos, N.en
dc.contributor.authorLemeille, F.en
dc.contributor.authorStavrakakis, G.en
dc.contributor.departmentIstituto Nazionale di Geofisica e Vulcanologia, Sezione Roma1, Roma, Italiaen
dc.contributor.departmentIstituto Nazionale di Geofisica e Vulcanologia, Sezione Roma1, Roma, Italiaen
dc.contributor.departmentUniversity of Athens, Department of Geology, Panepistimiopolis Zografou, 157 84 Athens, Greeceen
dc.contributor.departmentInstitut de Protection et de Sûreté Nucléaire, F-92265 Fontenay-aux-Roses Cedex, Franceen
dc.contributor.departmentNational Observatory Athens, Institute of Geodynamics, P.O. Box 20048, Gr-11810, Greeceen
item.openairetypearticle-
item.cerifentitytypePublications-
item.languageiso639-1en-
item.grantfulltextrestricted-
item.openairecristypehttp://purl.org/coar/resource_type/c_18cf-
item.fulltextWith Fulltext-
crisitem.author.deptIstituto Nazionale di Geofisica e Vulcanologia (INGV), Sezione Roma1, Roma, Italia-
crisitem.author.deptIstituto Nazionale di Geofisica e Vulcanologia (INGV), Sezione Roma1, Roma, Italia-
crisitem.author.deptIstituto Nazionale di Geofisica e Vulcanologia (INGV), Sezione Roma1, Roma, Italia-
crisitem.author.deptInstitut de Radioprotection et de Surete Nucléaire, Seismic Hazard Division-
crisitem.author.deptNational Observatory of Athens, Institute of Geodynamics, Athens, Greece-
crisitem.author.orcid0000-0001-7308-9104-
crisitem.author.orcid0000-0002-3598-5191-
crisitem.author.parentorgIstituto Nazionale di Geofisica e Vulcanologia-
crisitem.author.parentorgIstituto Nazionale di Geofisica e Vulcanologia-
crisitem.author.parentorgIstituto Nazionale di Geofisica e Vulcanologia-
crisitem.classification.parent04. Solid Earth-
crisitem.department.parentorgIstituto Nazionale di Geofisica e Vulcanologia-
crisitem.department.parentorgIstituto Nazionale di Geofisica e Vulcanologia-
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