Flexural expression of European continental lithosphere under the western outer Carpathians

Zoetemeijer, R.; Tomek, Čestmǐr; Cloetingh, S.A.P.L.

doi:10.1029/1998tc900034

Cited by 41 publications

(31 citation statements)

References 38 publications

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“…"Planation surfaces" in the Polish Carpathians versus the Late Cenozoic time scale and timing of exhumation inferred from apatite fission track dating (compiled after Kováč et al, 1994, Baumgart-Kotarba andKrál, 2002;Oszczypko et al, 2005;Geological Time Scale, 2008;and Mazzoli et al, 2010). of non-isostatic processes leading to young uplift ranging between 250 m and 550 m (Zoetemeijer et al, 1999). A more reliable estimate is provided by fission track studies (cf.…”

Section: Discussionmentioning

confidence: 99%

Planation surfaces in the Polish Carpatians: myth or reality?

Zuchiewicz¹

2011

Geogr.Pol.

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Abstract:Previous views concerning the number and age of planation surfaces in the Polish segment of the Carpathians varied depending on the state of recognition of geological structure of the area. The most commonly accepted opinion says that at least three such surfaces, representing remnants of pre-existing landscapes, can be traced in the study region. These include the intramontane (Early Pliocene), foothills (Late Pliocene) and riverside (Early Pleistocene) levels. Scarce fission track data pertaining to the age of exhumation of the Carpathian orogen indicate that the preserved "planation surfaces" could not had formed before ca. 7 Ma. A possibility exists, however, that individual bevels could have been shaped at the same time at different altitudes, with respect to local base levels and differentiated bedrock resistance to erosion.

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Section: Discussionmentioning

confidence: 99%

Planation surfaces in the Polish Carpatians: myth or reality?

Zuchiewicz¹

2011

Geogr.Pol.

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“…In this concept, the development of the foreland basins has been regarded as the result of the lithosphere flexure caused by loading effect of the growing thrust belt. Although the first modelling studies confirmed this concept [14], the later studies (e.g., in the Carpathians and Appenines) revealed that the topographic load is not always sufficient to explain the observed deflection of the foreland plate [15,16] and must be connected with deep subcrustal load of the downgoing plate [17,18].…”

Section: Introductionmentioning

confidence: 99%

Stages of development in the Polish Carpathian Foredeep basin

Oszczypko

Oszczypko-Clowes

2012

Open Geosciences

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Abstract:In southern Poland, Miocene deposits have been recognised both in the Outer Carpathians and the Carpathian Foredeep (PCF). In the Outer Carpathians, the Early Miocene deposits represent the youngest part of the flysch sequence, while in the Polish Carpathian Foredeep they are developed on the basement platform. The inner foredeep (beneath the Carpathians) is composed of Early to Middle Miocene deposits, while the outer foredeep is filled up with the Middle Miocene (Badenian and Sarmatian) strata, up to 3,000 m thick. The Early Miocene strata are mainly terrestrial in origin, whereas the Badenian and Sarmatian strata are marine. The Carpathian Foredeep developed as a peripheral foreland basin related to the moving Carpathian front. The main episodes of intensive subsidence in the PCF correspond to the period of progressive emplacement of the Western Carpathians onto the foreland plate. The important driving force of tectonic subsidence was the emplacement of the nappe load related to subduction roll-back. During that time the loading effect of the thickening of the Carpathian accretionary wedge on the foreland plate increased and was followed by progressive acceleration of total subsidence. The mean rate of the Carpathian overthrusting, and north to north-east migration of the axes of depocentres reached 12 mm/yr at that time. During the Late Badenian-Sarmatian, the rate of advance of the Carpathian accretionary wedge was lower than that of pinch-out migration and, as a result, the basin widened. The Miocene convergence of the Carpathian wedge resulted in the migration of depocentres and onlap of successively younger deposits onto the foreland plate.

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“…An interpretation of the Vranca deep seismic zone in conection with detached sinking lithosphere slab (Constantinescu and Enescu, 1984) and the recognition of subducted lithosphere remnants underneath the Pannonian basin and internal Carpathian units (Spakman, 1990) resulted in the concept of final verticalization of the subduction zone, slab detachment, related deep subsurface load, and platform margin bending (Vortel and Spakman, 1992;Meulenkamp et al, 1996;Krzywiec and Jochym, 1997;Nemčok et al, 1998;Zoetemeijer et al, 1999). These gravity driven processes were not contemporaneous along the arc -rather they show a progression from west to east during the Early Miocene to Quaternary time (Vortel and Spakman, 1992;Nemčok et al, 1998;Konečný, 1998, Kováč, 2000).…”

Section: Introductionmentioning

confidence: 99%

Neogene evolution of the Carpatho-Pannonian region: an interplay of subduction and back-arc diapiric uprise in the mantle

Konečný¹,

Kováč²,

Lexa³

et al. 2002

Stephan Mueller Spec. Publ. Ser.

104

123

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Abstract. Geodynamic evolution of the Carpathian arc and Pannonian basin during the Neogene times is presented as a set of palinspastic reconstructions. The structural evolution is modeled in terms of a coupled system of: (1) Alpine (Atype) subduction and compressive orogene belt development owing to compression by the Adriatic microplate, (2) lateral extrusion of Alcapa lithosphere from the Alpine collision assisted by transform faults, (3) Carpathian gravity driven (Btype) subduction of oceanic or suboceanic lithosphere underlying former flysch basins and (4) back arc extension associated with the diapiric uprise of asthenospheric mantle.The variable timing of accretionary prism and back arc basin evolution in the Western Carpathians, the NW part of the Eastern Carpathians, and the SE part of the Eastern Carpathians confirms that the final Tertiary evolution of the Carpathian arc and Pannonian basin was not a uniform process. Rather, it took place successively in three segments, reflecting gravity driven subductions compensated by return asthenospheric flows (involving the back-arc diapiric uprise of asthenospheric mantle). The observed low subduction rate implies obstacles to the compensating asthenosphere flow, perhaps represented by confining thick lithosphere at the NW and SE sides of the arc. This segmentation may arise from a gravity driven process allowing asthenospheric side flow to take place speeding up the gravity driven overturn (subduction). Structural evolution as well as the timing and spatial distribution of the arc-type (subduction-related) andesite volcanics suggests that subduction halted because the subducting plate became nearly vertical, followed closely by the detachment of the sinking lithosphere slab from the continental margin. Late stage alkali basalt volcanic rocks imply that during the final stage of back arc basin evolution the related diapiric uprise of asthenospheric mantle incorporated unmetasomatized mantle material, brought possibly into the area of the diapiric uprise by compensating athenosheric mantle counterflows.Correspondence to: J. Lexa (lexa@gssr.sk)

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Flexural expression of European continental lithosphere under the western outer Carpathians

Cited by 41 publications

References 38 publications

Planation surfaces in the Polish Carpatians: myth or reality?

Planation surfaces in the Polish Carpatians: myth or reality?

Stages of development in the Polish Carpathian Foredeep basin

Neogene evolution of the Carpatho-Pannonian region: an interplay of subduction and back-arc diapiric uprise in the mantle

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