Do faults trigger folding in the lithosphere?

Gerbault, Muriel; Burov, E. B.; Poliakov, Alexei N. B.; Daignières, M.

doi:10.1029/1998gl900293

Cited by 80 publications

(79 citation statements)

References 23 publications

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“…11). On the other hand, the observed folds are consistent with the results of analogue and numerical models, where horizontal shortening of the lithosphere produces periodic buckle folds Davy 1992, 1994;Martinod and Molnar 1995;Gerbault et al 1999;Cloetingh et al 1999;Gerbault 2000). Wavelengths on the order of 270 km and amplitudes on the order of 1,500 m are obtained in models of buckling, when the crust is not decoupled from the mantle.…”

Section: Folding Processsupporting

confidence: 87%

“…Some analogue and numerical models suggest that the primary response of the lithosphere to horizontal shortening could be the development of periodic buckle folds (Bull et al 1992;Davy 1992, 1994;Burov et al 1993;Martinod and Molnar 1995;Ziegler et al 1995;Gerbault et al 1999;Cloetingh et al 1999;Gerbault 2000). According to these models, lithospheric folds would develop over distances of several thousands of kilometres from plate borders.…”

Section: Intraplate Bucklingmentioning

confidence: 97%

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Separation of rifting and lithospheric folding signatures in the NW-Alpine foreland

Bourgeois

Ford

Diraison

et al. 2007

Int J Earth Sci (Geol Rundsch)

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International audienceThe development of the Alpine mountain belt has been governed by the convergence of the African and European plates since the Late Cretaceous. During the Cenozoic, this orogeny was accompanied with two major kinds of intraplate deformation in the NW-European foreland: (1) the European Cenozoic Rift System (ECRIS), a left-lateral transtensional wrench zone striking NNE-SSW between the western Mediterranean Sea and the Bohemian Massif; (2) long-wavelength lithospheric folds striking NE and located between the Alpine front and the North Sea. The present-day geometry of the European crust comprises the signatures of these two events superimposed on all preceding ones. In order to better define the processes and causes of each event, we identify and separate their respective geometrical signatures on depth maps of the pre-Mesozoic basement and of the Moho. We derive the respective timing of rifting and folding from sedimentary accumulation curves computed for selected locations of the Upper Rhine Graben. From this geometrical and chronological separation, we infer that the ECRIS developed mostly from 37 to 17 Ma, in response to north-directed impingement of Adria into the European plate. Lithospheric folds developed between 17 and 0 Ma, after the azimuth of relative displacement between Adria and Europe turned counter-clockwise to NW SE. The geometry of these folds (wavelength = 270 km; amplitude = 1,500 m) is consistent with the geometry, as predicted by analogue and numerical models, of buckle folds produced by horizontal shortening of the whole lithosphere. The development of the folds resulted in ca. 1,000 m of rock uplift along the hinge lines of the anticlines (Burgundy Swabian Jura and Normandy Vogelsberg) and ca. 500 m of rock subsidence along the hinge line of the intervening syncline (Sologne Franconian Basin). The grabens of the ECRIS were tilted by the development of the folds, and their rift-related sedimentary infill was reduced on anticlines, while sedimentary accumulation was enhanced in synclines. We interpret the occurrence of Miocene volcanic activity and of topographic highs, and the basement and Moho configurations in the Vosges Black Forest area and in the Rhenish Massif as interference patterns between linear lithospheric anticlines and linear grabens, rather than as signatures of asthenospheric plumes

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Section: Folding Processsupporting

confidence: 87%

Section: Intraplate Bucklingmentioning

confidence: 97%

Separation of rifting and lithospheric folding signatures in the NW-Alpine foreland

Bourgeois

Ford

Diraison

et al. 2007

Int J Earth Sci (Geol Rundsch)

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“…Ultimately, however, it is not surprising that boudinage of Ganymede's surface layer should be accompanied by macroscopic brittle failure at smaller scales, for there are many paths to localization (e.g., Neumann and Zuber 1995, Gerbault et al 1999, Montési and Zuber 2001a. Multiple generations of fractures and faults may form, on which graben and tilt blocks may move and at spacings similar to or less than the thickness of the brittle layer.…”

Section: Multiple Scales Of Extensionmentioning

confidence: 98%

Formation of Grooved Terrain on Ganymede: Extensional Instability Mediated by Cold, Superplastic Creep

Dombard¹,

McKinnon²

2001

Icarus

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“…Natural settings, especially on the crustal and lithospheric scales, are more complicated because of strong pressure and temperature dependence of material properties, complex rheologies, large strains, effects of shear heating, etc. Numerical methods are required to investigate large strain folding under more complex conditions [e.g., Burov and Molnar, 1998;Burg and Podladchikov, 1999;Gerbault et al, 1999;Schmalholz et al, 2001] because even powerful analytical methods, such as thick-plate or perturbation methods, are unsuitable to incorporate many complex natural conditions. This study does not investigate folding under lithospheric conditions but focuses on the simultaneously acting resistances due to gravity, matrix viscosity, and matrix thickness against fold amplification and especially on the transitions at which one of these resistances starts to control folding.…”

Section: Discussionmentioning

confidence: 99%

Control of folding by gravity and matrix thickness: Implications for large‐scale folding

2002

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[1] We show that folding of a non-Newtonian layer resting on a homogeneous Newtonian matrix with finite thickness under influence of gravity can occur by three modes: (1) matrix-controlled folding, dependent on the effective viscosity contrast between layer and matrix, (2) gravitycontrolled folding, dependent on the Argand number (the ratio of the stress caused by gravity to the stress caused by shortening), and (3) detachment folding, dependent on the ratio of matrix thickness to layer thickness. We construct a phase diagram that defines the transitions between each of the three folding modes. Our priority is transparency of the analytical derivations (e.g., thin-plate versus thick-plate approximations), which permits complete classification of the folding modes involving a minimum number of dimensionless parameters. Accuracy and sensitivity of the analytical results to model assumptions are investigated. In particular, depth dependence of matrix rheology is only important for folding over a narrow range of material parameters. In contrast, strong depth dependence of the viscosity of the folding layer limits applicability of ductile rheology and leads to a viscoelastic transition. Our theory is applied to estimate the effective thickness of the folded central Asian upper crust using the ratio of topographic wavelength to Moho depth. Phase diagrams based on geometrical parameters show that gravity does not significantly control folding in the Jura and the Zagros Mountains but does control folding in central Asia. Applicability conditions of viscous and thin sheet models for large-scale lithospheric deformation, derived in terms of the Argand number, have implications for the plate-like style of planetary tectonics.

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Do faults trigger folding in the lithosphere?

Cited by 80 publications

References 23 publications

Separation of rifting and lithospheric folding signatures in the NW-Alpine foreland

Separation of rifting and lithospheric folding signatures in the NW-Alpine foreland

Formation of Grooved Terrain on Ganymede: Extensional Instability Mediated by Cold, Superplastic Creep

Control of folding by gravity and matrix thickness: Implications for large‐scale folding

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