Structural permeability of fluid-driven fault-fracture meshes

Abstract

Fluid redistribution in the crust is influenced by hydraulic gradient, by existing permeability anisotropy arising from bedding and other forms of layering, and by structural permeability developed under the prevailing stress field. Field evidence suggests that mesh structures, comprising faults interlinked with extensional-shear and purely extensional vein-fractures, form important conduits for large volume flow of hydrothermal and hydrocarbon fluids. Meshes may be ‘self-generated’ by the infiltration of pressurised fluids into a stressed heterogeneous rock mass with varying material properties, developing best where bulk coaxial strain is symmetric with existing layering, but they also form under predominantly simple shear. Fluid passage through such structures generates earthquake swarm activity by distributed fault-valve action along suprahydrostatic gradients that may arise from compaction overpressuring, metamorphic dewatering, magmatic intrusion, and mantle degassing. Within mesh structures, strong directional permeability may develop in the σ 2 direction parallel to fault-fracture intersections and orthogonal to fault slip vectors. In particular tectonic settings, this promotes strongly focused flow with high potential for mineralisation. Mesh activation requires the condition P f ~ σ 3 to be maintained for the structures to remain high permeability conduits, requiring fluid overpressuring at other than shallow depths in extensional-transtensional regimes. Favoured localities for mesh development include linkage structures along large-displacement fault zones such as dilational jogs, lateral ramps, and transfer faults. In some circumstances, mesh formation appears to precede the development of major faults.