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Fault Maps - Israel

Interactive Active Fault Map of Israel - GSI (opens a new window)

**Active Faults around the Sea of Galilee (SOG)**
Description	Image	Source
Figure 1b Structural framework of the Tiberias area Quaternary faults in the central part of the DSF, modified after Sneh and Weinberger (2014), Sagy et al. (2016), Hamiel et al. (2016) and Sharon et al. (2018, 2020); the red rectangle is the area enlarged in 1c. JVWB Jordan Valley Western Boundary Fault JVF: Jordan Valley Fault CG: Carmel-Gilboa Fault Ferrario et al (2020)	Faults in Jordan River Valley and SOG	Fig 1b - Ferrario et al (2020)
Figure 1c Structural framework of the Tiberias area Simplified geologic map (after Bogoch & Sneh, 2008; Sneh, 2008), epicenters of M_w > 3.0 events since 1980 (data from Geophysical Institute of Israel) and focal mechanism of the 2018 M_w 4.5 event after Wetzler et al (2019) Ferrario et al (2020)	Faults around SOG	Fig 1c - Ferrario et al (2020)
Figure 1B Main faults and shaded relief of the Dead Sea–Sea of Galilee (Kinneret) area (after Hall, 1994; Ben-Avraham et al., 1996). Hazan et al (2004)	Faults around SOG	Fig 1b - Hazan et al (2004)
Figure 1 a) Plate tectonic settings of the Middle East, with major faults. EAFS – East Anatolia Fault DST – Dead Sea Transform J – Jerusalem K – Kerak P – Petra B – Beteiha trench site b) Location of major and minor faults of the DST in the vicinity of Hula basin and the Sea of Galilee. The latest earthquake known to have ruptured is mentioned below each fault name. JGF, Jordan Gorge fault JVF, Jordan Valley fault RaF, Rachaya fault RoF, Roum fault SF, Serghaya fault YF, Yammouneh fault c) Map of the Beteiha paleoseismic site with outlines of all trenches dug during the 3-year campaign, and the approximate location (based on air photos) of the trenches of Marco et al. (2005). The trenches discussed in this paper are highlighted and labeled.Topography model was obtained using TLS (Terrestrial Laser Scanner) prior to 2nd year trenching, courtesy of O. Katz from the Geological Survey of Israel. The contour lines represent elevation b.m.s.l. Wechsler et al (2018)	Faults N of SOG	Fig. 1 - Wechsler et al (2018)
Figure 6 Neotectonic map of the Sea of Galilee compiled using available geophysical data; all faults (thick red lines) have a sinistral strike-slip component; main epicentres of the July 2018 earthquake sequence (> M_w 3.5) are indicated by blue circles, with yellow pattern boundings the 250–300 events isoline. Inset: orientation and relative motion of observed strain patterns in our study area in comparison with a reference strain ellipse. CCA 4.0. Gasperini et al (2020)	Neotectonic map of SOG	Fig. 6 - Gasperini et al (2020)
Figure 9 Tectonic map of the Sea of Galilee area including regional tectonic lineaments from previous studies Whiticar (1999) "Carbon and hydrogen isotope systematics of bacterial formation and oxidation of methane.", Ben-Avraham and Hall (1977) "Geophysical survey of Mount Carmel structure and its extension into the eastern Mediterranean.", and Nur and Ben-Avraham (1978) "The Eastern Mediterranean and the levant: tectonics of continental collision." and those derived from this work. Coloured circles represent intensity distribution of the AD 1837 earthquake according to Ambraseys (1997) "The earthquake of 1 January 1837 in southern Lebanon and northern Israel." (see legend for MSK intensities). We note that maximum intensities (yellow circles) align with structures located to the west of the SoG. Data available to date could not allow us to determine whether a connection between CT (Capharnaum Though) and RF (Roum Fault) could eventually exist. Satellite image is from Google Earth; Map data: Google, Data SIO, NOAA, U.S: Navy, NGA, GEBCO, Image Landsat/Copernicus). CCA 4.0. Gasperini et al (2020)	Tectonic map of SOG	Fig. 2 - Gasperini et al (2020)
Figure 2 Different tectonic models proposed by various authors for the Sea of Galilee . CCA 4.0. Gasperini et al (2020)	Tectonic models for SOG	Fig. 2 - Gasperini et al (2020)
Fig. 31.1 Location of faults near Megiddo and recent earthquake epicentres in the vicinity of the Carmel Fault. Y Yoqne'am M Meggido T Ta'anach Earthquake data from the Geophysical Institute of Israel (www.gii.co.il) Marco et al (2006)	Carmel & Gilboa Faults	Fig. 31.1 - Marco et al (2006)

**Dead Sea**
Description	Image	Source
Figure 1 Mapped faults and salt bodies, DSB (after Neev and Hall (1979), ten Brink and Ben-Avraham (1989), and Ben-Avraham et al. (1993)). Wetzler et al (2012)	Dead Sea	Fig 1 - Wetzler et al (2012)
Figure 1 Map of the 11/2/2004 earthquake sequence and the associated events during the time period 1/1/2003-30/9/2004 (GII catalog), superimposed on the geological map (Sneh et al., 1998). Note that most of the activity is concentrated along the northeastern margins of the Dead Sea. EMSC and USGS main shock epicenter locations are also shown. Potentially Active Faults (PAF) relate only to the western side of the Dead Sea while the eastern side has not been yet mapped. Salamon (2004)	PAF - W side of Dead Sea	Fig 1 - Salamon (2004)
Figure 17.4a Location map showing the location of the En Geddi, Lisan and Sedom diapirs. Faults are marked as heavy lines (dashed where inferred) (after Ben-Avraham, 1997). Seismic profiles are indicated by thin dotted lines. Ben-Avraham et al (2012)	Tectonic Map Dead Sea	Fig 17.4a - Ben-Avraham et al (2012)
Fig. 2.6 Map of Dead Sea area showing major faults. The Dead Sea Graben or trough has downdropped between the Western and Eastern Border Faults as much as 10 km since Miocene time. Cross-faults such as the Kerak Graben are sites where enhanced erosion has produced features such as the Wadi Kerak. Rast and Schaub (2003)	Dead Sea Faults	Fig. 2.6 - Rast and Schaub (2003)

**Entire Country**
Description	Image	Source
Figure 7 Quaternary fault map of Israel. Colours indicate the corresponding criterion for each fault. Inferred subsurface faults are marked by dashed lines. Abbreviations are for the main strike-slip segments of the DST. Sharon et al (2020)	Quaternary Fault Map	Fig 7 - Sharon et al (2020)
Map of Active and Potentially Active Faults in Israel Geologic Survey of Israel	Active and Potentially Active Fault Map	Geologic Survey of Israel

References

Ferrario, M. F., et al. (2020). "The mid-8 th century CE surface faulting along the Dead Sea Fault at Tiberias (Sea of Galilee, Israel)." Tectonics 39(9).

Gasperini, L., et al. (2020). "Neotectonics of the Sea of Galilee (northeast Israel): implication for geodynamics and seismicity along the Dead Sea Fault system." Scientific Reports 10(1): 11932.

Marco, S., Agnon, A. , Finkelstein, I., Ussishkin, D. (2006). Megiddo earthquakes. Megiddo IV: The 1998–2002 Seasons. I. e. a. Finkelstein. Tel Aviv, Israel: pp. 568–575.

Rast, W. E., Schaub, R. T. (2003). Bab Edh-Dhra': Excavations at the Town Site - Part 1. United States: Eisenbrauns. - can be borrowed with a free account from archive.org

Salamon, Amos (2004). Seismically induced ground effects of the February 11, 2004, ML=5.2, northeastern Dead Sea earthquake. Jerusalem, Geological Survey of Israel.

Sharon, M., et al. (2020). "Assessment of seismic sources and capable faults through hierarchic tectonic criteria: implications for seismic hazard in the Levant." Natural Hazards and Earth System Sciences 20: 125-148.

Wechsler, N., et al. (2018). "Variable slip-rate and slip-per-event on a plate boundary fault: The Dead Sea fault in northern Israel." Tectonophysics 722.

Wetzler, N., Amir S. and Marco, S.(2012). Analysis of micro‐earthquakes cluster, Dead Sea Basin Jerusalem, Israel, Geologic Survey of Israel.

Fault Maps - Jordan

**Jordan River Valley**
Description	Image	Source
Segmented Faults in Jordan River Valley	Figure 1b Detailed map of the JVF (Jordan Valley Fault) segment between the Sea of Galilee and the Dead Sea. The segment itself is organized as six 15-km to 30-km-long right-stepping sub segments limited by 2 km to 3 km wide transpressive relay zones. The active trace of the JVF (Jordan Valley Fault) continues for a further ~10 km northward into the Sea of Galilee (SG) and ~20 km southward into the northern Dead Sea (DS). Ferry et al (2011)	Fig 1b - Ferry et al (2011)
Segmented Faults in Jordan River Valley	Figure 6 Archaeology of the Jordan Valley. White squares, main populated areas cited in historical documents; white dots, archaeological sites visited and reappraised in this study; gray dots are archaeological sites not studied here (lack of evidence and/or available literature) but of potential interest for future studies; gray squares, paleoseismic sites; black squares, geomorphological sites studied by Ferry et al. (2007). Ferry et al (2011)	Fig 6 - Ferry et al (2011)
Segmented Faults in Jordan River Valley	Fig. 1 a) Location of the Dead Sea fault (black line) in the Jordan Valley between the Sea of Galilee and the Dead Sea. The fault rupture appears to be subdivided into fault sub-segments by prominent pressure ridges at Tell Arba'een, Tell Al-Qarn and Karameh. Inset shows plate tectonics in the eastern Mediterranean with GPS velocities (McClusky et al., 2003). Shaded topography is from 90-m-resolution SRTM3f data. b) Geomorphological map of the Jordan Valley around Karameh. Most prominent units include the badland-type Ghor areas, which contain a dense network of deeply incised streams and that separate the flat top surface of Lisan and Damya units and the flood plain of the present-day Jordan River. The Ghor area exhibits numerous natural outcrops and provides favourable fault mapping conditions. Ferry et al (2007)	Fig 1 - Ferry (2007)
Closeup of Faulting at Ghor Khabed	Fig. 3 Aerial photograph (original scale of 1:20,000) of the area between Ghor Kabed and Wadi Russayf. The conspicuous fault trace displays en-echelon features, pull-apart basins and left- laterally offset drainage systems. See Fig. 1b for location. Ferry et al (2007)	Fig 3 - Ferry (2007)
Seismotectonic Map Jordan Valley	Figure 2 Seismotectonic sketch of the Jordan Valley region - symbols as in Figure 1 (JW:see Araba Valley Table) and satellite view of the Wadi Araba-Jordan Valley Fault (AJF) area (Landsat-Spot combination, from an original 1:150,00 scale image; open arrows indicate the AJF trace). Inset A is a detailed map of the Jacob Ford area. Galli (1999)	Fig 2 - Galli (1999)
Dead Sea Faults	Fig. 2.6 Map of Dead Sea area showing major faults. The Dead Sea Graben or trough has downdropped between the Western and Eastern Border Faults as much as 10 km since Miocene time. Cross-faults such as the Kerak Graben are sites where enhanced erosion has produced features such as the Wadi Kerak. Rast and Schaub (2003)	Fig. 2.6 - Rast and Schaub (2003)

**Araba Valley**
Segmented Faults in Araba Valley	Figure 1 Inset map shows the entire Dead Sea fault, including major relay zones of the Dead Sea basin and the Lebanese bend. Y, LT, JV and Q indicate paleoseismological sites of Yammouneh, Lake Tiberias, Jordan Valley and Qatar, respectively T, K, J, H and SC indicate cities of Tabuk, Al-Karak, Jerusalem,Hula basin and St Catherine monastery, respectively EAFS stands for East Anatolia Fault System The main ﬁgure shows the Wadi Araba fault segments after (Le Beon et al., 2012), with location of the trench site in Yotvata Playa. The site of Tilah is also indicated. Dashed red box indicates Fig. 2. Topography from SRTM3 (pixel size, ~90 m) Klinger et al (2015)	Fig 1 - Klinger et. al. (2015)
Closeup of Yotvata Extension jog	Figure 2 Satellite image of the Qatar trench site (29° 48" 46.4' N 35° 04" 26.3' E) at the Yotvata extensional jog. The push-ups are well visible at the southern tip of the relay zone, deforming the toe of alluvial fans. North of the trench, the fault can be located only from the pressure ridges (Fig. 3) that mark the ﬂat playa deposits, and the offset shoreline. To the southwest the depression is limited by normal faults with minor vertical throw. Background image is submetric pixel size imagery from Digitalglobe (GoogleEarth extract). Klinger et al (2015)	Fig 2 - Klinger et. al. (2015)
Morphotectonic Map Araba Valley	Figure 3a Morphotectonic map and drainage network of the Wadi Araba. Box shows location of Figure 3b. Boxes show location of detailed morphotectonic maps of the large abandoned alluvial fans. Question marks indicate uncertain correlations of alluvial surfaces far from any absolute age constraints. Le Béon et al (2012)	Fig 3a - Le Béon et al (2012)
Morphotectonic Map N Araba Valley	Figure 3b Morphotectonic map of the northern Wadi Araba. See legend on Figure 3a. Boxes show location of detailed morphotectonic maps of the large abandoned alluvial fans. Question marks indicate uncertain correlations of alluvial surfaces far from any absolute age constraints. Le Béon et al (2012)	Fig 3b - Le Béon et al (2012)
Seismotectonic Map Araba Valley	Figure 1 Seismotectonic sketch of the Wadi Araba region. Inset A shows the regional tectonics of the Dead Sea Rift; the black arrow indicate plate direction and velocities of Africa and Arabia relative to Eurasia. Inset B shows the seismicity distribution (Mo) along the Dead Sea Rift from Aqaba Gulf to Lebanon (period 31 B.C. to 1994 A.D.) Galli (1999)	Fig 1 - Galli (1999)
Geologic Map N Araba	Figure 2 Generalized geologic map of Wadi Araba showing juxtaposition of different bedrock lithologies across the valley. The Wadi Araba fault is an active, strike-slip fault of the DST. The study area is located at the intersection of the Wadi Araba fault and the Khunayzira normal fault. Map modified after Bender, 1975. JW: Khunayzira normal fault is also known as the Amatzyahu fault Atallah (2002)	Fig 2 - Atallah (2002)
Geologic Map N Araba tighter scale	Figure 3 Geologic map of the study area constructed from interpretation of 1:10000 scale black and white air photos from 1978 and field mapping. Atallah (2002)	Fig 3 - Atallah (2002)
Dead Sea Transform	Figure 1 The Dead Sea Transform (DST) is the plate boundary fault system that separates the Sinai and Arabian plates (after Garfunkel,1981). G: Ghab fault Y: Yammouneh fault R: Rachaiya fault E: Ed Damor fault CN-S: Central Negev-Sinai shear belt. Atallah (2002)	Fig 1 - Atallah (2002)

**Gulf of Aqaba (GOA)**
Main transform faults GOA	Figure 2 (a)Generalized tectonic settings of the GEA (modified after Ben Avraham [1985]). The main transform fault segments as suggested by Ben Avraham [1985] are marked with thick lines. The bathymetric deeps of the GEA are circled and noted. The GEA contains three transform basins (marked by light blue), of which the Aragonese-Arnona Basin is bound by strike-slip faults as a true pull-apart basin (marked by darker blue). Note that the main transform fault is marked on the eastern side of the asymmetric Elat Basin. The main transform fault north of the Elat Basin is mapped as suggested by Ben Avraham and Tibor [1993] and Ehrhardt et al. [2005]. The Evrona and Timna basins are mapped from gravimetric and magnetic data [ten Brink et al., 1999; Frieslander, 2000; ten Brink et al., 2007]. The red dashed box at the northern GEA outlines the study area. The red star marks the epicenter of the 1995 M_w 7.2 Nuweiba earthquake [Hofstetter et al., 2003]. (b) Schematic models of the deep section of the basins (modified after Ben Avraham [1985] and ten Brink et al.[1999]). The marine basins of the GEA are deeper (3–5 km) than the on-land basins of the southern Arava Valley (LT 1 km). Hartman at al (2014)	Fig 2 - Hartman at al (2014)
Geologic Map N GOA	Figure 3 Geological map of the study area overlaid with the outline of major faults suggested in previous studies(modiied after Garfunkel [1970], Reches et al.[1987], Ben Avraham and Tibor [1993], Frieslander [2000], Niemi andSmith [1999], Slater and Niemi, [2003], Shaked et al. [2004], Ehrhardt et al. [2005], and Makovsky et al. [2008]). AF = Aragonese fault. Hartman at al (2014)	Fig 3 - Hartman at al (2014)
Faults N GOA	Figure 7 Interpreted faults along the northern shelf of the Gulf of Elat/Aqaba. The location of each fault was picked from the seismic profiles, and each fault interpretation is marked by a grey dot. The fault lines were interpolated between these data points and projected onto the bathymetric image of the seaﬂoor. Hartman at al (2014)	Fig 7 - Hartman at al (2014)
Main transform faults GOA	Figure 15 A map of the major faults (black lines) that divide the northern GEA and their estimated slip rates (internal frames), overlaid on the curvature of the seaﬂoor. Faults are marked by solid lines where they were interpreted from the seismic data across the shelf. The continuation of the faults southward is suggested based on their extrapolation from the curvature analysis of the bathymetric data and in similarity to the fault outlines that were previously suggested [Recheset al., 1987; Ben Avraham and Tibor, 1993; Ehrhardt et al., 2005; Tibor et al., 2010]. Their continuation northward is suggested based on their extrapolation from presettlement (1945) aerial photographs. The graphs of average slip rates and tilt rates as a function of the averaging time-span are shown for their relevant faults. Average slip rates are marked by black lines and calculated uncertainty indicated by gray boxes. Hartman at al (2014)	Fig 15 - Hartman at al (2014)
Seismicity & Faults GOA	Figure 2 Historical and seismicity map of Gulf of Aqaba. Salama et al (2021)	Fig 2 - Salama et al (2021)

References

Al-Taj, M. M., et al. (2007). "The Tectonic Geomorphology and the Archeoseismicity of the Dead Sea Transform in Jordan Valley." AGU Fall Meeting Abstracts 41.

Atallah, M., et al. (2002). "Deformation at a strike-slip, stepover zone along the southeastern margin of the Dead Sea pullapart basin, Jordan." Stephan Mueller Special Publication Series 2.

Ferry, M., et al. (2011). "Episodic Behavior of the Jordan Valley Section of the Dead Sea Fault Inferred from a 14-ka-Long Integrated Catalog of Large Earthquakes." Bulletin of the Seismological Society of America 101(1): 39-67.

Ferry, M., et al. (2007). "A 48-kyr-long slip rate history for the Jordan Valley segment of the Dead Sea Fault." Earth and Planetary Science Letters 260(3-4): 394-406.

Klinger, Y., et al. (2015). "5000 yr of paleoseismicity along the southern Dead Sea fault." Geophysical Journal International 202(1): 313-327.

Le Béon, M., et al. (2010). "Early Holocene and Late Pleistocene slip rates of the southern Dead Sea Fault determined from 10Be cosmogenic dating of offset alluvial deposits." Journal of Geophysical Research: Solid Earth 115 (B11)

Le Béon, M., et al. (2012). "Quaternary morphotectonic mapping of the Wadi Araba and implications for the tectonic activity of the southern Dead Sea fault." Tectonics 31(5): TC5003.

Galli, P. (1999). "Active tectonics along the Wadi Araba-Jordan Valley transform fault." Journal of Geophysical Research: Solid Earth 104(B2): 2777-2796.

Hartman, G., et al. (2014). "Quaternary tectonic evolution of the Northern Gulf of Elat/Aqaba along the Dead Sea Transform." Journal of Geophysical Research: Solid Earth 119(12): 9183-9205.

Rast, W. E., Schaub, R. T. (2003). Bab Edh-Dhra': Excavations at the Town Site - Part 1. United States: Eisenbrauns. - can be borrowed with a free account from archive.org

Salama, A., et al. (2021). "Review of Tsunami Hazard Potential for Gulf of Aqaba, Egypt." Journal of the Geological Society of India 97: 1545-1550.

Tectonic and Bathymetric Maps - Gulf of Aqaba

Tectonic setting of entire Gulf of Aqaba

from Matthieu et al. (2021)

Figure 1

(A) Tectonic setting of the sinistral strike-slip Dead Sea Fault (DSF). Seismicity from the ISC earthquake catalogue 1964 - 2015 (http://www.isc.ac.uk). The DSF connects to the North to the East Anatolian Fault System (EAFS) and to the South to the Red Sea ridge (modified from Le Béon et al., (2008)) GA: Gulf of Aqaba, ST: Strait of Tiran.

(B) Multibeam bathymetric map of GA and ST with the main active faults, combining R/V Thuwal (2018), F/S Meteor (1999) and Hall & Ben Avraham (1978) datasets. The main strike-slip faults are in red while normal faults are in black. Fault traces have been simplified for clarity. The grey focal mechanisms corresponding to the successive sub-events for the, M_w 7.3, 1995 earthquake, and location of the seismic swarms in 1983, 1990, 1993 and other focal mechanisms after Klinger et al., (1999). Grey background is Landsat 8 Imagery, courtesy of the U.S. Geological Survey (2018).

ArF: Arnona Fault
AF: Aragonese Fault
DF: Dakar Fault
EF: Eilat Fault
HF: Haql Fault
TF: Tiran Fault

Matthieu et al. (2021)

Bathymetric Maps

from Matthieu et al. (2021)

Figure 2

Bathymetric map of the Gulf of Aqaba combining R/V Thuwal (2018), F/S Meteor (1999) and Hall & Ben Avraham (1978) datasets
Shade bathymetry of the Gulf of Aqaba with an azimuth of 315N and a sun angle of 25°
Slope map of the Gulf of Aqaba from low slope angle (white: 0°) to high slope angle (black: >45°)

All maps are projected in WGS 84 - UTM 36N. On-land grey background from a Landsat-8 image, courtesy of the U.S. Geological Survey.

Matthieu et al. (2021)

Fault Map - North Gulf of Aqaba

from Matthieu et al. (2021)

Figure 3

Zoom-in of the northern part of the Gulf of Aqaba, along the morphological trace of the Haql fault (see location on Figure 2) with location of the cross sections shown in (B). The fault lines are more detailed than in Figure 1. Red lines represent the main strike-slip faults, black lines the main normal faults. Along the Eilat fault, a long-term displaced channel as well as the left-lateral displacement of a small hill confirm the strike-slip character of the Eilat fault.
Cross-sections along the longitudinal shape of the alluvial fans, North of the city of Haql. No vertical offsets are visible on these cross-sections, with the exception of a possible knickpoint along profile D-D’. The continuous convex shape of the fans suggests no recent activity of the Haql fault.
The trace of the Haql fault is buried by fans coming from the coastal plain, with no visible recent perturbations of the fans at this location. Nevertheless, the high relief shows the long-term normal or oblique character of the Haql fault. In few places, the shaded topography suggests that a small part of strike-slip motion is also accommodated along the Haql fault.
At the southern termination of the Haql fault, discontinuous small scarps across the fans suggest that this section of the fault might have been activated recently.

Matthieu et al. (2021)

Fault Map - Central Gulf of Aqaba

from Matthieu et al. (2021)

Figure 4

Detailed fault map of the sinistral strike-slip fault system in the central GA. Direct evidence of surface rupture associated to the main subevent (see Fig. 2) of the 1995 M_w = 7.3 Nuweiba earthquake are found in box B.
Sharp fault morphology suggesting very recent fault activation. Small changes of geometry along the Aragonese fault are responsible for small pull-apart (black squares) and counterslope scarp (white square).
Detail of the fault zone between Aragonese Deep and Arnona Deep resulting from a complexity in the geometry of the Arnona fault. The red line represents the main active strike slip fault.

Matthieu et al. (2021)

Fault Map - South Gulf of Aqaba

from Matthieu et al. (2021)

Figure 5

Southern part of the Gulf of Aqaba (see location on Figure 2). Dakar and Tiran Deeps are located between the sinistral strike-slip Arnona fault (red line) and the normal Dakar fault (bold black lines). The location of the main strike-slip fault is partly masked by diapiric foldings (black arrows) and secondary faulting (thin black and dashed black lines) associated with the destabilization of large salt deposits moving down from the Dahab plateau.
Cross-sections across the Dahab plateau showing the eastward sloping and the topographic drop from the Dahab plateau toward the Dakar and Tiran deeps.

Matthieu et al. (2021)

Fault Map - Strait of Tiran

from Matthieu et al. (2021)

Figure 6

Strait of Tiran (see location on Figure 2).

The sinistral strike-slip Tiran Fault is located between the Woodhouse and Jackson reefs. The sharp bathymetry to the North and to the South of the reef emphasizes the location of the fault. Red lines represent the main strike slip faults, black lines represent the main normal faults.
Slope map of the Strait of Tiran, from low slope angle (white: 0°) to high slope angle (black: >45°).

Matthieu et al. (2021)

Fault Maps - Lebanon

. . .

Description	Image	Source
Major Faults	Figure 1 Regional tectonic setting. Map of the Levant fault system. Active faults of the Lebanese restraining bend. Daeron et al (2007)	Fig 1- Daeron et al (2007)
Tectonic Map of DSF	Figure 1 Regional tectonic map of the Dead Sea fault system. Directions (white arrows) and rates (mm/a) of motion of the Arabian plate relative to the Sinai plate are based on the plate model of Reilinger et al. (2006). Abbreviations: JAA, Jebel Abdel Aziz EFS, Euphrates fault system NAF, North Anatolian fault EAF, East Anatolian fault Inset depicts the plate-tectonic setting of the Arabian–Eurasian collision. Gomez et al (2007)	Fig 1- Gomez et al (2007)
Topography of LRB	Figure 2a Map showing the topography of the Lebanese restraining bend from a 20-metre-pixel, InSAR-derived DEM (Gomez et al. 2006). Gomez et al (2007)	Fig 2a- Gomez et al (2007)
Geology of LRB	Figure 2b Map showing general geology (simplified from Dubertret 1955) and the structure of the restraining bend (simplified from Gomez et al. 2006). Arrows indicate velocities of continuous GPS sites (red circles) in an Arabia-fixed reference frame (Reilinger et al. 2006). GPS velocities depict the net left-lateral shear across the Dead Sea fault system in this area. White line = location of the cross-section in Figure 3. Abbreviations YF Yammouneh Fault SF Serghaya Fault RF Roum Fault RAF Rachaya Fault JF Jhar Fault HB Hula Basin MH Mount Hermon TNP Tyre–Nabatieh Plateau ZV Zebadani Valley Gomez et al (2007)	Fig 2b- Gomez et al (2007)
Roum Fault	Fig. 4 Trace of Roum fault area (location on Fig. 1b) based on field and aerial photograph mapping. Note the river offsets (thick blue) that decrease north. Labelled circles indicate places, numbered circles indicate drainage offsets plotted in b, numbers in brackets indicate offset length in m ± 2 (cf. Table 1). X-X' is cross-section shown in c. Filled circle indicates the location of the kinematic measurements shown in d. Log-normal plot of offset drainage distribution along the Roum fault from south to north as shown in a. Note that the cumulative offsets recorded by the Litani (L), Zahrani (Z), and Awali (A) rivers decrease northward. Numbers indicate the offset labels given in Table 1. Cross-section drawn to scale along the flexing segment of Roum fault. Stereographic projection of fault planes and corresponding slickenlines measured along the Roum fault at N 33° 21'.71 - E 35° 31'.35 shown in a. The rake points out the strike-slip movement along this segment of the Roum fault. Nemer and Meghraoui (2006)	Fig 4 - Nemer and Meghraoui (2006)
DST in Lebanon	Fig. 1 (a) The left-lateral Dead Sea Transform Fault extending from the Gulf of Aqaba to southeast Turkey. Modified from McBride et al. [1990] with permission from Elsevier. Box shows location of Figure 1b. White arrows indicate the GPS velocities (mm/a) of the Arabian plate relative to Africa after Gomez et al. [2006]. (b) Shuttle Radar Topography Mission 90-m-resolution digital elevation model of the Lebanese restraining bend showing the main units and structures: CF, Coastal Flexure CM, Chouf Monocline DF, Damascus fault HB, Hula basin HF, Hasbaya fault JGF, Jordan Gorge fault MF, Missyaf fault OM, Offshore monocline RcF, Rachaya fault RF, Roum fault SF, Serghaya fault YF, Yammouneh fault White circles indicate the estimated locations of epicenters of historical earthquakes as reported by Sbeinati et al. [2005] and references therein. Box indicates location of Figure 2. Nemer et al (2008)	Fig 1 - Nemer et al (2008)
DST in Lebanon	Fig. 1 (a) The Dead Sea Transform Fault extending from the Gulf of Aqaba to southeast Turkey. It is a left-lateral transform fault with a general NeS trend except in Lebanon where it bends rightward to form a restraining bend. Modified from McBride et al. (1990). Box shows location of b. White arrows indicate the GPS velocities of the Arabian plate relative to adjacent plates after McClusky et al. (2003). (b) Shuttle Radar Topography Mission 90-m-resolution digital elevation model of the Lebanese restraining bend showing the main units and structures: BdF, Beit-ed-Dine fault CF, Coastal Flexure CM, Chouf Monocline HB,Hula basin HF, Hasbaya fault JB, Jarmaq basin MF, Missyaf fault OM, Offshore monocline RcF, Rachaya fault RF, Roum fault SF, Serghaya fault YF, Yammouneh fault Note the epicentre location of the double-shock 1956 earthquake at the intersection between Roum fault and Chouf Monocline. Coloured faults are associated with large historical events (indicated by date and magnitude) that took place within the Lebanese restraining bend. Box around the Roum fault indicates location of Fig. 4a. Nemer and Meghraoui (2006)	Fig 1 - Nemer and Meghraoui (2006)
Active Faults of Lebanon	Fig. 1b Active faults of Lebanese re-straining bend. Circled numbers mark locations of studied sites: Aajaˆqa (1) and Zalqa (2). Daëron et al (2004)	Fig 1b - Daëron et al (2004)
Rachaya Serghaya Fault Area	Fig. 2b (a) Digital elevation model of the RcF-SF area (location on Figure 1b) showing the different places referred to throughout the text. White boxes indicate the locations of subsequent figures. White arrows indicate the slope break at the base of the northern flank of Mount Hermon. Probable faulting (broken line southwest and northeast) of SF is after Gomez et al. [2003]. Nemer et al (2008)	Fig 2 - Nemer et al (2008)
Major Faults	Figure 1 Structural map of Lebanon Restraining bend. Different tectonic structural styles along the Dead Sea Transform: Inactive distributed shear along the onshore margins of the Gulf of Aqaba, and southward increasing transtension forming the gulf pure strike-slip deformation in the Araba and Jordan valleys; with three step-over basins in the Dead Sea, Sea of Galilee and Hula Valley a restraining bend and transpressional structures along the LRB transtensional structures within the Ghab and Amik basins 90 m DEM of the studied area (red square in a). The white lines are the main faults of the LRB. The yellow lines are thrust faults along the Palmyride fold belt. Map obtained from maps-for-free.com. Seismicity between 2006 and 2018 as recorded by GRAL. Data provided by CNRS Lebanon—National Center for Geophysical Research Fedorik et al (2022)	Fig 1 - Fedorik et al (2022)
Geotectonic Map	Figure 1a Location map of the Levant area with major faults and the modeled area (magenta rectangle); the Harrat Ash-Shaam volcanic field (gray polygon) and the direction of the relative regional plate motions (black arrows). Light red polygons mark uplifted regions, and yellow polygons mark subsided regions. Wetzler et al. (2022)	Fig 1a - Wetzler et al. (2022)
Tectonic and Fault Map	Figure 1b Tectonic map of the model area with major faults (Segev et al., 2021; Styron and Pagani, 2020). Coordinate system are UTM zone 36 N (external) and WGS84 (internal). Wetzler et al. (2022)	Fig 1b - Wetzler et al. (2022)

**Mount Lebanon Thrust**
Description	Image	Source
Mount Lebanon Thrust	Figure 1 Active faults of Lebanese restraining bend. Map projected upon Shuttle Radar Topography Mission relief and new SHALIMAR EM300 bathymetry. Hitherto unknown thrust system (Mount Lebanon thrust) hugs continental slope base offshore Mount Lebanon. Red box in inset shows location of Lebanese bend along Levant fault system. Red circles are coastal cities that suffered Tsunami effects during the 551 A.D. event. City abbreviations: Ar—Arqa Ba—Batroun By—Byblos Ch—Chekka Sa—Sarafand AT—Aakkar thrust TT—Tripoli thrust R-AF—Rankine-Aabdeh fault RF—Roum fault RaF—Rachaya fault SaF—Saida fault. Elias et al (2007)	Fig 1- Elias et al (2007)
Historical Earthquakes in Lebanon	Figure 4 Most likely sources of A.D. 551 (open star—inferred epicenter, this study) and other large historical earthquakes in Lebanon (modified from Daëron et al., 2005). Colored patches enclose areas where macro-seismic intensities > VIII were reported. Blue color corresponds to A.D. 551. (VIII isoseismal from Sieberg, 1932). Elias et al (2007)	Fig 4- Elias et al (2007)

**Area around Tripoli**
Description	Image	Source
Region of Tripoli	Figure 6 (a) Map showing simplified geology (from Dubertret 1955) (b) map of topography in the region of Tripoli (based on Gomez et al. 2006). Locations of the profiles in Figures 7 & 9a are shown, as well as the location of the photograph in Figure 8. Gomez et al (2007)	Fig 6- Gomez et al (2007)

**Bekaa Valley**
Description	Image	Source
Southern Bekaa Valley	Fig. 12a Shaded relief of the southern Bekaa Valley. See Figure 3 for location. A, B, C, & D correspond with offset notched ridges L corresponds with the Litani river offset by the Yammouneh fault (~ 4 km) R1 is the Litani river offset by the Roum fault R2 is the Zahrani river offset by the Roum fault Ra1 – Ra3 denote large deflections along the Rachaya fault MD = Merj Depression Gomez et al (2006)	Fig. 12a - Gomez et al (2006)

Maps from Nemer et al. (2023)

Fig. 1 - Faults and Geologic Features of Lebanon and vicinity

from Nemer et al. (2023)

Fig. 2 - Faults, Folds, and seismicity of Lebanon and vicinity

from Nemer et al. (2023)

Fig. 4 - Faults, Folds, and focal mechanism solutions of Lebanon and vicinity

from Nemer et al. (2023)

Focal Mechanisms

from Focal Mechanisms - Wikipedia

Focal Mechanisms vs. Fault Type

from Focal Mechanisms - Wikipedia

Development of Beach Ball

from Focal Mechanisms - Wikipedia

Fig. 5 - Velocity Polygons and Geological Map of Lebanon and vicinity

from Nemer et al. (2023)

Fig. 5b - Geological Map of Lebanon and vicinity

from Nemer et al. (2023)

References

Daëron, M., et al. (2007). "12,000-Year-Long Record of 10 to 13 Paleoearthquakes on the Yammoûneh Fault, Levant Fault System, Lebanon." Bulletin of the Seismological Society of America 97(3): 749-771.

Daëron, M., et al. (2004). "Constraints on the post ∼25-ka slip rate of the Yammoûneh fault (Lebanon) using in situ cosmogenic 36Cl dating of offset limestone-clast fans." Earth and Planetary Science Letters 227(1): 105-119.

Elias, A., et al. (2007). "Active thrusting offshore Mount Lebanon: Source of the tsunamigenic A.D. 551 Beirut-Tripoli earthquake." Geology 35(8): 755-758.

Gomez, F., et al. (2006). "Late Cenozoic uplift along the northern Dead Sea transform in Lebanon and Syria." Earth and Planetary Science Letters 241(3): 913-931.

Gomez, F., et al. (2007). Strain partitioning of active transpression within the Lebanese restraining bend of the Dead Sea Fault (Lebanon and SW Syria).

Nemer, T. and M. Meghraoui (2006). "Evidence of coseismic ruptures along the Roum fault (Lebanon): a possible source for the AD 1837 earthquake." Journal of Structural Geology 28(8): 1483-1495.

Nemer, T., et al. (2008). "The Rachaya-Serghaya fault system (Lebanon): Evidence of coseismic ruptures, and the AD 1759 earthquake sequence." Journal of Geophysical Research: Solid Earth 113(B5)

Nemer, T. S., et al. (2023). "Seismic Hazard Assessment of the Lebanese Restraining Bend: A Neo-deterministic Approach." Pure and Applied Geophysics 180(5): 1835-1859.

Fault Maps - Syria

Description	Image	Source
Regional tectonic map	Figure 1 Regional tectonic map of the northern Arabian Plate and the surrounding regions, showing the proximity of Syria to many active plate boundaries. Dam Damascus NAF North Anatolian Fault (modified from Brew et al. 2001) The yellow square shows the area in Figures 2, 3, 4 and 5. Abdul-Wahed and Ibrahim (2010)	Fig 1 - Abdul-Wahed and Ibrahim (2010)
Tectonic Zones	Figure 2 Tectonic zones of Syria (modified from Brew et al. (2001). Abdul-Wahed et al (2018)	Fig 2 - Abdul-Wahed et al (2018)
Principal Faults	Figure 3 Map showing geographical distribution of the Syrian National Seismological Network (▲) and the principal faults. Fault geometry is summarized from Brew et al. (2001). Abbreviations: fault (F.), basin (B.). Abdul-Wahed et al (2018)	Fig 3 - Abdul-Wahed et al (2018)
Principal Faults	Figure 2 Map of the geographical distribution of the Syrian National Seismological Network ( ▲ ) and the principal faults in this area. Abdul-Wahed and Ibrahim (2010)	Fig 2 - Abdul-Wahed and Ibrahim (2010)
Seismicity	Figure 5 Earthquake activity in Syria and nearby countries recorded by Syrian National Seismological Network from 1995 to 2012. Abdul-Wahed et al (2018)	Fig 5 - Abdul-Wahed et al (2018)
Focal Mechanisms	Figure 7 The focal mechanisms map of some largest events an earthquake of Palmyra which happened on December 24, 1996 M_c=5.6 an event from the Rouj basin on May 20, 2003 M_c=4.0 an event from the Ghab basin on January 3, 1997, M_c=3.5 an event from Latakia-Killis faults system on July 19, 1996 M_c=3.9 an event from Abd-el-Aziz uplift faults on January 11. 1996 M_c=3.5 an earthquake of Bishri fault on December 18, 1994 M_c=5.0 the composite focal mechanism of the detected multiplet in Asharneh Plain the composite focal mechanism of the biggest multiplet detected in Serghaya swarm on November 22. 1995 an earthquake of Roum fault on March 26, 1997, M_c=4.9 the composite focal mechanism of the detected doublet in Zobeideh fault M_c = coda magnitude Abdul-Wahed et al (2018)	Fig 7 - Abdul-Wahed et al (2018)
Focal Mechanisms	Figure 4 The focal mechanisms of the main events recorded over the last ten years in Syria and its nearby regions. The adjacent numbers indicate the event numbers in Appendix 1. The fault plane solutions are presented with lower-hemisphere, equal-area projections: white quadrants for dilatation, and black for compression. The base map showing the surface geology was modified by Brew et al. [2001], from Dubertret [1955], Ponikarov [1966] and Devyatkin et al. [1997]. Abdul-Wahed and Ibrahim (2010)	Fig 4 - Abdul-Wahed and Ibrahim (2010)
Simplified Focal Mechanisms	Figure 5 Simplified interpretation of the focal mechanisms over the last decade for the largest events in Syria. The active faults proposed to be generating these events were: East Anatolian Fault System Northern section of the Dead Sea Transform System Rouge Faults Normal faults in the Al-Ghab pull-apart basin Normal faults in the coastal ranges Manbeg Fault Al-Sa'an Fault Dextral fault separating the Bilas-Bishri Blocs Bilas Bloc Faults Abdel-Aziz uplift Faults Palmyra Faults Yammouneh Fault Ma'alola Fault Serghaya Fault Dextral fault in the north of Beirut Roum Fault Normal faults on the margins of the DSFS The DSFS Bishri Faults Khanaser Fault Abdul-Wahed and Ibrahim (2010)	Fig 5 - Abdul-Wahed and Ibrahim (2010)
Epicentral Map Damascus	Figure 8 Detailed epicenters map of some important seismic activities observed in Damascus region. Abdul-Wahed et al (2018)	Fig 8 - Abdul-Wahed et al (2018)
Detailed Epicentral Map Damascus	Figure 10 Detailed epicenters map of the seismic activity observed in Damascus region during the period 1995-2012. Abdul-Wahed et al (2018)	Fig 10 - Abdul-Wahed et al (2018)
Epicentral Map Central Syria	Figure 9 Detailed epicenters map of the seismic activity recorded in central part of Syria. Abdul-Wahed et al (2018)	Fig 9 - Abdul-Wahed et al (2018)
Epicentral Map N Aleppo	Figure 11 Detailed epicenters map of northern Aleppo. Abdul-Wahed et al (2018)	Fig 11 - Abdul-Wahed et al (2018)
Missyaf fault segment	Fig. 7 Missyaf fault segment (yellow arrows) limited by the El Boquea and Ghab pull-apart basins, to the south and north,respectively (Meghraoui et al. 2003). Topography data is from SRTM (3-arc-second) Meghraoui (2015)	Fig 7 - Meghraoui (2015)
Active Faults Syria	Fig. 1B Fault zone (black line; Meghraoui et al., 2003; Gomez et al., 2003; Elias, 2006; Nemer et al., 2008) and global positioning system (GPS) velocities (Eurasia fixed; Reilinger et al., 2006; Gomez et al., 2007; Le Beon et al., 2008; Alchalbi et al., 2009) emphasizing the left-lateral movements between the Sinai block and Arabia plate. Thick line is strike-slip fault; thin line is thrust fault. DSF—Dead Sea Fault EAF—East Anatolian Fault KF—Karasu Fault Sbeinati et al (2010)	Fig 1B - Sbeinati et al (2010)
Major Historical Earthquakes	Fig. 2 Major historical earthquakes (white dots) and areas of maximum damage (shaded) for the 29 June 1170 earthquake (I_o = IX using EMS98 intensity definition of Grünthal, 1998) as recorded along the northern Dead Sea fault (local intensities are from Guidoboni et al., 2004b; Sbeinati et al., 2005). The shaded area of maximum damage (I_o = IX) for the A.D. 1170 large earthquake is along the Missyaf fault segment and Ghab Basin (see also Figs. 1B and 3 for legend) and overlaps with the maximum intensity VIII (MSK, black dashed line) as drawn by Ambraseys (2009). DSF—Dead Sea Fault EAF—East Anatolian Fault KF—Karasu Fault Sbeinati et al (2010)	Fig 2 - Sbeinati et al (2010)
Major Historical Earthquakes	Fig. 1a Map showing the tectonic setting and instrumental seismicity from 1963 – 1997 (International Seismological Centre data file, M > 1) of the study area along the Missyaf segment of the Dead Sea fault (DSF). Focal mechanisms along the DSF are of moderate earthquakes (5 < M_w < 6; from CMT Harvard and MEDNET-INGV Rome). PFB = Palmyride fold belt EAF = East Anatolian fault Meghraoui et al (2003)	Fig 1a - Meghraoui et al (2003)
Tectonic Map of Syria	Fig. 15 Tectonic Map of Syria Brew et al (2001)	Fig. 15 - Brew et al (2001)
Tectonic Map of Syria	Fig. 5 Preliminary structural map showing the top of Lower Cretaceous horizon. This is one of a series of subsurface structural maps under construction within the GIS (see Table 1). Brew et al (2001)	Fig. 5 - Brew et al (2001)
Palmyride mountains tectonics	Fig. 1 Left side: map showing bounding faults and folds of the Arabian platform. Right side: location map of the intersection of the Euphrates depression with the Palmyride mountains. Alsdorf et al (1995)	Fig. 1 - Alsdorf et al (1995)
Simplified neotectonic map of Syria	Fig. 1 Simplified neotectonic map of Syria. Anticline ridges: Abdel Aziz Anti-Leban Bassit Coastal Kurd Dagh Leban. Volcanic plateaus: Jebel Arab Shin. Basins Ad Daw Bekkaa Valley Bokaieh El Ghab Amik Galilean Lake Homs Hula Nahr El-Kabir Yammuneh. Faults Akfan Amanos Jhar Jordan River Olab Roum Serghaya Aafrin St. Simeon Cities Al, city of Aleppo An, city of Antaki Be, Beyrouth Da, Damascus Ha, city of Haifa IB, Iskenderun Bay La, city of Lattaqie M, town of Myssiaf P, town of Palmyra Rukieh et al (2005)	Fig. 1 - Rukieh et al (2005)
topography and boundaries of the neotectonic provinces	Fig. 2 A model of topography and boundaries of the neotectonic provinces in Syria and Lebanon. The provinces: (WB) the western boundary zone between the Arabian and African plates (NW) the northwestern boundary zone between the Arabian and Anatolian plates (JA) the Jebel Arab volcanic province (PA) the Palmyrides (AL) the Aleppo Plateau (MB) the northwestern termination of the Mesopotamian basin (RU) the stable part of the Arabian plate (the Rutbah province) Basins: (A) Amik (B) Bekkaa valley (D) Damascus (E) El Ghab (G) Galilean Lake (H) Homs (K) Nahr El-Kabir (IB) Iskenderun Bay Cities: (Al) Aleppo (Be) Beyrouth (Da) Damascus (Ha) Haifa (La) Lattaqie Rukieh et al (2005)	Fig. 2 - Rukieh et al (2005)
Schematic map of the main neotectonic features	Fig. 7 Schematic map of the main neotectonic features in the convergent and transform boundaries of the Arabian plate. Segments of the Levant fault zone DS, Dead Sea JR, Jordan River YM, Yammuneh EG, El Ghab Other fault zones LT, Lattaqie fault MR, main recent fault of Zagros MT, main thrust of Zagros TU, Taurus (Bitlis) thrust Folded and thrusted belts: B, Bassit F, marginal Folds of Turkey K, Kurd Dagh P, Palmyrides Z, folded Belt of Zagros M, Mesotopamian Basin Symbols for faults are explained in Fig. 1. Rukieh et al (2005)	Fig. 7 - Rukieh et al (2005)
Active faults in Syria	Fig. 12 Active faults in Syria and adjacent territories. Abdel Aziz Anti-Leban Bassit Coastal Kurd Dagh Leban. Volcanic plateaus: Jebel Arab Shin. Basins Ad Daw Bekkaa Valley Bokaieh El Ghab Amik Galilean Lake Homs Hula Nahr El-Kabir Yammuneh. Faults Akfan Amanos Jhar Jordan River Olab Roum Serghaya Aafrin St. Simeon Cities Al, city of Aleppo An, city of Antaki Be, Beyrouth Da, Damascus Ha, city of Haifa IB, Iskenderun Bay La, city of Lattaqie M, town of Myssiaf P, town of Palmyra Rukieh et al (2005)	Fig. 12 - Rukieh et al (2005)
topography and boundaries of the neotectonic provinces	Fig. 13 Space imagery (Space Image Atlas of Syria, 1996) and interpreted active faults of the Levant fault zone segment near town of Missyaf. B, El Beida H, Al Harif M, Missyaf S, Sakhlieh Rukieh et al (2005)	Fig. 13 - Rukieh et al (2005)
Overall structure of DSF	Fig. 1 Overall structure of the Dead Sea Fault Zone (DSFZ). The present-day triple junction between the African, Arabian and Anatolian plates is located at Maras in the Bitlis belt, or east of Cyprus, according to various interpretations (see text). Frame shows the location of the study area. Chorowicz et al (2005)	Fig. 1 - Chorowicz et al (2005)
SOG to Homs Basalts	Fig. 2 Structure of the Dead Sea Fault Zone from the Sea of Galilee to the El- Ghab basin, and location of the Homs basalts. Chorowicz et al (2005)	Fig. 2 - Chorowicz et al (2005)
Geological Map	Fig. 3 Synthetic geological map digitized in MapInfo, which comprises all the outcrops of the Homs basalts. Extracts from the Geological Map of Syria at 1:200 000, sheets Homs and Hama (Ponikarov et al. 1963a, b), and from the Carte Geologique de la Republique Libanaise at 1:50 000, sheets Tell-Kalakh and Hamidiye´ –Halba (Guerre 1968, 1975). Chorowicz et al (2005)	Fig. 3 - Chorowicz et al (2005)
Sat Map Homs Basalts	Fig. 5 ERS SAR image (positive print) of the Homs basalts area and northern end of the Lebanon Mountains. The northwestern tip of the Shin volcano is displaced c. 16 km left-laterally. The topographic northern ends of the Eastern and Western Lebanon Mountains, separated by the Yammuneh fault, are offset c. 11 km. PA1–PA4, pull-apart structures. Chorowicz et al (2005)	Fig. 5 - Chorowicz et al (2005)
Shin Volcanoe faulting	Fig. 7 Analysis of a Landsat Thematic Mapper image. (a) Black and white display of a colour composite image extracted from a Landsat TM view acquired on 21 September 1995, using bands TM2, TM4 and TM5. (b) Structural analysis of the image, showing the main active faults and the volcanic ridges (stripped lines) on top of the Shin volcano, indicating NE–SW extension (large white arrows). F1, F2 and f are faults; PA3 is a pull-apart structure that opened between faults F1 and F2; 1–8 are sites of structural observations in the field arrows are horizontal component of movement directions observed on the slickensides (see Fig. 9). Fine black lines are tributaries displaced as a result of fault motion. Chorowicz et al (2005)	Fig. 7 - Chorowicz et al (2005)
Overall Scheme DSF	Fig. 11 Overall scheme of the Dead Sea Fault Zone, comprising four segments; from south to north, these are the Dead Sea transform the Lebanon–Anti-Lebanon–Palmyrides belt the Al-Ghab transform the Amanos belt The Dead Sea and the Al-Ghab transforms follow concentric circles. Chorowicz et al (2005)	Fig. 11 - Chorowicz et al (2005)
Simplified Geol. Map	Fig. 1 Simplified geology map of the northern Dead Sea Fault System (modified from [50]) Abbreviations GF = Ghab fault YF = Yammouneh fault SF = Serghaya fault RF = Roum fault KSF = Kara Su fault RaF = Rachaya fault HF = Hasbaya fault AF = Akkar fault PFB = Palmyride Fold Belt ML = Mt. Lebanon BV = Bekaa Valley AL = Anti Lebanon AM = Amanous Mountains SCR = Syrian Coastal Ranges GV = Ghab Valley KSV = Kara Su Valley Inset: Regional tectonic map of the eastern Mediterranean region. Gomez et al (2006)	Fig. 1 - Gomez et al (2006)
Central DSF	Fig. 3a Shaded relief and simplified neotectonic interpretation of the central Dead Sea fault system on shaded relief image Faults RF = Roum fault HF = Hasbaya fault SF = Serghaya fault YF = Yammouneh fault AF = Akkar fault JF = Jhar fault Other labels MH = Mt. Hermon D = Damour Profiles A-A’ and B-B’ are shown in Figure 4. Gomez et al (2006)	Fig. 3a - Gomez et al (2006)
Northern DSF	Fig. 5a Simplified neotectonic interpretation of the northern DSFS on shaded relief image (see Figure 2 for location). See Figure 3 for an explanation of symbols. Gomez et al (2006)	Fig. 5a - Gomez et al (2006)
Damascus Region	Fig. 9 Shaded topography image of the Damascus region encompassing the Serghaya fault. Large drainage offsets are prominent along the Serghaya fault. Antecedent streams drain from the Anti Lebanon Mountains eastward across Jebel Kassioun (the westernmost fold of the Palmyride Fold Belt), indicating that late Cenozoic uplift and folding of the western Palmyrides postdates the initiation of the last episode of uplift in the Anti Lebanon Mountains. ZV = Zebadani Valley. White arrows denote large stream deflections . See Figure 3 for location. Gomez et al (2006)	Fig. 9 - Gomez et al (2006)

References

Abdul-Wahe, M. K. and J. Asfahani (2018). "The recent instrumental seismicity of Syria and its implications." Geofísica Internacional 57: 121-138.

Abdul-Wahed, M. K. and A.-T. Ibrahim (2010). "Preliminary outlining of the seismological active zones in Syria." Annals of Geophysics 53: 1-9.

BREW, G., et al. (2001). "Structure and tectonic development of the Ghab basin and the Dead Sea fault system, Syria." Journal of the Geological Society 158(4): 665-674.

Meghraoui, M. (2015). Paleoseismic History of the Dead Sea Fault Zone. Encyclopedia of Earthquake Engineering. M. Beer, I. A. Kougioumtzoglou, E. Patelli and I. S.-K. Au. Berlin, Heidelberg, Springer Berlin Heidelberg: 1-20.

Sbeinati, M. R., et al. (2010). "Timing of earthquake ruptures at the Al Harif Roman aqueduct (Dead Sea fault, Syria) from archaeoseismology and paleoseismology." Geological Society of America Special Papers 471: 243-267.

Meghraoui, M., et al. (2003). "Evidence for 830 years of seismic quiescence from palaeoseismology, archaeoseismology and historical seismicity along the Dead Sea fault in Syria." Earth and Planetary Science Letters 210(1–2): 35-52.

Brew, G., et al. (2000). "Tectonic map and geologic evolution of Syria: The role of GIS." Geophysics 19: 176-182.

Mcbride, J. H., et al. (1990). "Seismic reflection structure of intracratonic Palmyride fold-thrust belt and surrounding Arabian platform, Syria." AAPG Bulletin 74(3): 238-259.

Alsdorf, D., et al. (1995). "The intraplate Euphrates fault system-Palmyrides mountain belt junction and relationship to Arabian plate boundary tectonics." Annals of Geophysics 38.

Rukieh, M., et al. (2005). "Neotectonic map of Syria and some aspects of Late Cenozoic evolution of the northwestern boundary zone of the Arabian plate." Journal of Geodynamics - J GEODYNAMICS 40: 235-256.

Chorowicz, J., et al. (2005). "Tectonics of the Pliocene Homs basalts (Syria) and implications for the Dead Sea Fault Zone activity." Journal of The Geological Society - J GEOL SOC 162: 259-271.

Fault Maps - Turkey

Active Fault Map Quadrangles (click on map to open)

Updating of Active Fault Map of Turkey and its Database (Archived Project on Research Gate - 72 references including quadrangle maps)

Description	Image	Source
Figure 2 - Active fault map of the Eastern Mediterranean region. AA Aegean arc CA Cyprian arc DSFZ Dead Sea fault zone EAFZ East Anatolian fault zone NAFZ North Anatolian fault zone SATZ Southeast Anatolian Thrust Zone PE Pontic Escarpment LC Lesser Caucasus GC Great Caucasus WEAP West Anatolian Extensional Provence CAP Central Anatolian Provence EACP East Anatolian Compressional Provence NAP North Anatolian Provence PFFZ Palmyra fault and Fold Zone Arrows indicate direction of plate motion Subduction zones - heavy lines with open triangles: the tips of triangles indicate polarity. Heavy lines with filled triangles at hanging wall indicate thrust zones. Heavy lines with half arrows are transform faults: the half arrows show relative movement along these faults. Lines with open triangles represent reverse fault zones. Duman et al (2018)	Active Fault Map - E Med.	Fig 2 - Duman et al (2018)
Figure 1 - Active fault map of the Eastern Mediterranean region and tectonic provinces. HA Hellenic arc CA Cyprian arc DSFZ Dead Sea Fault Zone EAFZ East Anatolian Fault Zone NAFZ North Anatolian Fault Zone SATZ Southeast Anatolian Thrust Zone PE Pontic Escarpment LC Lesser Caucasus GC Great Caucasus WEAP West Anatolian Extensional Provence West Anatolia graben systems Outer Isparta Angle Inner Isparta Angle Northwest Anatolia transition zone CAP Central Anatolian Provence EACP East Anatolian Compressional Provence NAP North Anatolian Provence SEAP Southeast Anatolia Province PFFZ Palmyra Fault and Fold Zone Subduction zones - heavy lines with open triangles: the tips of triangles indicate polarity. Heavy lines with filled triangles at hanging wall indicate thrust zones. Heavy lines with half arrows are transform faults: the half arrows show relative movement along these faults. Lines with open triangles represent reverse fault zones. Bold arrows indicate the direction of plate motion. Thick hatched red lines show plate boundary fault zones. Thick dashed grey lines represent boundaries of major and sub-tectonic provinces Emre et al (2018)	Active Fault Map - E Med.	Fig 1 - Emre et al (2018)
Active Fault Map of Turkey with an Explanatory Text 1:1,250,000 Scale	Active Fault Map - Turkey	Active Fault Map of Turkey with an Explanatory Text 1:1,250,000 Scale
Active Fault Map of Turkey with an Explanatory Text 1:1,250,000 Scale	Active Fault Map - Turkey (Big)	Active Fault Map of Turkey with an Explanatory Text 1:1,250,000 Scale
Active Fault Map of Turkey Antakya Quadrangle 1:250,000 Scale	Active Fault Map - Antakya Quadrangle	Active Fault Map of Turkey Antakya Quadrangle 1:250,000 Scale
Figure 3a - Spatial distribution of the active faults of Turkey. Each fault or fault segment was defined by an identification number. The fault segments were numbered with sub class numbers. In this notation the first number shows that the fault has multi-segments, a fault system or a zone, the second number indicates the fault segment. The identification numbers of the faults associated with the names are in Table 1. BMGS Büyük Menderes Graben System GGS Gediz Graben System DGS Denizli Graben System AGS Acıgöl Graben System BGS Burdur Graben System ÇGS Çivril Graben system AAGS Afyon-Akşehir Graben System KGS Karamuk Graben System Emre et al (2018)	Active Faults - W Turkey	Fig 3a - Emre et al (2018)
Figure 3b - Spatial distribution of the active faults of Turkey. Each fault or fault segment was defined by an identification number. The fault segments were numbered with sub class numbers. In this notation the first number shows that the fault has multi-segments, a fault system or a zone, the second number indicates the fault segment. The identification numbers of the faults associated with the names are in Table 1. BMGS Büyük Menderes Graben System GGS Gediz Graben System DGS Denizli Graben System AGS Acıgöl Graben System BGS Burdur Graben System ÇGS Çivril Graben system AAGS Afyon-Akşehir Graben System KGS Karamuk Graben System Emre et al (2018)	Active Faults - Central Turkey	Fig 3b - Emre et al (2018)
Figure 3c - Spatial distribution of the active faults of Turkey. Each fault or fault segment was defined by an identification number. The fault segments were numbered with sub class numbers. In this notation the first number shows that the fault has multi-segments, a fault system or a zone, the second number indicates the fault segment. The identification numbers of the faults associated with the names are in Table 1. BMGS Büyük Menderes Graben System GGS Gediz Graben System DGS Denizli Graben System AGS Acıgöl Graben System BGS Burdur Graben System ÇGS Çivril Graben system AAGS Afyon-Akşehir Graben System KGS Karamuk Graben System Emre et al (2018)	Active Faults - E Turkey	Fig 3c - Emre et al (2018)
Table 1	Table 1 - for Fig 3 a,b,c	Table 1 - Emre et al (2018)
Figure 4 - Fault bend systems in NW Anatolia. Fault bends are parallel to the Central Marmara arc of the North Anatolian fault zone. South Marmara bend corresponds to the western tip of the southern strand of the North Anatolian fault zone. Fault segments of the bends simplified from Emre et al. (2013). NAF North Anatolian Fault Zone (1) ZF Zeytinbağı Fault (11) BF Bandırma Fault (10) EDF Edincik Fault (9) SNF Sinekçi Fault (8) ÇBF Çan-Biga Fault Zone (6) EF Evciler Fault (4) YGF Yenice-Gönen Fault (16) MFZ Manyas Fault Zone (17) MKF Mustafakemalpaşa Fault (13) OF Orhaneli Fault (134) UF Uluabat Fault (12) BRF Bursa Fault (136) İFZ İnegöl Fault Zone (137) OYF Oylat Fault (138) DF Dodurga Fault (139) EŞ Eskişehir fault(140) HBFZ Havran-Balya Fault Zone (23) BAF Balıkesir Fault (24) ZFZ Zeytindağ Fault Zone SKFZ Soma-Kırkağaç Fault Zone (27) GFZ Gelenbe Fault Zone (28) SFM, Simav Fault Zone (30) BKF, Bekten Fault (19) Emre et al (2018)	Fault Bend Systems NW Anatolia	Fig 4 - Emre et al (2018)
Figure 4 Seismicity of Anatolia region, 1900–2012, M_w, C 4.0. Faults are as in Fig. 2 Duman et al (2018)	Seismicity in Turkey vs. M_w	Fig 4 - Duman et al (2018)
Figure 5 The distribution of the seismicity according to the focal depth across Turkey and surrounding region, 1900–2012, Mw C 4.0 (from Duman et al. 2016) Emre et al (2018)	Focal Depth Seismicity in Turkey	Fig 5 - Emre et al (2018)
Figure 9 Based on focal depth, distribution of the seismicity across Turkey and surrounding region, 1900–2012, Mw. Faults are as in Fig. 2. The lines with labelled A–A 0, B–B0, C–C0 and D–D0 are locations of the cross sections given in Fig. 10 Duman et al (2018)	Focal Depth Seismicity in Turkey	Fig 9 - Duman et al (2018)
Figure 8 Crustal thickness cross sections across from Pontides to Tauride and Anatolide to Arabian platform across Turkey. A–A0 B–B0 C–C0 The location of the cross sections is given in Fig. 7. NAFZ North Anatolian fault zone EAFZ East Anatolian fault zone PE Pontic Escarpment MEF Merzifon-Esençay fault SF Sungurlu fault GF Gümüşkent fault TF Tuzgölü fault BHFZ Balıkesir-Havran fault zone SFZ Simav fault zone GGS Gediz Graben system BMGS Büyük Menderes Graben system BFFZ Burdur Fethiye fault zone TF Tercan fault SATZ Southeast Anatolian Thrust zone Duman et al (2018)	Crustal Cross-Sections	Fig 8 - Duman et al (2018)
Figure 6 Map showing distributions of the lower hemisphere equal area projection plots of the focal mechanism solutions of earthquakes and active faults in and surrounding Turkey. The size of each ‘beachball’ is related to the earthquake magnitude. Faults are as in Fig. 2 Duman et al (2018)	Focal mechanism map	Fig 6 - Duman et al (2018)
Figure 5 Historical earthquake distribution across Turkey and surrounding region, BC 2000–AD 1900. Faults are as in Fig. 2 Duman et al (2018)	Historical Earthquakes in Turkey	Fig 5 - Duman et al (2018)
Figure 6 Spatial distribution of earthquakes from 1900 to 2012 larger than Mw C 4.0 within the 8-km wide buffer zones of the active faults. Earthquake data was taken from Kadirioğlu et al. (2016) Emre et al (2018)	Earthquakes in Turkey (1900-2012)	Fig 6 - Emre et al (2018)
Figure 12 Major Turkey seismotectonics domains, defined primarily by seismicity and fault zones with similar characteristics. North Anatolian fault zone East Anatolian fault zone Southeast Anatolian fault zone Eastern Anatolian Munzur Splays of North Anatolian fault zone Tuzgölü fault zone NW Anatolia transition fault zone Faults of İsparta Angle Western Anatolia graben systems Aegean arc Anaximander Cyprian arc Dead Sea fault zone Harran Caucasus thrust zone Faults of Pontide Thrace Faults are as in Fig. 2. Heavy lines with open triangles show sutures: the tips of triangles indicate polarity. Heavy lines with filled triangles with on the uplift side indicate thrust belts. Heavy lines are major intra-plate undifferentiated major faults. Duman et al (2018)	Seismotectonic domains	Fig 12 - Duman et al (2018)
Fig. 1 a) General map of the Dead Sea Fault Zone between the Red Sea in south and East Anatolian Fault Zone (EAFZ) in north. Simplified from Zilberman et al. (2000), Meghraoui et al. (2003) and Westaway (2003) b) DEM of the northern part of the Dead Sea Fault Zone. The Hacıpaşa fault (red line) was drawn on the basis of authors' field observations; other faults (black lines) are taken from Perinçek and Çemen (1990), Lyberis et al.(1992), Yürür and Chorowicz (1998), Rojay et al. (2001) and Westaway (2003). Akyuz et al (2006)	Amik Basin	Fig 1 - Akyuz et al (2006)
Fig. 2 Simplified map of the offset stream beds between the Syrian-Turkish border in south and Amik Basin in north. Note that the western fault does not extend further north of Hacıpaşa town and it does not offset any stream bed. The border between Turkey and Syria is the dashed bold line in south and Asi River. Numbers indicate locations of offset measurements given in Table 2. Map also shows trench locations. Akyuz et al (2006)	Hacipasa Fault	Fig 2 - Akyuz et al (2006)
Fig. 8 DSF - Northern Dead Sea fault EAF - East Anatolian fault LRB - Lebanese Restraining Bend and Missyaf-El Ghab segments Afrin fault branch KF - Karasu fault KB - Karasu block KOF - Karatas-Osmaniye fault CA - Cyprus Arc Large historical earthquakes and their extent along fault segments are marked by colored areas (Sbeinati et al., 2005). The Arabian, Anatolian, and African plates mark the triple junction. Large arrows are plate velocities from GPS results, and focal mechanisms are from Harvard CMT solutions. Topography data is from SRTM (3-arc-second) Meghraoui (2015)	DST into EAF	Fig 8 - Meghraoui (2015)
Figure 1 Tectonic setting of the study region with shaded topography. North direction is indicated on the top left. Thick and thin red lines show the East and North Anatolian Faults, respectively. Secondary faults are shown by thin black lines (Emre et al., 2013). Black arrows on the fault traces indicate the relative motion of the faults. White arrows indicate the GPS velocities with Arabia fixed reference frame (Reilinger et al., 2006). (Inset) Figure shows the major plate boundaries surrounding the study region. Red arrows represent direction of the plate motions of Anatolia and Arabia. Hellenic and Cyprus Arcs are shaded in red. Blue triangle represents the position of the Euler pole from Bletery et al., (2020). Study region is bounded by the red box. For simplicity, we refer to the SW and NE of the EAF in the text as west and east, respectively. EAF: East Anatolian Fault NAF: North Anatolian Fault LH. Lake Hazar. BZFTB: Bitlis-Zagros Fold and Thrust Belt T: Türkoğlu MOF: Malatya-Ovacık Fault SF: Sürgü Fault AF: Amanos Fault YsF: Yesemek Fault YF: Yumurtalık Fault TF: Toprakkale Fault NFZ: Narlı Fault Zone DSF: Dead Sea Fault VFZ: Varto Fault Zone K: Kahramanmaraş Junction Ç: Çelikhan Krl: Karlıova CA: Cyprus Arc HA: Hellenic Arc Güvercin et al (2022)	Tectonic Setting - EAF	Fig 1 - Güvercin et al (2022)
Figure 2 Fault segmentation based on the historical earthquakes and geology along the EAF and the faults further west of KMTJ (Duman and Emre, 2013). The major structural features, e.g., releasing and restraining bends, are also shown. The colored bands indicate the segments of the EAF: Palu (blue) Pütürge (red) Erkenek(green) Pazarcık (orange) Amanos (cyan) Karlıova (gray) The basins are shaded in yellow. The locations of historical earthquakes are from Ambraseys (1988), Ambraseys and Jackson (1998) and Tan et al. (2008). FC: Fault Complex RB: Releasing Bend RtB: Restraining Bend DRrB: Double Restraining Bend PB: Paired Bend Ulv: Uluova NAF: North Anatolian Fault Güvercin et al (2022)	Fault segmentation - EAF	Fig 2 - Güvercin et al (2022)
Figure 3 (a) Map view and (b) Depth section of the seismicity along the EAF during the period 2007– 2019. Earthquakes greater than M2.5 around the fault trace are shown by colored circles colors based on the segment that they belong. The depth section includes seismicity ±15km around the fault trace at surface. Faults are shown by black lines (Emre et al., 2013). Numbers on the map are the ID’s of the events with M>5 which are represented by yellow stars. Red dashed lines indicate segment boundaries as introduced in Figure 2. White stars represent the locations of the near-repeating earthquakes (Konca et al., 2021). KMTJ: Kahramanmaraş Triple Junction LH: Lake Hazar BZFTB: Bitlis-Zagros Fold and Thrust Belt SF: Sürgü Fault AF: Amanos Fault YsF: Yesemek Fault YF: Yumurtalık Fault TF: Toprakkale Fault NFZ: Narlı Fault Zone The basins are shaded in yellow. The locations of historical earthquakes are from Ambraseys (1988), Ambraseys and Jackson (1998) and Tan et al. (2008). Güvercin et al (2022)	Seismicity - EAF	Fig 3 - Güvercin et al (2022)
Figure 7 a) Moment tensor solutions of 160 events with magnitudes M>3.7 obtained in this study. ID number of each solution is above the beach ball and the source parameters are presented in Table S2. Blue ellipses mark the geometrical complexities in Figure 2. Black boxes bound the area of each depth cross section in (b). b) Fault perpendicular cross sections of the seismicity and dip of the fault plane solutions. The dip variations are displayed, from west to east Box 1: Pazarcık segment Box 2: Erkenek segment Box 3-4-5-6: Pütürge segment Box 7-8: Palu segment The earthquakes projected to the profiles within ±15 width in related boxes in (a). Box numbers are at the upper left corner of each depth profile. Black lines indicate the dip angles for the selected fault plane parallel to EAF in each box in (a). Solid red lines show the location of the EAF. Dashed red lines show the average dip angle from the earthquake source mechanisms. The average dip angle is at the lower right corner of each cross section panel. Güvercin et al (2022)	Moment tensor solutions - EAF	Fig 7 - Güvercin et al (2022)

References

Duman, T., et al. (2018). "Seismotectonic database of Turkey." Bulletin of Earthquake Engineering 16: 3277-3316.

Emre, Ö., et al. (2018). "Active fault database of Turkey." Bulletin of Earthquake Engineering 16: 3229-3275.

1:25 000 Scale Basic Active Fault Maps - GIS data available for a fee

References for Emre et al (2018) Fig 1 (Active Fault Map of the Eastern Mediterranean)

Faults in Turkey are from Emre et al. (2013)
Faults in the south and east are simplified from Garfunkel (2014), Hessami et al. (2003) and Gudjabidze (2003)
Faults in Aegean and Balkans are from Burchfiel et al. (2006), Caputo et al. (2012, 2015), Woessner et al. (2015)
Faults in Mediterranean are re-evaluated from Angelier et al. (1982) and Papazachos and Papaioannou (1999)
Faults in Black Sea are re-evaluated from Şengör et al. (1985) and Barka and Reilinger (1997)
Neotectonic Provence modified from Şengör (1980) and Koçyiğit and Özacar (2003)
For the other details of the faults in Turkey see Fig. 3.

References for Duman et al (2018) Fig 2 (Active Fault Map of the Eastern Mediterranean)

Faults in Turkey are from Emre et al. (2013)
Faults in the south and east are simplified from Hessami et al. (2003) and Gudjabidze (2003)
Faults in Aegean and Balkans are from Burchfiel et al. (2006), Caputo et al. (2012, 2015), Woessner et al. (2015), Garfunkel et al. (2014).
Faults in Mediterranean are re-evaluated from Angelier et al. (1982) and Papazachos and Papaioannou (1999)
Faults in Black Sea are re-evaluated from Şengör et al. (1985) and Barka and Reilinger (1997)
Neotectonic Provence modified from Şengör (1980)

Akyuz, H. S., et al. (2006). "Historical earthquake activity of the northern part of the Dead Sea Fault Zone, southern Turkey." Tectonophysics 426(3–4): 281-293.

Meghraoui, M. (2015). Paleoseismic History of the Dead Sea Fault Zone. Encyclopedia of Earthquake Engineering. M. Beer, I. A. Kougioumtzoglou, E. Patelli and I. S.-K. Au. Berlin, Heidelberg, Springer Berlin Heidelberg: 1-20.

Active Fault Map Quadrangles - Big Detailed Maps - click on map to open

Maps of Turkey - MTA

Güvercin, S. E., et al. (2022). "Active Seismotectonics of the East Anatolian Fault." Geophysical Journal International.

Notes

Bitlis Suture Info - find and upload images and then sort - add DEMS to arcgis pro

1

2

1

4

add image reference table to geoscience refs - incl this on tectonic geomorphology

Fault Maps - Entire Transform

Description	Image	Source
Fig. 3 Dead Sea fault trace from the detailed mapping of individual segments using aerial and satellite photographs combined with ﬁeld investigations. The fault detailed mapping is from the results of the APAME Project (APAME 2007). Various late Holocene offsets from published works are indicated along with geological offsets (e.g., 107-km left-lateral offset of the erosion surface of late Jurassic units; see text for references). Topography data is from SRTM (3-arc-second) Meghraoui (2015)	Entire DST	Fig 3 - Meghraoui (2015)
Figure 7 Quaternary fault map of Israel. Colours indicate the corresponding criterion for each fault. Inferred subsurface faults are marked by dashed lines. Abbreviations are for the main strike-slip segments of the DST. Sharon et al (2020)	Quaternary Fault Map	Fig 7 - Sharon et al (2020)
Figure 1 Tectonic sketch map (after Picard, 1943;Bartov, 1990). Karcz (2004)	Tectonic sketch map	Fig 1 - Karcz (2004)
Figure 25.1 (a) The Dead Sea fault segments, Fault mapping and slip rates from (Gomez et al., 2007; AU1 Khair et al., 2000; Meghraoui, 2015; Westaway, 2004) Abbreviations for some key tectonic features: AGF Al-Ghab fault AF Afrin fault CA Cyprus Arc KB Karasu basin KF Karasu fault KOF Karatas-Osmaniye fault LF Lattakia fault DSF Dead Sea fault EAF East Anatolian fault MF Missyaf fault SF Serghaya fault RF Roum fault YF Yammuneh fault (b) Instrumental seismicity of the Dead Sea fault between 1964 and 2011, M GT 3. Data are from: IRIS; Incorporated Research Institutions for Seismology (http://www.iris.edu/hq/), ISC; The International Seismological Center (http://www.isc.ac.uk/) and NEIC; The National Earthquake Information Center. The seismicity depending on international organizations lists for this area’s earthquakes of magnitudes LT 4 is misleading. The clusters of yellow “epicenters” around (30°N, 36.4°E and 31.2°N,36.4°E) are most probably explosions these areas correspond to the “Phosphate Mines Co.” locations of Al-Shidiah and Al-Hisa exploitation areas south of Jordan respectively where up to 10 Tons of explosives are detonated frequently on routine basis in the framework of the industrial exploitation of the mines. See Fig. 25.5b Abou Karaki et al. (2022)	Dead Sea Fault Segments + Seismicity	Fig 25.1 - Abou Karaki et al. (2022)

References

Karcz, I. (2004). "Implications of some early Jewish sources for estimates of earthquake hazard in the Holy Land." Ann. Geophys. 47: 759–792.

Meghraoui, M. (2015). Paleoseismic History of the Dead Sea Fault Zone. Encyclopedia of Earthquake Engineering. M. Beer, I. A. Kougioumtzoglou, E. Patelli and I. S.-K. Au. Berlin, Heidelberg, Springer Berlin Heidelberg: 1-20.

Sharon, M., et al. (2020). "Assessment of seismic sources and capable faults through hierarchic tectonic criteria: implications for seismic hazard in the Levant." Natural Hazards and Earth System Sciences 20: 125-148.

Reference Images

Description	Image	Source
Common Geologic Map Symbols	Fig. 4-54 Common symbols representing geologic features on geologic maps. Concepts illustrated describe strike and dip for describing the orientation of strata (beds), and illustrations of structural features (folds and faults). Introduction to Physical Geology (miracosta.edu)	Fig. 4-54 - Introduction to Physical Geology (miracosta.edu)
Reverse and Thrust Faults	Figure 10.3.4 Block model and corresponding plan view depictions of reverse (a) and normal (b) faulting. Black arrows on the south-facing side of each block indicate the sense of displacement along the fault. Symbols in plan view indicate the type of fault and are always drawn on the hanging wall side Introduction to Physical Geology (miracosta.edu)	Figure 10.3.4 - A Practical Guide to Introductory Geology by Siobhan McGoldrick

References

Introduction To Physical Geology - free online textbook from miracosta.edu

A Practical Guide to Introductory Geology by Siobhan McGoldrick - CC BY 4.0 License

Federal Geographic Data Committee Geologic Data Subcommittee

Charts and Illustrations

Earthquake Archeological Effects (EAE)

from Rodríguez-Pascua et al (2013: 221-224)

Potential Earthquake Archeological Effects (PEAEs)

from Jusseret et al. (2013)

Environmental Effects (ESI 2007)

from Amos Salamon

Synoptic Table of ESI 2007 Intensity Degrees

from Michetti et al. (2007)

Surface Faulting vs. Intensity

from Michetti et al. (2007)

Environmental Effects vs. Intensity

from Michetti et al. (2007)

Simple MMI Intensity Scale

from ?

More Subjective MMI Intensity Scale

from ?

Intensity vs. PGA

from Abdelmonem (2014)

Focal Mechanisms

from Focal Mechanisms - Wikipedia

Focal Mechanisms vs. Fault Type

from Focal Mechanisms - Wikipedia

Development of Beach Ball

from Focal Mechanisms - Wikipedia

Easily create .kml file to plot focal mechanisms in Google Earth

from geophysique.be

All Charts and Illustrations in a Thumbnail Table

**Charts**
Description	Image	Source
Earthquake Archeological Effects	Earthquake Archeological Effects Chart Rodríguez-Pascua et al (2013)	Rodríguez-Pascua et al (2013: 221-224)
Environmental Effects (ESI 2007)	Graphic Representation of ESI 2007 Intensity click on image to open a higher resolution version in a new tab
Synoptic Table of ESI 2007 Intensity Degrees	Plate I Synoptic Table of ESI 2007 Intensity Degrees - The accuracy of the assessment improves in the higher degrees of the scale, in particular in the range of occurrence of primary effects, typically starting from intensity VIII, and with growing resolution for intensity IX, X, XI and XII. Hence, in the yellow group of intensity degrees (XI-XII) they become the most effective tool for intensity assessment. Michetti et al. (2007)	Michetti et al. (2007)
Surface Faulting vs. Intensity	Table 1 Ranges of surface faulting parameters (primary effects) and typical extents of total area (secondary effects) for each intensity degree. Michetti et al. (2007)	Michetti et al. (2007)
Environmental Effects vs. Intensity	Table 2 Diagnostic range of intensity degrees for each class of environmental effects. Michetti et al. (2007)	Michetti et al. (2007)
Simple MMI Intensity Scale	Simple MMI Intensity Scale
More Subjective MMI Intensity Scale	More Subjective MMI Intensity Scale
Intensity vs. PGA	Table 3.8 Correlation of PGA with the Instrumental Intensity scale and Richter scale Abdelmonem (2014)	Abdelmonem (2014)
Focal Mechanisms	Focal Mechanisms Wikipedia Mikenorton - CC BY-SA 3.0	Focal Mechanisms - Wikipedia
Focal Mechanisms vs. Fault Type	Focal Mechanisms vs. Fault Type Wikipedia Mikenorton - CC BY-SA 3.0	Focal Mechanisms - Wikipedia
Development of Beach Ball	Development of the Focal Mechanism Beach Ball Wikipedia Mikenorton - CC BY-SA 3.0	Focal Mechanisms - Wikipedia

Short Descriptions of Various Intensity Scales

Scale	Description	Reference(s)
MMI	The MMI scale estimates the intensity of an earthquake by considering its effects on people, objects, buildings and environment on a specific locality. (anonymous reviewer of JW's Mid 8th century Earthquakes article)	MMI (USGS) MMI (wikipedia) Wood and Neumann (1931)
MSK		MSK Scale (wikipedia) Medvedev et al.(1965)
EMS		EMS at GFZ Potsdam EMS at GFZ Potsdam (Item Record) Grünthal (1998)
INQUA (ESI- 2007)	The Environmental Seismic Intensity scale (ESI07) is only based on the local effects triggered by the earthquake in the natural environment (Michetti et al. 2007). (anonymous reviewer of JW's Mid 8th century Earthquakes article)	ESI Scale (wikipedia) Michetti et al. (2004)

Environmental Seismic Intensity scale - ESI 2007

ESI 2007 Intensity Scale

Textual Descriptions

I-III

There are no environmental effects that can be used as diagnostic.

IV -LARGELY OBSERVED - First unequivocal effects in the environment

Primary Effects

absent

Secondary Effects

Rare small variations of the water level in wells and/or of the flow-rate of springs are locally recorded, as well as extremely rare small variations of chemical-physical properties of water and turbidity in springs and wells, especially within large karstic spring systems, which appear to be most prone to this phenomenon.

In closed basins (lakes, even seas) seiches with height not exceeding a few centimeters may develop, commonly observed only by tidal gauges, exceptionally even by naked eye, typically in the far field of strong earthquakes. Anomalous waves are perceived by all people on small boats, few people on larger boats, most people on the coast. Water in swimming pools swings and may sometimes overflows.

Hair-thin cracks (millimeter-wide) might be occasionally seen where lithology (e.g., loose alluvial deposits, saturated soils) and/or morphology (slopes or ridge crests) are most prone to this phenomenon.

Exceptionally, rocks may fall and small landslide may be (re)activated, along slopes where the equilibrium is already near the limit state, e.g. steep slopes and cuts, with loose and generally saturated soil.

Tree limbs shake feebly.

V -STRONG - Marginal effects in the environment

Primary Effects

absent

Secondary Effects

Rare variations of the water level in wells and/or of the flow-rate of springs are locally recorded, as well as small variations of chemical-physical properties of water and turbidity in lakes, springs and wells.

In closed basins (lakes, even seas) seiches with height of decimeters may develop, sometimes noted also by naked eye, typically in the far field of strong earthquakes. Anomalous waves up to several tens of cm high are perceived by all people on boats and on the coast. Water in swimming pools overflows.

Thin cracks (millimeter-wide and several cms up to one meter long) are locally seen where lithology (e.g., loose alluvial deposits, saturated soils) and/or morphology (slopes or ridge crests) are most prone to this phenomenon.

Rare small rockfalls, rotational landslides and slump earth flows may take place, along often but not necessarily steep slopes where equilibrium is near the limit state, mainly loose deposits and saturated soil. Underwater landslides may be triggered, which can induce small anomalous waves in coastal areas of sea and lakes.

Tree limbs and bushes shake slightly, very rare cases of fallen dead limbs and ripe fruit.

Extremely rare cases are reported of liquefaction (sand boil), small in size and in areas most prone to this phenomenon (highly susceptible, recent, alluvial and coastal deposits, near-surface water table).

VI -SLIGHTLY DAMAGING - Modest effects in the environment

Primary Effects

absent

Secondary Effects

Significant variations of the water level in wells and/or of the flow-rate of springs are locally recorded, as well as small variations of chemical-physical properties of water and turbidity in lakes, springs and wells.

Anomalous waves up to many tens of cm high flood very limited areas nearshore. Water in swimming pools and small ponds and basins overflows.

Occasionally, millimeter-centimeter wide and up to several meters long fractures are observed in loose alluvial deposits and/or saturated soils; along steep slopes or riverbanks they can be 1-2 cm wide. A few minor cracks develop in paved (either asphalt or stone) roads.

Rockfalls and landslides with volume reaching ca. 10³ m³ can take place, especially where equilibrium is near the limit state, e.g. steep slopes and cuts, with loose saturated soil, or highly weathered / fractured rocks. Underwater landslides can be triggered, occasionally provoking small anomalous waves in coastal areas of sea and lakes, commonly seen by instrumental records.

Trees and bushes shake moderately to strongly; a very few tree tops and unstable-dead limbs may break and fall, also depending on species, fruit load and state of health.

Rare cases are reported of liquefaction (sand boil), small in site and in areas most prone to this phenomenon (highly susceptible, recent, alluvial and coastal deposits, near surface water table).

VII -DAMAGING - Appreciable effects in the environment

Primary Effects

observed very rarely, and almost exclusively in volcanic areas. Limited surface fault ruptures, tens to hundreds of meters long and with centimetric offset, may occur, essentially associated to very shallow earthquakes.

Secondary Effects - The total affected area is in the order of 10 km²

Significant temporary variations of the water level in wells and/or of the flow-rate of springs are locally recorded. Seldom, small springs may temporarily run dry or appear. Weak variations of chemical-physical properties of water and turbidity in lakes, springs and wells are locally observed.

Anomalous waves even higher than a meter may flood limited nearshore areas and damage or wash away objects of variable size. Water overflows from small basins and watercourses.

Fractures up to 5-10 cm wide and up to hundred metres long are observed, commonly in loose alluvial deposits and/or saturated soils; rarely, in dry sand, sand-clay, and clay soil fractures are also seen, up to 1 cm wide. Centimeter-wide cracks are common in paved (asphalt or stone) roads.

Scattered landslides occur in prone areas, where equilibrium is unstable (steep slopes of loose / saturated soils), while modest rock falls are common on steep gorges, cliffs). Their size is sometimes significant (10³ - 10⁵ m³); in dry sand, sand-clay, and clay soil, the volumes are usually up to 100 m³. Ruptures, slides and falls may affect riverbanks and artificial embankments and excavations (e.g., road cuts, quarries) in loose sediment or weathered / fractured rock. Significant underwater landslides can be triggered, provoking anomalous waves in coastal areas of sea and lakes, directly felt by people on boats and ports.

Trees and bushes shake vigorously; especially in densely forested areas, many limbs and tops break and fall.

Rare cases are reported of liquefaction, with sand boils up to 50 cm in diameter, in areas most prone to this phenomenon (highly susceptible, recent, alluvial and coastal deposits, near surface water table).

VIII - HEAVILY DAMAGING - Extensive effects in the environment

Primary Effects

observed rarely - Ground ruptures (surface faulting) may develop, up to several hundred meters long, with offsets not exceeding a few cm, particularly for very shallow focus earthquakes such as those common in volcanic areas. Tectonic subsidence or uplift of the ground surface with maximum values on the order of a few centimeters may occur.

Secondary Effects - The total affected area is in the order of 100 km²

Springs may change, generally temporarily, their flow-rate and/or elevation of outcrop. Some small springs may even run dry. Variations in water level are observed in wells. Weak variations of chemical-physical properties of water, most commonly temperature, may be observed in springs and/or wells. Water turbidity may appear in closed basins, rivers, wells and springs. Gas emissions, often sulphureous, are locally observed.

Anomalous waves up to 1-2 meters high flood nearshore areas and may damage or wash away objects of variable size. Erosion and dumping of waste is observed along the beaches, where some bushes and even small weak-rooted trees can be eradicated and drifted away. Water violently overflows from small basins and watercourses.

Fractures up to 50 cm wide and up to hundreds metres long, are commonly observed in loose alluvial deposits and/or saturated soils; in rare cases fractures up to 1 cm can be observed in competent dry rocks. Decimetric cracks are common in paved (asphalt or stone) roads, as well as small pressure undulations.

Small to moderate (10³ - 10⁵ m³) landslides are widespread in prone areas; rarely they can occur also on gentle slopes; where equilibrium is unstable (steep slopes of loose / saturated soils; rock falls on steep gorges, coastal cliffs) their size is sometimes large (10⁵ - 10⁶ m³). Landslides can occasionally dam narrow valleys causing temporary or even permanent lakes. Ruptures, slides and falls affect riverbanks and artificial embankments and excavations (e.g., road cuts, quarries) in loose sediment or weathered / fractured rock. Frequent is the occurrence of landslides under the sea level in coastal areas.

Trees shake vigorously; branches may break and fall, trees may be uprooted, especially along steep slopes.

Liquefaction may be frequent in the epicentral area, depending on local conditions; the most typical effects are: sand boils up to ca. 1 m in diameter; apparent water fountains in still waters; localised lateral spreading and settlements (subsidence up to ca. 30 cm), with fissuring parallel to waterfront areas (river banks, lakes, canals, seashores).

In dry areas, dust clouds may rise from the ground in the epicentral area.

Stones and even small boulders and tree trunks may be thrown in the air, leaving typical imprints in soft soil.

IX - DESTRUCTIVE - Effects in the environment are a widespread source of considerable hazard and become important for intensity assessment

Primary Effects

observed commonly - Ground ruptures (surface faulting) develop, up to a few km long, with offsets generally in the order of several cm. Tectonic subsidence or uplift of the ground surface with maximum values in the order of a few decimeters may occur.

Secondary Effects - The total affected area is in the order of 1000 km²

Springs can change, generally temporarily, their flow-rate and/or location to a considerable extent. Some modest springs may even run dry. Temporary variations of water level are commonly observed in wells. Variations of chemical physical properties of water, most commonly temperature, are observed in springs and/or wells. Water turbidity is common in closed basins, rivers, wells and pings. Gas emissions, often sulphureous, are observed, and bushes and grass near emission ones may burn.

Meters high waves develop in still and running waters. In flood plains water streams may even change their course, also because of land subsidence. Small basins may appear or be emptied. Depending on shape of sea bottom and coastline, dangerous tsunamis may reach the shores with runups of up to several meters flooding wide areas. Widespread erosion and dumping of waste is observed along the beaches, where bushes and trees can be eradicated and drifted away.

Fractures up to 100 cm wide and up to hundreds metres long are commonly observed in loose alluvial deposits and/or saturated soils; in competent rocks they can reach up to 10 cm. Significant cracks are common in paved (asphalt or stone) roads, as well as small pressure undulations.

Landsliding is widespread in prone areas, also on gentle slopes; where equilibrium is unstable (steep slopes of loose / saturated soils; rock falls on steep gorges, coastal cliffs) their site is frequently large (10⁵ m³), sometimes very large (10⁶ m³). Landslides can dam narrow valleys causing temporary or even permanent lakes. Riverbanks, artificial embankments and excavations (e.g., road cuts, quarries) frequently collapse. Frequent are large landslides under the sea level.

Trees shake vigorously; branches and thin tree trunks frequently break and fall. Some trees might be uprooted and fall, especially along steep slopes.

Liquefaction and water upsurge are frequent; the most typical effects are: sand boils up to 3 m in diameter; apparent water fountains in still waters; frequent lateral spreading and settlements (subsidence of more than ca. 30 cm), with fissuring parallel to waterfront areas (river banks, lakes, canals, seashores).

In dry areas, dust clouds may rise from the ground.

Small boulders and tree trunks may be thrown in the air and move away from their site for meters, also depending on slope angle and roundness, leaving typical imprints in soft soil.

X - VERY DESTRUCTIVE - Effects on the environment become a leading source of hazard and are critical for intensity assessment

Primary Effects

Primary Effects become leading. Surface faulting can extend for few tens of km, with offsets from tens of cm up to a few meters. Gravity grabens and elongated depressions develop; for very shallow focus earthquakes in volcanic areas rupture lengths might be much lower. Tectonic subsidence or uplift of the ground surface with maximum values in the order of few meters may occur.

Secondary Effects - The total affected area is in the order of 5,000 km²

Many springs significantly change their flow-rate and/or elevation of outcrop. Some springs may run temporarily or even permanently dry. Temporary variations of water level are commonly observed in wells. Even strong variations of chemical-physical properties of water, most commonly temperature, are observed in springs and/or wells. Often water becomes very muddy in even large basins, rivers, wells and springs. Gas emissions, often sulphureous, are observed, and bushes and grass near emission zones may burn.

Meters high waves develop in even big lakes and rivers, which overflow from their beds. In flood plains rivers may change their course, temporary or even permanently, also because of widespread land subsidence. Basins may appear or be emptied. Depending on shape of sea bottom and coastline, tsunamis may reach the shores with runups exceeding 5 m flooding flat areas for thousands of meters inland. Small boulders can be dragged for many meters. Widespread deep erosion is observed along the shores, with noteworthy changes of the coastline profile. Trees nearshore are eradicated and drifted away.

Open ground cracks up to more than 1 m wide and up to hundred metres long are frequent, mainly in loose alluvial deposits and/or saturated soils; in competent rocks opening reaches several decimeters. Wide cracks develop in paved (asphalt or stone) roads, as well as pressure undulations.

Large landslides and rockfalls (> 10⁵ - 10⁶ m³) are frequent, practically regardless of equilibrium state of slopes, causing temporary or permanent barrier lakes. River banks, artificial embankments, and sides of excavations typically collapse. Levees and earth dams may also incur serious damage. Frequent are large landslides under the sea level in coastal areas.

Trees shake vigorously; many branches and tree trunks break and fall. Some trees might be uprooted and fall.

Liquefaction, with water upsurge and soil compaction, may change the aspect of wide zones; sand volcanoes even more than 6 m in diameter; vertical subsidence even > 1 m; large and long fissures due to lateral spreading are common.

In dry areas, dust clouds may rise from the ground.

Boulders (diameter in excess of 2-3 meters) can be thrown in the air and move away from their site for hundreds of meters down even gentle slopes, leaving typical imprints in soil.

XI - DEVASTATING - Effects on the environment become decisive for intensity assessment, due to saturation of structural damage

Primary Effects

Primary Effects are dominant. Surface faulting extends from several tens of km up to more than one hundred km, accompanied by slips reaching several meters. Gravity graben, elongated depressions and pressure ridges develop. Drainage lines can be seriously offset. Tectonic subsidence or uplift of the ground surface with maximum values in the order of numerous meters may occur.

Secondary Effects - The total affected area is in the order of 10,000 km²

Many springs significantly change their flow-rate and/or elevation of outcrop. Many springs may run temporarily or even permanently dry. Temporary or permanent variations of water level are generally observed in wells. Even strong variations of chemical-physical properties of water, most commonly temperature, are observed in springs and/or wells. Often water becomes very muddy in even large basins, rivers, wells and springs. Gas emissions, often sulphureous, are observed, and bushes and grass near emission zones may burn.

Large waves develop in big lakes and rivers, which overflow from their beds. In flood plains rivers can change their course, temporary or even permanently, also because of widespread land subsidence and landsliding. Basins may appear or be emptied. Depending on shape of sea bottom and coastline, tsunamis may reach the shores with runups reaching 15 meters and more devastating flat areas for kilometers inland. Even meter-sited boulders can be dragged for long distances. Widespread deep erosion is observed along the shores, with noteworthy changes of the coastal morphology. Trees nearshore are eradicated and drifted away.

Open ground cracks up to several meters wide are very frequent, mainly in loose alluvial deposits and/or saturated soils. In competent rocks they can reach 1 m. Very wide cracks develop in paved (asphalt or stone) roads, as well as large pressure undulations.

Large landslides and rock-falls (> 10⁵ - 10⁶ m³) are frequent, practically regardless of equilibrium state of slopes, causing many temporary or permanent barrier lakes. River banks, artificial embankments, and sides of excavations typically collapse. Levees and earth dams incur serious damage. Significant landslides can occur even at 200 - 300 km distance from the epicenter. Frequent are large landslides under the sea level in coastal areas.

Trees shake vigorously; many branches and tree trunks break and fall. Many trees are uprooted and fall.

Liquefaction changes the aspect of extensive zones of lowland, determining vertical subsidence possibly exceeding several meters; numerous large sand volcanoes, and severe lateral spreading can be observed.

In dry areas, dust clouds may rise from the ground.

Big boulders (diameter of several meters) can be thrown in the air and move away from their site for long distances down even gentle slopes, leaving typical imprints in soil.

XII - COMPLETELY DEVASTATING - Effects in the environment are the only tool for intensity assessment

Primary Effects

Primary Effects are dominant. Surface faulting is at least few hundreds of km long, accompanied by offsets reaching several tens of meters. Gravity graben, elongated depressions and pressure ridges develop. Drainage lines can be seriously offset. Landscape and geomorphological changes induced by primary effects can attain extraordinary extent and site (typical examples are the uplift or subsidence of coastlines by several meters, appearance or disappearance from sight of signcant landscape elements, rivers changing course, origination of waterfalls, formation or disappearance of lakes).

Secondary Effects - The total affected area is in the order of 50,000 km²

Many springs significantly change their flow-rate and/or elevation of outcrop. Temporary or permanent variations of water level are generally observed in wells. Many springs and wells may run temporarily or even permanently dry. Strong variations of chemical-physical properties of water, most commonly temperature, are observed in springs and/or wells. Water becomes very muddy in even large basins, rivers, wells and springs. Gas emissions, often sulphureous, are observed, and bushes and grass near emission zones may burn.

Giant waves develop in lakes and rivers, which overflow from their beds. In flood plains rivers change their course and even their flow direction, temporary or even permanently, also because of widespread land subsidence and landsliding. Large basins may appear or be emptied. Depending on shape of sea bottom and coastline, tsunamis may reach the sho¬res with runups of several tens of meters devastating flat areas for many kilometers inland. Big boulders can be dragged for long distances. Widespread deep erosion is observed along the shores, with outstanding changes of the coastal morphology. Many trees are eradicated and drifted away. All boats are tore from their moorings and swept away or carried onshore even for long distances. All people outdoor are swept away.

Ground open cracks are very frequent, up to one meter or more wide in the bedrock, up to more than 10 m wide in loose alluvial deposits and/or saturated soils. These may extend up to several kilometers.

Large landslides and rock-falls (> 10⁵ - 10⁶ m³) are frequent, practically regardless to equilibrium state of the slopes, causing many temporary or permanent barrier lakes. River banks, artificial embankments, and sides of excavations typically collapse. Levees and earth dams incur serious damage. Significant landslides can occur at more than 200 - 300 km distance from the epicenter. Frequent are very large landslides under the sea level in coastal areas.

Trees shake vigorously; many branches and tree trunks break and fall. Many trees are uprooted and fall.

Liquefaction occurs over large areas and changes the morphology of extensive flat zones, determining vertical subsidence exceeding several meters, widespread large sand volcanoes, and extensive severe lateral spreading can be observed.

In dry areas, dust clouds may rise from the ground.

Also very big boulders can be thrown in the air and move for long distances even down very gentle slopes, leaving typical imprints in soil.

Master Textual Chart

from Michetti et al. (2007)

Master Graphical Chart

from Amos Salamon

Surface Faulting vs. Intensity

from Michetti et al. (2007)

Environmental Effects vs. Intensity

from Michetti et al. (2007)

Correlation between ESI 2007 and Traditional Macroseismic Scales

In principle, the correlations of intensity scales, degree by degree, should be never allowed because each scale classifies the effects in a different way. Hence, for the comparison of two earthquakes it should be advisable to use the same intensity scale, even if it is necessary to reclassify all the effects. For instance, in the MSK64 scale the concepts of "typical" damage and building types are used. As a result this is a scale of constant intervals. The MCS and Modified Mercalli scales, based on maximum effects, are scales of order. As a consequence intensity VIII is much easier to get in original Mercalli than applying MSK64.

Indeed, the "classic" twelve degrees scales, though they included environmental effects, were not able to differentiate intensities above IX, because (a) they did not make difference between primary and secondary effects, (b) they did not use quantitative approach for the effects on nature. Therefore, it is expected that when we deal with the strongest earthquakes the application of the ESI 2007 scale will yield an intensity value that is different, and more physically meaningful, from that obtained with the others scales. That is exactly the reason why it is necessary to develop this new intensity scale.

As a matter of fact, in the practice of macro-seismic investigation, very often one is obliged to compare earthquakes intensities classified with different scales. This has promoted the use of conversion tables, such as those proposed by KRINITZSKY & CHANG (1978), REITER (1990), and PANZA (2004). On the other hand, the application of such kind of tables has often caused the introduction of additional uncertainties, such as the use of half-degrees or fractional degrees.

In order to avoid these inconveniences, the correlation among the most important intensity scales has to be simply based on one-to-one relationships. As discussed in MICHETTI et al. (2004), due to the level of uncertainty inherent in the structure itself of the macroseismic scales, and in case a conversion between scales is a step that cannot be absolutely avoided, the best we can do is to consider all the twelve degrees scales as equivalent. This includes also the Chinese macroseismic intensity scale, which has been originally designed to be consistent with the MM scale (e.g., XIE, 1957; WANG, 2004). Nevertheless, the correlation with the 7-degrees JMA intensity scale (KRINITZSKY & CHANG, 1977; REITER, 1990; HANCOX et al., 2002), and with other scales not based on twelve degrees, inevitably requires grouping of some intensity degrees.

Structure of the Scale

Introduction

The ESI 2007 scale has been developed to be consistent with the Modified Mercalli macroseismic scale (MM-31, WOOD & NEUMANN, 1931; MM-56, RICHTER, 1958) and the MSK-64 ( Medvedev-Sponheuer-Karnik scale), since these are the most applied worldwide and includes many explicit references to environmental effects.

More in general, the new scale was carefully designed in order to keep the internal consistency of the original twelve degrees scale, as discussed in depth by MICHETTI et al. (2004). A great deal of work in seismic hazard assessment is accomplished in the world, and intensity is a basic parameter in this. Any "new word" in this research field must not result in dramatic changes. The members of the WG are aware that, by definition, the twelve-degree macroseismic scales are based essentially on effects on humans in the range of intensity II to V, on damage in the range of intensity VI to IX, and on natural environment in the range of intensity X to XII. The ESI 2007 scale is therefore really useful only for the assessment of the highest intensities. But, as mentioned above, to avoid any confusion, the classical numbering is kept.

Main Groups of Intensity Degrees

The ESI 2007 scale starts where environmental effects become regularly observed in favorable conditions, i.e. at intensity IV. The scale is linear and works well up to XII degree. In the first version of the scale, intensity I, II and III were also defined using environmental effects (MICHETTI et al. (2004)). It is important to remark that several effects on nature, especially concerning water bodies and hydrogeological phenomena (MONTGOMERY & MANGA, 2003 and references therein), but also instrumentally-detected primary tectonic deformations (permanent fault offset measured at the INFN Gran Sasso, Italy, strain-meter; cf., AMORUSO & CRESCENTINI, 1999), have been observed for very low intensity. Perhaps future investigation will allow a new revision of the scale in order to include environmental effects suitable for intensity assessment in the range from I to III. However, after 4 years of application at a global scale through the INQUA scale project, it was clear that with the knowledge available today, effects on natural environment in this range are not diagnostic.

Therefore, comparing the ESI 2007 with the other 12 degrees scales, we can identify three main subsets:

From I to III: There are no environmental effects that can be used as diagnostic.

From IV to IX: Environmental effects are easily observable starting from intensity IV, and often permanent and diagnostic especially starting from intensity VII. However, they are necessarily less suitable for intensity assessment than effects on humans and manmade structures. Their use is therefore recommended especially in sparsely populated areas

From X to XII: Effects on humans and manmade structures saturate, while environmental effects become dominant; in fact, several types of environmental effects do not suffer saturation in this range. Thus, environmental effects are the most effective tool to evaluate the intensity.

Entire article

References

Articles and Books

Aki, K. and P. G. Richards (2002). Quantitative Seismology, Second Edition University Science Books.. AKIR

Bolt, B. A. (1999). Earthquakes. NewYork, W.H. Freeman and Company.. EQBB

Garfunkel, Ben-Avraham, and Kagan (2014). Dead Sea Transform Fault System: Reviews, Springer Netherlands, Dordrecht.. DSTF

Kramer, S. L. (1996). Geotechnical Earthquake Engineering, First Edition, Prentice Hall.. GTEQE

McCalpin, J. (1996). Paleoseismology, First Edition Academic Press.. PSMCO

McCalpin, J. P. (2009). Paleoseismology, Second Edition Elsevier Science.. PSMCN

Moczo, P., Kristek, J., and Galis, M. (2014) The Finite-Difference Modelling of Earthquake Motions Waves and Ruptures, Cambridge University Press.. FDMEQ

Scholz, C. H. (2019). The Mechanics of Earthquakes and Faulting, Third Edition Cambridge University Press.. MEQF

Segall, P. (2010). Earthquake and Volcano Deformation. United Kingdom: Princeton University Press.. EVD

Yeats, R. S. A., et al. (1997). The Geology of Earthquakes, Oxford University Press.

Websites

Focal Mechanisms

GHEA - Global Historical Earthquake Archive

AHEAD - European Archive of Historical Earthquake Data

DST Geomechanics

from Dead Sea Geomechanics

Earthquake Geomechanics Researchers

Christopher H. Scholz Lamont-Doherty Geological Observatory at Columbia University - Google Scholar

Christopher H. Scholz Lamont-Doherty Geological Observatory at Columbia University - ORCID

David Dempsey Univ. of Canterbury Christchurch New Zealand - Google Scholar

Emily Brodsky UC Santa Cruz - ORCID

Emily Brodsky UC Santa Cruz - Scopus

Paul Segall Stanford - Google Scholar

Ross Stein Temblor - Google Scholar

Ross Stein Temblor - Temblor.net

Artificial Intelligence and Machine Learning in Seismology

from Artificial Intelligence and Machine Learning in Seismology

Software

GeoMapApp

Digital Paleoseismic Trench Surveying (workflow) by Ian Pierce

Software and Applications at paleoseismicity.org

PEACH (Paleoseismic EArthquake CHronologies) at paleoseismicity.org

Data for "Deciphering past earthquakes from the probabilistic modelling of paleoseismic records – The Paleoseismic EArthquake CHronologies code (PEACH, version 1)" - Code

Data for "Deciphering past earthquakes from the probabilistic modelling of paleoseismic records – The Paleoseismic EArthquake CHronologies code (PEACH, version 1)" - Article

References

Arora, K., et al. (2011). Encyclopedia of Solid Earth Geophysics, Springer Netherlands.. ESEG

Allaby, M. (2013). A Dictionary of Geology and Earth Sciences, Oxford University Press.. DG

Nof et al (2017) Seismic data at the Seismological Division New Online Services - Geophysical Institute of Israel

References

Walker, M. (2013). Quaternary Dating Methods, Wiley.. MEQF

Buck, C. and M. Juarez (2017). Bayesian radiocarbon modelling for beginners.. BFB

Bronk Ramsey, C. (2016). "Bayesian Analysis of Radiocarbon Dates." Radiocarbon 51(1): 337-360.. BAY

Bronk Ramsey, C., et al. (2001). "‘Wiggle Matching’ Radiocarbon Dates." Radiocarbon 43(2A): 381-389.. WIG

BACON info

BACON Manual 2.3.9.1

R Studio login for BACONQUAKE, etc.

OxCal

OxCal Manual 4.4

References

Horowitz, A. (2001). The Jordan Rift Valley, A.A. Balkema Publishers.. JRV

Horowitz, A. (1979). The Quaternary of Israel, Academic Press.. QI

Enzel, Y. and O. Bar-Yosef (2017). Quaternary of the Levant, Cambridge University Press.. QL

References

Horowitz, A. (1992). Palynology of Arid Lands, Elsevier Science Limited.. PAL

Zohary, M. (1962). Plant life of Palestine : Israel and Jordan. New York, Ronald Press.. PLIPJ

Moore, P. D., et al. (1991). Pollen Analysis, Blackwell Scientific Publications.. PA

Sample Calculator for Palynology

1500 grains needed per layer for good statistics
Suzanne Leroy appears to get 1500 grains in 1-2 grams of Dead Sea Mud Layers
Sediment Density of 2.2 g/cc is assumed - will be replaced with a measurement

Variable	Input	Units	Notes
Mass Required		g
Sediment Density		g/cm³
Layer Thickness		cm.	choose minimum
Variable	Output	Units	Notes
Volume		cm³	necessary sample volume
Length		cm.	Required Minimum Sample Dimension
Width		cm.	Required Minimum Sample Dimension
Mass		g	Calculation Check

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