Post-collisional Tertiary–Quaternary mafic alkalic magmatism in the Carpathian–Pannonian region: a review

Abstract

Mafic alkalic volcanism was widespread in the Carpathian Pannonian region (CPR) between 11 and 0.2 Ma. It followed the Miocene continental collision of the Alcapa and Tisia blocks with the European plate, as subduction-related calc-alkaline magmatism was waning. Several groups of mafic alkalic rocks from different regions within the CPR have been distinguished on the basis of ages and/or trace-element compositions. Their trace element and Sr-Nd-Pb isotope systematics are consistent with derivation from complex mantle source regions, which included both depleted asthenosphere and metasomatized lithosphere. The mixing of DMM-HIMU-EMII mantle components within asthenosphere-derived magmas indicates variable contamination of the shallow asthenosphere and/or thermal boundary layer of the lithosphere by a HIMU-like component prior to and following the introduction of subduction components.Various mantle sources have been identified: Lower lithospheric mantle modified by several ancient asthenospheric enrichments (source A); Young asthenospheric plumes with OIB-like trace element signatures that are either isotopically enriched (source B) or variably depleted (source C); Old upper asthenosphere heterogeneously contaminated by DM-HIMU-EMII-EMI components and slightly influenced by Miocene subduction-related enrichment (source D); Old upper asthenosphere heterogeneously contaminated by DM-HIMU-EMII components and significantly influenced by Miocene subduction-related enrichment (source E). Melt generation was initiated either by: (i) finger-like young asthenospheric plumes rising to and heating up the base of the lithosphere (below the Alcapa block), or (ii) decompressional melting of old asthenosphere upwelling to replace any lower lithosphere or heating and melting former subducted slabs (the Tisia block).

Neogene-Quaternary Volcanic forms in the Carpathian-Pannonian Region: a review

“…Alkalic basaltic rocks from Perșani Mts. are similar to other continental intraplate alkali 252 Brought to you by | MIT Libraries Authenticated Download Date | 5/9/18 10:40 PM basalts and plot in the trachybasaltic field [348], but have distinctively higher La/Nb and lower Ce/Pb ratios than the other alkaline basalts in the Pannonian Basin, suggesting a subduction-related component in their source region [23,348,349].…”

“…One of the specific features of intermediate composition volcanic complexes and/or fields in the CPR is their spatial and temporal coincidence with back-arc extension [23,93,213,275,276]. Due to this coincidence, extension-controlled grabens in volcanic areas show a spatial relationship with major volcanic centers and are filled by volcanic fields, hence the term "volcano-tectonic depressions/grabens".…”

“…Attention is paid also to this aspect in discussion of volcanic forms and/or evolution of volcanic fields and sub-regions. General information concerning petrology of volcanic rocks in the CPR and their compositional variability has been widely reported recently [5][6][7][23][24][25][26][27].…”

K/Ar geochronology of igneous amphibole phenocrysts in Miocene to Pliocene volcaniclastics, Styrian Basin, Austria

“…The Limbach tuff is lo cated be tween zones three and four. 410 Hans-Peter Bojar, Ana-Voica Bojar, Stanis³aw Ha³as and Artur Wójtowicz The Neo gene evo lu tion of the Al pine-Carpathian-Pannonian (ALCAPA) area was ac com pa nied by fre quent vol ca nic ac tiv ity (Szabó et al, 1992;Balogh et al, 1994;Dobosi et al, 1995;Downes and Vaselli et al, 1995;Downes et al, 1995a;Ebner and Sachsenhofer, 1995;Embey-Isztin and Dobosi, 1995;Harangi et al, 1995a, b;Kali èiak and Žec, 1995;Koneèný et al, 1995b;Lyashkevich, 1995;Pécskay et al, 1995aPécskay et al, , b, 2006Seghedi et al, 1995Seghedi et al, , 2004Seghedi et al, , 2011Moriya et al, 1996;Sachsenhofer, 1996;Slapansky et al, 1999;Németh et al, 2001;Ebner et al, 2002;Han dler et al, 2006;Bojar et al, 2008;Kralj, 2011).…”

“…The pe riph eral por tions of the Styrian Ba sin are down-bended, with depocentres mov ing eastwards dur ing tilt ing, which is con tem po ra ne ous with ma jor sub si dence in the Lit tle Hun gar ian Plane. The sec ond phase of ba saltic vol ca nism took place in this pe riod (Balogh et al, 1994;Seghedi et al, 2004).…”