Pressure solution of plagioclase and garnet during Nagahama folding in the Sambagawa belt of Central Shikoku.

Hara, Ikuo; Shiota, Tsugio; Hide, Kei

doi:10.5575/geosoc.90.33

Cited by 8 publications

(4 citation statements)

References 6 publications

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“…Further evidence of the relationship between the growth of garnet and the D1 deformation is given by the existence of pull-apart fracturing of garnet parallel to L1 (Fig. 7) and possible pressure solution along S, (Hara et al 1984).…”

Section: The East-westpow In the Sanbagawa Belt 181mentioning

confidence: 94%

Kinematics, structure and relationship to metamorphism of the east‐west flow in the Sanbagawa Belt, southwest Japan

1992

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Deformation in the Sanbagawa Belt is characterized by ductile flow in an east-west direction sub-parallel to its length. The east-west flow (D1) caused large-scale recumbent folding of the metamorphic sequence in central Shikoku, which can explain the inverted thermal structure of this region. Chemical zoning of metamorphic minerals associated with D1 microstructures also suggest that the east-west flow developed under retrograde conditions. D1 is therefore related to exhumation rather than subduction processes. A variety of kinematic indicators show that during the east-west flow, deformation was partitioned into structurally continuous domains with opposed senses of shear. This suggests that bulk deformation was not simple shear but included a component of flattening.1985; Higashino 1990) have been proposed. The Asemigawa route cross-cuts the inverted thermal structure of Central Shikoku (Fig. 2). There is good exposure along this traverse that affords good structural control across this section making it ideal for studying the structures responsible for the inverted metamorphic zonation.

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Section: The East-westpow In the Sanbagawa Belt 181mentioning

confidence: 94%

Kinematics, structure and relationship to metamorphism of the east‐west flow in the Sanbagawa Belt, southwest Japan

1992

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“…The Sanbagawa schists in central Shikoku show the maximum metamorphic grade in a middle structural level. This has been interpreted either to be the result of a pile of thrust nappes (Hara, Siota & Hide, 1984;Faure, 1983) or to be the result of a recumbent fold accompanied by a few thrusts (Banno & Sakai. 1989).…”

Section: Implication For Thermal Structurementioning

confidence: 99%

Prograde and retrograde metamorphism of hematitebearing basic schists in the Sanbagawa belt in central Shikoku

Otsuki

Banno

1990

Journal Metamorphic Geology

147

134

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The mineral assemblages of hematite-bearing basic schists in intermediate high-pressure metamorphism are temperature dependent. For assemblages with excess hematite. albite, muscovite and quartz, the paragenetic relations can be dealt with in terms of a fourcomponent system, without omitting or grouping major components.In the Sanbagawa belt in central Shikoku, the dominant amphibole in the hematite-bearing basic schists changes from winchite, via crossite and barroisite to hornblende. The stability of amphibole is described chemographically within a pseudoternary system with another excess phase, epidote. Many amphiboles are chemically heterogeneous owing to retrograde reactions which produced low-TIP amphibole around the prograde amphibole. The examination of amphibole zoning makes it possible to draw a retrograde P-T trajectory which passes on the lower pressure side of the prograde one.

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“…The most probable mechanism for the acquisition of GSPO is thus growth under stress. Garnet deformation by pressure solution has already been observed in metamorphic rocks (Álvarez‐Valero et al., 2005; Bell et al., 1986; Bell & Rubenach, 1983; Duebendorfer & Frost, 1988; Hara et al., 1984; Smit et al., 2011; Wassmann & Stöckhert, 2013a).…”

Section: Discussionmentioning

confidence: 93%

Mineral Dissolution and Precipitation Under Stress: Model Formulation and Application to Metamorphic Reactions

Malvoisin

Baumgartner

2021

Geochem Geophys Geosyst

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Stylolites, pressure shadows or flattened pebbles are common observations in the first 15 km of the Earth's crust (Gratier et al., 2013). They are markers of anisotropic mineral dissolution and mass transfer. Dissolution occurs when fluid is undersaturated with respect to equilibrium. As many mineral solubilities increase with pressure (Dolejš & Manning, 2011;Eugster & Baumgartner, 1987), grain-to-grain surfaces under high normal stress can locally dissolve. The dissolved aqueous species then diffuse and precipitate at surfaces under low normal stress. This process of mass transfer called pressure solution induces compaction by creep at large scale (Durney, 1972). In the presence of fluid and at temperature below 500 °C, pressure solution is thought to be the dominant deformation mechanism in Earth's crust (Gratier & Gamond, 1990;Rutter, 1976). Pressure solution theory is based on the presence at grain contacts of a thin aqueous film to provide the dissolved aqueous species necessary for crystal growth and transmit the normal stress across the grain contact (Rutter, 1976(Rutter, , 1983. The thinner estimates of aqueous film thickness ranges from 1 to 100 nm (

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Pressure solution of plagioclase and garnet during Nagahama folding in the Sambagawa belt of Central Shikoku.

Cited by 8 publications

References 6 publications

Kinematics, structure and relationship to metamorphism of the east‐west flow in the Sanbagawa Belt, southwest Japan

Kinematics, structure and relationship to metamorphism of the east‐west flow in the Sanbagawa Belt, southwest Japan

Prograde and retrograde metamorphism of hematitebearing basic schists in the Sanbagawa belt in central Shikoku

Mineral Dissolution and Precipitation Under Stress: Model Formulation and Application to Metamorphic Reactions

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