The<i>S</i>receiver functions: synthetics and data example

Yuan, Xiaohui; Kind, R.; Li, Xueqing; Wang, Rongjiang

doi:10.1111/j.1365-246x.2006.02885.x

Cited by 197 publications

(186 citation statements)

References 38 publications

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“…Another important step in receiver function processing is the migration from the time domain into the depth domain using a known velocity model. For migration, the seismic energy is back-projected along the ray path within a given model and stacked, assuming that the energy is distributed in the Fresnel zone (Jones and Phinney, 1998;Kosarev et al, 1999;Yuan et al, 2006). The onedimensional IASP91 reference model is used for moveout correction and migration.…”

Section: Methodsmentioning

confidence: 99%

“…We use the S-receiver function technique (meaning S-to-P conversions) to image seismic discontinuities between the crust-mantle boundary (Moho) and the seismic discontinuity at 410 km depth (see, e.g., Yuan et al, 2006, or Kind et al, 2012, for a description of the technique). The receiver function method determines the response of the Earth structure below a seismic station.…”

Section: Methodsmentioning

confidence: 99%

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Structure of the upper mantle in the north-western and central United States from USArray S-receiver functions

et al. 2015

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Abstract. We used more than 40 000 S-receiver functions recorded by the USArray project to study the structure of the upper mantle between the Moho and the 410 km discontinuity from the Phanerozoic western United States to the cratonic central US. In the western United States we observed the lithosphere-asthenosphere boundary (LAB), and in the cratonic United States we observed both the midlithospheric discontinuity (MLD) and the LAB of the craton. In the northern and southern United States the western LAB almost reaches the mid-continental rift system. In between these two regions the cratonic MLD is surprisingly plunging towards the west from the Rocky Mountain Front to about 200 km depth near the Sevier thrust belt. We interpret these complex structures of the seismic discontinuities in the mantle lithosphere as an indication of interfingering of the colliding Farallon and Laurentia plates. Unfiltered S-receiver function data reveal that the LAB and MLD are not single discontinuities but consist of many small-scale laminated discontinuities, which only appear as single discontinuities after longer period filtering. We also observe the Lehmann discontinuity below the LAB and a velocity reduction about 30 km above the 410 km discontinuity.

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Section: Methodsmentioning

confidence: 99%

Section: Methodsmentioning

confidence: 99%

Structure of the upper mantle in the north-western and central United States from USArray S-receiver functions

et al. 2015

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“…However, S wave receiver functions introduce additional data-processing complexities. Careful data culling and time windowing are required to avoid contamination by secondary S wave arrivals near the 84 S-SKS crossover distance [Wilson et al, 2006;Yuan et al, 2006]. Prior to deconvolution, the culled S wave traces are time-reversed to account for the precursory nature of S p scattering.…”

Section: Scattered Wave Imagingmentioning

confidence: 99%

A rootless rockies—Support and lithospheric structure of the Colorado Rocky Mountains inferred from CREST and TA seismic data

Hansen

Dueker

Stachnik

et al. 2013

Geochem Geophys Geosyst

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[1] Support for the Colorado high topography is resolved using seismic data from the Colorado Rocky Mountain (CRM) Experiment and Seismic Transects. The average crustal thickness, derived from P wave receiver function imaging, is 48 km. However, a negative correlation between Moho depth and elevation is observed, which negates Airy-Heiskanen isostasy. Shallow Moho (<45 km depth) is found beneath some of the highest elevations, and therefore, the CRM are rootless. Deep Moho (45-51 km) regions indicate structure inherited from the Proterozoic assembly of the continent. Shear wave velocities from surface wave tomography are mapped to density employing empirical velocity-to-density relations in the crust and mantle temperature modeling. Predicted elastic plate flexure and gravity fields derived from the density model agree with observed long-wavelength topography and Bouguer gravity. Therefore, lowdensity crust and mantle are sufficient to support much of the CRM topography. Centers of Oligocene volcanism, e.g., the San Juan Mountains, display reduced crustal thicknesses and lowest average crustal velocities, suggesting that magmatic modification strongly influenced modern lithospheric structure and topography. Mantle velocities span 4.02-4.64 km/s at 73-123 km depth, and peak lateral temperature variations of 600 C are inferred. S wave receiver function imaging suggests that the lithosphereasthenosphere boundary is 100-150 km deep beneath the Colorado Plateau, and 150-200 km deep beneath the High Plains. A region of negative arrivals beneath the CRM above 100 km depth correlates with low mantle velocities and is interpreted as thermally modified/metasomatized lithosphere resulting from Cenozoic volcanism.

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“…The P receiver function technique is a conventional seismic method routinely used to investigate the Earth's structure. A description of the more recent S receiver function technique can be found; e.g., in Yuan et al (21). The essential point of this technique is that seismic waves from far away penetrate the Tibetan plateau from below.…”

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confidence: 99%

The boundary between the Indian and Asian tectonic plates below Tibet

Zhao

Yuan

Liu

et al. 2010

Proc. Natl. Acad. Sci. U.S.A.

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359

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The fate of the colliding Indian and Asian tectonic plates below the Tibetan high plateau may be visualized by, in addition to seismic tomography, mapping the deep seismic discontinuities, like the crust-mantle boundary (Moho), the lithosphere-asthenosphere boundary (LAB), or the discontinuities at 410 and 660 km depth. We herein present observations of seismic discontinuities with the P and S receiver function techniques beneath central and western Tibet along two new profiles and discuss the results in connection with results from earlier profiles, which did observe the LAB. The LAB of the Indian and Asian plates is well-imaged by several profiles and suggests a changing mode of India-Asia collision in the east-west direction. From eastern Himalayan syntaxis to the western edge of the Tarim Basin, the Indian lithosphere is underthrusting Tibet at an increasingly shallower angle and reaching progressively further to the north. A particular lithospheric region was formed in northern and eastern Tibet as a crush zone between the two colliding plates, the existence of which is marked by high temperature, low mantle seismic wavespeed (correlating with late arriving signals from the 410 discontinuity), poor Sn propagation, east and southeast oriented global positioning system displacements, and strikingly larger seismic (SKS) anisotropy.Tibetan lithosphere | receiver functions | anisotropy I t has long been recognised that the Tibetan plateau was created by the collision of the northward moving Indian plate and the relatively stationary Asian plate, which began about 50 million yr ago (1). However, the mode of deformation of the mantle lithospheres (2) remained largely unknown. A fundamental question is whether the postcollision convergence of India and Asia, estimated at >2;000 km (3, 4), was accommodated by homogeneous thickening or plate subduction (2). Global positioning systems (GPS) measurements have shown that at present an eastward motion dominates the surface deformation of northern and eastern Tibet (5). GPS and seismic anisotropy (6) indicate extrusion also of the deep Tibetan lithosphere to the east and southeast. Most surface wave studies revealed a thick lithosphere beneath much of the plateau (7-12), whereas body wave tomography observed the subducted Indian mantle lithosphere characterized by high wavespeed, in contrast to the Asian mantle lithosphere (13-15). Recently a high resolution P travel time tomographic study (15) imaged the high velocity Indian lithosphere in western Tibet below the entire plateau down to 300-400 km depth. In eastern Tibet, however, the front of the Indian plate is located south of the Yarlong-Zangbo Suture (YZS) (15). Relatively slow wave speeds are found in the upper mantle below the central and northeastern parts of the plateau. Modeling indicates that the Tibetan part of the lithosphere originated from the progressive accretion of a number of continental or island-arc type blocks before India came into direct contact with Asia (16) or stepwise subduction of the Asian pl...

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TheSreceiver functions: synthetics and data example

Cited by 197 publications

References 38 publications

Structure of the upper mantle in the north-western and central United States from USArray S-receiver functions

Structure of the upper mantle in the north-western and central United States from USArray S-receiver functions

A rootless rockies—Support and lithospheric structure of the Colorado Rocky Mountains inferred from CREST and TA seismic data

The boundary between the Indian and Asian tectonic plates below Tibet

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