Orocline and syntaxes formation during subduction and collision

Bajolet, Flora; Replumaz, Anne; Lainé, Romain

doi:10.1002/tect.20087

Cited by 27 publications

(42 citation statements)

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“…In the interest of simplicity in the models and because the shape of Greater India is still highly debated [see review Ali and Aitchison , ], the Indian continent is approximated as a square shape extending 2100 km × 2100 km laterally (Figure b, map view). We note that a similar geometry of the model setup was also explored in analogue models [ Bajolet et al ., ].…”

Section: Methodsmentioning

confidence: 99%

Development of topography in 3‐D continental‐collision models

Pusok

Kaus

2015

Geochem Geophys Geosyst

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Understanding the formation and evolution of high mountain belts, such as the Himalayas and the adjacent Tibetan Plateau, has been the focus of many tectonic and numerical models. Here we employ 3-D numerical simulations to investigate the role that subduction, collision, and indentation play on lithosphere dynamics at convergent margins, and to analyze the conditions under which large topographic plateaus can form in an integrated lithospheric and upper mantle-scale model. Distinct dynamics are obtained for the oceanic subduction side (trench retreat, slab rollback) and the continental-collision side (trench advance, slab detachment, topographic uplift, lateral extrusion). We show that slab pull alone is insufficient to generate high topography in the upper plate, and that external forcing and the presence of strong blocks such as the Tarim Basin are necessary to create and shape anomalously high topographic fronts and plateaus. Moreover, scaling is used to predict four different modes of surface expression in continentalcollision models: (I) low-amplitude homogeneous shortening, (II) high-amplitude homogeneous shortening, (III) Alpine-type topography with topographic front and low plateau, and (IV) Tibet-Himalaya-type topography with topographic front and high plateau. Results of semianalytical models suggest that the Argand number governs the formation of high topographic fronts, while the amplitude of plateaus is controlled by the initial buoyancy ratio of the upper plate. Applying these results to natural examples, we show that the Alps belong to regime (III), the Himalaya-Tibet to regime (IV), whereas the Andes-Altiplano fall at the boundary between regimes (III) and (IV).

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Section: Methodsmentioning

confidence: 99%

Development of topography in 3‐D continental‐collision models

Pusok

Kaus

2015

Geochem Geophys Geosyst

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“…of the order 2 × 10 2 (Schellart, 2004a,b;Meyer and Schellart, 2013;Chen et al, 2015b), 6 × 10 2 (Mériaux et al, 2015a,b) and 3.5−10 × 10 2 , to intermediate values, i.e. of the order 1.5 × 10 3 (Bajolet et al, 2013), 6 × 10 3 (Guillaume et al, 2009), 1.2 × 10 4 (Heuret et al, 2007) and 1.5 × 10 4 (Martinod et al, 2013), to relatively high values, i.e. of the order 10 4 -10 5 (Funiciello et al, 2006) and 10 6 -10 7 (e.g.…”

Section: Scaling Of Subduction Modelsmentioning

confidence: 97%

“…The most commonly used materials include hydrocarbon compositional systems, which are mixtures of solid hydrocarbons, powders and mineral oils (Shemenda, 1992(Shemenda, , 1993Chemenda et al, 1995Chemenda et al, , 2000Boutelier et al, 2003;Boutelier and Cruden, 2013), plasticine (Tapponnier et al,1982), wax (Brune and Ellis, 1997), petrolatum or petroleum jelly (e.g. Heuret et al, 2007;Bajolet et al, 2013) and paraffin oil-petrolatum mixtures (Duarte et al, 2013(Duarte et al, , 2014Edwards et al, 2015). The latter two materials have in particular been used to coat the subduction zone interface in subduction experiments.…”

Section: Materials With Linear Viscous Non-linear Viscous Visco-plamentioning

confidence: 99%

“…Examples of mantle-scale experiments include a variety of subduction experiments with negatively buoyant slabs in which the rate of plate motion is externally controlled by one or more pistons (e.g. Shemenda, 1992Shemenda, , 1993Faccenna et al, 1999;Regard et al, 2003;Boutelier et al, 2003;Schellart, 2005;Heuret et al, 2007;Guillaume et al, 2009;Gögüş et al, 2011;Martinod et al, 2013;Bajolet et al, 2013;Agard et al, 2014), experiments that include buoyancy-driven subduction and externally-controlled plume injection (e.g. Mériaux et al, 2015aMériaux et al, , 2015b, and thermochemical convection and plume formation experiments, where motions in the system are driven by temperature gradients applied externally and by internal density heterogeneities of chemical origin (Davaille et al, 2002;Le Bars and Davaille, 2004;Kumagai et al, 2007).…”

Section: Combined (External + Internal) Approachmentioning

confidence: 99%

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A review of analogue modelling of geodynamic processes: Approaches, scaling, materials and quantification, with an application to subduction experiments

Schellart

Strak

2016

Journal of Geodynamics

126

105

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a b s t r a c tWe present a review of the analogue modelling method, which has been used for 200 years, and continues to be used, to investigate geological phenomena and geodynamic processes. We particularly focus on the following four components: (1) the different fundamental modelling approaches that exist in analogue modelling; (2) the scaling theory and scaling of topography; (3) the different materials and rheologies that are used to simulate the complex behaviour of rocks; and (4) a range of recording techniques that are used for qualitative and quantitative analyses and interpretations of analogue models. Furthermore, we apply these four components to laboratory-based subduction models and describe some of the issues at hand with modelling such systems. Over the last 200 years, a wide variety of analogue materials have been used with different rheologies, including viscous materials (e.g. syrups, silicones, water), brittle materials (e.g. granular materials such as sand, microspheres and sugar), plastic materials (e.g. plasticine), viscoplastic materials (e.g. paraffin, waxes, petrolatum) and visco-elasto-plastic materials (e.g. hydrocarbon compounds and gelatins). These materials have been used in many different set-ups to study processes from the microscale, such as porphyroclast rotation, to the mantle scale, such as subduction and mantle convection. Despite the wide variety of modelling materials and great diversity in model set-ups and processes investigated, all laboratory experiments can be classified into one of three different categories based on three fundamental modelling approaches that have been used in analogue modelling: (1) The external approach, (2) the combined (external + internal) approach, and (3) the internal approach. In the external approach and combined approach, energy is added to the experimental system through the external application of a velocity, temperature gradient or a material influx (or a combination thereof), and so the system is open. In the external approach, all deformation in the system is driven by the externally imposed condition, while in the combined approach, part of the deformation is driven by buoyancy forces internal to the system. In the internal approach, all deformation is driven by buoyancy forces internal to the system and so the system is closed and no energy is added during an experimental run. In the combined approach, the externally imposed force or added energy is generally not quantified nor compared to the internal buoyancy force or potential energy of the system, and so it is not known if these experiments are properly scaled with respect to nature. The scaling theory requires that analogue models are geometrically, kinematically and dynamically similar to the natural prototype. Direct scaling of topography in laboratory models indicates that it is often significantly exaggerated. This can be ascribed to (1) The lack of isostatic compensation, which causes topography to be too high.(2) The lack of erosion, which causes topography to be too high....

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“…The plate boundary stays almost straight unlike the arcuate Himalaya bounded by syntaxes. This implies that processes not reproduced in the experiments and controlled by earlier oceanic subduction stages and/or the shape of Greater India [ Ali and Aitchison , ; Replumaz et al ., ; van Hinsbergen et al ., ; Bajolet et al ., ] would be responsible for specific features of the orogen such as (i) the Himalayan orocline and the variable strike of rifts potentially due to oroclinal bending [ Ratschbacher et al ., ], (ii) the lateral variations in strain orientation along the orogenic front [ Seeber and Pecher , ; Kapp and Guynn , ], and (iii) southward propagation of the orogenic front [ Murphy and Copeland , ; Bajolet et al ., ]. In our models, the grabens are also restricted to the plate boundary area and within the cratonic lithosphere, and transpression is confined to the inner plateau (Figures ), whereas central Tibet is under transtension [ Andronicos et al ., ].…”

Section: Discussionmentioning

confidence: 99%

Synconvergence flow inside and at the margin of orogenic plateaus: Lithospheric‐scale experimental approach

et al. 2015

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This study investigates three‐dimensional flow modes of orogenic plateaus by means of physical modeling. Experiments consist of shortening two contiguous lithospheres of contrasting strength, one being a weak plateau‐type lithosphere and the other a strong craton‐type lithosphere. The lateral boundaries are either totally confined or allow escape toward a lateral foreland on one side. Two synconvergence flow regimes are distinguished, which are governed by the balance between the gravity potential and the strength of the plateau crust and the resistance of its lateral foreland. The first regime implies transversal (orogen‐normal) injection of plateau lower crust into the collision zone as a result of confinement of the plateau by an increasingly stiffer lateral boundary. As a precursor mechanism to channel flow, transversal injection responds to downward thickening of the plateau crust that is forcedly extruded into the orogenic wedge. The second regime is that of collapse‐driven lateral escape of the plateau. This regime is established after a threshold is attained in the interplate coupling in the collision zone, which allows the gravity potential of the plateau to overcome the resistance of its lateral boundary. Under the collapse‐driven escape regime (orogen parallel), such as that governing Tibet during the last 13 Ma, most of the convergence in the plateau and the top and rear of the collisional wedge is transformed into lateral flow and extension.

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Orocline and syntaxes formation during subduction and collision

Cited by 27 publications

References 82 publications

Development of topography in 3‐D continental‐collision models

Development of topography in 3‐D continental‐collision models

A review of analogue modelling of geodynamic processes: Approaches, scaling, materials and quantification, with an application to subduction experiments

Synconvergence flow inside and at the margin of orogenic plateaus: Lithospheric‐scale experimental approach

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