How much time is needed for laccolith formation? A new approach based on a case study from Csódi-hegy, Dunabogdány, Hungary

Bendő, Zsolt; Korpás, László

doi:10.1556/ageol.48.2005.3.4

Cited by 1 publication

(2 citation statements)

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“…It is found in the CPR as an exposed subvolcanic intrusion in the sedimentary basement in the Visegrád area in Hungary (Figure 1-2b) [209], Salgótarján area at the Hungary/Slovakia boundary (Figure 1-2e) [224], the Lysá Stráž -Oblík zone in eastern Slovakia (Figure 1-4b) [225,226], and in the "Subvolcanic zone" of the Eastern Carpathians (Figure 1-6) [207]. Laccoliths take part also in the structure of volcanic core complexes [219].…”

Section: Laccolithsmentioning

confidence: 99%

“…Intermediate calc-alkaline subsurface intrusions show a large petrographic range from basalts (gabbro-diorite) to andesite (diorite) to rhyolites (granite) and a wide range of textures, commonly related to the depth of cooling. They usually form independent bodies piercing various basement lithologies (metamorphic or sedimentary) [207][208][209][210]. The independent intrusions are mostly outcropping in strongly eroded terranes [211].…”

Section: Intrusive Forms Related To Intermediate Calcalkaline Rocksmentioning

confidence: 99%

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

et al. 2010

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Neogene to Quaternary volcanic/magmatic activity in the Carpathian-Pannonian Region (CPR) occurred between 21 and 0.1 Ma with a distinct migration in time from west to east. It shows a diverse compositional variation in response to a complex interplay of subduction with roll-back, back-arc extension, collision, slab break-off, delamination, strike-slip tectonics and microplate rotations, as well as in response to further evolution of magmas in the crustal environment by processes of differentiation, crustal contamination, anatexis and magma mixing. Since most of the primary volcanic forms have been affected by erosion, especially in areas of post-volcanic uplift, based on the level of erosion we distinguish: (1) areas eroded to the basement level, where paleovolcanic reconstruction is not possible; (2) deeply eroded volcanic forms with secondary morphology and possible paleovolcanic reconstruction; (3) eroded volcanic forms with remnants of original morphology preserved; and (4) the least eroded volcanic forms with original morphology quite well preserved. The large variety of volcanic forms present in the area can be grouped in a) monogenetic volcanoes and b) polygenetic volcanoes and their subsurface/intrusive counterparts that belong to various rock series found in the CPR such as calc-alkaline magmatic rock-types (felsic, intermediate and mafic varieties) and alkalic types including K-alkalic, shoshonitic, ultrapotassic and Na-alkalic. The following volcanic/subvolcanic forms have been identified: (i) domes, shield volcanoes, effusive cones, pyroclastic cones, stratovolcanoes and calderas with associated intrusive bodies for intermediate and basic calc-alkaline volcanism; (ii) domes, calderas and ignimbrite/ash-flow fields for felsic calc-alkaline volcanism and (iii) dome flows, shield volcanoes, maars, tuffcone/tuff-rings, scoria-cones with or without related lava flow/field and their erosional or subsurface forms (necks/ plugs, dykes, shallow intrusions, diatreme, lava lake) for various types of K-and Na-alkalic and ultrapotassic magmatism. Finally, we provide a summary of the eruptive history and distribution of volcanic forms in the CPR using several sub-region schemes.

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Section: Laccolithsmentioning

confidence: 99%