Experimental calcite dissolution under stress: Evolution of grain contact microstructure during pressure solution creep

Croizé, Delphine; Renard, François; Bjørlykke, Knut; Dysthe, Dag Kristian

doi:10.1029/2010jb000869

Cited by 59 publications

(65 citation statements)

References 60 publications

(67 reference statements)

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“…Note, however, that empirical laws have also been experimentally measured and showed another category of strain-stress relationship where 1) a dependence of the strain rate on the total strain was observed van Noort et al, 2008a); 2) the strain rate displays a power law dependence on time during deformation along a single contact Dysthe et al, 2003) or during compaction of aggregates (Chester et al, 2007;Croize et al, 2010b;Renard et al, 2001). Such power law behaviour in time was related either to some dynamics of grain boundary roughness, or the presence of another mechanism of deformation, for example subcritical crack growth or fracturing processes (Gratier, 2011b;Gratier et al, 1999), that acted concomitantly with pressure solution creep.…”

Section: Rate Laws For Aggregate Deformation: the Non-linear Casementioning

confidence: 99%

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

Gratier

Dysthe

Renard

2013

Advances in Geophysics

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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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Section: Rate Laws For Aggregate Deformation: the Non-linear Casementioning

confidence: 99%

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

Gratier

Dysthe

Renard

2013

Advances in Geophysics

Self Cite

239

274

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“…Further evidence for inhibition of dissolution and precipitation can be obtained by comparing estimates of the compaction rate of calcitic aggregates in the absence of associated organic inhibitors [Zhang and Spiers, 2005;Croizé et al, 2010] with compaction rates estimated from our core samples. Compaction of aggregates by pressure solution can best be described by a power law, expressed by the equation " = a (t/t 0 )…”

Section: Organic Materials Associated With Coccolithsmentioning

confidence: 99%

A compaction front in North Sea chalk

et al. 2011

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[1] North Sea chalk from 18 wells shows a pronounced porosity drop, from ∼20% to less than 10% over a compaction front of less than 300 m. The position of the compaction front is independent of stratigraphic position, temperature, and actual depth, but closely tied to an effective stress (load stress minus fluid pressure) of ∼17 MPa. These observations require a strongly nonlinear rheology with a marked increase in compaction rate at a specific effective stress. Grain-scale observations demonstrate that the compaction front coincides with marked grain coarsening and recrystallization of fossils and fossil fragments. We propose that this nonlinear rheology is caused by stress-driven failure of the larger pores and the associated generation of reactive surface area by subcritical crack propagation away from these pores. Before the onset of this instability, compaction by pressure solution is slowed down by the inhibitory effect of organic compounds associated with the fossils. Although the compaction mechanism is mainly by pressure solution, the rheological response to burial may still be dominantly plastic and controlled by the (fracturing controlled) rate of exposure of reactive surface area. The nonlinear compaction of chalk has significant implications for the evolution of petroleum systems in the central North Sea, both with respect to sea-floor subsidence above hydrocarbon-producing chalk reservoirs and for the formation of low-porosity pressure seals within the chalk.

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“…If this is the case then the contact stresses could be sufficient for pressure-solution of calcite grains to occur [22,24]. With time pressure solution leads to localized dissolution, thereby increasing the solid-to-solid contact areas as sketched in Figures 7B,C, where granular contact areas have increase in size.…”

Section: Figure 7 | (A)mentioning

confidence: 99%

“…The stress-driven dissolution at grain contacts is termed pressure solution and has been used to understand the longterm creep experiments (see [22,23] for a review). Croize et al [24] performed single-indenter experiments on calcite crystals showing that measurable pressure solution occurs at stresses above approximately 400 MPa.…”

Section: Introductionmentioning

confidence: 99%

How Stress and Temperature Conditions Affect Rock-Fluid Chemistry and Mechanical Deformation

et al. 2016

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We report the results from a series of chalk flow-through-compaction experiments performed at three effective stresses (0.5, 3.5, and 12.3 MPa) and two temperatures (92 and 130 • C). The results show that both stress and temperature are important to both chemical alteration and mechanical deformation. The experiments were conducted on cores drilled from the same block of outcrop chalks from the Obourg quarry within the Saint Vast formation (Mons, Belgium). The pore pressure was kept at 0.7 MPa for all experiments with a continuous flow of 0.219 M MgCl 2 brine at a constant flow rate; 1 original pore volume (PV) per day. The experiments have been performed in tri-axial cells with independent control of the external stress (hydraulic pressure in the confining oil), pore pressure, temperature, and the injected flow rate. Each experiment consists of two phases; a loading phase where stress-strain dependencies are investigated (approximately 2 days), and a creep phase that lasts for 150-160 days. During creep, the axial deformation was logged, and the effluent samples were collected for ion chromatography analyses. Any difference between the injected and produced water chemistry gives insight into the rock-fluid interactions that occur during flow through the core. The observed effluent concentration shows a reduction in Mg 2+ , while the Ca 2+ concentration is increased. This, together with SEM-EDS analysis, indicates that magnesium-bearing mineral phases are precipitated leading to dissolution of calcite. This is in-line with other flow-through experiments reported earlier. The observed dissolution and precipitation are sensitive to the effective stress and test temperature. Higher stress and temperature lead to increased Mg 2+ and Ca 2+ concentration changes. The observed strain can be partitioned additively into a mechanical and chemical driven component.

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Experimental calcite dissolution under stress: Evolution of grain contact microstructure during pressure solution creep

Cited by 59 publications

References 60 publications

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

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

A compaction front in North Sea chalk

How Stress and Temperature Conditions Affect Rock-Fluid Chemistry and Mechanical Deformation

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