An S receiver function analysis of the lithospheric structure in South America

Heit, B.; Sodoudi, F.; Yuan, Xiaohui; Bianchi, Marcelo; Kind, R.

doi:10.1029/2007gl030317

Cited by 106 publications

(131 citation statements)

References 22 publications

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“…This might be due to the fact that the observations are more representative of the islands. The LAB depth found below RPN is consistent with the results obtained earlier from S receiver functions (Heit et al, 2007;Li, et al, 2003). This study suggests that the numerical value corresponding to the negative discontinuity below RPN might correspond to an oceanic LAB.…”

Section: Rano Kau Ridge (Rpn) and Macquarie Ridge (Mcq)supporting

confidence: 81%

“…2, 4 and 5) show an additional negative phase for stations RPN, ROSA and ASCN. We interpret the shallower LVLs as conversions from the LAB, since they are consistent with previous receiver function studies (Li et al, 2003;Heit et al, 2007;Rychert and Shearer, 2009 etc.). These values are close to those predicted by the cooling model for the ocean lithosphere.…”

Section: Sub-lithospheric Low-velocity Layersupporting

confidence: 70%

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Seismic structure of the lithosphere and upper mantle beneath the ocean islands near mid-oceanic ridges

Haldar

Kumar

2014

Solid Earth

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Abstract. Deciphering the seismic character of the young lithosphere near mid-oceanic ridges (MORs) is a challenging endeavor. In this study, we determine the seismic structure of the oceanic plate near the MORs using the P -to-S conversions isolated from quality data recorded at five broadband seismological stations situated on ocean islands in their vicinity. Estimates of the crustal and lithospheric thickness values from waveform inversion of the P -receiver function stacks at individual stations reveal that the Moho depth varies between ∼ 10 ± 1 km and ∼ 20 ± 1 km with the depths of the lithosphere-asthenosphere boundary (LAB) varying between ∼ 40 ± 4 and ∼ 65 ± 7 km. We found evidence for an additional low-velocity layer below the expected LAB depths at stations on Ascension, São Jorge and Easter islands. The layer probably relates to the presence of a hot spot corresponding to a magma chamber. Further, thinning of the upper mantle transition zone suggests a hotter mantle transition zone due to the possible presence of plumes in the mantle beneath the stations.

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Section: Rano Kau Ridge (Rpn) and Macquarie Ridge (Mcq)supporting

confidence: 81%

Section: Sub-lithospheric Low-velocity Layersupporting

confidence: 70%

Seismic structure of the lithosphere and upper mantle beneath the ocean islands near mid-oceanic ridges

Haldar

Kumar

2014

Solid Earth

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“…2;Whitman et al 1992;Whitman 1994;Dorbath et al 1993;Beck et al 1996;Beck and Zandt 2002;Lyon-Caen et al 1985;Watts et al 1995;Stewart and Watts 1997;Myers et al 1998;Yuan et al 2000Yuan et al , 2002Tassara 2005;Heit et al 2007;Pérez-Gussinyé et al 2008;Tassara and Echaurren 2012). These show that the high Andes form a broad region, ϳ500 km wide, where the thick crust is up to 75 km thick, but the lithosphere is less than 100 km thick.…”

Section: Lithospheric Profilesmentioning

confidence: 84%

Cenozoic uplift of the Central Andes in northern Chile and Bolivia—reconciling paleoaltimetry with the geological evolution

Lamb

2016

Can. J. Earth Sci.

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Abstract:The Cenozoic geological evolution of the Central Andes, along two transects between ϳ17.5°S and 21°S, is compared with paleo-topography, determined from published paleo-altimetry studies. Surface and rock uplift are quantified using simple 2-D models of crustal shortening and thickening, together with estimates of sedimentation, erosion, and magmatic addition. Prior to ϳ25 Ma, during a phase of amagmatic flat-slab subduction, thick-skinned crustal shortening and thickening (nominal age of initiation ϳ40 Ma) was focused in the Eastern and Western Cordilleras, separated by a broad basin up to 300 km wide and close to sea level, which today comprises the high Altiplano. Surface topography at this time in the Altiplano and the western margin of the Eastern Cordillera appears to be ϳ1 km lower than anticipated from crustal thickening, which may be due to the pull-down effect of the subducted slab, coupled to the overlying lithosphere by a cold mantle wedge. Oligocene steepening of the subducted slab is indicated by the initiation of the volcanic arc at ϳ27-25 Ma, and widespread mafic volcanism in the Altiplano between 25 and 20 Ma. This may have resulted in detachment of mantle lithosphere and possibly dense lower crust, triggering 1-1.5 km of rapid uplift (over Ͻ Ͻ5 Myrs) of the Altiplano and western margin of the Eastern Cordillera and establishing the present day lithospheric structure beneath the high Andes. Since ϳ25 Ma, surface uplift has been the direct result of crustal shortening and thickening, locally modified by the effects of erosion, sedimentation, and magmatic addition from the mantle. The rate of crustal shortening and thickening varies with location and time, with two episodes of rapid shortening in the Altiplano, lasting <5 Myrs, that are superimposed on a long-term history of ductile shortening in the lower crust, driven by underthrusting of the Brazilian Shield on the eastern margin.

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“…In our case, the Moho depth along 21˚ is from receiver function data (Yuan et al, 2000 andHeit et al, 2007 andWoelbern et al, 2007).…”

Section: Preparation Of the Residualsmentioning

confidence: 99%

“…We define the top of the subducted slab as an envelope of seismicity (hypocenters) located by Engdahl et al (1998) (Figure 8A). The shape of the slab is also defined by receiver function data from the ReFuCA dataset Heit et al, 2007;Woelbern et al, 2007). The thickness of the oceanic lithosphere was fixed at ~100 km according to a worldwide plot of age versus thickness for oceanic lithosphere from Turcotte and Schubert (1982).…”

Section: Reconstruction Of Slabmentioning

confidence: 99%

More constraints to determine the seismic structure beneath the Central Andes at 21°S using teleseismic tomography analysis

Heit¹,

Koulakov²,

Asch³

et al. 2008

Journal of South American Earth Sciences

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A set of seismological stations was deployed in the Central Andes region along a ~600 km long profile at 21°S between Chile and Bolivia and operated for a period of almost two years, from March 2002 to January 2004. Here we present the results of the tomographic inversion for P-wave velocity anomalies, based on teleseismic data recorded at the stations. The reliability of the results has been checked by a series of synthetic tests. The tomographic images show high-velocities on the west of the profile that are indicative of cold material from the fore-arc. A low-velocity anomaly is detected at the border between the fore-and the volcanic arc where the Quebrada Blanca seismic anomaly was previously described. This anomaly might be related to the presence of fluids that originate at the cluster of earthquakes at a depth of ~100 km in the subducted plate. A strong low-velocity anomaly is detected beneath the entire Altiplano plateau and part of the Eastern Cordillera, in agreement with previous receiver function results. The Brazilian Shield is thought to be responsible for the strong high-velocity anomaly underneath the Interandean and Subandean regions.

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An S receiver function analysis of the lithospheric structure in South America

Cited by 106 publications

References 22 publications

Seismic structure of the lithosphere and upper mantle beneath the ocean islands near mid-oceanic ridges

Seismic structure of the lithosphere and upper mantle beneath the ocean islands near mid-oceanic ridges

Cenozoic uplift of the Central Andes in northern Chile and Bolivia—reconciling paleoaltimetry with the geological evolution

More constraints to determine the seismic structure beneath the Central Andes at 21°S using teleseismic tomography analysis

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