Surface faulting caused by the Kalamata (Greece) earthquakes (13.9.86)

Μαριολάκος, Ι.; Fountoulis, I.; Λόγος, Ε.; Lozios, Stylianos

doi:10.1016/0040-1951(89)90257-6

Cited by 11 publications

(12 citation statements)

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Section: The Dimiova-perivolakia Grabenmentioning

confidence: 99%

“…The study of the structural and geomorphological elements of this graben has proved that the endogenetic processes related to its creation and its evolution until present are very complex from both kinematic and dynamic viewpoints [Mariolakos et al , 1987[Mariolakos et al , 1989. Mariolakos et al [1989] interpreted the kinematic regime of this macrostructure based on the integration of data derived from the study of active marginal faults, the structural contour map of the basement of the Pindos nappe and the geomorphological elements such as the planation surfaces and the river incision. They suggest that the graben is the result of rotational movements which took place around a N-S striking principal axis located at the area of Arachova and secondarily around an E-W striking axis located parallel to the Kato Karveli-Venitsa and Xerilas fault zones (Figure 2b), so that the western part of the graben is relatively the most subsiding area.…”

Section: The Dimiova-perivolakia Grabenmentioning

confidence: 99%

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Application of the Environmental Seismic Intensity scale (ESI 2007) and the European Macroseismic Scale (EMS-98) to the Kalamata (SW Peloponnese, Greece) earthquake (Ms=6.2, September 13, 1986) and correlation with neotectonic structures and active faults

Fountoulis

Mavroulis

2014

Annals of Geophysics

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On September 13, 1986, a shallow earthquake (Ms=6.2) struck the city of Kalamata and the surrounding areas (SW Peloponnese, Greece) resulting in 20 fatalities, over 300 injuries, extensive structural damage and many earthquake environmental effects (EEE). The main shock was followed by several aftershocks, the strongest of which occurred two days later (Ms=5.4). The EEE induced by the 1986 Kalamata earthquake sequence include ground subsidence, seismic faults, seismic fractures, rockfalls and hydrological anomalies. The maximum ESI 2007 intensity for the main shock has been evaluated as IXESI 2007, strongly related to the active fault zones and the reactivated faults observed in the area as well as to the intense morphology of the activated Dimiova-Perivolakia graben, which is a 2nd order neotectonic structure located in the SE margin of the Kalamata-Kyparissia mega-graben and bounded by active fault zones. The major structural damage of the main shock was selective and limited to villages founded on the activated Dimiova-Perivolakia graben (IXEMS-98) and to the Kalamata city (IXEMS-98) and its eastern suburbs (IXEMS-98) located at the crossing of the prolongation of two major active fault zones of the affected area. On the contrary, damage of this size was not observed in the surrounding neotectonic structures, which were not activated during this earthquake sequence. It is concluded that both intensity scales fit in with the neotectonic regime of the area. The ESI 2007 scale complemented the EMS-98 seismic intensities and provided a completed picture of the strength and the effects of the September 13, 1986, Kalamata earthquake on the natural and the manmade environment. Moreover, it contributed to a better picture of the earthquake scenario and represents a useful and reliable tool for seismic hazard assessment.

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Section: The Dimiova-perivolakia Grabenmentioning

confidence: 99%

Section: The Dimiova-perivolakia Grabenmentioning

confidence: 99%

Application of the Environmental Seismic Intensity scale (ESI 2007) and the European Macroseismic Scale (EMS-98) to the Kalamata (SW Peloponnese, Greece) earthquake (Ms=6.2, September 13, 1986) and correlation with neotectonic structures and active faults

Fountoulis

Mavroulis

2014

Annals of Geophysics

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“…The Messinian plain and the Messinian Gulf correspond to a tectonic graben formed in Mesozoic rocks, the Messinian graben, filled mainly with marine Pliocene and Quaternary sediments (Keraudren 1979, Koutsouveli 1987. To the east, this graben is bounded by the West Mani Fault Zone (WMFZ; Mariolakos and Papanikolaou 1981/82), a NNW trending normal fault zone which corresponds to the range-front fault of the at least partly east-tilted Mesozoic massif of Taygetos Mt., up to 2400 m high (Mariolakos et al 1989, Doutsos et al 2000. The WMFZ consists of various segments with somewhat variable characteristics, is marked by large escarpments and impressive alluvial fans (Lyon-Caen et al 1988) and seems to be responsible for a vertical o¤set of more than 3 km in 5-6 myr between the relief of the Taygetos Mt and the top of the Alpine basement in the Messinian Gulf (Papanikolaou et al 1988).…”

Section: Geologic Settingmentioning

confidence: 99%

Modelling of the 1986 Kalamata (SW Greece) earthquake faulting using geodetic data

Stiros¹,

Kontogianni²

2008

Journal of Applied Geodesy

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Elastic dislocation modelling of high accuracy repeated levelling data, constrained by seismological and structural data, permits a refinement of the seismic fault model of the 1986, Kalamata (SW Greece mainland), M S ¼ 5.8 destructive earthquake. The authors' preferred solution is a blind normal fault, selected on the basis of minimum misfits between observed and predicted elevation changes. This fault pattern is broadly consistent with seismological and geologic evidence.

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“…(1985); Ko00: Koral (2000); Ko01: Koukouvelas et al . (2001); Ma89: Mariolakos et al . (1989); Me02: Meyer et al .…”

Section: Seismic Cataloguesmentioning

confidence: 99%

Magnitude distribution of linear morphogenic earthquakes in the Mediterranean region: insights from palaeoseismological and historical data

Caputo

Mucciarelli

Pavlides

2008

Geophysical Journal International

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We analyse the earthquake magnitude distribution of ‘linear morphogenic earthquakes’ that reactivated dip‐slip normal faults within the Mediterranean region. Information on past events is obtained following two distinct methodological approaches: the geological one (morphotectonic investigations and palaeoseismological excavations) and the historical one (contemporaneous descriptions and surveys of coseismic ruptures). In order to homogenize the different data sets, and, therefore, enabling a comparison, we calculate moment magnitudes (Mw) starting from seismic moments (M0) estimates. The cumulative distributions thus obtained for the two data sets show differences that a series of non‐parametric tests suggests to be statistically significant. Coseismic displacements are systematically overestimated for strong (Mw > 6.5) historically based earthquakes and for moderate (5.0–6.0) palaeoseismologically observed events. Also concerning the rupture length, the geological information generally provides larger values for moderate earthquakes. The possible causes of this discrepancy and the consequences in using the two data sets for seismic hazard assessment analyses are also discussed.

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Surface faulting caused by the Kalamata (Greece) earthquakes (13.9.86)

Cited by 11 publications

References 1 publication

Application of the Environmental Seismic Intensity scale (ESI 2007) and the European Macroseismic Scale (EMS-98) to the Kalamata (SW Peloponnese, Greece) earthquake (Ms=6.2, September 13, 1986) and correlation with neotectonic structures and active faults

Application of the Environmental Seismic Intensity scale (ESI 2007) and the European Macroseismic Scale (EMS-98) to the Kalamata (SW Peloponnese, Greece) earthquake (Ms=6.2, September 13, 1986) and correlation with neotectonic structures and active faults

Modelling of the 1986 Kalamata (SW Greece) earthquake faulting using geodetic data

Magnitude distribution of linear morphogenic earthquakes in the Mediterranean region: insights from palaeoseismological and historical data

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