Integrated 3D density modelling and segmentation of the Dead Sea Transform

Götze, Hans‐Jürgen; El‐Kelani, R.; Schmidt, Stefan; Rybakov, Michael; Hassouneh, M.; Förster, Hans‐Jürgen; Ebbing, J.

doi:10.1007/s00531-006-0108-4

Cited by 8 publications

(19 citation statements)

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“…Additionally, variations in long‐term lithospheric strength may also correspond with segmentation of the southern DSF. For example, Götze et al [2007] documented variations in long‐term, flexural rigidity (effective elastic thickness) along the southern DSF consistent with inferred seismogenic segmentation. Those authors found weaker elastic lithosphere around the Dead Sea (and areas northward) compared with the Wadi Araba region.…”

Section: Discussion and Tectonic Implicationsmentioning

confidence: 61%

GPS measurements of near-field deformation along the southern Dead Sea Fault System

Tarazi

Rajab

Gomez

et al. 2011

Geochem. Geophys. Geosyst.

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[1] Analysis of short-term deformation along the southern part of Dead Sea Fault (DSF) provides a systematic view of kinematics this part of the continental transform. The southern DSF consists of two principal segments: the Wadi Araba and Jordan Valley faults. In addition to other regional continuous GPS data, this study uses new data from 25 survey sites and 4 continuous GPS stations in Jordan for improved near-field observations. Resulting velocities are reported with 1-s uncertainties ranging from 0.4-1.0 mm/yr. Application of elastic dislocation models yields estimates of slip rates for Wadi Araba and Jordan Valley faults are 4.9 ± 0.4 mm/yr and 4.7 ± 0.4 mm/yr, respectively. Modeling also suggests different depths of effective fault locking with 15 ± 5 km and 8 ± 5 km for the Wadi Araba and Jordan Valley faults, respectively. These slip rates are generally consistent with the upper end of the range of slip rates estimated from late Quaternary geology. Spatial variations in effective fault locking generally correspond with a heterogeneous mantle lithosphere. A similar observation can be observed along the southern San Andreas Fault, and this may reflect the influence of heterogeneity in the uppermost mantle on crustal faulting processes.

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Section: Discussion and Tectonic Implicationsmentioning

confidence: 61%

GPS measurements of near-field deformation along the southern Dead Sea Fault System

Tarazi

Rajab

Gomez

et al. 2011

Geochem. Geophys. Geosyst.

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“…The effective elastic thickness (T e ) of the DSR flanks has been estimated as 11–12.5 km [ Basile and Allemand , ] and 10 km in the field area by Götze et al . []. These relatively low values indicate that the flexural wavelengths are similar or smaller than the 100–120 km wide zone bordering the DSR where most of the erosion has occurred.…”

Section: Discussionmentioning

confidence: 99%

Uplift and denudation history of the eastern Dead Sea rift flank, SW Jordan: Evidence from apatite fission track thermochronometry

et al. 2013

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The Dead Sea rift (DSR), developed along the Dead Sea transform plate boundary, is characterized by salient flanks and morphotectonic asymmetry. Apatite fission track thermochronology (AFT) along ~1200 m high vertical profiles in Neoproterozoic basement and overlying Cambrian sandstone in southwestern Jordan is used to reconstruct timing, magnitude, and rate of uplift and denudation of the eastern DSR flank and examine its relationship to rift development and its flank landscape. Time‐temperature models based on AFT data suggest three major Phanerozoic heating and cooling episodes, Late Paleozoic, Early Cretaceous, and Oligocene. The latest episode, on which this study focuses, indicates uplift of ~3.8±0.3 km under a moderate paleogeothermal gradient. About 40% of the uplift was tectonically driven with the remainder attributed to isostatic rebound in response to denudation and erosion. Models suggest that uplift commenced in the Oligocene with a considerable part occurring prior to development of the DSR, despite being ~200 km from the Red Sea‐Gulf of Suez rift margin. Uplift is probably part of a regional rearrangement along the western Arabian platform margin occurring at the time of Red Sea rift initiation. Transition from primarily sedimentary layer stripping, most likely by scarp retreat, to one of dominantly incision of the underlying crystalline basement occurred in Late Miocene‐Pliocene time following enhanced subsidence and development of a low base level in the DSR. Consequently, the magnitude of uplift by isostatic rebound due to incision exceeded lowering by surface truncation and increased summit elevation and riftward flexing of the flank.

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“…About 5 km east of the AF, several small outcrops of Cretaceous sediments (sticking out of the recent deposits) confirm that here the basement is shallower than 1 km. Furthermore, the gravity anomalies along the seismic section show [ Tašárová et al , 2006; Götze et al , 2006] that no significant structural depression was crossed.…”

Section: Discussionmentioning

confidence: 99%

The shallow velocity structure across the Dead Sea Transform fault, Arava Valley, from seismic data

et al. 2007

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[1] Tomographic inversion techniques were applied to first-arrival traveltimes of refracted P waves to study the shallowest part of the crust in the vicinity of the Arava Fault (AF), the Dead Sea Transform (DST) segment between the Dead Sea and the Red Sea; tomographic inversion techniques were applied to first-arrival traveltimes of refracted P waves. A 100-km-long seismic line was centered on and oriented approximately perpendicular to the AF. A large number of P wave traveltimes from vibroseis and explosive shots (>280,000) were picked manually and used to invert for shallow P wave velocity structure. The regularized inversion approach (Zelt and Barton, 1998) was used for the tomographic inversion of the traveltimes. Extensive testing of model and inversion parameters was carried out to derive a reliable P wave velocity model. Complementary checker-board tests indicate that depending on the size of velocity homogeneities, the velocity structure is well resolved down to a depth of several kilometers. This model represents the first shallow P wave velocity across the whole width of the DST system, showing features that correlate well with surface geology and also some buried structures. The model further suggests that the AF extends vertically downward to at least 3 km. The observed variation in upper-crustal velocity implies the existence of a simple deformation compatible with a large lateral fault offset. From this model, a structural and dynamic interpretation of the DST system is then presented. The depth extension and geometry of several additional major faults and DST-associated shallow sedimentary basins were successfully imaged through the integration of the well-known surface geology and nearby boreholes. This work again confirms the DST as a typical transform fault system with a dominant strike-slip motion confined to a narrow zone.Citation: Ryberg, T., M. H. Weber, Z. Garfunkel, and Y. , The shallow velocity structure across the Dead Sea Transform fault, Arava Valley, from seismic data,

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Integrated 3D density modelling and segmentation of the Dead Sea Transform

Cited by 8 publications

References 0 publications

GPS measurements of near-field deformation along the southern Dead Sea Fault System

GPS measurements of near-field deformation along the southern Dead Sea Fault System

Uplift and denudation history of the eastern Dead Sea rift flank, SW Jordan: Evidence from apatite fission track thermochronometry

The shallow velocity structure across the Dead Sea Transform fault, Arava Valley, from seismic data

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