Surface waveform tomography of the Turkish-Iranian plateau

Maggi, Alessia; Priestley, Keith

doi:10.1111/j.1365-246x.2005.02505.x

Cited by 195 publications

(166 citation statements)

References 75 publications

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“…Further evidence for a thin lithosphere overlying hot and partially molten asthenospheric material beneath eastern Anatolia has been found in other P-and S-receiver function images Özacar et al, 2008;Vanacore et al, 2013). Other indications of a shallow LAB are strong attenuation of Lg and Sn phases (Gök et al, 2003) and relatively low Pn-and uppermost mantle S-velocities (Al-Lazki et al, 2004, Maggi andPriestley, 2005). The slow velocity anomaly was attributed to the ascending asthenosphere that is emplaced beneath the plateau following the detachment of the northward-subducting Arabian oceanic lithosphere (Keskin, 2003;Faccenna, 2003;Şengör et al, 2003;Biryol et al, 2011;Fichtner et al, 2013a, b).…”

Section: Introductionmentioning

confidence: 88%

“…Sodoudi et al (2006) found the northern Aegean LAB near 150 km depth. Additional indications of a thin lithosphere are strong Lg and Sn attenuation observations (Gök et al, 2003), and relatively low Sand Pn-wave velocity anomalies (e.g., Maggi and Priestley, 2005;Gök et al, 2007;Al-Lazki et al, 2004). A joint analysis of surface wave group velocities (Rayleigh and Love waves) and teleseismic receiver functions suggests that the average LAB depth is about 90 km in the Arabian plate and about 70 km in the Anatolian block (Gök et al, 2007).…”

Section: Lithosphere-asthenosphere Boundarymentioning

confidence: 99%

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Thickness of the lithosphere beneath Turkey and surroundings from S-receiver functions

et al. 2015

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Abstract. We analyze S-receiver functions to investigate variations of lithospheric thickness below the entire region of Turkey and surrounding areas. The teleseismic data used here have been compiled combining all permanent seismic stations which are open to public access. We obtained almost 12 000 S-receiver function traces characterizing the seismic discontinuities between the Moho and the discontinuity at 410 km depth. Common-conversion-point stacks yield wellconstrained images of the Moho and of the lithosphereasthenosphere boundary (LAB). Results from previous studies suggesting shallow LAB depths between 80 and 100 km are confirmed in the entire region outside the subduction zones. We did not observe changes in LAB depths across the North and East Anatolian faults. To the east of Cyprus, we see indications of the Arabian LAB. The African plate is observed down to about 150 km depth subducting to the north and east between the Aegean and Cyprus with a tear at Cyprus. We also observed the discontinuity at 410 km depth and a negative discontinuity above the 410, which might indicate a zone of partial melt above this discontinuity.

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Section: Introductionmentioning

confidence: 88%

Section: Lithosphere-asthenosphere Boundarymentioning

confidence: 99%

Thickness of the lithosphere beneath Turkey and surroundings from S-receiver functions

et al. 2015

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“…The difference in mantle structure between using the CMT and PDE locations in the inversion is small. Maggi & Priestley (2005) showed that artefacts due to event mislocation in the 3-D upper-mantle models were further minimized during the tomography.…”

Section: Extracting Structure Of the Upper Mantlementioning

confidence: 99%

A global horizontal shear velocity model of the upper mantle from multimode Love wave measurements

Ho¹,

Priestley²,

Debayle

2016

Geophys. J. Int.

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S U M M A R YSurface wave studies in the 1960s provided the first indication that the upper mantle was radially anisotropic. Resolving the anisotropic structure is important because it may yield information on deformation and flow patterns in the upper mantle. The existing radially anisotropic models are in poor agreement. Rayleigh waves have been studied extensively and recent models show general agreement. Less work has focused on Love waves and the models that do exist are less well-constrained than are Rayleigh wave models, suggesting it is the Love wave models that are responsible for the poor agreement in the radially anisotropic structure of the upper mantle. We have adapted the waveform inversion procedure of Debayle & Ricard to extract propagation information for the fundamental mode and up to the fifth overtone from Love waveforms in the 50-250 s period range. We have tomographically inverted these results for a mantle horizontal shear wave-speed model (β h (z)) to transition zone depths. We include azimuthal anisotropy (2θ and 4θ terms) in the tomography, but in this paper we discuss only the isotropic β h (z) structure. The data set is significantly larger, almost 500 000 Love waveforms, than previously published Love wave data sets and provides ∼17 000 000 constraints on the upper-mantle β h (z) structure. Sensitivity and resolution tests show that the horizontal resolution of the model is on the order of 800-1000 km to transition zone depths. The high wave-speed roots beneath the oldest parts of the continents appear to extend deeper for β h (z) than for β v (z) as in previous β h (z) models, but the resolution tests indicate that at least parts of these features could be artefacts. The low wave speeds beneath the mid-ocean ridges fade by ∼150 km depth except for the upper mantle beneath the East Pacific Rise which remains slow to ∼250 km depth. The resolution tests suggest that the low wave speeds at deeper depths beneath the East Pacific Rise are not solely due to vertical smearing of shallow, low wave speeds. Four prominent, low wave-speed features occur at transition zone depths-one aligned along the East African Rift, one centred south of the Indian peninsula, one located south of New Zealand and one in the south Pacific Ocean coinciding with the location of the South Pacific Superswell. The low wave-speed features south of New Zealand and south of the Indian peninsula correspond spatially with the two largest negative geoid lows on Earth.

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“…A significant number of publications have brought new insights on the current and Quaternary tectonics of the Zagros mountain belt (Nilforoushan et al 2003;Masson et al 2005;Vernant et al 2004;Walpersdorf et al 2006;Oveisi et al 2009) and on the deep geophysical settings beneath the Iranian plateau and the Zagros belt Maggi & Priestley, 2005;Paul et al 2006;Kaviani et al 2009;Hatzfeld & Molnar, 2010). Allen, Jackson & Walker (2004) pointed out that major reorganization of the ArabiaEurasia collision has occurred in the past 5 ± 2 Ma to account for the rates of motion along major active faults.…”

Section: Introductionmentioning

confidence: 99%

Timing of uplift in the Zagros belt/Iranian plateau and accommodation of late Cenozoic Arabia–Eurasia convergence

Mouthereau¹

2011

Geol. Mag.

145

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-The motion of Arabia was stable with respect to Eurasia over the past 22 Ma. Deformation and exhumation in the Zagros is seen to initiate at the same time as argued by new detrital thermochronologic constraints and increasing accumulation rates in synorogenic sediments. A recent magnetostratigraphic dating of the Bakhtyari conglomerates in the northern Fars region of the Zagros further suggests that shortening and uplift in the Zagros Folded Belt accelerated after 12.4 Ma. Available temporal constraints from surrounding collision belts indicate that shortening and uplift focused in regions bordering the Iranian plateau to the south between 15 and 5 Ma. As boundary velocity was kept constant this requires concomitant decreasing strain rates in the Iranian plateau. Slab detachment has been proposed to explain the observed changes as well as mantle delamination, but the insignificant change in the Arabian slab motion and lack of unambiguous constraints make both hypotheses difficult to account for. It is proposed based on a review of shortening estimates provided throughout the Arabia-Eurasia collision that the total 440 km of convergence predicted by geodesy and plate reconstruction over the past 22 Ma can be accounted for by distributed shortening. I suggest that the topography and expansion of the Iranian plateau over Late Miocene-Pliocene time can be reproduced by the progressive thickening of the originally thin Iranian continental lithosphere presumably thermally weakened during the Eocene extensional and magmatic event.

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Surface waveform tomography of the Turkish-Iranian plateau

Cited by 195 publications

References 75 publications

Thickness of the lithosphere beneath Turkey and surroundings from S-receiver functions

Thickness of the lithosphere beneath Turkey and surroundings from S-receiver functions

A global horizontal shear velocity model of the upper mantle from multimode Love wave measurements

Timing of uplift in the Zagros belt/Iranian plateau and accommodation of late Cenozoic Arabia–Eurasia convergence

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