科研之友
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摘要
Strain localization processes in the continental crust generate faults and ductile shear zones over a broad range of scales affecting the long-term lithosphere deformation and the mechanical response of faults during the seismic cycle. Seismic anisotropy originated within the continental crust can be applied to deduce the kinematics and structures within orogens and is widely attributed to regionally aligned minerals， e.g.， hornblende. However， naturally deformed rocks commonly show various structural layers (e.g.， strain localization layers). It is necessary to reveal how both varying amphibole contents and fabrics in the structural layers of strain localization impact seismic property and its interpretations in terms of deformation. We present microstructures， petrofabrics， and calculate seismic properties of deformed amphibolite with the microstructures ranging from mylonite to ultramylonite. The transition from mylonite to ultramylonite is accompanied by a slight decrease of amphibole grain size， a disintegration of amphibole and plagioclase aggregates， and amphibole aspect ratio increase (from 1.68 to 2.23)， concomitant with the precipitation of feldspar and/or quartz between amphibole grains. The intensities of amphibole crystallographic preferred orientations (CPOs) show a progressively increasing trend from mylonitic layers to homogeneous ultramylonitic layers， as indicated by the J_(Am) index increasing from 1.9-4.0 for the mylonitic layers and 4.0-4.8 for the transition layer， to 5.1-6.9 for the ultramylonitic layers. CPO patterns are nearly random for plagioclase and quartz. Polycrystalline amphibole aggregates in the amphibolitic mylonite deform by diffusion， mechanical rotation， and weak dislocation creep， and develop CPOs collectively. The polymineralic matrix (such as quartz and plagioclase) of the mylonite and the ultramylonite deform dominantly by dissolution-precipitation， combined with weak dislocation creep. The mean P and S wave velocities are estimated to be 6.3 km/s and 3.5 km/s， respectively， for three layers of the mylonitic amphibolite. The respective maximum P and S anisotropies are 1.5%-6.4% and 1.8%-4.5% for the mylonite layers of the mylonitic amphibolite， and 6.0%-6.9% and 4.5%-5.0% for the transition layers; but for the ultramylonite layers， these values increase significantly to 8.0%-9.1% and 5.1%-6.0%， respectively. Furthermore， increasing strain (strain localization) generates significant variations in the geometry of the seismic anisotropy. This effect， coupled with the geographical orientations of structures in the Hengshan-Wutai-Fuping complex terrains， can generate substantial variations in the orientation and magnitude of seismic anisotropy for the continental crust as measured by the existing North China Geoscience Transect. Thickened amphibolitic layers by extensively folding or thrusting in the middle crust can explain the strong shear wave splitting and the tectonic boundary parallel fast shear wave polarization beneath the Hengshan-Wutai-Fuping complex terrains. Therefore， signals of seismic anisotropy varying with depth in the deforming continent crust need not deduce depth-varying kinematics or/and tectonic decoupling.
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