Figure 2Morphotectonic map of the studied area (coordinates are in Israeli TM grid). The map is based mainly on areal photos (dated 1945), interpretation, and complementary field work. Mapped are all lineaments, landslides, fluvial systems (with sites of channel displacement marked by open black circle) and alluvial fans located within the study area. Also shown are the sites of the paleoseismic trenches and the highest shore line of the Sea of Galilee, 170 m below sea level, achieved at 25 ka (Hazan et al., 2005).
JW: Ein Gev landslides are shaded purple
Katz et al (2009)
Katz et al (2009) found evidence for five to seven MW > 6 earthquakes from paleoseismic trenching and an analysis of paleo landslides around the Sea of Galilee. They dated five of these events to 45, 40, 35, 10, and 5 ka BP using the optically stimulated luminescence (OSL) method. They detected what may be a landslide evidence for an event younger than 5 ka BP which they suggested might have been caused by one of the mid 8th century CE earthquakes.
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Map showing Ein Gev landslides at large scale
from Katz et al (2009)
Figure 2
Morphotectonic map of the studied area (coordinates are in Israeli TM grid). The map is based mainly on areal photos (dated 1945), interpretation, and complementary field work. Mapped are all lineaments, landslides, fluvial systems (with sites of channel displacement marked by open black circle) and alluvial fans located within the study area. Also shown are the sites of the paleoseismic trenches and the highest shore line of the Sea of Galilee, 170 m below sea level, achieved at 25 ka (Hazan et al., 2005).
JW: Ein Gev landslides are shaded purple
Katz et al (2009) -
Two dimensional section of the Ein Gev landslides from
Katz et al (2009)
Figure 9
Geometrical comparison of the northern landslide and the slope to its south. (a) Geological cross section of the slope south of the northern landslide
- Me —Ein-Gev Fm.
- Mh—Hordos Fm.
- Pβc —Cover Basalt Fm.
- Al— alluvium
The [blue] dotted line is a reconstruction of the sliding plane according to:
- point 1 is the slide base where the sliding plane daylights, points 2 and 3 are the landslide scar base and top, respectively.
- Geological cross section of the northern landslide (the bedrock is not exposed on the slope below the Pβc and therefore the mapped unit is LS: landslide material and colluvium).
- Geometrical comparison of the northern landslide (black line) and the slope to its south (gray line), showing the area of material depletion (landslide source) and area of material excess (landslide toe). Overlap is based on the contact of Mh and Pβc and the local slope profile at this contact.
Katz et al (2009)
The northern Ein Gev landslide exhibited a multi-phase sliding history where the youngest slide was dated to ca. 5 ka BP.
However, because the youngest slide had a fresh face with no colluviation
Figure 3Surface rupture and the scarp of the youngest fault studied
- Surface rupture of a colluvium unit. This site was later used for paleoseismic trenching (trench TEG-0 in Fig. 2).
- Surface rupture of bedrock (Eocene Maresha Fm.), about 100 m north of (a).
- Close-up of one of the scarps that appear in (b).
Katz et al (2009)
might be related toone of the mid 8th century CE earthquakes.