Effect of aqueous and carbonic fluids on the dislocation creep strength of quartz

Chernak, L. J.; Hirth, Greg; Selverstone, Jane; Tullis, Jan

doi:10.1029/2008jb005884

Cited by 62 publications

(71 citation statements)

References 61 publications

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“…The effects of water on dislocation creep of quartz, including the nucleation, glide, climb and recovery of dislocations, and recrystallization are well known from (1) experimental studies of natural crystals, in which water was introduced into grain interiors (e.g., Griggs, 1967;Blacic, 1975Blacic, , 1981FitzGerald et al, 1991), (2) studies of synthetic and natural quartz varieties with large initial water contents (e.g., Griggs and Blacic, 1965;Hobbs, 1968;Baeta and Ashby, 1970;Kekulawala et al, 1978;Kirby and McCormick, 1979;McLaren et al, 1983;Linker et al, 1984;Gerretsen et al, 1989;Muto et al, 2011;Holyoke and Kronenberg, 2013;Stünitz et al, 2017), and (3) quartzites and polycrystalline quartz aggregates with water added or removed before or during experiments (e.g., Jaoul et al, 1984;Kronenberg and Tullis, 1984;Tullis and Yund, 1989;Hirth and Tullis, 1992;Gleason and Tullis, 1995;Post et al, 1996;Chernak et al, 2009). IR spectroscopy has played a key role in experimental studies of water weakening, through the characterization and measurement of OH absorption bands due to different hydrogen defects and forms of molecular water within quartz interiors (e.g., Kats, 1962;Griggs and Blacic, 1965;Stipp et al, 2006).…”

Section: Introductionmentioning

confidence: 99%

Synchrotron FTIR imaging of OH in quartz mylonites

et al. 2017

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Abstract. Previous measurements of water in deformed quartzites using conventional Fourier transform infrared spectroscopy (FTIR) instruments have shown that water contents of larger grains vary from one grain to another. However, the non-equilibrium variations in water content between neighboring grains and within quartz grains cannot be interrogated further without greater measurement resolution, nor can water contents be measured in finely recrystallized grains without including absorption bands due to fluid inclusions, films, and secondary minerals at grain boundaries.Synchrotron infrared (IR) radiation coupled to a FTIR spectrometer has allowed us to distinguish and measure OH bands due to fluid inclusions, hydrogen point defects, and secondary hydrous mineral inclusions through an aperture of 10 µm for specimens > 40 µm thick. Doubly polished infrared (IR) plates can be prepared with thicknesses down to 4-8 µm, but measurement of small OH bands is currently limited by strong interference fringes for samples < 25 µm thick, precluding measurements of water within individual, finely recrystallized grains. By translating specimens under the 10 µm IR beam by steps of 10 to 50 µm, using a software-controlled x − y stage, spectra have been collected over specimen areas of nearly 4.5 mm 2 . This technique allowed us to separate and quantify broad OH bands due to fluid inclusions in quartz and OH bands due to micas and map their distributions in quartzites from the Moine Thrust (Scotland) and Main Central Thrust (Himalayas).Mylonitic quartzites deformed under greenschist facies conditions in the footwall to the Moine Thrust (MT) exhibit a large and variable 3400 cm −1 OH absorption band due to molecular water, and maps of water content corresponding to fluid inclusions show that inclusion densities correlate with deformation and recrystallization microstructures. Quartz grains of mylonitic orthogneisses and paragneisses deformed under amphibolite conditions in the hanging wall to the Main Central Thrust (MCT) exhibit smaller broad OH bands, and spectra are dominated by sharp bands at 3595 to 3379 cm −1 due to hydrogen point defects that appear to have uniform, equilibrium concentrations in the driest samples. The broad OH band at 3400 cm −1 in these rocks is much less common. The variable water concentrations of MT quartzites and lack of detectable water in highly sheared MCT mylonites challenge our understanding of quartz rheology. However, where water absorption bands can be detected and compared with deformation microstructures, OH concentration maps provide information on the histories of deformation and recovery, evidence for the introduction and loss of fluid inclusions, and water weakening processes.

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Section: Introductionmentioning

confidence: 99%

Synchrotron FTIR imaging of OH in quartz mylonites

et al. 2017

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“…The water surrounded and penetrated the sample during the deformation experiment. The construction of the assembly is based on Chernak et al (2009). The assembly is shown in Fig.…”

Section: Methodsmentioning

confidence: 99%

“…As for the effects of supplied water on rock deformation, several deformation experiments have been conducted on the addition of water into quartz and feldspar as major constituents of the crust (Kronenberg and Tullis 1984;Den Brok and Spiers 1991;Den Brok et al 1994;Post et al 1996;Post and Tullis 1998;Stünitz et al 2003;Vernooij et al 2006;Chernak et al 2009). These studies revealed that added water reduces the strengths of samples via the enhancement of dislocation creep, diffusion creep, reaction creep, and/or solution-precipitation creep, which are also associated with the development of microstructures.…”

Section: Introductionmentioning

confidence: 99%

Strain localization and fabric development in polycrystalline anorthite + melt by water diffusion in an axial deformation experiment

Fukuda

Muto

Nagahama

2018

Earth Planets Space

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We performed two axial deformation experiments on synthetic polycrystalline anorthite samples with a grain size of ~ 3 μm and 5 vol% Si-Al-rich glass at 900 °C, a confining pressure of 1.0 GPa, and a strain rate of 10 −4.8 s −1. One sample was deformed as-is (dry); in the other sample, two half-cut samples (two cores) with 0.15 wt% water at the boundary were put together in the apparatus. The mechanical data for both samples were essentially identical with a yield strength of ~ 700 MPa and strain weakening of ~ 500 MPa by 20% strain. The dry sample appears to have been deformed by distributed fracturing. Meanwhile, the water-added sample shows plastic strain localization in addition to fracturing and reaction products composed of zoisite grains and SiO 2 materials along the boundary between the two sample cores. Infrared spectra of the water-added sample showed dominant water bands of zoisite. The maximum water content was 1500 wt ppm H 2 O at the two-core boundary, which is the same as the added amount. The water contents gradually decreased from the boundaries to the sample interior, and the gradient fitted well with the solution of the one-dimensional diffusion equation. The determined diffusion coefficient was 7.4 × 10 −13 m 2 /s, which agrees with previous data for the grain boundary diffusion of water. The anorthite grains in the water-added sample showed no crystallographic preferred orientation. Textural observations and water diffusion indicate that water promotes the plastic deformation of polycrystalline anorthite by grain-size-sensitive creep as well as simultaneous reactions. We calculated the strain rate evolution controlled by water diffusion in feldspar aggregates surrounded by a water source. We assumed water diffusion in a dry rock mass with variable sizes. Diffused water weakens a rock mass with time under compressive stress. The calculated strain rate decreased from 10 −10 to 10 −15 s −1 with an increase in the rock mass size to which water is supplied from < 1 m to 1 km and an increase in the time of water diffusion from < 1 to ~ 10,000 years. This indicates a decrease in the strain rate in a rock mass with increasing deformation via water diffusion.Keywords: Anhydrous polycrystalline anorthite, Water diffusion, Griggs-type deformation apparatus, Plastic deformation, Reaction © The Author(s) 2018. This article is distributed under the terms of the Creative Commons Attribution 4.0 International License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made.

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“…Assuming equilibrium relationships between dissolved 'water' in the crystal and the surrounding vapor phase, Paterson (1989) derived m values of 1 to 2 for quartz. High-PT experiments with quartz suggested that m ≤ 1 (Chernak et al 2009). Under experimental conditions at temperatures higher than 900°C, water is in a vapor phase and f H 2 O is nearly equal to water pressure.…”

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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Effect of aqueous and carbonic fluids on the dislocation creep strength of quartz

Cited by 62 publications

References 61 publications

Synchrotron FTIR imaging of OH in quartz mylonites

Synchrotron FTIR imaging of OH in quartz mylonites

Strain localization and fabric development in polycrystalline anorthite + melt by water diffusion in an axial deformation experiment

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

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