The Different Processes Involved in the Mechanism of Pressure Solution in Quartz‐Rich Rocks and their Interactions

Renard, François; Brosse, É.; Gratier, Jean‐Pierre

doi:10.1002/9781444304237.ch5

Cited by 31 publications

(30 citation statements)

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“…Sheppard, 2002), nevertheless, it is not generally agreed whether the pressure dissolution of chalk is mainly controlled by stress at the grain contacts or by temperature dependent diffusion and precipitation (Renard et al, 2000). Bjørkum (1996) and Bjørkum et al (1998) interpreted petrographic data as indicating a temperature control on stylolite formation in quartzose sandstones, and supported their conclusion by referring to geochemical modeling data by Oelkers et al Fig.…”

Section: Discussionmentioning

confidence: 50%

Stylolites, porosity, depositional texture, and silicates in chalk facies sediments. Ontong Java Plateau – Gorm and Tyra fields, North Sea

Fabricius¹,

Borre²

2006

Sedimentology

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Comparison of chalk on the Ontong Java Plateau and chalk in the Central North Sea indicates that, whereas pressure dissolution is controlled by effective burial stress, pore‐filling cementation is controlled by temperature. Effective burial stress is caused by the weight of all overlying water and sediments as counteracted by the pressure in the pore fluid, so the regional overpressure in the Central North Sea is one reason why the two localities have different relationships between temperature and effective burial stress. In the chalk of the Ontong Java Plateau the onset of calcite‐silicate pressure dissolution around 490 m below sea floor (bsf) corresponds to an interval of waning porosity‐decline, and even the occurrence of proper stylolites from 830 m bsf is accompanied by only minor porosity reduction. Because opal is present, the pore‐water is relatively rich in Si which through the formation of Ca–silica complexes causes an apparent super‐saturation of Ca and retards cementation. The onset of massive pore‐filling cementation at 1100 m bsf may be controlled by the temperature‐dependent transition from opal‐CT to quartz. In the stylolite‐bearing chalk of two wells in the Gorm and Tyra fields, the nannofossil matrix shows recrystallization but only minor pore‐filling cement, whereas microfossils are cemented. Cementation in Gorm and Tyra is thus partial and has apparently not been retarded by opal‐controlled pore‐water. A possible explanation is that, due to the relatively high temperature, silica has equilibrated to quartz before the onset of pressure dissolution and thus, in this case, dissolution and precipitation of calcite have no lag. This temperature versus effective burial stress induced difference in diagenetic history is of particular relevance when exploring for hydrocarbons in normally pressured chalk, while most experience has been accumulated in the over‐pressured chalk of the central North Sea.

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Section: Discussionmentioning

confidence: 50%

Stylolites, porosity, depositional texture, and silicates in chalk facies sediments. Ontong Java Plateau – Gorm and Tyra fields, North Sea

Fabricius¹,

Borre²

2006

Sedimentology

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“…Once dissolution precipitation occurs in presence of external stresses, such as in compaction studies (e.g. Renard et al 2000;Miyakawa and Kawabe 2014), we refer to pressure solution. It is a well study process that can be driven not only by chemical changes but above all by deformation within the whole upper crust (e.g.…”

Section: Introductionmentioning

confidence: 99%

Pressure solution in rocks: focused ion beam/transmission electron microscopy study on orthogneiss from South Armorican Shear Zone, France

Bukovská

Wirth

Morales

2015

Contrib Mineral Petrol

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In order to characterize the µm-to-nm structures related to operation of pressure solution on phase boundaries in naturally deformed rocks, we have performed a detailed focused ion beam/transmission electron microscopy study in ultramylonite samples from South Armorican Shear Zone (France) that focused on grain boundary scale. We have studied phase boundaries between quartz, K-feldspar and white mica both in 2 and 3D and compare our evidences with theoretical dissolution-precipitation models in the current literature. The dissolution (re)precipitation processes lead to the development of different features at different phase boundaries. In both quartz-white mica and quartz-K-feldspar phase boundaries, voids were ubiquitously observed. These voids have different shapes and the development of some of them is crystallographically controlled. In addition, part of these voids might be filled with vermiculite.Amorphous leached layers with kaolinite composition were observed at the boundaries of Kfeldspar-quartz and K-feldspar-white mica. The development of different features along the phase boundaries is mainly controlled by the crystallography of the phases sharing a common interface, together with the presence of fluids that either leaches or directly dissolve the mineral phases. In addition, the local dislocation density in quartz may play an important role during pressure solution.We suggest that the nano-scale observations of the quartz -white mica phase boundaries show direct evidence for operation of island-and-channel model as described in Wassmann and Stöckhert (2013), while K-feldspar -quartz phase boundaries represents amorphous layers formed via interface-coupled dissolution-reprecipitation as described by Hellmann et al. (2012).

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“…At zero porosity, we assume that A c ! pd 2 /z, where z is the average grain packing coordination number, d is the average grain diameter and pd 2 is the equivalent surface area of a spherical grain of diameter d. At intermediate porosities of 5 -35%, an analysis of the geometry of a simple cubic, or body-centered cubic pack of initially spherical grains compacting isotropically by pressure solution [Gundersen et al, 2002;Renard et al, 2000Renard et al, , 1999 shows that the relation between contact area and porosity is well described by the relation…”

Section: Microstructural Model and Associated State Variablesmentioning

confidence: 99%

A microphysical model for strong velocity weakening in phyllosilicate‐bearing fault gouges

2007

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[1] Previous rotary shear experiments, performed on a halite-muscovite fault gouge analogue system have shown that the presence of phyllosilicates, under conditions favoring the operation of cataclasis and pressure solution in the matrix phase, can have major effects on the frictional behavior of gouges. While 100% halite and 100% muscovite samples exhibit rate-independent frictional/brittle behavior, the strength of mixtures containing 10-30% muscovite is both normal stress and sliding velocitydependent. At high sliding velocities (>1 mm s À1 ), such mixtures show unusually marked velocity weakening, along with the development of a structureless, cataclastic microstructure. In the present paper, a micromechanical model is developed in an attempt to explain this behavior. The model assumes a granular flow process involving competition between intergranular dilatation and compaction by pressure solution. The predictions of the model agree favorably with the experimental results. Extension of the model to quartz-mica systems implies that the presence of phyllosilicates plus the operation of pressure solution can strongly promote (unstable) velocity-weakening behavior at rapid slip rates on natural faults, under midcrustal conditions. Static stress drop predictions based on the model agree reasonably well with estimates from seismic observations. Our results may help explain the discrepancy between laboratory-derived rate-and-state friction parameter values, obtained for dry, low-strain and/or single-phase rock systems, and the values for natural fault rocks inferred from seismological data.Citation: Niemeijer, A. R., and C. J. Spiers (2007), A microphysical model for strong velocity weakening in phyllosilicate-bearing fault gouges,

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The Different Processes Involved in the Mechanism of Pressure Solution in Quartz‐Rich Rocks and their Interactions

Cited by 31 publications

References 0 publications

Stylolites, porosity, depositional texture, and silicates in chalk facies sediments. Ontong Java Plateau – Gorm and Tyra fields, North Sea

Stylolites, porosity, depositional texture, and silicates in chalk facies sediments. Ontong Java Plateau – Gorm and Tyra fields, North Sea

Pressure solution in rocks: focused ion beam/transmission electron microscopy study on orthogneiss from South Armorican Shear Zone, France

A microphysical model for strong velocity weakening in phyllosilicate‐bearing fault gouges

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