Crustal Models Assessment in Western Part of Romania Employing Active Seismic and Seismologic Methods

Bălă, Andrei; Toma-Dănilă, Dragoş; Tǎtaru, Dragoș; Grecu, Bogdan

doi:10.1088/1755-1315/95/3/032026

Cited by 2 publications

(1 citation statement)

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“…35 mohometers applicable to these samples yield a crust‐mantle transition at 46 ± 6 km (Figure 4b). In contrast, present‐day Moho depths beneath the Apuseni and Banat are significantly shallower, averaging about ∼30–35 km (Bala et al., 2017; Molinari & Morelli, 2011), implying that significant crustal thinning followed the demise of the Late Cretaceous magmatism. Two major extensional events could be responsible for crustal thinning since late Cretaceous, an Eocene episode responsible for the unroofing of the Danubian units in the South Carpathians (Fügenschuh & Schmid, 2005) and the Miocene and younger extension that led to the formation of the Pannonian basin (Schmid et al., 2020).…”

Section: Application To Paleo‐mohometrymentioning

confidence: 99%

Carpathian‐Pannonian Magmatism Database

Vlăsceanu

Ducea

Luffi

et al. 2021

Geochem Geophys Geosyst

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Magmatic arcs and intracontinental extensional domains active in the geological past of the Carpathian-Pannonian region host a wealth of plutonic and volcanic suites, which have been studied in various details over the past decades. Today, the primary geochemical information delivered by different studies-a valuable resource for new regional petrogenetic and tectonic interpretations-is still scattered in well over one hundred papers that are more or less accessible to the interested researchers. In order to facilitate the access of the geoscience community to this information, here we present an up-to-date compilation of geochronologic, geochemical and isotopic data characterizing the region.The area covered in this compilation is shown in Figure 1. The aggregate Carpathian Mountains start in the west from near Vienna (Austria) and form a broad east-west arc (the West and East Carpathians), followed by a sharp bend in the Vrancea region; the east-west oriented South Carpathians complete geographically this segment of the long scar marking the closure of various Alpine and Neotethyan basins, which extends from the Alps in the west, to the Himalayas in its far east. The Carpathians have a complex geologic history, but the present-day mountain ranges and basins formed as a result of Cenozoic compression and crust consumption by subduction and collision (Schmid et al., 2020) of a series of back arc basins, whereas the main Tethyan Ocean was located further to the south. A prominent fold and thrust belt of Miocene and younger ages marks the suture between the Eastern European craton to the east and mobile Europe, represented by several peri-Gondwanan terranes (Balintoni et al., 2014). To the interior of this arc lies the Pannonian-Transylvanian basin, a continental extensional domain most recently related to the rollback of the slab since the early Miocene (Royden & Burchfiel, 1989). A smaller mountain range, the Apuseni Mountains, occupies a less extended area within the eastern part of the Pannonian basin.Magmatic products of this region span an 800 Ma range, from a Neoproterozoic arc preserved in the basement of the South Carpathians (Balintoni et al., 2014) to the youngest volcanoes found in the Carpathian bend region; here, at least one volcanic center, Ciomadul, is documented to be active (e.g., Harangi et al., 2015;Popa et al., 2012). We did not compile data on igneous rocks making up various basement terrains, which are Neoproterozoic to late Paleozoic in age; many of those have been metamorphosed during the Paleozoic (Medaris et al., 2003). We did, however, include the following igneous provinces composed of unmetamorphosed volcanic and/or intrusive rocks of the region; (a) a Jurassic island arc province found in the South Apuseni Mts. and buried under younger rocks of the Transylvanian basin (Gallhofer et al., 2017),

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