Discussion

• Earthquake Archeological   
  Earthquake Archeological Effects Chart
  
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  Rodríguez-Pascua et al (2013)
  Effects from Rodríguez-Pascua et al (2013: 221-224)
• Environmental Effects (ESI 2007)
  Graphic Representation of ESI 2007 Intensity
  
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• Synoptic Table of ESI 2007   
  Synoptic Table of ESI 2007 Intensity Degrees
  
  Accuracy improves in higher degrees, especially VIII–XII.
  
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  Michetti et al. (2007)
  Intensity Degrees from Michetti et al. (2007)
• Environmental Effects vs. Intensity
  Diagnostic ranges for environmental effects by intensity
  
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  Michetti et al. (2007)
  from Michetti et al. (2007)

Effect	Location	Image(s)	Description	Intensity
Submarine Debris Flows	Dead Sea Seismic Line A Figure 1 Mapped faults and slump In northern Dead Sea. Location of active faults that deform subbottom strata in north basin of Dead Sea are based on analyses of 3.5 kHz and Sparker high-resolution seismic-reflection data (Neev and Hall, 1976). Seismic-reflection profiles A and B across submarine slump (stippled area) are shown in Figures 2 and 3, respectively. Map also shows International Seismological Summary (ISS) catalogue epicenter of July 11, 1927, Jericho earthquake, although location of epicenter beneath Dead Sea fits seismological data better (Shapira et al., 1993). Contours are in metres below sea level. Niemi and Ben-Avraham (1994)	Line A Figure 2 North-south 3.5 kHz seismic-reflection profile A showing cross-sectional detail of submarine slump and correlation of seismic reflectors (B-E; with major, radiocarbon-dated lowstands of Dead Sea (Frumkin et al., 1991); m bsl is metres below sea level. Arrow indicates headwall scarp of slump. Two seismically triggered slump events are labeled 1 and 2 (see text for description). Niemi and Ben-Avraham (1994)	"The lower reflectors have a different deformation pattern and apparently slumped in an earthquake prior to 1927. Therefore, at least one earthquake occurred after the deposition of the lower sequence and before deposition of the parallel reflectors involved in the 1927 slumping. Four prominent seismic reflectors (B—E, Fig. 2) in the deep-water basin represent, on the basis of limited short cores (Elazari-Volcani, 1943; Neev and Emery, 1967; Garber, 1980; Stiller et al., 1983; Levy, 1984, 1988; Stiller et al., 1988), the top of rock-salt layers (Fig. 2). By using an actualistic model provided by a recent change in Dead Sea sedimentation from marl to halite, we interpret strong seismic reflections as halite deposited during Dead Sea lowstands. We correlate these reflectors to major lowstands of the Dead Sea over the past 5 ka (Frumkin et al., 1991). The two slumping events are interpreted on the profiles (1 and 2 in Fig. 2). The basal glide plane of the upper slump is within a thick seismically transparent interval between reflectors D and E. Evidence of an earlier seismically triggered slump is found in a lower sequence (2 in Fig. 2) that was apparently deformed after the deposition of reflector E and before the deposition of the parallel reflectors A—C involved in the 1927 slump. On the basis of a sediment accumulation rate of 3-5 mm/yr (Stiller et al., 1988) and a correlation of the seismic reflectors with major, radiocarbon-dated lowstands of the Dead Sea (Frumkin et al., 1991), the lower sequence is younger than 3-5 ka. Therefore, at least two earthquakes occurred during an interval of a few thousand years." - Niemi and Ben-Avraham (1994)	IV-VIII+

Estimated Minimum Intensity is VI (6).

• from Niemi and Ben-Avraham (1994)

To study active tectonic processes in the Dead Sea, >1250 km of 3.5 kHz high-resolution seismic-reflection data were collected with a 1 km grid spacing in the north basin. From analyses of the 3.5 kHz and Sparker single-channel seismic-reflection data (Neev and Hall, 1976, 1979), we mapped active faults flanking the margins of the deep north basin of the Dead Sea (Fig. 1). Adjacent to a segment boundary of the main fault, we discovered a large submarine slump characterized by backward rotational blocks covering an area 6.15 by 2.75 km (Fig. 1) and having a basal glide plane at ~10 m depth (Fig. 2). The toe of the slump is not very well developed. The headwall scarp is located in the stable bottomset region of the Jordan River delta on a slope of less than 1° in ~250 m water depth ~5.5 km south of the mouth of the river (Fig. 1).

Given the Dead Sea sediment characteristics and that gravity-induced sliding on slopes of less than 3° occurs only where silt and clay are overpressured and underconsolidated (Crans et al., 1980), we conclude that this large submarine slump was triggered by an earthquake. The Dead Sea bottom sediments consist of chemical precipitates (aragonite, calcite, and gypsum) and detrital mud interbedded with layers of rock salt (Elazari-Volcani, 1943; Neev and Emery, 1967; Garber, 1980; Levy, 1984, 1988) that are continuous across the deep basin (Ben-Avraham et al., 1993). Geotechnical measurements on short cores from the Jordan River delta show that the sediments are consolidated and have a high effective angle of internal friction (Almagor, 1990). The predominance of chemical precipitates also leads to a low sediment porosity (Stiller et al., 1983). These characteristics show that Dead Sea sediments are extremely stable in the bottomset slopes of the Jordan River delta and that slump was produced by ground shaking caused by a large earthquake.