Deformation at low and high stress-loading rates
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摘要
In an extensional shear zone in the Talea Ori, Crete, quartz veins occur in high-pressure low-temperature metamorphic sediments at sites of dilation along shear band boundaries, kink band boundaries and boudin necks. Bent elongate grains grown epitactically from the host rock with abundant fluid inclusion trails parallel to the vein wall indicate vein formation by crack-seal increments during dissolutionprecipitation creep of the host rock. The presence of sutured high-angle grain boundaries and subgrains shows that temperatures were sufficiently high for recovery and strain-induced grain boundary migration, i.e. higher than 300 -350℃, close to peak metamorphic conditions. The generally low amount of strain accumulated by dislocation creep in quartz of the host rock and most veins indicates low bulk stress conditions of a few tens of MPa on a long term. The time scale of stress-loading to cause cyclic cracking and sealing is assumed to be lower than the Maxwell relaxation time of the metasediments undergoing dissolution-precipitation creep at high strain rates(10~(-10) s~(-1) to 10~(-9) s~(-1)), which is on the order of hundred years. In contrast, some veins discordant or concordant to the foliation show heterogeneous quartz microstructures with micro-shear zones, sub-basal deformation lamellae, shortwavelength undulatory extinction and recrystallized grains restricted to high strain zones. These microstructures indicate dislocation glide-controlled crystal-plastic deformation(low-temperature plasticity) at transient high stresses of a few hundred MPa with subsequent recovery and strain-induced grain boundary migration at relaxing stresses and temperatures of at least 300 -350℃. High differential stresses in rocks at greenschist-facies conditions that relieve stress by creep on the long term, requires fast stress-loading rates, presumably by seismic activity in the overlying upper crust. The time scale for stress loading is controlled by the duration of the slip event along a fault, i.e. a few seconds to minutes.This study demonstrates that microstructures can distinguish between deformation at internal low stress-loading rates(to tens of MPa on a time scale of hundred years) and high(coseismic) stress-loading rates to a few hundred MPa on a time scale of minutes.
In an extensional shear zone in the Talea Ori, Crete, quartz veins occur in high-pressure low-temperature metamorphic sediments at sites of dilation along shear band boundaries, kink band boundaries and boudin necks. Bent elongate grains grown epitactically from the host rock with abundant fluid inclusion trails parallel to the vein wall indicate vein formation by crack-seal increments during dissolutionprecipitation creep of the host rock. The presence of sutured high-angle grain boundaries and subgrains shows that temperatures were sufficiently high for recovery and strain-induced grain boundary migration, i.e. higher than 300 -350℃, close to peak metamorphic conditions. The generally low amount of strain accumulated by dislocation creep in quartz of the host rock and most veins indicates low bulk stress conditions of a few tens of MPa on a long term. The time scale of stress-loading to cause cyclic cracking and sealing is assumed to be lower than the Maxwell relaxation time of the metasediments undergoing dissolution-precipitation creep at high strain rates(10~(-10) s~(-1) to 10~(-9) s~(-1)), which is on the order of hundred years. In contrast, some veins discordant or concordant to the foliation show heterogeneous quartz microstructures with micro-shear zones, sub-basal deformation lamellae, shortwavelength undulatory extinction and recrystallized grains restricted to high strain zones. These microstructures indicate dislocation glide-controlled crystal-plastic deformation(low-temperature plasticity) at transient high stresses of a few hundred MPa with subsequent recovery and strain-induced grain boundary migration at relaxing stresses and temperatures of at least 300 -350℃. High differential stresses in rocks at greenschist-facies conditions that relieve stress by creep on the long term, requires fast stress-loading rates, presumably by seismic activity in the overlying upper crust. The time scale for stress loading is controlled by the duration of the slip event along a fault, i.e. a few seconds to minutes.This study demonstrates that microstructures can distinguish between deformation at internal low stress-loading rates(to tens of MPa on a time scale of hundred years) and high(coseismic) stress-loading rates to a few hundred MPa on a time scale of minutes.
In an extensional shear zone in the Talea Ori, Crete, quartz veins occur in high-pressure low-temperature metamorphic sediments at sites of dilation along shear band boundaries, kink band boundaries and boudin necks. Bent elongate grains grown epitactically from the host rock with abundant fluid inclusion trails parallel to the vein wall indicate vein formation by crack-seal increments during dissolutionprecipitation creep of the host rock. The presence of sutured high-angle grain boundaries and subgrains shows that temperatures were sufficiently high for recovery and strain-induced grain boundary migration, i.e. higher than 300 -350℃, close to peak metamorphic conditions. The generally low amount of strain accumulated by dislocation creep in quartz of the host rock and most veins indicates low bulk stress conditions of a few tens of MPa on a long term. The time scale of stress-loading to cause cyclic cracking and sealing is assumed to be lower than the Maxwell relaxation time of the metasediments undergoing dissolution-precipitation creep at high strain rates(10~(-10) s~(-1) to 10~(-9) s~(-1)), which is on the order of hundred years. In contrast, some veins discordant or concordant to the foliation show heterogeneous quartz microstructures with micro-shear zones, sub-basal deformation lamellae, shortwavelength undulatory extinction and recrystallized grains restricted to high strain zones. These microstructures indicate dislocation glide-controlled crystal-plastic deformation(low-temperature plasticity) at transient high stresses of a few hundred MPa with subsequent recovery and strain-induced grain boundary migration at relaxing stresses and temperatures of at least 300 -350℃. High differential stresses in rocks at greenschist-facies conditions that relieve stress by creep on the long term, requires fast stress-loading rates, presumably by seismic activity in the overlying upper crust. The time scale for stress loading is controlled by the duration of the slip event along a fault, i.e. a few seconds to minutes.This study demonstrates that microstructures can distinguish between deformation at internal low stress-loading rates(to tens of MPa on a time scale of hundred years) and high(coseismic) stress-loading rates to a few hundred MPa on a time scale of minutes.
引文
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Hilgers, C., Urai, J.L., 2002. Experimental study of syntaxial vein growth during lateral fluid flow in transmitted light:first results. Journal of Structural Geology24,1029-1043.
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Kilian, R., Heilbronner, R., 2017. Analysis of crystallographic preferred orientations of experimentally deformed Black Hills Quartzite. Solid Earth 8,1095-1117.
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Birtel, S., Stockhert, B., 2008. Quartz veins record earthquake-related brittle failure and short term ductile flow in the deep crust. Tectonophysics 457, 53-63.
Bons, P.D., Elburg, M.A., Gomez-Rivas, E., 2012. A review of the formation of tectonic veins and their microstructures. Journal of Structural Geology 43, 33-62.
Ceccato, A., Pennacchioni, G., Bestmann, M., 2017. Crystallographic control and texture inheritance duringmylonitization of coarse grained quartz veins. Lithos290-291, 210-227.
Christie, J.M., Ardell, A.J., 1974. Substructures of deformation lamellae in quartz.Geology 2, 405-408.
Cox, S.F., Etheridge, M.A., 1983. Crack-seal fibre growth mechanisms and their significance in the development of oriented layer silicate microstructures. Tectonophysics 92,147-170.
Drury, M.R., 1993. Deformation Lamellae in Metals and Minerals. Defects and processes in the solid state:Geoscience applications:McLaren volume. Elsevier,Amsterdam, The Netherlands, pp. 195-212.
Durney, D.W., Ramsay, J.G., 1973. Incremental strains measured by syntectonic crystal growth. In:De Jong, K.A., Scholten, R.(Eds.), Gravity and Tectonics.Wiley, New York, pp. 67-69.
Ellis, S., Beavan, J., Eberhart-Phillips, D., Stockhert, B., 2006. Simplified models of the Alpine Fault seismic cycle:stress transfer in the mid-crust. Geophysical Journal International 166, 386-402.
Ellis, S., Stockhert, B., 2004. Elevated stresses and creep rates beneath the brittleductile transition caused by seismic faulting in the upper crust. Journal of Geophysical Research Solid Earth 109. B05407.
Epting, M., Kudrass, H.-R., Leppig, U., Schafer, A., 1972. Geologie der Talea Ori/Kreta.Neues Jahrbuch der Geologie und Palaontologie 141, 259-285.
Fagereng, A., Diener, J.F.A., Meneghini, F., Harris, C., Kvadsheim, A., 2018. Quartz vein formation by local dehydration embrittlement along the deep, tremorgenic subduction thrust interface. Geology 46, 67-70.
Fagereng, A., Sibson, R.H., 2010. Melange rheology and seismic style. Geology 38,751-754.
Famin, V., Philippot, P., Jolivet, L., Agard, P., 2004. Evolution of hydrothermal regime along a crustal shear zone, Tinos Island, Greece. Tectonics 23. https://doi.org/10.1029/2003TC001509. B05407.
Fassoulas, C., Kilias, A., Mountrakis, D., 1994. Postnappe stacking extension and exhumation of high-pressure/low-temperature rocks in the island of Crete,Greece. Tectonics 13,127-138.
Fisher, D.M., Brantley, S.L., 1992. Models of quartz overgrowth and vein formation:deformation and episodic fluid flow in an ancient subduction zone. Journal of Geophysical Research Solid Earth 97(B13), 20043-20061.
Fisher, D.M., Brantley, S.L., Everett, M., Dzvonik, J., 1995. Cyclic fluid flow through a regionally extensive fracture network within the Kodiak accretionary prism.Journal of Geophysical Research Solid Earth 100(B7), 12881-12894.
Fisher, D., Byrne, T., 1990. The character and distribution of mineralized fractures in the Kodiak Formation, Alaska:implications for fluid flow in an underthrust sequence. Journal of Geophysical Research Solid Earth 95(B6), 9069-9080.
Henderson,I.H.C., McCaig, A.M., 1996. Fluid pressure and salinity variations in shear zone-related veins, central Pyrenees, France:implications for the fault-valve model. Tectonophysics 262, 321-348.
Hilgers, C., Dilg-Gruschinski, K., Urai, J.L.,2003. Microstructures grown experimentally from advective supersaturated solution and their implication for natural vein systems. Journal of Geochemical Exploration 78, 221-225.
Hilgers, C., Koehn, D., Bons, P.D., Urai,J.L., 2001. Development of crystal morphology during unitaxial growth in a progressively widening vein:Ⅱ. Numerical simulations of the evolution of antitaxial fibrous veins. Journal of Structural Geology23, 873-885.
Hilgers, C., Urai, J.L., 2002. Experimental study of syntaxial vein growth during lateral fluid flow in transmitted light:first results. Journal of Structural Geology24,1029-1043.
Hobbs, B.E., 1968. Recrystallization of single crystals of quartz. Tectonophysics 6,353-401.
Hobbs, B.E., Ord, A., Teyssier, C., 1986. Earthquakes in the ductile regime? Pure and Applied Geophysics 124, 309-336.
Johnson, R.B., DeGraff, J.V., 1988. Principles of Engineering Geology. Wiley, p. 497pp..
Jolivet, L., Goffe, B., Monie, P., Truffert-Luxey, C., Patriat, M., Bonneau, M., 1996.Miocene detachment in Crete and exhumation P-T-t paths of high-pressure metamorphic rocks. Tectonics 15,1129-1153.
Kilian, R., Heilbronner, R., 2017. Analysis of crystallographic preferred orientations of experimentally deformed Black Hills Quartzite. Solid Earth 8,1095-1117.
Kj(?)ll, H.J., Viola, G., Menegon, L., S(?)rensen, B.E., 2015. Brittle-viscous deformation of vein quartz under fluid-rich lower greenschist facies conditions. Solid Earth 6,681.
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