Stretching instabilities and lithospheric boudinage

Ricard, Yanick; Froidevaux, C.

doi:10.1029/jb091ib08p08314

Cited by 102 publications

(95 citation statements)

References 13 publications

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“…The extension in the back-arc propagates eastward like the roll-back of the subduction zone. The stretching is discontinuous, producing basins and swells that recall the Ž boudinage Ricard and Froidevaux, 1986;Gueguen . et al, 1997 .…”

Section: Back-arc Basinsmentioning

confidence: 99%

Orogens and slabs vs. their direction of subduction

Doglioni

Harabaglia

Merlini

et al. 1999

Earth-Science Reviews

303

198

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Section: Back-arc Basinsmentioning

confidence: 99%

Orogens and slabs vs. their direction of subduction

Doglioni

Harabaglia

Merlini

et al. 1999

Earth-Science Reviews

303

198

View full text Add to dashboard Cite

“…It was subsequently shown that lithospheric necking for slow spreading rates (1-3 cm yr −1 ) is feasible for creep flow laws considered typical for the lithosphere (Tapponnier and Francheteau, 1978). Later, the stability analysis (described above for folding) has been applied to study necking instability during lithospheric extension (Fletcher and Hallet, 1983;Ricard and Froidevaux, 1986;, including lithospheric models with two competent layers (upper crust and upper mantle) separated by a weak lower crust . Compared to small-scale necking models, models of lithospheric necking are usually more complex because they consider (i) gravity, (ii) one or more competent layers with a very high power-law stress exponent mimicking effectively plastic deformation, (iii) a viscosity that decays exponentially with depth in the weak layers to mimic the temperature dependence and (iv) some kind of stress limit to mimic the brittle yield strength of rock.…”

Section: Multilayer Neckingmentioning

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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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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“…We assume the mass of the necking region is conserved; hence hb is a constant. Moreover, we assume h 0 = αD 0 , which is half the wavelength of the initial infinitesimal necking instability (38,39); α itself is dependent on rheology, and for our model, with a Newtonian surrounding mantle and a slab initially in dislocation creep (see Rheology), α ≈ 5. Therefore, hb = αD 2 0 , and since w = dh=dt, then…”

Section: Significancementioning

confidence: 99%

Abrupt tectonics and rapid slab detachment with grain damage

Bercovici

Schubert

Ricard

2015

Proc. Natl. Acad. Sci. U.S.A.

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A simple model for necking and detachment of subducting slabs is developed to include the coupling between grain-sensitive rheology and grain-size evolution with damage. Necking is triggered by thickened buoyant crust entrained into a subduction zone, in which case grain damage accelerates necking and allows for relatively rapid slab detachment, i.e., within 1 My, depending on the size of the crustal plug. Thick continental crustal plugs can cause rapid necking while smaller plugs characteristic of ocean plateaux cause slower necking; oceanic lithosphere with normal or slightly thickened crust subducts without necking. The model potentially explains how large plateaux or continental crust drawn into subduction zones can cause slab loss and rapid changes in plate motion and/or induce abrupt continental rebound.subduction zones | slab detachment | plate tectonics | continent rebound

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Stretching instabilities and lithospheric boudinage

Cited by 102 publications

References 13 publications

Orogens and slabs vs. their direction of subduction

Orogens and slabs vs. their direction of subduction

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

Abrupt tectonics and rapid slab detachment with grain damage

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