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viscous materials
Reply to “Comment on ‘If Not Brittle: Ductile, Plastic, or Viscous?’ by Kelin Wang” by Marco A. Lopez‐Sanchez, Sylvie Demouchy, and Catherine Thoraval
Comment on “If Not Brittle: Ductile, Plastic, or Viscous?” by Kelin Wang
Long-lasting viscous drainage of eclogites from the cratonic lithospheric mantle after Archean subduction stacking
Tectonic pressure gradients during viscous creep drive fluid flow and brittle failure at the base of the seismogenic zone
An analytic signal-based accurate time-domain viscoacoustic wave equation from the constant- Q theory
Least-squares reverse time migration of multiples in viscoacoustic media
Load-indentation testing to assess porewater pressure effects on linear drag and disc cutting of a saturated permeable brittle rock
Laboratory investigation of nonlinear flow characteristics through natural rock fractures
Wave modeling in viscoacoustic media with transverse isotropy
Coupling of fluid flow to permeability development in mid- to upper crustal environments: a tale of three pressures
Abstract Orogenic gold systems are open, flow-controlled thermodynamic systems and generally occur in mid- to upper crustal environments where there is strong coupling between fluid flow and dilatant plastic deformation. This paper considers the principles involved in such coupling, with an emphasis on the elastic and plastic volume changes and their influence on the fluid, mechanical and thermodynamic pressures. Some misconceptions regarding the magnitudes of these three distinctly different pressures and their influences on fluid flow and chemical equilibrium are addressed, with examples at both the tens of metres scale and the crustal scale. We show that the mean stress is less than twice the lithostatic stress for Mohr–Coulomb materials with cohesion and the thermodynamic pressure only has meaning under isentropic conditions and hence is less than many previously published estimates based on high mean stresses. At the crustal scale, we also include the role of critical behaviour in influencing the geometry and magnitudes of fluid pressure gradients and fluid flow velocities in open, flow-controlled systems.
Shape of Time Domain Reflectometry Signals during the Passing of Wetting Fronts
Abstract: Salt is mechanically weaker than other sedimentary rocks in rift basins. It commonly acts as a strain localizer, and decouples supra- and sub-salt deformation. In the rift basins discussed in this paper, sub-salt faults commonly form wide and deep ramp synclines controlled by the thickness and strength of the overlying salt section, as well as by the shapes of the extensional faults, and the magnitudes and slip rates along the faults. Upon inversion of these rift basins, the inherited extensional architectures, and particularly the continuity of the salt section, significantly controls the later contractional deformation. This paper utilizes scaled sandbox models to analyse the interplay between sub-salt structures and supra-salt units during both extension and inversion. Series 1 experiments involved baseline models run using isotropic sand packs for simple and ramp-flat listric faults, as well as for simple planar and kinked planar faults. Series 2 experiments involved the same fault geometries but also included a pre-extension polymer layer to simulate salt in the stratigraphy. In these experiments, the polymer layer decoupled the extensional and contractional strains, and inhibited the upwards propagation of sub-polymer faults. In all Series 2 experiments, the extension produced a synclinal hanging-wall basin above the polymer layer as a result of polymer migration during the deformation. During inversion, the supra-polymer synclinal basin was uplifted, folded and detached above the polymer layer. Changes in thickness of the polymer layer during the inversion produced primary welds and these permitted the sub-polymer deformation to propagate upwards into the supra-salt layers. The experimental results are compared with examples from the Parentis Basin (Bay of Biscay), the Broad Fourteens Basin (southern North Sea), the Feda Graben (central North Sea) and the Cameros Basin (Iberian Range, Spain).