Folding and faulting of strain-hardening sedimentary rocks

Johnson, Abigail M.

doi:10.1016/0148-9062(81)90357-0

Cited by 4 publications

(5 citation statements)

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“…Several studies have therefore investigated the parameters that control whether shortening of rock layers is more likely to take place by folding or faulting (e.g. Johnson, 1980;Erickson, 1996;Simpson, 2009;Yamato et al, 2011). The question of "folding vs. faulting" is of particular interest for fold-and-thrust belts (e.g.…”

Section: Lithospheric Foldingmentioning

confidence: 99%

“…Jura, Zagros or Appalachians). For example, Johnson (1980) applied the stability analysis described above to elasto-plastic, strainhardening layers and showed that during shortening of such layers folding is more likely than faulting for (i) multilayers and (ii) frictionless layer contacts. In many analytical studies involving plastic deformation, the plastic layer is characterised either by a representative, constant yield stress or by a large power-law stress exponent, which mimics a constant von Mises stress (e.g.…”

Section: Lithospheric Foldingmentioning

confidence: 99%

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Folding and necking across the scales: a review of theoretical and experimental results and their applications

Schmalholz

Mancktelow

2016

Solid Earth

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Abstract. The shortening and extension of mechanically layered ductile rock generates folds and pinch-and-swell structures (also referred to as necks or continuous boudins), which result from mechanical instabilities termed folding and necking, respectively. Folding and necking are the preferred deformation modes in layered rock because the corresponding mechanical work involved is less than that associated with a homogeneous deformation. The effective viscosity of a layered rock decreases during folding and necking, even when all material parameters remain constant. This mechanical softening due to viscosity decrease is solely the result of fold and pinch-and-swell structure development and is hence termed structural softening (or geometric weakening). Folding and necking occur over the whole range of geological scales, from microscopic up to the size of lithospheric plates. Lithospheric folding and necking are evidence for significant deformation of continental plates, which contradicts the rigid-plate paradigm of plate tectonics. We review here some theoretical and experimental results on folding and necking, including the lithospheric scale, together with a short historical overview of research on folding and necking. We focus on theoretical studies and analytical solutions that provide the best insight into the fundamental parameters controlling folding and necking, although they invariably involve simplifications. To first order, the two essential parameters to quantify folding and necking are the dominant wavelength and the corresponding maximal amplification rate. This review also includes a short overview of experimental studies, a discussion of recent developments involving mainly numerical models, a presentation of some practical applications of theoretical results, and a summary of similarities and differences between folding and necking.

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Section: Lithospheric Foldingmentioning

confidence: 99%

Section: Lithospheric Foldingmentioning

confidence: 99%

Folding and necking across the scales: a review of theoretical and experimental results and their applications

Schmalholz

Mancktelow

2016

Solid Earth

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“…The strength of a multilayer is determined by the mechanical nature of the contacts between the layers (Johnson, 1980). It has been shown that a blind thrust fault propagating upward will induce folding of a multilayer if the layer contacts are weak (i.e., low shear strength) (Nino et al, 1998).…”

Section: Influence Of Mechanical Properties On Fault Geometrymentioning

confidence: 99%

Elastic dislocation modeling of wrinkle ridges on Mars

Watters

2004

Icarus

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“…Whatever the scale, an important result of these analytical studies is a maximum of amplification rate for a certain fold wavelength, which is designated the dominant wavelength [Biot, 1961]. Dominant wavelengths of small-scale folds were investigated for elastic [e.g., Biot, 1961], elastoplastic [e.g., Johnson, 1980], viscous [e.g., Biot, 1961], ductile (non-Newtonian, power law) [e.g., Fletcher, 1974], and viscoelastic [e.g., Schmalholz andPodladchikov, 1999, 2001a] layers embedded in an infinitely thick (half-space) matrix and for elastic layers resting on a viscoelastic matrix [e.g., Hunt et al, 1996], elastic layers resting on a finite, viscous matrix [Sridhar et al, 2001], and viscous layers embedded in a finite, viscous matrix [Ramberg, 1963]. Dominant wavelengths of large-scale folds were expressed for elastic [Ramberg and Stephansson, 1964;Turcotte and Schubert, 1982] and ductile [Burov and Molnar, 1998;Cloetingh et al, 1999] layers.…”

Section: Introductionmentioning

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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Folding and faulting of strain-hardening sedimentary rocks

Cited by 4 publications

References 0 publications

Folding and necking across the scales: a review of theoretical and experimental results and their applications

Folding and necking across the scales: a review of theoretical and experimental results and their applications

Elastic dislocation modeling of wrinkle ridges on Mars

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

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