Structure of the West Carpathian accretionary wedge: Insights from cross section construction and sandbox validation

Němčok, Michal; Coward, M. P.; Sercombe, William J.; Klecker, R. A.

doi:10.1016/s1464-1895(99)00096-4

Cited by 22 publications

(13 citation statements)

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“…Additionally, the mechanisms by which crustal shortening and thickening are achieved, as well as the magnitudes, are known to vary along strike (e.g., Allmendinger and Gubbels, 1996;Giambiagi et al, 2012;Ramos et al, 2004). Factors that significantly affect the structural style and magnitude of deformation include the inherited structural and stratigraphic architecture of a region (e.g., Lowell, 1995;Boyer, 1995;DeCelles and Mitra, 1995;Macedo and Marshak, 1999;Kley et al, 1999;Nemcok et al, 1999;Mouthereau et al, 2002;Marshak, 2004;Thomas, 2007) and the degree of coupling between brittle deformation in the upper crust and ductile strain in the lower crust (e.g., Brown, 2004;Yin, 2006;Lamb, 2011;Giambiagi et al, 2014Giambiagi et al, , 2012. In this paper, we address two questions regarding the kinematic development of a retroarc fold-and-thrust belt: (1) How is the structure of the fold-and-thrust belt influenced by the antecedent stratigraphic architecture of a predecessor basin?…”

Section: Introductionmentioning

confidence: 99%

Along-strike variation in crustal shortening and kinematic evolution of the base of a retroarc fold-and-thrust belt: Magallanes, Chile 53°S-54°S

Betka¹,

Klepeis²,

Mosher³

2015

Geological Society of America Bulletin

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The Late Cretaceous closure of the Late Jurassic-Early Cretaceous Rocas Verdes basin resulted in the development of the Patagonian fold-and-thrust belt and Magallanes foreland basin between 50°S and 54.5°S. New geologic maps, structural data, and two retrodeformed, line-balanced cross sections from the Magallanes region of Chile (53°S-54°S) constrain the kinematic evolution and along-strike correlations of deformation that occurred at the base of the fold-and-thrust belt near the brittle-ductile transition. The stratigraphic architecture of the predecessor basin controlled the position of regional décollement levels. During the initial stage of closure (Albian-Campanian), the floor of the Rocas Verdes basin was imbricated and thrust onto the continental margin to form a regional décollement within Jurassic-Lower Cretaceous shale. Continued shortening resulted in the deepening of the décollement to a ductile shear zone that formed <1 km below the basement-cover contact. Ductile polyphase folding accommodated basement shortening and was mechanically decoupled from the overlying fold-and-thrust belt below the lower décollement. Ramps that cut Jurassic volcanic deposits linked the lower and upper décollements and transferred displacement into the nascent foreland basin. A second stage of shortening, characterized by basement-involved reverse faults that cut the early décollements, reflects complete closure of the Rocas Verdes basin by the Maastrichtian-Eocene. Coniacian to Eocene shortening estimates indicate a northwestsoutheast increase from 26% to 37% over 100 km along strike and are consistent with regional models of the Patagonian fold-andthrust belt. The results provide an important example of the kinematic evolution of the base of a retroarc fold-and-thrust belt in an "Andean-style" orogen.

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Section: Introductionmentioning

confidence: 99%

Along-strike variation in crustal shortening and kinematic evolution of the base of a retroarc fold-and-thrust belt: Magallanes, Chile 53°S-54°S

Betka¹,

Klepeis²,

Mosher³

2015

Geological Society of America Bulletin

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“…lb), except profile 1, which goes further to the Inner Carpathians. As profiles 1 and 2 have already been discussed in detail in Nem~ok et al (1999Nem~ok et al ( , 2000Nem~ok et al ( , 2001, this paper focuses on the description of the remaining profiles 3 to 5 (Fig. 3).…”

Section: Balancing Resultsmentioning

confidence: 95%

“…lb). Details for cross-section construction are partly described in Nem~ok et al (1999Nem~ok et al ( , 2000Nem~ok et al ( , 2001 and further information is given below. Data constraints for balancing were provided by:…”

Section: Balancingmentioning

confidence: 99%

“…(1) magnetotelluric data (e.g., Rytko & Tomas, 1995) that helped to determine the basement top; (2) reflection seismic profiles (e.g., profiles 5-3-73K, 5-1-78K, 5A-1-78K; Nem~ok et al 1999Nem~ok et al , 2000 that imaged thrust sheet geometries; (3) bore holes that provided thicknesses of thrust sheets and thicknesses of involved sediments; and…”

Section: Balancingmentioning

confidence: 99%

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Oil reservoirs in foreland basins charged by thrustbelt source rocks: insights from numerical stress modelling and geometric balancing in the West Carpathians

Němčok

Henk

2006

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The West Carpathian thrustbelt advanced northeastwards over the European Platform. Its thrust sheets comprise sediments of the Early Cretaceous rifts that evolved on a passive margin of the European Platform, the Late Cretaceous-Paleocene basins formed by rift inversion, and the Eocene-Oligocene flexural basin. Geochemical analyses established a clear link between pooled oils in the foreland and the Oligocene Menilite Formation inside the thrustbelt. In order to understand the driving forces for this oil migration scenario, finite-element models of fault-propagation and fold-bend folds are used to study the mean stress distribution in the thrust sheets and the foreland. Mean stress has a profound control on the pore fluid pressure through the relationship affected by sediment porosity, and sediment skeleton and fluid compressibilities. Modelling results suggest that only faultpropagation folds are capable of generating foreland-directed mean stress gradients as they are characterized by a large foreland area of decreased mean stress, by coupled increased/decreased mean stress areas on advancing/receding sides of the ramp tip, and an overall mean stress decrease inside the thrust sheet in the direction towards the foreland. This interpretation is in accordance with the dominant fold-and-thrust style in the Western Carpathians inferred from balanced cross-section restoration. It shows that frontal faultpropagation folding was active during the late Oligocene-Early Miocene, providing an effective tectonic driving force for hydrocarbon migration from source rocks inside the thrustbelt towards reservoirs in the foreland.

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“…(b) Scenario with subduction zone retreat manages to create space for crustal accretion without a need for retro-thrusting. (400-450 km) with that of the Carpathians (75-223 km; Platt et al 1989;Roca et al 1995;Schmid et al 1996;Nemčok et al 1999). The difference is also indicated by the fact that the entire upper crust of the more proximal parts of the European plate was accreted to the Alpine orogenic wedge, while involvement of the basement of the European plate in the West Carpathian accretionary wedge is minor (Roure et al 1993;Roca et al 1995;Schmid et al 1996;Nemčok et al 2000).…”

Section: Dynamic Setting Categories Of Thick-skin Provincesmentioning

confidence: 93%

Thick-skin-dominated orogens; from initial inversion to full accretion: an introduction

Němčok

Mora

Cosgrove

2013

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Fifty per cent of orogens have a thick-skin character, and have evolved from passive margin and intra-cratonic rift systems. One group of thick-skin provinces can be found at both pro-and retro-wedges of orogens associated with advancing subduction zones, that is, orogenic wedges whose advance vectors oppose the mantle flow. A second group can be found at prowedges of orogens associated with retreating subduction zones, that is, orogens whose advance vectors have the same direction as mantle flow. A third group is formed in intra-plate settings where mechanical strengthening is produced by internal shortening. Thick-skin province development is controlled by driving factors such as individual plate movement rates, overall convergence rates, orogen movement sense with respect to mantle flow, and pro-wedge v. retro-wedge location. These driving factors are themselves constrained by numerous internal and external factors. This introductory chapter focusses primarily on least-deformed case areas in order to understand the role of different factors in controlling the evolution of thick-skin tectonic provinces from the initial inversion stage to full accretion stage.Many thrust belts exhibit both thin-and thick-skin structural styles in different portions of the belt. Some thrust belts, such as the Andes, change style along-strike (Allmendinger et al. 1997;Baby et al. 2013; Carrera & Muñoz 2013;Iaffa et al. 2013;Moretti et al. 2013). Other thrust belts, such as the US Cordillera -Rocky Mountains, exhibit thin-skin structural styles in their interior and thick-skin style in their exterior (Hamilton 1988). A quick screening of the basic characteristics of orogens whose deformation styles are known (see Nemčok et al. 2005) shows that 50% of orogens have a thick-skin character. They have evolved from either passive margins or intra-cratonic rift systems. The most typical examples of the former (initial passive margin setting) are various Andean thick-skin provinces, the Tienshan and the Western Alps (Schmid et al. 1996(Schmid et al. , 1997Escher & Beaumont 1997 Each of these examples underwent a different portion of the complete deformation history of a thick-skin orogen, that is, from initial inversion to full accretion. An excellent introduction to this complete history can be found in Teixell & Babault (2013), who look at shortening across a number of orogens. They record a total shortening of 20 -25% across the High Atlas, 25-30% across the Eastern Cordillera of Colombia and about 40% across the Pyrenees. While Teixell & Babault (2013) reconstructed the complex deformation sequence in the Pyrenees and understood that mountain building comes from the numerous large-scale footwall edge short-cut faults through the rift margin, a less deformed record of the Eastern Cordillera allows one to see that a slow Paleocene -Eocene deformation was followed by the faster Oligocene-Early Miocene deformation and then by an accelerated deformation that took place since Late Miocene Silva et al. 2013). Work on the timing of ...

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Structure of the West Carpathian accretionary wedge: Insights from cross section construction and sandbox validation

Cited by 22 publications

References 5 publications

Along-strike variation in crustal shortening and kinematic evolution of the base of a retroarc fold-and-thrust belt: Magallanes, Chile 53°S-54°S

Along-strike variation in crustal shortening and kinematic evolution of the base of a retroarc fold-and-thrust belt: Magallanes, Chile 53°S-54°S

Oil reservoirs in foreland basins charged by thrustbelt source rocks: insights from numerical stress modelling and geometric balancing in the West Carpathians

Thick-skin-dominated orogens; from initial inversion to full accretion: an introduction

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