Redeposition patterns in Mississippian carbonate breccias
(Moravo-Silesian Basin, Central Europe): from passive margin to
foreland basin

D 2007

Redeposition patterns in Mississippian carbonate breccias (Moravo-Silesian Basin, Central Europe): from passive margin to foreland basin

BÁBEK, Ondřej, Jiří KALVODA and Francois-Xavier DEVUYST

Basic information

Original name

Redeposition patterns in Mississippian carbonate breccias (Moravo-Silesian Basin, Central Europe): from passive margin to foreland basin

Name in Czech

Redepozice ve spodnokarbonských karbonátových brekciích (Moravskoslezská zóna, střední Evropa): od pasivního okraje k přepolní pánvi

Authors

BÁBEK, Ondřej, Jiří KALVODA and Francois-Xavier DEVUYST

Edition

Patras, Greece, 25th IAS Meeting of Sedimentology 2007, Patras - Greece, Book of Abstracts, p. 198-198, 1 pp. 2007

Publisher

IAS, International Association of Sedimentologists

Other information

Language

English

Type of outcome

Stať ve sborníku

Field of Study

10500 1.5. Earth and related environmental sciences

Country of publisher

Greece

Confidentiality degree

není předmětem státního či obchodního tajemství

Organization unit

Faculty of Science

Keywords in English

microfacies; conodonts; foraminifers; biostratigraphy; erosion; tectonic subsidence; foreland basin

Abstract

ORIG CZ

V originále

Carbonate successions deposited during the passive-margin phase of the Moravo-Silesian Basin (MSB) and younger siliciclastic turbidites deposited during its foreland-basin phase are separated by sparse bodies of Middle Tournaisian to Viséan rudstones and pack/grainstones with phosphate intraclasts (phosphatic breccias). Compositional analysis and conodont biostratigraphy data suggest this facies represents an important lithology in our understanding of this tectono-stratigraphic boundary. The breccias are preserved in lens-like bodies consisting of graded, grain-supported heterolithic rudstones to pack/grainstones, massive, coarse-grained rudstones with packstone/grainstone matrix, and thin, parallel-laminated and/or normally graded pack/grainstones. Allochems include abundant carbonate intraclasts, angular clasts of phosphatised radiolarian mudstones/wackestones, ooids, peloids, oncoids, echinoderms, and less frequently rugose corals, brachiopods, bryozoans, foraminifers and rare conodonts. Their analogues were also found in neptunian dikes. The onset of the breccia sedimentation was distinctly diachronic within the interval from the Middle Tournaisian to the Viséan. The breccias contain reworked conodonts and corals of Tournaisian, Famennian and even Frasnian age. The breccias are often underlain by Famennian carbonates suggesting that their deposition followed an erosional episode. Sedimentary characteristics and composition of the breccias suggest that they were deposited in a high-energy marine environment associated with deep erosion of their source areas, presumably at the toes of submarine slopes. Diachronic start of the breccia sedimentation and their lens-like geometry suggest that local controls prevailed during their deposition, most presumably in a fault-related setting. This is supported by the neptunian dikes and Tournaisian differential subsidence patterns derived from isopach maps of the MSB. Temporal and spatial distribution of the breccias indicates their rejuvenation in W-to-E to NW-to-SE direction, roughly parallel to the distal-to-proximal cross-section of the former passive margin. The breccias recorded a period of intense faulting and surface morphology changes due to plate collision, prior to the flexural subsidence and deposition of the siliciclastic flysch. This tectonic regime presumably acted on the background of eustatic oscillations in the typicus and lower anchoralis CZ. In this respect, the situation resembles the late Tournaisian phosphorite deposition of the Antler foreland of North America.

In Czech

Carbonate successions deposited during the passive-margin phase of the Moravo-Silesian Basin (MSB) and younger siliciclastic turbidites deposited during its foreland-basin phase are separated by sparse bodies of Middle Tournaisian to Viséan rudstones and pack/grainstones with phosphate intraclasts (phosphatic breccias). Compositional analysis and conodont biostratigraphy data suggest this facies represents an important lithology in our understanding of this tectono-stratigraphic boundary. The breccias are preserved in lens-like bodies consisting of graded, grain-supported heterolithic rudstones to pack/grainstones, massive, coarse-grained rudstones with packstone/grainstone matrix, and thin, parallel-laminated and/or normally graded pack/grainstones. Allochems include abundant carbonate intraclasts, angular clasts of phosphatised radiolarian mudstones/wackestones, ooids, peloids, oncoids, echinoderms, and less frequently rugose corals, brachiopods, bryozoans, foraminifers and rare conodonts. Their analogues were also found in neptunian dikes. The onset of the breccia sedimentation was distinctly diachronic within the interval from the Middle Tournaisian to the Viséan. The breccias contain reworked conodonts and corals of Tournaisian, Famennian and even Frasnian age. The breccias are often underlain by Famennian carbonates suggesting that their deposition followed an erosional episode. Sedimentary characteristics and composition of the breccias suggest that they were deposited in a high-energy marine environment associated with deep erosion of their source areas, presumably at the toes of submarine slopes. Diachronic start of the breccia sedimentation and their lens-like geometry suggest that local controls prevailed during their deposition, most presumably in a fault-related setting. This is supported by the neptunian dikes and Tournaisian differential subsidence patterns derived from isopach maps of the MSB. Temporal and spatial distribution of the breccias indicates their rejuvenation in W-to-E to NW-to-SE direction, roughly parallel to the distal-to-proximal cross-section of the former passive margin. The breccias recorded a period of intense faulting and surface morphology changes due to plate collision, prior to the flexural subsidence and deposition of the siliciclastic flysch. This tectonic regime presumably acted on the background of eustatic oscillations in the typicus and lower anchoralis CZ. In this respect, the situation resembles the late Tournaisian phosphorite deposition of the Antler foreland of North America.

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