Theories and applicability of grain size piezometers: The role of dynamic recrystallization mechanisms

Shimizu, Ichiko

doi:10.1016/j.jsg.2008.03.004

Cited by 149 publications

(133 citation statements)

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“…In contrast, the fine-grained ore yields at low stresses (~7MPa) and inelastic deformation presumably continues preferentially GBS accommodated by single slip on the dominant basal glide system (0001)<11-20> at relaxed v. Mises condition (Lee et al [25] , Drury and Fitz Gerald [27] ). With ongoing deformation grain growth to a steady state grain size (Shimizu [28] ) occurs combined with slip, which may additionally promote the development of preferred orientation. A strong texture (J=2.9) evolves by rotation of (0001) parallel to the shear plane and prism planes normal to the shearing direction.…”

Section: Discussionmentioning

confidence: 99%

Development of Microstructure and Texture of Hematite Ores Deformed to Large Strain in Torsion: Can Texture Identify the Prevailing Strength and Creep Mechanisms During Deformation?

et al. 2010

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Samples of fine‐grained (approximately 9 µm) and coarse‐grained (approximately 45 µm) hematite ores with almost random crystallographic preferred orientation (CPO) were deformed in high pressure, high temperature (400 MPa, 850–1 000 °C) torsion experiments up to shear strains of 4.7. Samples with large initial grain size, preferably deformed by dislocation creep attended by dynamic recrystallization, showed grain size reduction and a weak CPO (J ∼ 1.4 at 950 °C). In contrast, fine‐grained ores, deformed mainly by grain boundary sliding accompanied by dislocation activity with slip on the dominant basal glide system, showed grain growth and a strong CPO (J ∼ 2.9). At high strain both ores attained similar strength and grain size, but different CPOs. The experiments demonstrate that the texture intensity of highly deformed rocks strongly depends on initial microstructure and may not reflect unambiguously the prevailing deformation mechanism and strength as often assumed in field studies.

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Section: Discussionmentioning

confidence: 99%

Development of Microstructure and Texture of Hematite Ores Deformed to Large Strain in Torsion: Can Texture Identify the Prevailing Strength and Creep Mechanisms During Deformation?

et al. 2010

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“…The recrystallized grain size is assumed to be in a steady state during dynamic recrystallization, while it might depend on the recrystallization mechanism or temperature (e.g., Poirier and Guillope, 1979;Shimizu, 2008). However, before exploring any of those dependencies, finding this grain size is not trivial, mostly because what we see of the grain size distribution is a 2-D section of it.…”

Section: The Recrystallized Grain Size In the Dislocation Creep Regimementioning

confidence: 99%

“…Coaxial and general shear experiments have been carried out, for example, to define the dislocation creep regimes of quartz (Hirth and Tullis, 1992), to derive flow law parameters (Gleason et al, 1993), to determine the effect of annealing (Heilbronner and Tullis, 2002;Kidder et al, 2016) and the effect of the chemical environment on deformation processes (Post et al, 1996;Chernak et al, 2009), to compare deformation processes to nature (Stipp and Kunze, 2008), and to study the development of texture and microstructure with strain (Tullis et al, 1973;Tullis, 1977;DellAngelo and Tullis, 1989;Heilbronner and Tullis, 2006). BHQ was also used to determine the widely used recrystallized quartz grain size piezometer of Stipp and Tullis (2003).…”

Section: Introductionmentioning

confidence: 99%

The grain size(s) of Black Hills Quartzite deformed in the dislocation creep regime

Heilbronner

Kilian

2017

Solid Earth

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Abstract. General shear experiments on Black Hills Quartzite (BHQ) deformed in the dislocation creep regimes 1 to 3 have been previously analyzed using the CIP method Tullis, 2002, 2006). They are reexamined using the higher spatial and orientational resolution of EBSD. Criteria for coherent segmentations based on c-axis orientation and on full crystallographic orientations are determined. Texture domains of preferred c-axis orientation (Y and B domains) are extracted and analyzed separately. Subdomains are recognized, and their shape and size are related to the kinematic framework and the original grains in the BHQ. Grain size analysis is carried out for all samples, high-and low-strain samples, and separately for a number of texture domains. When comparing the results to the recrystallized quartz piezometer of Stipp and Tullis (2003), it is found that grain sizes are consistently larger for a given flow stress. It is therefore suggested that the recrystallized grain size also depends on texture, grain-scale deformation intensity, and the kinematic framework (of axial vs. general shear experiments). DedicationThis contribution is dedicated to Jan Tullis, whose superb work on experimental rock deformation and microstructure analysis continues to be an inspiration to us all.

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“…The semi-empirical flow law of Hirth et al (2001) was, however, not used in the present model because the tectonic setting, grain size, and water contents of the quartzite samples are far different from those of chert in subduction zones. Moreover, they used a temperature-independent grain size piezometer to estimate differential stress during natural deformation, although considerably large effects of temperature are theoretically predicted (De Bresser et al 2001;Shimizu 2008Shimizu , 2012.…”

Section: Figurementioning

confidence: 99%

“…The weakness of the flint samples may be related to the formation of localized shear bands that were observed in the deformed samples. The total water contents of the synthetic quartz aggregates used by Rutter and Brodie (2004) were relatively small (e.g., 100 to 200 H/10 6 Si after deformation), and the pore fluids were not saturated with H 2 O during deformation (see discussion by Shimizu (2008)). A series of experiments conducted by Paterson and Luan (1990) and Luan and Paterson (1992) used starting materials that were synthesized from powders of natural quartz, silicic acid, and silica gel; silicic-acidand silica-gel-origin samples have water contents (approximately 10 4 H/10 6 Si) comparable to those of weakly metamorphosed cherts (Ito and Nakashima 2002).…”

Section: Figurementioning

confidence: 99%

Rheological profile across the NE Japan interplate megathrust in the source region of the 2011 Mw9.0 Tohoku-oki earthquake

Shimizu

2014

Earth Planet Sp

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A strength profile across the NE Japan interplate megathrust was constructed in the source region of the 2011 Tohoku-oki earthquake (M w 9.0) using friction, fracturing, and ductile flow data of the oceanic crustal materials obtained from laboratory experiments. The depth-dependent changes in pressure, temperature, and pore fluid pressure were incorporated into a model. The large tsunamigenic slips during the M9 event can be explained by a large gradient in fault strength on the up-dip side of the M9 hypocenter, which was located 17 to 18 km beneath sea level. A large stress drop (approximately 80 MPa) induced by the collapse of a subducted seamount possibly triggered the M9 earthquake. In the deep (>35 km) part of the thrust fault, where M7-class Miyagi-oki earthquakes have repeatedly occurred, plastic deformation occurs in siliceous rocks but not in gabbroic rocks. Thus, the asperity associated with the M7-class earthquakes was most likely a gabbroic body, such as a broken seamount, surrounded by siliceous sedimentary rocks. The conditionally stable nature of the surrounding region can be explained by the frictional behavior of wet quartz in the brittle-ductile transition zone. In contrast to the deep M7-class asperity, the M9 asperity (i.e., a region that was strongly coupled before the M9 Tohoku-oki earthquake) extended to a large area of the plate interface because shear strength is relatively insensitive to lithological variation at intermediate depths. However, the along-arc extension of the M9 asperity was constrained by fluid-rich regions on the plate interface.

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Theories and applicability of grain size piezometers: The role of dynamic recrystallization mechanisms

Cited by 149 publications

References 89 publications

Development of Microstructure and Texture of Hematite Ores Deformed to Large Strain in Torsion: Can Texture Identify the Prevailing Strength and Creep Mechanisms During Deformation?

Development of Microstructure and Texture of Hematite Ores Deformed to Large Strain in Torsion: Can Texture Identify the Prevailing Strength and Creep Mechanisms During Deformation?

The grain size(s) of Black Hills Quartzite deformed in the dislocation creep regime

Rheological profile across the NE Japan interplate megathrust in the source region of the 2011 Mw9.0 Tohoku-oki earthquake

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