Propagation and localization of stylolites in limestones

Carrio‐Schaffhauser, Elisabeth; Raynaud, Suzanne; Latiere, H. J.; Mazerolle, Frédéric

doi:10.1144/gsl.sp.1990.054.01.19

Cited by 29 publications

(15 citation statements)

References 8 publications

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“…Therefore, stylolitization can greatly impact on the porosity and permeability of the host rock. Previous studies report a higher-porosity zone in the range of a few micrometers from the stylolite (Carrio-Schaffhauser et al 1990), but then a low-porosity zone farther from the stylolite, up to several centimeters in width, derived from sandstone examples in the North Sea and East Greenland (Harris 2006;Baron and Parnell 2007;Harris 2006). FIG.…”

Section: Fluids Generated During Pressure Solution and Fluid Flowmentioning

confidence: 86%

Diagenetic Implications of Stylolitization In Pelagic Carbonates, Canterbury Basin, Offshore New Zealand

Vandeginste¹,

John²

2013

Journal of Sedimentary Research

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Stylolites are irregular discontinuity surfaces that are thought to result from localized stress-induced dissolution during burial or tectonic compression. The genesis of stylolites and the controls on stylolitization are still debated, and the interplay between stylolitization, generation of carbonate-rich fluids, diagenetic fluid flow within fractures and matrix, cementation, and porosity modifications is complex. All of these processes have important diagenetic effects potentially altering the intrinsic properties of the host rock, with implications for hydrocarbon exploration and water resources in aquifers. We investigate the process of stylolitization by a macroscopic, petrographic, and geochemical study of pressure-solution features in Eocene to early Oligocene limestones in cores from the Integrated Ocean Drilling Program (IODP) Hole 317-U1352C (Canterbury Basin). The results indicate correlations among stylolite amplitude, stylolite density, and siliciclastic content of the host rock. These relationships are interpreted to suggest that siliciclastic content in carbonate rocks increases heterogeneity, which in turn impacts stylolite nucleation. Moreover, the geochemical data support that clay along the stylolite is not authigenic, but a relict from impurities in the limestone host rock. The statistical approach of stylolite spacing used in this study, which is different than previous studies, reinforces the model of random occurrence of stylolites in (carbonate) lithologic units.This study shows that local stresses in tectonically passive areas may allow the formation of rare oblique stylolites with peaks perpendicular to the stylolite plane. Estimation of the amount of limestone dissolved during stylolitization (minimum 7% to 12% of the depositional limestone) and the volume of sparite in the host rock (up to 1.6% of the compacted limestone) suggests that the pressure-solution fluids cemented the micropores, reducing porosity to about 10% (from a common porosity of about 40% in mechanically compacted chalk). This study thus highlights the importance of microporosity as a sink for burial cements, an observation difficult to make in thin-section. Analysis of stylolite infills at Site U1352 shows no evidence that the stylolites acted as conduits for diagenetic fluids, unless if the fluid was host-rock buffered and thus its chemistry indistinguishable from that of the host rock.The link between siliciclastic content in carbonate rocks and the spacing and amplitude of stylolites improves understanding of burial compaction processes. Predicting the morphology and spacing of stylolites in the subsurface can be used to identify baffles to cross-stylolite fluid flow or cementation (of microporosity) influencing heterogeneity of petrophysical properties in (subsurface reservoir) host rocks.

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Section: Fluids Generated During Pressure Solution and Fluid Flowmentioning

confidence: 86%

Diagenetic Implications of Stylolitization In Pelagic Carbonates, Canterbury Basin, Offshore New Zealand

Vandeginste¹,

John²

2013

Journal of Sedimentary Research

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“…Stylolites occur most often in sets, in carbonates and other essentially soluble rocks including mainly calcite but also dolomites (Carrio-Schaffhauser et al, 1990;Ebner et al, 2009;Ebner et al, 2010b;Karcz and Scholz, 2003;Pennock et al, 2006), quartz (Heald, 1955;Wangen, 1998;Weibel and Keulen, 2008), feldspars (Thomas et al, 1993), gypsum and halite (Bauerle et al, 2000). Therefore, stylolites play an important role in compaction and in creep processes and therefore in the rheological properties of the upper crust (Dewers and Ortoleva, 1990).…”

Section: Nature and Amount Of Dissolved Mineralsmentioning

confidence: 99%

“…It must be noted that, in this case, the driving force is the difference in mean normal stresses between the stress concentration zone and the deposition site. Observations of Carrio-Schaffhauser et al (1990) revealing high porosity within the dissolution seam propagation zone suggest that it could be associated with high fluid pressure.…”

Section: Model Of Solution Seam 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

241

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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“…More recently, Dewers and Ortoleva (1994) have provided a reaction-transport mechanical model to describe various types of pressure-solution features (including stylolites, marl/limestone alterations, and dissolution seams) in clay-rich limestone based on coupled process of diffusional mass transport, texture-dependent effective stress distribution, different reaction rates and driving forces for grain contacts and grain-free faces, and rate inhibition due to solute inhibitors and clay coatings. Pressure-solution results in porosity loss in the host rock; material dissolved along a pressure-solution seam is transported locally to precipitate in pore space beyond the process zone, which is a zone of enhanced porosity area that surrounds the solution seam (Carrio-Schaffhauser et al, 1990). Cores showing the direct association of stylolite zones with cemented dtightT zones of lower porosity have been imaged by Wong and Oldershaw (1981), and indicate pressure-solution leads to an overall decrease in matrix porosity.…”

Section: Fracture Typesmentioning

confidence: 94%

Influence of depositional setting and sedimentary fabric on mechanical layer evolution in carbonate aquifers

Wall

2006

Sedimentary Geology

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Propagation and localization of stylolites in limestones

Cited by 29 publications

References 8 publications

Diagenetic Implications of Stylolitization In Pelagic Carbonates, Canterbury Basin, Offshore New Zealand

Diagenetic Implications of Stylolitization In Pelagic Carbonates, Canterbury Basin, Offshore New Zealand

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

Influence of depositional setting and sedimentary fabric on mechanical layer evolution in carbonate aquifers

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