Mechanical and transport constitutive models for fractures subject to dissolution and precipitation

Transient changes in the permeability of fractures in systems driven far‐from‐equilibrium are described in terms of proxy roles of stress, temperature and chemistry. The combined effects of stress and temperature are accommodated in the response of asperity bridges where mineral mass is mobilized from the bridge to the surrounding fluid. Mass balance within the fluid accommodates mineral mass either removed from the flow system by precipitation or advection, or augmented by either dissolution or advection. Where the system is hydraulically closed and initially at equilibrium, reduction in aperture driven by the effects of applied stresses and temperatures will be augmented by precipitation on the fracture walls. Where the system is open, the initial drop in aperture may continue, and accelerate, where the influent fluid is oversaturated with respect to the equilibrium mineral concentration within the fluid, or may reverse, if undersaturated. This simple zero‐dimensional model is capable of representing the intricate behavior observed in experiments where the feasibility of fracture sealing concurrent with net dissolution is observed. This zero‐order model is developed as a constitutive model capable of representing key aspects of changes in the transport parameters of the continuum response of fractured media to changes in stress, temperature and chemistry. Copyright © 2009 John Wiley & Sons, Ltd.

[1]  Yasuhiro Mitani,et al.  Evolution of fracture permeability through fluid–rock reaction under hydrothermal conditions , 2006 .

[2]  I. Main,et al.  Fault gouge diagenesis at shallow burial depth: Solution precipitation reactions in well-sorted and poorly sorted powders of crushed sandstone , 2006 .

[3]  Jishan Liu,et al.  A fully-coupled hydrological-mechanical-chemical model for fracture sealing and preferential opening , 2006 .

[4]  Derek Elsworth,et al.  Dissolution-induced preferential flow in a limestone fracture. , 2005, Journal of contaminant hydrology.

[5]  B. Berkowitz,et al.  The role of fractures on coupled dissolution and precipitation patterns in carbonate rocks , 2005 .

[6]  C. Spiers,et al.  Structure and diffusive properties of fluid-filled grain boundaries: An in-situ study using infrared (micro) spectroscopy , 2005 .

[7]  I. Kockum,et al.  Hydrogeochemical changes before and after a major earthquake , 2004 .

[8]  M. Nakatani,et al.  Frictional healing of quartz gouge under hydrothermal conditions: 1. Experimental evidence for solution transfer healing mechanism , 2004 .

[9]  F. Chester,et al.  Mechanisms of compaction of quartz sand at diagenetic conditions , 2004 .

[10]  D. Elsworth,et al.  Evolution of permeability in a natural fracture: Significant role of pressure solution , 2004 .

[11]  P. Meakin,et al.  Three-dimensional roughness of stylolites in limestones , 2004 .

[12]  I. Main,et al.  Loading rate dependence of permeability evolution in porous aeolian sandstones , 2004 .

[13]  D. Elsworth,et al.  A mechanistic model for compaction of granular aggregates moderated by pressure solution , 2003 .

[14]  Phillip M. Halleck,et al.  Permeability reduction of a natural fracture under net dissolution by hydrothermal fluids , 2003 .

[15]  C. Scholz,et al.  The fractal geometry of some stylolites from the Calcare Massiccio Formation, Italy , 2003 .

[16]  François Renard,et al.  Modeling fluid transfer along California faults when integrating pressure solution crack sealing and compaction processes , 2003 .

[17]  B. Berkowitz,et al.  Evolution of hydraulic conductivity by precipitation and dissolution in carbonate rock , 2003 .

[18]  A. Grader,et al.  Spontaneous switching of permeability changes in a limestone fracture with net dissolution , 2002 .

[19]  S. Cox,et al.  Evolution of strength recovery and permeability during fluid–rock reaction in experimental fault zones , 2002 .

[20]  François Renard,et al.  Fluid pressure evolution during the earthquake cycle controlled by fluid flow and pressure solution crack sealing , 2002 .

[21]  A. Niemeijer,et al.  Compaction creep of quartz sand at 400-600°C: Experimental evidence for dissolution-controlled pressure solution , 2002 .

[22]  C. Spiers,et al.  Frictional-viscous flow of phyllosilicate-bearing fault rock: Microphysical model and implications for crustal strength profiles , 2002 .

[23]  M. Paterson,et al.  Microcrack growth and healing in deformed calcite aggregates , 2001 .

[24]  Dag Kristian Dysthe,et al.  Enhanced pressure solution creep rates induced by clay particles: Experimental evidence in salt aggregates , 2001 .

[25]  E. Burton,et al.  Direct observation of reactive flow in a single fracture , 2001 .

[26]  François Renard,et al.  Kinetics of crack-sealing, intergranular pressure solution, and compaction around active faults , 2000 .

[27]  C. Peach,et al.  Slip behavior of simulated gouge‐bearing faults under conditions favoring pressure solution , 2000 .

[28]  S. Cox,et al.  Effects of dissolution-precipitation processes on the strength and mechanical behavior of quartz gouge at high-temperature hydrothermal conditions , 2000 .

[29]  C. Scholz,et al.  Precipitation sealing and diagenesis: 1. Experimental results , 1998 .

[30]  C. Scholz,et al.  Precipitation sealing and diagenesis: 2. Theoretical analysis , 1998 .

[31]  T. Dewers,et al.  Dissolution and time-dependent compaction of albite sand: experiments at 100°C and 160°C in pH-buffered organic acids and distilled water , 1998 .

[32]  François Renard,et al.  Pressure solution in sandstones: influence of clays and dependence on temperature and stress , 1997 .

[33]  G. Dresen,et al.  Effect of semibrittle deformation on transport properties of calcite rocks , 1997 .

[34]  S. Hickman,et al.  Kinetics of pressure solution at halite‐silica interfaces and intergranular clay films , 1995 .

[35]  D. Lockner,et al.  Reduction of Permeability in Granite at Elevated Temperatures , 1994, Science.

[36]  M. Paterson,et al.  The influence of room temperature deformation on porosity and permeability in calcite aggregates , 1994 .

[37]  A. Howard,et al.  Minimum hydrochemical conditions allowing limestone cave development , 1994 .

[38]  Larry W. Lake,et al.  Effect of partial local equilibrium on the propagation of precipitation/dissolution waves , 1993 .

[39]  J. Gratier.  Experimental pressure solution of Halite by an indenter technique , 1993 .

[40]  Derek Elsworth,et al.  Laboratory assessment of the equivalent apertures of a rock fracture , 1993 .

[41]  A. Hajash,et al.  Changes in quartz solubility and porosity due to effective stress: An experimental investigation of pressure solution , 1992 .

[42]  M. Paterson,et al.  Experimental dissolution‐precipitation creep in quartz aggregates at high temperatures , 1991 .

[43]  W. Daily,et al.  Hydrological properties of Topopah Spring tuff under a thermal gradient—Laboratory results , 1990 .

[44]  Raymond Siever,et al.  Pressure solution during diagenesis , 1989 .

[45]  R. Groshong.  Low-temperature deformation mechanisms and their interpretation , 1988 .

[46]  Thomas A. Buscheck,et al.  Hydrological properties of Topopah Spring tuff: Laboratory measurements , 1987 .