Kinematics of stylolite formation and physics of the pressure-solution process

Guzzetta, Giuseppe

doi:10.1016/0040-1951(84)90122-7

Cited by 34 publications

(20 citation statements)

References 13 publications

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“…The fact that stylolites can be found in a variety of rocks and display a wide range of morphologies, even within a single outcrop, makes comparison and description of natural stylolites a difficult task (Park and Schot, 1968). Early classifications were mainly based on qualitative parameters such as the visual appearance of the interface and the orientation with respect to the bedding (Park and Schot, 1968;Guzzetta, 1984). Moreover, the necessary overburden for the formation of beddingparallel stylolites is still debated: up to 800-1000 m (e.g.…”

Section: Introductionmentioning

confidence: 99%

Stress sensitivity of stylolite morphology

Ebner

Koehn

Toussaint

et al. 2009

Earth and Planetary Science Letters

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Stylolites are rough surfaces that form by localized stress-induced dissolution. Using a set of limestone rock samples collected at different depths from a vertical section in Cirque de Navacelles (France), we study the influence of the lithostatic stress on the stylolites morphology on the basis of a recent morphogenesis model. We measured the roughness of a series of bedding-parallel stylolites and show that their morphology exhibits a scaling invariance with two self-affine scaling regimes separated by a crossover-length (L) at the millimeter scale consistent with previous studies. The importance of the present contribution is to estimate the stylolite formation stress σ from the sample position in the stratigraphic series and compare it to the crossover-length L using the expected relationship: L ∼ σ −2 . We obtained a successful prediction of the crossover behavior and reasonable absolute stress magnitude estimates using relevant parameters: depth of stylolite formation between 300 to 600 m with corresponding normal stress in the range of 10-18 MPa. Accordingly, the stylolite morphology contains a signature of the stress field during formation and we thus suggest that stylolites could be used as paleo-stress gauges of deformation processes in the upper crust.

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Section: Introductionmentioning

confidence: 99%

Stress sensitivity of stylolite morphology

Ebner

Koehn

Toussaint

et al. 2009

Earth and Planetary Science Letters

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“…Finally, many studies have tried to model the development of dissolution interfaces either by means of a kinematic approach (Guzzetta, 1984) or a quasi-static mechanical approach, stylolites being viewed as ''anticracks'' (Fletcher and Pollard, 1981). The idea is that a solution seam, considered as weak material due to passive clay concentration, propagates in its own plane along the direction of maximum mean compressive stress (see spaced solution cleavage below).…”

Section: Model Of Stylolite Developmentmentioning

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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“…The asperity shapes of these stylolitic PSSs can in most cases be approximated as rectangular, triangular, and semicircular or any combination of these as shown in the examples presented earlier (see Figure 6b). In the literature, roughness is thought to be generated by differential dissolution rates along the seam [Guzzetta, 1984] and it increases as the magnitude of the dissolution [Stockdale, 1922] (or volumetric plastic strain) increases. It is also quite obvious that both the lateral and transverse linkage and coalescence of the neighboring PSS would increase the roughness of the combined structure (see, for example, overprinted sylolitic PSSs in the work of Stockdale [1922]).…”

Section: Interpretation and Discussionmentioning

confidence: 99%

Mechanics of pressure solution seam growth and evolution

Zhou

Aydin

2010

J. Geophys. Res.

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[1] Pressure solution seams (PSSs) can be idealized as localized volume reduction structures (LVRSs) in terms of their mechanics. Previous mechanical analyses of LVRSs, including compaction bands, showed that the normal stresses at the tips of LVRSs are compressive and significantly amplified with respect to the remote stresses, whereas on the flanks they are slightly reduced. These results can be used to rationalize the in-plane growth of PSSs for a certain distance, however, based on these stress conditions alone, it is not possible to explain the widening and transverse coalescence of PSSs. In this study, based on laboratory and field observations that the PSS surfaces are extremely rough, we introduced asperities with triangular, semicircular, and rectangular geometries on the flanks of the LVRSs into our mechanical model to see if these asperities can raise stresses in these locations, which may rationalize the transverse growth of PSSs. It is found that these asperities can produce strong stress perturbations on the LVRS flanks thereby inducing a significant increase in the compressive normal stresses. In addition, to account for the rate factor of the pressure solution process, a creep law was adopted to simulate growth and coalescence of the LVRSs. Using the calculated normal compressive stresses and volumetric plastic strains as proxy for the growth, we show that (1) a single LVRS is able to grow both laterally and transversely for a short distance and (2) two in-plane aligned neighboring LVRSs with a short distance between the adjacent tips and two parallel echelon and overlapped LVRSs with a small spacing may be able to link and coalesce to form a longer and wider LVRS, respectively. The influences of the LVRS geometric configurations, the material properties within the LVRSs, and the distance and spacing of the aligned in-plane, echelon, and overlapping neighboring parallel LVRSs on the growth and coalescence of the LVRSs are investigated and their implications specifically for the PSSs are also discussed.

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Kinematics of stylolite formation and physics of the pressure-solution process

Cited by 34 publications

References 13 publications

Stress sensitivity of stylolite morphology

Stress sensitivity of stylolite morphology

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

Mechanics of pressure solution seam growth and evolution

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