Erosion of the continental lithosphere at the cusps of the Calabrian arc: Evidence from<i>S</i>receiver functions analysis

Miller, Meghan; Agostinetti, Nicola Piana

doi:10.1029/2011gl049455

Cited by 20 publications

(14 citation statements)

References 51 publications

(70 reference statements)

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“…In southern peninsular Italy the Moho is at 27 km below Apulia and deepens to 32 km in Calabria and 37 km in the central Apennines (Figure ). Our value for Apulia is close to results based on SRF (Miller & Piana Agostinetti, , ) and PRF (Piana Agostinetti & Amato, ; Steckler et al, ). Our estimate for the central Apennines agrees with Miller and Piana Agostinetti () and Piana Agostinetti and Amato () and falls between the value of Megna and Morelli () and the deeper ones by Miller and Piana Agostinetti () and Mele et al ().…”

Section: Discussionsupporting

confidence: 90%

“…Our value for Apulia is close to results based on SRF (Miller & Piana Agostinetti, , ) and PRF (Piana Agostinetti & Amato, ; Steckler et al, ). Our estimate for the central Apennines agrees with Miller and Piana Agostinetti () and Piana Agostinetti and Amato () and falls between the value of Megna and Morelli () and the deeper ones by Miller and Piana Agostinetti () and Mele et al (). Below Apulia, we detect the LAB at 68‐km depth, an estimate that matches the finding by Miller and Piana Agostinetti (), who explain such a thin lithosphere as a result of thermo‐mechanical erosion produced by toroidal flow around the edge of the Calabrian slab (Miller & Piana Agostinetti, ).…”

Section: Discussionsupporting

confidence: 90%

“…Below southeastern Sicily our estimate also indicates a shallow Moho depth (26 km). It combines data from five nearby stations (IBLEE), and is in agreement with Miller and Piana Agostinetti () (station HAVL), but not with Miller and Piana Agostinetti () (stations HAVL and HVZN). The LAB depth offshore eastern Sicily, below the oceanic‐continental transition, is at 63 km, a much shallower depth than the estimate by Miller and Piana Agostinetti ().…”

Section: Discussionsupporting

confidence: 58%

“…In the central Mediterranean area a number of RF studies have focused on the crust (Amato et al, ; Piana Agostinetti & Amato, ; van der Meijde et al, ) and the lithosphere‐asthenosphere boundary (Belinić et al, ; Bianchi et al, ; Geissler et al, ; Miller & Piana Agostinetti, ; Miller & Piana Agostinetti, ). Several PRF studies investigated the upper mantle down to the transition zone (Cottaar & Deuss, ; Liu et al, ; Lombardi et al, ; van der Meijde et al, ; van der Meijde et al, ) and a very recent SRF work focused on the sublithospheric discontinuities (midlithospheric discontinuity and sublithospheric discontinuity) below central Europe (Kind et al, ).…”

Section: Introductionmentioning

confidence: 99%

“…Piana Agostinetti and Amato () observe a Moho topography that from the shallow values of the peri‐Tyrrhenian area (20–25 km), deepens below the Apennines belt (reaching 50 km), and suddenly dips in the Ionian subduction. The continental lithospheric thickness as detected by SRFs varies between 60 and 170 km along the Italian peninsula (Miller & Piana Agostinetti, , ).…”

Section: Introductionmentioning

confidence: 99%

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Mantle Structure in the Central Mediterranean Region From P and S Receiver Functions

Monna

Montuori

Piromallo

et al. 2019

Geochem Geophys Geosyst

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We investigate the upper mantle discontinuities in the central Mediterranean region by applying the P and S receiver function techniques on waveforms recorded at broadband stations located around the Tyrrhenian basin. P and S wave velocity profiles (down to 300‐km depth) are calculated with joint inversion of P and S receiver functions. We could identify the Moho, lithosphere‐asthenosphere boundary, and an underlying low‐velocity layer between ~60‐ and ~200‐km depth. The low‐velocity layer is interpreted as asthenospheric material, and its lower boundary is identified below the western Ionian and Tyrrhenian basins as a sharp Lehmann discontinuity. Although the stations are located on different lithospheric domains we find a strong correlation between Moho and the lithosphere‐asthenosphere boundary depths, which suggests ubiquitous coupling of the crust and lithospheric mantle, consistently with the southward opening of the Tyrrhenian basin. The Tyrrhenian and western Ionian basins present thinning of the transition zone of ~14 km, as inferred from a reduced P660s‐P410s differential time. Below the southern Apennines we observe a standard differential time that implies an average mantle transition zone thickness. We explain these mantle transition zone thickness variations as due to temperature heterogeneity linked to the area's subduction history. Finally, under central Europe (the location of the deep S‐to‐P conversion points) two strong signals from nonstandard discontinuities within the mantle transition zone are observed. These signals can be explained as being generated at the boundaries of high seismic velocity layers that are spatially correlated with stagnant slabs in the transition zone detected by seismic tomography.

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Section: Discussionsupporting

confidence: 90%

Section: Discussionsupporting

confidence: 90%

Section: Discussionsupporting

confidence: 58%

Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Mantle Structure in the Central Mediterranean Region From P and S Receiver Functions

Monna

Montuori

Piromallo

et al. 2019

Geochem Geophys Geosyst

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Lithospheric discontinuity structure in Alaska, thickness variations determined bySpreceiver functions

O'Driscoll

Miller

2015

Tectonics

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We present the first broad-scale image of lithospheric thickness across the major tectonic domains of Alaska based on S wave receiver functions and joint interpretation with the potential field, seismic velocity, and heat flow measurements. Thus, we provide context for the distribution of strain throughout the Alaskan orocline. In the north, below the Brooks Range, a 130 km thick lithosphere is resolved, consistent with the presence of strong lithosphere that deflects strain to the south into central and southern Alaska. In southern Alaska beneath the Chugach and St. Elias Mountains, multiple interfaces are present, and we interpret a thinner (80-90 km) North American lithosphere above a deeper interface that represents the base of the Yakutat microplate, thereby extending it to the area below the Wrangell Volcanic Field and St. Elias Mountains. Immediately north of the E-W striking Denali Fault, shallow negative conversions (80 km) denote thin lithosphere in the greater back-arc region where heat flow is observed to be high. Thin lithosphere in eastern Alaska and adjacent Yukon Territory coincides with the occurrence of inboard crustal seismicity and may be indicative of transmitted compression caused by the collision of the Yakutat microplate. Relatively thin lithosphere (<90 km) south of the Arctic Alaska domain that is deforming throughout the Alaskan orocline may result from lithospheric thinning associated with guided deformation. Expansion of this model using the upcoming Transportable Array will be critical to establish lateral continuity (or lack thereof) of lithospheric structure and directly discriminate between existing regional deformation models.

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Lithospheric architecture beneath Hudson Bay

Porritt

Miller

Darbyshire

2015

Geochem Geophys Geosyst

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Hudson Bay overlies some of the thickest Precambrian lithosphere on Earth, whose internal structures contain important clues to the earliest workings of plate formation. The terminal collision, the Trans-Hudson Orogen, brought together the Western Churchill craton to the northwest and the Superior craton to the southeast. These two Archean cratons along with the Paleo-Proterozoic Trans-Hudson internides, form the core of the North American craton. We use S to P converted wave imaging and absolute shear velocity information from a joint inversion of P to S receiver functions, new ambient noise derived phase velocities, and teleseismic phase velocities to investigate this region and determine both the thickness of the lithosphere and the presence of internal discontinuities. The lithosphere under central Hudson Bay approaches 350 km thick but is thinner (200-250 km) around the periphery of the Bay. Furthermore, the amplitude of the LAB conversion from the S receiver functions is unusually large for a craton, suggesting a large thermal contrast across the LAB, which we interpret as direct evidence of the thermal insulation effect of continents on the asthenosphere. Within the lithosphere, midlithospheric discontinuities, significantly shallower than the base of the lithosphere, are often imaged, suggesting the mechanisms that form these layers are common. Lacking time-history information, we infer that these discontinuities reflect reactivation of formation structures during deformation of the craton.

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Erosion of the continental lithosphere at the cusps of the Calabrian arc: Evidence fromSreceiver functions analysis

Cited by 20 publications

References 51 publications

Mantle Structure in the Central Mediterranean Region From P and S Receiver Functions

Mantle Structure in the Central Mediterranean Region From P and S Receiver Functions

Lithospheric discontinuity structure in Alaska, thickness variations determined bySpreceiver functions

Lithospheric architecture beneath Hudson Bay

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