What is/are Uppermost Mantle?
Uppermost Mantle - We apply the wave equation dispersion spectrum inversion to three real datasets of different scales: tens of meters scale active-source data for estimating shallow targets, tens of kilometers scale ambient noise data for reservoir characterization and a continental-scale seismic array data for imaging the crust and uppermost mantle. [1] The resistivity model shows a well-developed shallow low-resistivity zone in the west of Changliu-Xiangou Fault corresponding to the Fushan depression, two high conductors in the depths of ~5–12 km, and a relatively low resistivity layer in the lower crust and uppermost mantle. [2] Here, we show results of newly reprocessed deep reflection seismic data of the PolandSPAN™ survey, portraying the whole crust and uppermost mantle in SE Poland. [3] These estimates are significantly deeper than the Moho, suggesting the uppermost mantle is ferromagnetic for these cold and old cratonic regions. [4] Pressure–temperature diagrams show to what extent these hypocentral conditions match the thermodynamic stability limits for minerals typical of the uppermost mantle, oceanic crust and lower continental crust. [5] Between the north and south islands, obvious high-Vs anomalies exist in the uppermost mantle down to a depth of ∼100–150 km beneath the Atlantic Ocean, whereas obvious low-Vs anomalies exist in the uppermost mantle beneath the volcanic islands including the active Fogo volcano. [6] Within thick lithosphere, and especially on its edges, the entire crust may be seismogenic, with earthquakes sometimes extending into the uppermost mantle if the Moho is colder than 600°C, but the continental mantle is generally aseismic. [7] 5) occur actively in the uppermost mantle. [8] The analyses obtained from these two techniques is jointly inverted to determine the 1-D S-wave velocity structure of crust and uppermost mantle for each station. [9] Ophiolites, which provide a window into the uppermost mantle, contain dunite bodies often interpreted as relics of melt flow conduits, formed by pyroxene dissolution during melt-peridotite interaction. [10] For the Taiyuan Basin, Linfen Basin, and Yuncheng Basin in the central and southern parts, the structure is dominant by slow materials in the upper crust but changes to strong high-velocity anomalies in the lower crust and the uppermost mantle at depth deeper than 25 km. [11] We investigate the scattering attenuation characteristics of the Martian crust and uppermost mantle to understand the structure of the Martian interior. [12] For more than half a century, exploring a complete sequence of the oceanic crust from the seafloor through the Mohorovicic discontinuity (Moho) and into the uppermost mantle has been one of the most challenging missions of scientific ocean drilling. [13] The area east of about 13° E is known to have been affected by severe late-stage modifications of the structure of crust and uppermost mantle during the Miocene when the ALCAPA (Alpine, Carpathian, Pannonian) block was subject to E-directed lateral extrusion. [14] Two clusters occurred between ~10 km to ~16 km depth below sea surface, within the lower crust and uppermost mantle. [15]The present-day structure of the lithosphere and uppermost mantle of Northern Apennines and Dinarides region results from a complex tectonic scenario mainly driven by subduction of Tethyan oceanic domains.
[16] The inversion is regularized towards an initial model constructed from an a priori model of the crust and uppermost mantle and a standard earth model beneath. [17] They display negative anomalies along ridges in the uppermost mantle, but those are stronger than for regularized inversions. [18] Firstly, a high-velocity zone is found in the uppermost mantle (50–150 km) beneath the Southeast China; its location is comparable to the distribution of the Cretaceous igneous rocks. [19] We find strong positive radial anisotropy (ξ > 1) across the entire region in the middle to lower crust and uppermost mantle. [20] For the major part of the considered territory, the same relation between the CPD and Moho depths is observed, except for two areas at the Siberian Platform and the Vitim volcanic field, where the uppermost mantle is magnetic. [21] Our seismic images highlight a strong correlation between the basalt geochemistry and upper-mantle seismic velocity structure: Sodic volcanoes are all characterized by prominent low seismic velocities in the uppermost mantle, while potassic volcanoes still possess a normal but thin upper-mantle “lid” depicted by high seismic velocities. [22] Previous seismological investigations suggest that anelasticity and velocity variations exhibit strong sensitivity to temperature anomalies in the uppermost mantle (Anderson, 1967; Faul & Jackson, 2005; Goes et al. [23] In the northern sections of the East Africa Rift System, earthquakes are confined to the upper crust shallower than ∼15 km, but in the southern and western sections of the rift, we observe earthquakes occurring much deeper, into the lower crust and potentially the uppermost mantle. [24] Most of the information in the models is associated with a few features: large low-shear-velocity provinces (LLSVPs) in the lowermost mantle, subduction signals and low-velocity anomalies likely associated with mantle plumes in the upper and lower mantle, and ridges and cratons in the uppermost mantle. [25] (2019) presented 3D seismic velocity models (VP and VS) of crust and uppermost mantle of continental China using seismic body-wave travel-time tomography, which are referred to as Unified Seismic Tomography Models for Continental China Lithosphere 1. [26] Deep low-frequency earthquakes (DLFs) beneath volcanoes are possible evidence for deep-seated magmatic activity in the mid-to-lower crust and uppermost mantle. [27] In the basin, earthquake clusters occur in the lower crust and uppermost mantle and are related to re-activated, inverted, normal faults created during rifting. [28] Preliminary results show that extrinsic is responsible for an increase of the upwelling speed of hot material from the lowermost mantle, different convective cell shapes, and deflection of mantle plumes at the uppermost mantle. [29] Episodes of high-flux granitoid magmatism in the upper crust occur as orogenic compressive stress wanes from peak values, permitting escape of buoyant magmas from long-term storage in stress traps in the deeper crust (or uppermost mantle). [30] Utilizing ∼4 yr of new broadband seismic data, we imaged the structure of the crust through the uppermost mantle. [31] Where and how melt is stored in the crust and uppermost mantle is important for understanding the dynamics of magmatic plumbing systems and the evolution of rifting. [32] In this study, we aim at building a high-resolution CVM (both VP and VS) of the crust and uppermost mantle in southwest China along with earthquake locations by joint inversion of body- and surface-wave travel-time data. [33] In this work, we have obtained tomographic images of the crust and uppermost mantle using inversion of Rayleigh waveform data to augment information about the subsurface gleaned by previous works. [34] Our preliminary findings from the harmonic decomposition technique performed on radial and tangential RFs suggest relatively more substantial anisotropic signals in the lower crust and uppermost mantle with respect to upper and middle crustal structure in the region. [35]shear wave velocity
We have successfully derived a new 3-D high resolution shear wave velocity model of the crust and uppermost mantle of a large part of W-Europe from transdimensional ambient-noise tomography. [1] We present an improved 3-D shear wave velocity image of the uppermost mantle beneath the Bay of Bengal (BoB), the Bengal basin and the adjoining Indian shield to their west. [2] The uppermost mantle shear wave velocity beneath the Indian shield is hitherto not known. [3] We present a 3-D probabilistic model of shear wave velocity and radial anisotropy of the crust and uppermost mantle of Europe, focusing on the mountain belts of the Alps and Apennines. [4] In this study, we present a high-resolution crustal and uppermost mantle 3-D shear-wave velocity (Vs) model of Myanmar to fill this knowledge gap, using ambient noise data from newly deployed seismic arrays. [5] In this study, we used receiver function technique to determine the shear wave velocity profile of the crust and uppermost mantle beneath the eastern part of Indonesia region. [6] The uppermost mantle shear wave velocity ranges between 3. [7] Here we present a 3‐D absolute shear wave velocity model of the crust and uppermost mantle of the northern EAR generated from ambient noise tomography. [8]