Structure and properties of loaded silica contacts during pressure solution: impedance spectroscopy measurements under hydrothermal conditions

Noort, Reinier van; Spiers, Christopher J.; Peach, C. J.

doi:10.1007/s00269-011-0423-6

Cited by 15 publications

(12 citation statements)

References 43 publications

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“…The values obtained for the grain boundary diffusivity product Z* lie in the range 5.7 AE 4Á10 À20 m 3 /s. This agrees well with values in the range of 10 À19 -10 À20 m 3 /s obtained for pressure solution creep in other salts and minerals Spiers et al, 1990;Spiers and Brzesowsky, 1993;Spiers et al, 2004;van Noort et al, 2011;Zhang et al, 2010]. Though the present Z* values showed no dependence on stress or grain size in the range calculated, Z* was found to be up to a factor two smaller at 20% volumetric strain than at 10%.…”

Section: The High-stress Regime: Grain Boundary Diffusivitysupporting

confidence: 92%

Effects of interfacial energy on compaction creep by intergranular pressure solution: Theory versus experiments on a rock analog (NaNO₃)

2012

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[1] Pressure solution plays an important role in compaction and lithification of sediments and fault gouges, but the effects of interfacial energy on this process are generally neglected. Here, microphysical models for densification of solid/liquid systems by pressure solution are derived, accounting for interfacial energy besides stress-related driving forces. They predict that densification by pressure solution creep will slow down at very fine grain sizes, where opposing interfacial energy driving forces become important compared to applied stress, and will come to a halt below a certain "yield" stress. To test the models, uniaxial compaction creep experiments were performed at ambient conditions on granular NaNO 3 aggregates (d = 8-250 mm, s eff = 0.0062-4.9 MPa). Though no significant creep occurred in dry or oil-flooded material, rapid, grain-size sensitive creep occurred in the presence of saturated NaNO 3 solution. At high effective stresses (s eff > 0.025 MPa), wet-compacted, coarser-grained (d > 20 mm) samples showed compaction behavior roughly consistent with diffusion-controlled pressure solution involving negligible interfacial energy effects. Creep rates in this regime imply an effective grain boundary diffusivity product of 5.7 Â 10 À19 m 3 /s. At low effective stress (s eff < 0.025 MPa), finer-grained samples (d < 20 mm) showed a decrease in strain rate with decreasing grain size, reflecting a growing influence of interfacial energy-related driving forces. This demonstrates a yield stress effect, broadly consistent with the predictions of the models incorporating interfacial energy and imply that compaction by pressure solution can be strongly inhibited in very fine-grained materials, such as nanogouge in seismogenic faults.

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Section: The High-stress Regime: Grain Boundary Diffusivitysupporting

confidence: 92%

Effects of interfacial energy on compaction creep by intergranular pressure solution: Theory versus experiments on a rock analog (NaNO₃)

2012

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“…This was following later by the development of experimental techniques where a single grain-grain contact could be imaged optically during pressure solution creep (Gratier, 1993;Hickman and Evans, 1991;Hickman and Evans, 1995). In such kind of experiments, it is also possible to measure in-situ the strain (Croize et al, 2010b;Dysthe et al, 2002a;Dysthe et al, 2003;Hickman and Evans, 1991;Karcz et al, 2006;Zubtsov et al, 2005), and the transport properties of the interface under stress using infra-red spectroscopy (de Meer et al, 2005;de Meer et al, 2002), impedance spectroscopy (van Noort et al, 2011) or surface force apparatus (Greene et al, 2009;Kristiansen et al, 2011). The two families of experiments -deformation of aggregate or single contact studies -are described in more detail in the following sections.…”

Section: -Pressure Solution Creep Experimentsmentioning

confidence: 99%

“…And when the fluid film model breaks down, how does the interface evolve towards an island-and-channel structure? Experiments have been performed on four different materials, ionic salts (de Meer et al, 2002;Dysthe et al, 2002a;Dysthe et al, 2003;Gratier, 1993;Gratier et al, 1999;Hickman and Evans, 1991;Hickman and Evans, 1995;Jordan et al, 2005;Karcz et al, 2006;Martin et al, 1999;Skvortsova et al, 2003;Tada and Siever, 1986;Traskine et al, 2009), calcite (Croize et al, 2010a;Zubtsov et al, 2005), gypsum (PachonRodriguez et al, 2011) and quartz (Alcantar et al, 2003;Anzalone et al, 2006;Gratier et al, 2009;Greene et al, 2009;Kristiansen et al, 2011;van Noort et al, 2011) with a wide range of solubilities, interface kinetics and elastic/plastic properties.…”

Section: -Single Interface Experimentsmentioning

confidence: 99%

The Role of Pressure Solution Creep in the Ductility of the Earth’s Upper Crust

Gratier

Dysthe

Renard

2013

Advances in Geophysics

248

274

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The aim of this review is to characterize the role of pressure solution creep in the ductility of the Earth's upper crust and to describe how this creep mechanism competes and interacts with other deformation mechanisms. Pressure solution creep is a major mechanism of ductile deformation of the upper crust, accommodating basin compaction, folding, shear zone development, and fault creep and interseismic healing. However, its kinetics is strongly dependent on the composition of the rocks (mainly the presence of phyllosilicates minerals that activate pressure solution) and on its interaction with fracturing and healing processes (that activate and slow down pressure solution, respectively).The present review combines three approaches: natural observations, theoretical developments, and laboratory experiments. Natural observations can be used to identify the pressure solution markers necessary to evaluate creep law parameters, such as the nature of the material, the temperature and stress conditions or the geometry of mass transfer domains. Theoretical developments help to investigate the thermodynamics and kinetics of the processes and to build theoretical creep laws.Laboratory experiments are implemented in order to test the models and to measure creep law parameters such as driving forces and kinetic coefficients. Finally, applications are discussed for the modelling of sedimentary basin compaction and fault creep. The sensitivity of the models to time is given particular attention: viscous versus plastic rheology during sediment compaction; steady state versus non-steady state behaviour of fault and shear zones. The conclusions discuss recent advances for modelling pressure solution creep and the main questions that remain to be solved. -IntroductionIn order to investigate the role of pressure solution creep in the ductility of the Earth's upper crust the various mechanical behaviour patterns of the upper crust must first be discussed. Two types of approach can be considered on this topic.1 -The mechanical behaviour of the upper crust is modelled using brittle theories, that include friction laws (Byerlee, 1978;Marone, 1998). This modelling approach is supported by two kinds of observations: (i) the maximum frequency of earthquakes is located within the first 15-20 km of the upper crust (Chen and Molnar, 1983;Sibson, 1982); (ii) laboratory experiments run at relatively fast strain-rates (faster than 10 -7 s -1 ) indicate a transition from frictional to plastic deformation at pressure and temperature conditions appropriate for a depth of 10-20 km (Kohlstedt et al., 1995;Paterson, 1978;Poirier, 1985).2 -Conversely, the behaviour of the upper crust is also modelled by ductile behaviour with creep laws (Wheeler, 1992). This modelling approach is supported by two kinds of observations: (i) geological structures exhumed from depth, such as compacted basin, folds and shear zones, and regional cleavage, indicate ductile behaviour throughout the upper crust (Argand, 1924;Hauck et al., 1998;Schmidt et al., 1996) (Fig. ...

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“…Experiments of natural quartzites suggest that micro‐fracturing at grain contacts may lead to significant increase in deformation rate by several orders of magnitude [ Gratz , ; Den Brok , ]. Experimental investigations also show that pressure solution may strongly depend on the roughness of the grain contact [ Dysthe et al ., , ; Gratier et al ., ; Van Noort et al ., ]. These findings suggest that the calculated diffusivity at grain contact could be significantly escalated due to the enhanced deformation rates by micro‐fracturing along grain contacts.…”

Section: Equilibrium Concentration (Ceqb) Diffusivity (Dgb) and Prementioning

confidence: 99%

Reactive transport at stressed grain contact and creep compaction of quartz sand

Sparks

Hajash

2013

JGR Solid Earth

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[1] A kinetic model is developed to investigate intergranular pressure solution. This model couples stress-induced dissolution at grain contacts, diffusion through grain boundaries, and precipitation in pore spaces. The rate-controlling processes are evaluated according to the dimensionless concentrations at grain contacts and in the pore fluid. Constrained by the experimental results of creep compaction of quartz sands, calculations suggest that the equilibrium concentration at stressed grain contacts (c eqb ) does not exceed 1 order of magnitude higher than the hydrostatic equilibrium concentration (c eq ) at the initial stages of creep compaction. However, c eqb decays rapidly with increasing compaction and becomes close to c eq after several percent strain. The diffusivity at grain contacts is 1-2 orders of magnitude lower than the diffusivity in pore fluid. The rate-controlling process is related to grain size and strain. An increase in grain size shifts the systems toward the diffusion-controlled regime, while an increase in strain shifts the systems from dissolution-controlled regime toward either diffusion-controlled regime (larger grains) or precipitation-controlled regime (smaller grains).Intergranular pressure solution appears to be very sensitive to pore-fluid chemistry. Even a slight supersaturation in the pore fluid could prevent the diffusion along grain contacts. This may explain why the strength of intergranular pressure solution varies widely in natural sandstones.

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Structure and properties of loaded silica contacts during pressure solution: impedance spectroscopy measurements under hydrothermal conditions

Cited by 15 publications

References 43 publications

Effects of interfacial energy on compaction creep by intergranular pressure solution: Theory versus experiments on a rock analog (NaNO₃)

Effects of interfacial energy on compaction creep by intergranular pressure solution: Theory versus experiments on a rock analog (NaNO₃)

The Role of Pressure Solution Creep in the Ductility of the Earth’s Upper Crust

Reactive transport at stressed grain contact and creep compaction of quartz sand

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Structure and properties of loaded silica contacts during pressure solution: impedance spectroscopy measurements under hydrothermal conditions

Cited by 15 publications

References 43 publications

Effects of interfacial energy on compaction creep by intergranular pressure solution: Theory versus experiments on a rock analog (NaNO3)

Effects of interfacial energy on compaction creep by intergranular pressure solution: Theory versus experiments on a rock analog (NaNO3)

The Role of Pressure Solution Creep in the Ductility of the Earth’s Upper Crust

Reactive transport at stressed grain contact and creep compaction of quartz sand

Contact Info

Product

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Effects of interfacial energy on compaction creep by intergranular pressure solution: Theory versus experiments on a rock analog (NaNO₃)

Effects of interfacial energy on compaction creep by intergranular pressure solution: Theory versus experiments on a rock analog (NaNO₃)