Comment on “Improved inversion for seismic structure using transformed, <i>S</i>‐wavevector receiver functions: Removing the effect of the free surface” by Anya Reading, Brian Kennett, and Malcolm Sambridge

Svenningsen, L.; Jacobsen, Bo Holm

doi:10.1029/2004gl021413

Cited by 20 publications

(16 citation statements)

References 6 publications

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“…Data are filtered with a low‐pass filter with a corner frequency of 1 Hz. The vertical and radial components are then rotated into P and SV components, that are defined to be orthogonal to each other [e.g., Svenningsen and Jacobsen , 2004], using the incidence angle of the teleseismic reference phases. Here we search for the optimal angle of rotation such that the amplitude of the P ( SV ) component in case of PRF (SRF) is minimized at zero time, the arrival time of the reference phase P ( S ).…”

Section: Methodology and Datamentioning

confidence: 99%

Imaging the seismic lithosphere-asthenosphere boundary of the oceanic plate

Kumar¹,

Kawakatsu

2011

Geochem. Geophys. Geosyst.

104

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[1] The seismic lithosphere-asthenosphere boundary (LAB) or G discontinuity, a seismologically characterized abrupt drop in wave speed in the uppermost mantle, is one of the key issues in current geodynamics. Although plate tectonics started as a theory for the ocean, reports on LAB for normal oceanic regions are scarce due to paucity of seismic data, and whether or not the oceanic LAB grows with age is the key issue to be resolved. We conduct a systematic survey for the oceanic LAB using S-to-p converted seismic waves along three margins of oceanic plates whose crustal age ranges from ∼10 Myr to ∼130 Myr, and we observe laterally continuous oceanic LAB images. The thickness of the oceanic plate estimated from LABs increases with the plate age, though scattered, suggesting that the evolution of oceanic lithosphere is predominantly governed by temperature and that the oceanic seismic LAB represents a boundary that grows with age.

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Section: Methodology and Datamentioning

confidence: 99%

Imaging the seismic lithosphere-asthenosphere boundary of the oceanic plate

Kumar¹,

Kawakatsu

2011

Geochem. Geophys. Geosyst.

104

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“…The receiver function is computed by deconvolution of the Q-component with the filter which "spikes" the L-component. Thus, the receiver function approximates the arriving S-wave for an impulsive incoming P-wave (Vinnik, 1977;Svenningsen and Jacobsen, 2004).…”

Section: Appendix a Receiver Function Analysis In Southern Norwaymentioning

confidence: 99%

The evolution of western Scandinavian topography: A review of Neogene uplift versus the ICE (isostasy–climate–erosion) hypothesis

Nielsen

Gallagher

Leighton

et al. 2009

Journal of Geodynamics

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179

233

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a b s t r a c tTectonics and erosion are the driving forces in the evolution of mountain belts, but the identification of their relative contributions remains a fundamental scientific problem in relation to the understanding of both geodynamic processes and surface processes. The issue is further complicated through the roles of climate and climatic change. For more than a century it has been thought that the present high topography of western Scandinavia was created by some form of active tectonic uplift during the Cenozoic. This has been based mainly on the occurrence of surface remnants and accordant summits at high elevation believed to have been graded to sea level, the inference of increasing erosion rates toward the present-day based on the age of offshore erosion products and the erosion histories inferred from apatite fission track data, and on over-burial and seaward tilting of coast-proximal sediments.In contrast to this received wisdom, we demonstrate here that the evidence can be substantially explained by a model of protracted exhumation of topography since the Caledonide Orogeny. Exhumation occurred by gravitational collapse, continental rifting and erosion. Initially, tectonic exhumation dominated, although erosion rates were high. The subsequent demise of onshore tectonic activity allowed slow erosion to become the dominating exhumation agent. The elevation limiting and landscape shaping activities of wet-based alpine glaciers, cirques and periglacial processes gained importance with the greenhouse-icehouse climatic deterioration at the Eocene-Oligocene boundary and erosion rates increased. The flattish surfaces that these processes can produce suggest an alternative to the traditional tectonic interpretation of these landscape elements in western Scandinavia. The longevity of western Scandinavian topography is due to the failure of rifting processes in destroying the topography entirely, and to the buoyant upward feeding of replacement crustal material commensurate with exhumation unloading.We emphasize the importance of differentiating the morphological, sedimentological and structural signatures of recent active tectonics from the effects of long-term exhumation and isostatic rebound in understanding the evolution of similar elevated regions.

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“…In theory, the P-SV-SH transformation is an improvement over L-Q-T as it further prevents leakage of the converted waves into the incident signal, and it suppresses the signal associated with reflections at the free surface (Reading et al 2003). In practice, however, the difference between these two transformations is not always significant as it may be superseded by the effects caused by departure from the assumed 1-D geometry and errors in the estimates of near-surface velocity (Svenningsen and Jacobsen 2004). In any of these transformations, the presence of coherent signal on the transverse component, i.e., T or SH, indicates that the imaged structure does not conform to the assumed 1-D geometry and isotropic behaviour-it is indicative of anisotropy, dipping layers, and 2-D or 3-D scatterers.…”

Section: Partitioning Of the Signalmentioning

confidence: 99%

Upper Mantle Imaging with Array Recordings of Converted and Scattered Teleseismic Waves

2009

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This paper provides a review of array-based imaging techniques that use converted and scattered teleseismic waves. It addresses various aspects of the imaging process, from the preprocessing of the data to the application of the imaging algorithms. The reviewed techniques form a continuum with respect to the level of complexity adopted in the treatment of the scattering problem. On one end of the spectrum, images may be produced by simple stacking of normalized P-to-S conversion records (i.e., receiver functions), which are binned according to station or common conversion points (CCP) and mapped to depth. Finer resolution can be achieved through the stacking of singly scattered wavefields along diffraction hyperbolae to recover relative scattering intensity/potential at individual points through a 2-D or 3-D model space. Moving to higher levels of complexity, we find methods that involve inversion/backprojection of scattered teleseismic wavefield to recover estimates of localized material property perturbations with respect to an a priori background model.

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Comment on “Improved inversion for seismic structure using transformed, S‐wavevector receiver functions: Removing the effect of the free surface” by Anya Reading, Brian Kennett, and Malcolm Sambridge

Cited by 20 publications

References 6 publications

Imaging the seismic lithosphere-asthenosphere boundary of the oceanic plate

Imaging the seismic lithosphere-asthenosphere boundary of the oceanic plate

The evolution of western Scandinavian topography: A review of Neogene uplift versus the ICE (isostasy–climate–erosion) hypothesis

Upper Mantle Imaging with Array Recordings of Converted and Scattered Teleseismic Waves

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