Role of silica precipitation kinetics in determining the rate of quartz pressure solution

Mullis, Andrew M.

doi:10.1016/0148-9062(92)92131-u

Cited by 5 publications

(6 citation statements)

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“…The flux of solute from a grain contact is given by the diffusive flux at the edge of the contact multiplied by the surface area of the contact edge [ Tada et al ., ; Mullis , ; Lehner , ]:

J = - 2 πaδ D_{italicgb} {\frac{\partial c_{b}}{\partial r} |}_{r = a}

where δ is the mean grain‐contact thickness and

{\frac{\partial c_{b}}{\partial r} true|}_{r = a}

is the concentration gradient at the periphery of the contact. The resulting supply rate ( mol/cm 3 sample/s ) is

R_{s} = \frac{- 36 (1 - ϕ) aδ D_{italicgb}}{d^{3}} {\frac{\partial c_{b}}{\partial r} |}_{r = a}

…”

Section: Dissolution‐diffusion‐precipitation Modelmentioning

confidence: 99%

“…Various studies have reached very different assumptions about the rate‐controlling process [ Weyl , ; Rutter , , ; Raj , ; Gratier and Guiget , ; Tada et al ., ; Mullis , , ; De Meer and Spiers , ; De Meer et al ., ; Revil , ; Niemeijer et al ., ; Yasuhara et al ., ; Zhang and Spiers , ; Gratier et al ., ]. These differences may be related to the experimental conditions, material properties, or the modeling setting.…”

Section: Introductionmentioning

confidence: 99%

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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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“…The flux of solute from a grain contact is given by the diffusive flux at the edge of the contact multiplied by the surface area of the contact edge [ Tada et al ., ; Mullis , ; Lehner , ]:

J = - 2 πaδ D_{italicgb} {\frac{\partial c_{b}}{\partial r} |}_{r = a}

where δ is the mean grain‐contact thickness and

{\frac{\partial c_{b}}{\partial r} true|}_{r = a}

is the concentration gradient at the periphery of the contact. The resulting supply rate ( mol/cm 3 sample/s ) is

R_{s} = \frac{- 36 (1 - ϕ) aδ D_{italicgb}}{d^{3}} {\frac{\partial c_{b}}{\partial r} |}_{r = a}

…”

Section: Dissolution‐diffusion‐precipitation Modelmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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

Sparks

Hajash

2013

JGR Solid Earth

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“…Attention has been focused on (1) driving force for pressure solution (Rutter, 1983;Lehner, 1990;Spiers and Brzesowsky, 1993), (2) rate-controlling processes (Raj, 1982;Tada and others, 1987;Lehner, 1990;Spiers and Schutjens, 1990;Mullis, 1991), and (3) rate laws of pressure solution (Raj, 1982;Rutter, 1983;Ortoleva, 1994;Lehner, 1995;Lemee and Gueguen, 1996;Renard and others, 1999). Lehner (1995) was one of the first to consider pressure solution in open systems and theoretically addressed the importance of fluid flow on rates of intergranular pressure solution.…”

mentioning

confidence: 98%

Creep compaction of quartz aggregates: Effects of pore-fluid flow--A combined experimental and theoretical study

Hajash²,

Sparks³

2003

American Journal of Science

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Creep compaction experiments were conducted in flow-through reactors at 150°C and 34.5 MPa of effective pressure to investigate the effects of pore-fluid flow on creep compaction rate. The starting materials were St. Peter quartz sand (124-180 m and 250-350 m) and disaggregated novaculite (10-60 m). Theoretical analysis was carried out to investigate the relationships between flow velocity (residence time), solute concentration in pore fluid, the removal rate of dissolved material, the grain-convergence rate due to grain-contact dissolution, and compaction rate. Creep-compaction experiments indicate that the compaction rate of quartz aggregates is related to fluid flow rates. Compaction rates increase by factors up to 6 as flow rate increases from zero to between 0.13 and 0.15 ml/h. The modeling results are similar to the experiments, and indicates that pore-fluid flow affects compaction through its control of solute concentration. When the input-fluid concentration is lower than the pore-fluid equilibrium concentration, an increase in flow velocity (a decrease in residence time) leads to higher removal rate of dissolved materials from the system, lower solute concentration, and more rapid grain convergence and compaction. The grain-convergence rate would even become lower than that in a closed system if the input-fluid concentration is higher than the pore-fluid equilibrium concentration. The effects of fluid flow on grain convergence rate also vary with grain size, strain, and grain-boundary properties. In reservoir sandstones, descending fluids that heat up would become undersaturated and then enhance compaction, whereas ascending fluids that cool would become supersaturated and then slow or inhibit further compaction.

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“…This interest in IPS processes has provided an incentive for the development of numerous microphysical models for IPS and flow laws for compaction and deformation by IPS creep (Rutter‚ 1976‚ 1983Raj, 1982;Lehner and Bataille‚ 1984;Lehner, 1990Lehner, , 1995Spiers and Schutjens, 1990;Gratz, 1991;Mullis, 1991;Paterson, 1995;Shimizu, 1995). By comparison with petrographic information on IPS, two broad classes of grain scale IPS mechanism have been proposed.…”

Section: Introductionmentioning

confidence: 99%

Intergranular Pressure Solution in Nacl: Grain-To-Grain Contact Experiments under the Optical Microscope

Spiers

Schutjens

1999

Oil & Gas Science and Technology - Rev. IFP

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Résumé -Dissolution sous contrainte dans NaCl : expériences de contact grain à grain sous microscope optique -La dissolution sous contrainte (IPS -Intergranular Pressure Solution) représente un mécanisme de lithification, de compaction et de déformation à l'échelle géologique pour une large gamme de roches. Les études expérimentales d'IPS réalisées sur des agrégats de quartz n'ont pas été couronnées de succès en raison d'un taux faible d'IPS, et les expériences IPS réalisées en utilisant une halite saturée comme analogue de roche Hickman et Evans, 1991) ont laissé des incertitudes quant au détail des mécanismes IPS et à la structure/saturation au contact du grain dans ce matériau. La présente étude fait état de quatre expériences de dissolution de contact réalisées sous microscope optique afin d'étudier le mécanisme et la cinétique de l'IPS pour des contacts simples halite/halite et halite/verre, chargés en eau salée (température ambiante). Des forces normales de contact dans la gamme de 1,0 à 2,6 N ont été appliquées en présence d'eau salée saturée en NaCl, induisant des pressions de 0,8 à 7,4 MPa. Des pertes de masse et des convergences -fonction du temps -ont été observées pour tous les contacts. Dans tous les cas, le fait de charger le contact (ou d'augmenter la charge sur le contact) a conduit à la formation immédiate d'une morphologie de contact rugueuse, composée d'un motif d'îles et de canaux, contrôlé par des caractéristiques cristallographiques, à l'échelle de quelques microns. Cette microstructure non équilibrée a évolué dans le temps vers une face de contact optiquement plate. Le processus de convergence/lissage doit donc avoir compris une diffusion de masse en dehors du contact et une expulsion de la saumure par l'intermédiaire d'une phase d'eau salée connectée, à l'intérieur du contact. Le fait qu'une structure rugueuse à petite échelle ait persisté dans des contacts ayant évolué vers un aspect optiquement plat n'est pas établi, bien que les observations au microscope à balayage élec-tronique faites après l'essai le suggèrent. Si ce phénomène était confirmé, son amplitude serait inférieure à 500 nm. Les mesures des taux de dissolution ont permis une comparaison avec un modèle pour l'IPS. Les analyses suggèrent que la diffusion en solution, à travers le contact, contrôlait certainement le taux. La structure du contact et la diffusivité varient alors avec la force de contact et la convergence. Les résul-tats sont largement en adéquation avec ceux des expériences précédentes sur la compaction, réalisées en utilisant de la poudre d'halite saturée. Les divergences avec les résultats d'autres chercheurs, issus d'expériences de dissolution sur des contacts simples, peuvent être expliquées en termes de différence de configuration d'expérience et de concurrence entre les forces motrices.Mots-clés : dissolution sous pression, contact de grain, diffusion, dissolution de l'halite. Science and Technology -Rev. IFP, Vol. 54 (1999) Oil & Gas

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Role of silica precipitation kinetics in determining the rate of quartz pressure solution

Cited by 5 publications

References 0 publications

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

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

Creep compaction of quartz aggregates: Effects of pore-fluid flow--A combined experimental and theoretical study

Intergranular Pressure Solution in Nacl: Grain-To-Grain Contact Experiments under the Optical Microscope

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