Seismological observations of the northern Dead Sea basin earthquake on 11 February 2004 and its associated activity

Hofstetter, Rami; Gitterman, Yefim; Pinsky, Vladimir; Kraeva, Nadia; Feldman, Lea

doi:10.1560/ijes.57.2.101

Cited by 33 publications

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“…For example, from north to south: the aftershock sequence of the 2004 earthquake in the northern Dead Sea Basin illustrates such activity (Hofstetter et al 2008), the activity in the middle of the northern subbasin, which is related to the Ein-Gedi Fault (Neev & Hall 1979;Lazar et al 2006), and the activity in the middle of the southern subbasin, near the termination of the lake itself (also reported by van Eck & Hofstetter, 1989. For example, from north to south: the aftershock sequence of the 2004 earthquake in the northern Dead Sea Basin illustrates such activity (Hofstetter et al 2008), the activity in the middle of the northern subbasin, which is related to the Ein-Gedi Fault (Neev & Hall 1979;Lazar et al 2006), and the activity in the middle of the southern subbasin, near the termination of the lake itself (also reported by van Eck & Hofstetter, 1989.…”

Section: Seismic Activity In the Dead Sea Basinmentioning

confidence: 74%

“…1) is located at the southwest corner of the southern Dead Sea subbasin, with no clear tectonic feature, and is characterized by velocity values of 4.8-5.0 km s -1 . The earthquakes are distributed throughout the whole basin with some diffused clusters in several distinct areas: (1) northern part of the Dead Sea in the same area of the locations of the 2004 earthquake and its aftershocks (Hofstetter et al 2008), essentially along latitude 45; (2) two distinct areas in the central part of the northern subbasin, just north of the Lisan Peninsula (latitudes 17 and 28); (3) the Lisan Peninsula and west of it (latitude 0) and (4) the southern Dead Sea and especially the southeastern edge of the basin (latitude −25). dolomite) and granitic sequences on the flanks of the basin.…”

Section: R E S U Lt Smentioning

confidence: 99%

“…The M 6.2 earthquake of 1927 July 11, resulted in 285 deaths, 940 wounded and extensive damage in many towns and villages on both sides of the Dead Sea Fault (Ben-Menahem et al 1976;Shapira et al 1992;Avni 1998). Arieh et al 1982;Amiran et al 1994;Salamon 2005;Al-Tarazi et al 2006;Hofstetter et al 2008). 1), causing little or no damage in neighbouring regions (e.g.…”

Section: Introductionmentioning

confidence: 99%

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Crustal structure of the Dead Sea Basin from local earthquake tomography

Hofstetter

Dorbath²,

Calò³

2012

Geophysical Journal International

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International audienceNew findings of the velocity structure of the crust across the Dead Sea Basin are obtained by applying tomography-based method to local earthquakes. We use P-wave traveltime of 614 earthquakes that occurred in the Dead Sea Basin in 1983-2009. At all depths, the Dead Sea Basin is characterized by lower velocities relative to both the eastern and western sides of the basin. There is significant seismic activity at a depth of about 20 km, mainly in the centre and the northern part of the basin. At shallow depths (<15 km) there is more seismic activity on the eastern side of the basin than on the western side, and the northern basin is generally more active than the southern basin. Asymmetry is also observed in the faults that border the Dead Sea Basin. The Arava Fault on the eastern side, with nearly vertical dip faulting, appears to be a clear boundary at all depths down to about 20 km. The depth extension of the Jericho Fault on the western side of the basin is definitely limited to less than 15 km. At greater depths of 20 km or more, the western side is only partially bounded by a fault. The concentration of earthquakes in the central part of the basin at depths larger than 15 km suggests that the Dead Sea Fault at those depths acts as one single fault that is located in, or near, the central axis of the basin. The existence of a number of clusters of earthquakes that spread from shallow depths of a few kilometres up to a depth of about 22 km, points to several defined faults that traverse the Dead Sea Basin. One such example is the aftershock sequence of the 2004 earthquake that occurred in the northern Dead Sea Basin. Seismic activity near Mt Sodom is relatively low and occurs at shallow depths down to 10 km, whereas at larger depths (≥15 km) it ceases. This implies that the whole structure is relatively shallow with no wide and deeper extension. Seismic activity near and within the Lisan Peninsula extends to somewhat larger depths (∼15 km), and then it ceases. The occurrence of earthquakes at large depths suggests that the upper and the lower crust are relatively cool, as was also suggested by earlier studies, pointing to the fact that the heat flow is significantly below the global average value

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Section: Seismic Activity In the Dead Sea Basinmentioning

confidence: 74%

Section: R E S U Lt Smentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Crustal structure of the Dead Sea Basin from local earthquake tomography

Hofstetter

Dorbath²,

Calò³

2012

Geophysical Journal International

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“…(a) Map of the northern DSB including 10 clusters that contain 171 events; the M 5 event is shown by the red “star.” (b) South‐north depth cross section of the relocated clusters along the A′‐A dashed blue line. The focal mechanism of the M 5.2 event of 2004 is presented [ Hofstetter et al ., ], and black line points to the epicenter. The cluster details are presented in Table .…”

Section: Association Of the Clusters With The Mapped Faultsmentioning

confidence: 99%

“…One example is the 5.1 magnitude ( M w ) earthquake of 11 February 2004. This event was followed by a linear cluster at the northern tip of the basin that trends almost perpendicular to the main longitudinal faults [ Hofstetter et al ., ].…”

Section: Introductionmentioning

confidence: 99%

The association of micro‐earthquake clusters with mapped faults in the Dead Sea basin

2014

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About 1100 micro-earthquakes that occurred along the Dead Sea basin during the past 25 years express ongoing seismic activity along mostly obscured fault segments. We apply seismological and statistical methods in order to associate seismic activity with geological and geophysical data and to locate and characterize active fault segments in the basin; three regional 1-D velocity models and the double-difference method were used for the relocation of seismic events. Geostatistical analysis shows that in first order the micro-earthquakes reflect faulting along segments of the main longitudinal fault while seismic quiescence along historically active zones indicates locked segments and stress concentration. Based on waveform similarity, spatial and temporal proximity, we define earthquake clusters that comprise about 30% of the relocated seismicity and two thirds of the total seismic moment. About 80% of the clusters are associated with N-S trending faults. In two cases the clusters indicate a migration of the seismicity in time and space, one of which preceded the largest earthquake in our catalog (M5.2). In addition to the associated longitudinal activity, several clusters appear to represent faulting in east-west orientation which is interpreted here as a secondary fault system.

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Teleseismic traveltimes residuals across the Dead Sea basin

Hofstetter

Dorbath²

2014

JGR Solid Earth

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New findings of the structure of the Dead Sea sedimentary basin and its eastern and western bordering regions are obtained by P and PKP wave relative traveltime residuals of 644 teleseisms, as recorded by the Dead Sea Integrated Research portable seismic network in the Dead Sea basin and its neighboring regions. The Lisan Peninsula is characterized by relatively small teleseismic traveltime residuals of about 0.14 s, in the latitude range of 31.22°-31.37°and at the longitude of 35.50°, slowly decreasing toward the west. The largest teleseismic traveltime residuals are in the southern Dead Sea basin, south of the Lisan Peninsula in the latitude range of 31.05°-31.15°and along longitude 35.45°and continuing southward toward the Amaziahu Fault, reaching values of 0.4-0.5 s. There is a small positive residual at the Amaziahu Fault and a small negative residual south of it probably marking the southern end of the Dead Sea basin. East and west of the Dead Sea basin the mean teleseismic traveltime residuals are negative with overall averages of À0.35 s and À0.45 s, respectively. Using the teleseismic residuals, we estimate the horizontal dimensions of the Lisan salt diapir to be 23 km × 13 km at its widest and a maximal thickness of about 7.2 km. The thickness of the Mount Sodom salt diapir is estimated as 6.2 km.

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Seismological observations of the northern Dead Sea basin earthquake on 11 February 2004 and its associated activity

Cited by 33 publications

References 0 publications

Crustal structure of the Dead Sea Basin from local earthquake tomography

Crustal structure of the Dead Sea Basin from local earthquake tomography

The association of micro‐earthquake clusters with mapped faults in the Dead Sea basin

Teleseismic traveltimes residuals across the Dead Sea basin

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