Single layer folding in simple shear |
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| Institution: | 1. Departament of Geosciences, Eberhard Karls University Tübingen, Wilhemstr. 56, 72074 Tübingen, Germany;2. Departament de Geologia, Universitat Autònoma de Barcelona, 08193 Bellaterra, Barcelona, Spain;3. School of Geosciences, Monash University, Clayton, Victoria 3800, Australia;1. School of Environmental and Life Sciences, University of Newcastle, University Drive, Callaghan, 2308, NSW, Australia;2. School of Earth and Ocean Sciences, University of Victoria, Victoria, British-Columbia, Canada;3. Department of Earth and Atmospheric Sciences, University of Alberta, Edmonton, Alberta, Canada;4. School of Earth, Atmosphere and Environment, Monash University, Clayton, VIC, 3800, Australia;1. School of Mathematical Sciences, Monash University, Clayton, VIC, Australia;2. School of Earth Sciences, Melbourne University, Melbourne, VIC, Australia;3. Department of Earth and Atmospheric Sciences, University of Houston, Houston, TX, USA;4. Institute of Geophysics, ETH Zurich, Zurich, Switzerland;1. Geosciences Montpellier, CNRS & Université de Montpellier, F-34095 Montpellier cedex 5, France;2. Univ. Lille, CNRS, INRA, ENSCL, UMR 8207 – UMET – Unité Matériaux et Transformations, F-59000 Lille, France;1. Key Laboratory of Deep-Earth Dynamics of Ministry of Natural Resources, Institute of Geology, Chinese Academy of Geological Sciences, Beijing, 100037, China;2. Bureau of Economic Geology, The University of Texas at Austin, 10100 Burnet Rd, 78758, Austin, Texas, USA;3. Chinese Academy of Geological Sciences, Beijing, 100037, China |
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| Abstract: | Despite the common occurrence of simple shear deformation, laboratory and numerical simulations of folding have so far been almost exclusively in pure shear. Here we present a series of finite-element simulations of single layer folding in simple shear up to high shear strains (γ ≤ 4, and up to 75% shortening of the folding layer). In the simulations we vary the viscosity contrast between layer and its surroundings (25–100), the stress exponent (1 or 3) and the kinematics of deformation (pure- versus simple shear). In simple shear fold trains do not show a clear asymmetry, axial planes form perpendicular to the developing fold train and rotate along with the fold train. Differences in geometries between folds formed in simple and pure shear folds are thus difficult to distinguish visually, with simple shear folds slightly more irregular and with more variable axial plane orientation than in pure shear. Asymmetric refraction of an axial planar cleavage is a clearer indication of folding in simple shear. The main effect of an increase in stress exponent is an increase in effective viscosity contrast, with only a secondary effect on fold geometry. Naturally folded aplite dykes in a granodiorite are found in a shear zone in Roses, NE Spain. Comparison of the folded dykes with our numerical simulations indicates a viscosity contrast of around 25 and a stress exponent of 3. The natural folds confirm that at this moderate viscosity contrast, a significant amount of shortening (20–30%) is achieved by layer thickening instead of folding. |
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