Carbonate deposition in mixed siliciclastic–carbonate environments on top of an orogenic wedge (Late Cretaceous, Northern Calcareous Alps, Austria)

Sanders, Diethard; Höfling, Richard

doi:10.1016/s0037-0738(00)00084-1

Cited by 69 publications

(39 citation statements)

References 14 publications

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“…They may themselves contain an internal smaller-scale cyclicity. Examples of these occur within the Carboniferous strata of South Wales (Burchette and Wright 1992), Triassic Muschelkalk of Germany (Aigner 1984) and the Cretaceous of the central and western Pyrenees (Simo 1989;Lenoble and Canerot 1993) and Austrian Alps (Sanders and Hofling 2000). Broadly, the deeper-water mudrock lower parts represent transgressive facies, while the upper carbonates were prograding shallow-water highstand facies.…”

Section: Lower Mudrock -Upper Carbonate Sequencesmentioning

confidence: 99%

Sequence Stratigraphy: Methodology and Nomenclature

Catuneanu

Galloway

Kendall

et al. 2011

nos

766

460

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Abstract. The recurrence of the same types of sequence stratigraphic surface through geologic time defines cycles of change in accommodation or sediment supply, which correspond to sequences in the rock record. These cycles may be symmetrical or asymmetrical, and may or may not include all types of systems tracts that may be expected within a fully developed sequence. Depending on the scale of observation, sequences and their bounding surfaces may be ascribed to different hierarchical orders. Stratal stacking patterns combine to define trends in geometric character that include upstepping, forestepping, backstepping and downstepping, expressing three types of shoreline shift: forced regression (forestepping and downstepping at the shoreline), normal regression (forestepping and upstepping at the shoreline) and transgression (backstepping at the shoreline). Stacking patterns that are independent of shoreline trajectories may also be defined on the basis of changes in depositional style that can be correlated regionally. All stratal stacking patterns reflect the interplay of the same two fundamental variables, namely accommodation (the space available for potential sediment accumulation) and sediment supply. Deposits defined by specific stratal stacking patterns form the basic constituents of any sequence stratigraphic unit, from sequence to systems tract and parasequence. Changes in stratal stacking patterns define the position and timing of key sequence stratigraphic surfaces. Precisely which surfaces are selected as sequence boundaries varies as a function of which surfaces are best expressed within the context of the depositional setting and the preservation of facies relationships and stratal stacking patterns in that succession. The high degree of variability in the expression of sequence stratigraphic units and bounding surfaces in the rock record means ideally that the methodology used to analyze their depositional setting should be flexible from one sequence stratigraphic approach to another. Construction of this framework ensures the success of the method in terms of its objectives to provide a process-based understanding of the stratigraphic architecture. The purpose of this paper is to emphasize a standard but flexible methodology that remains objective.

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Section: Lower Mudrock -Upper Carbonate Sequencesmentioning

confidence: 99%

Sequence Stratigraphy: Methodology and Nomenclature

Catuneanu

Galloway

Kendall

et al. 2011

nos

766

460

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“…According to Zeller et al (2015), a mixing of carbonate production and siliciclastic input causes variable sedimentation conditions and a high degree of lateral and vertical facies heterogeneity. Generally, carbonate facies development is triggered by the requirements of the carbonate-secreting biota, which are controlled by temperature, salinity, sealevel change, input of siliciclastic sediments, and nutrients (Sanders and Höfling 2000). It seems that the sedimentary conditions of the Late Cretaceous low-energy basin in the Miechów Synclinorium have been predominately driven by blooms of coccolithophores (Saavedra-Pellitero et al 2014) as well as inputs of siliciclastic deposits of terrestrial origin.…”

Section: Discussionmentioning

confidence: 99%

Maastrichtian island in the central European Basin—new data inferred from palynofacies analysis and inoceramid stratigraphy

Jurkowska

Barski

2017

Facies

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“…Grain supported ooid grainstones without any mud indicate deposition in a high energy belt (Flugel, 2004); (Hofmann et al, 2004) and in ooid packstone (C1) facies, high mud shows the vicinity of the shoal to the lagoon. Skeletal grains in the D facies group consist of orbitolina, brachiopods, echinoderms and red algae, these are sensitive to salinity and an open marine environment is suitable for their life (Flugel, 2004); (Tucker and Wright, 1990); (Sanders and Hofling, 2000). According to the abundance of stenohalina, high abundance of mud and thin bedded layers, we can consider a low energy environment and low sedimentation for this facies which indicates open marine environment (Flugel, 2004); (Martini et al, 2007).…”

Section: B) Interpretation and Modeling Of Depositional Environmentsmentioning

confidence: 99%

Microfacies and Morphotectonic of the Tirgan Formation in Ghorogh Syncline (North of Chenaran)

Yavarmanesh

Vaziri

Aryaei

et al. 2017

International Journal of Geography and Geology

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Article HistoryIn this research, the Tirgan Formation in Ghorogh Syncline (north of Chenaran) with the thickness of 412 m in north flank and 251 m in south flank is studied. The Tirgan Formation in Ghorogh sectionsis included limestones, marlylimestones, shales and sandstones in lower parts of the formation. In these sections, there are impressions of echinoderms toxasteridae family, many of foraminifera from orbitolinidae family and also lots of calcareous algae that create facies variation along with other nonskeletal allochems. The study of sediment facies led to the recognition of four facies belts and six microscopic standard facies in the Tirgan Formation and shows the oscillation of sea level but totally it can be concluded that the basin was shallow and formed in the ramp platform. According to the evidence, the oolithic limestones and intercalated shales of the Tirgan Formation in south flank, Ghorogh Syncline are slided on the red sandstone of Shurijeh Formation as transition slides because of lubrication. These landslides are distinguished and formed (7times) because of the stresses which are done from the northern syncline to the south of Ghorogh valley and formed the current morphotectonic for the area. This phenomenon could name as decollement.Contribution/ Originality: The paper's primary contribution is finding real thickness of Tirgan Formation in south flank Ghorogh Syncline. Morphotectonic studies show transitional slides of Tirgan Formation in Chenaran map (1:100000) wrongly named Shurijeh Formation while this research led to the corrected and these transitional slides named Tirgan Formation.

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Carbonate deposition in mixed siliciclastic–carbonate environments on top of an orogenic wedge (Late Cretaceous, Northern Calcareous Alps, Austria)

Cited by 69 publications

References 14 publications

Sequence Stratigraphy: Methodology and Nomenclature

Sequence Stratigraphy: Methodology and Nomenclature

Maastrichtian island in the central European Basin—new data inferred from palynofacies analysis and inoceramid stratigraphy

Microfacies and Morphotectonic of the Tirgan Formation in Ghorogh Syncline (North of Chenaran)

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