Figure 57

Experimentally deformed quartzo-feldspathic rocks

Figure caption

Experimentally deformed quartzo- feldspathic rocks

starting material & regime1 / regime 2 / annealing & melting

57

EA shortened 50% at 900°C, 10-6/sec, and 1200 MPa; quartz regime 2 dislocation creep and feldspars regime 1.

EA shortened 50% at 900°C, 10-6/sec, 1200 MPa. At these conditions the quartz deforms by intermediate temperature (regime 2) dislocation creep and the feldspars deform by low temperature (regime 1) dislocation creep. Because dislocation climb is easy in the quartz grains, they can undergo homogeneous grain flattening; some grains show sub-basal deformation lamellae, and recrystallized grains formed by progressive subgrain misorientation are observed especially along some grain boundaries. The feldspars are stronger and deform less homogeneously; they tend to undergo micro-boudinage, although that is not obvious in this photo. (W314)

		Experimentally deformed quartzo-feldspathic rocks
		Figure caption

	Experimentally deformed quartzo- feldspathic rocks	starting material & regime1 / regime 2 / annealing & melting


57		EA shortened 50% at 900°C, 10-6/sec, and 1200 MPa; quartz regime 2 dislocation creep and feldspars regime 1. EA shortened 50% at 900°C, 10-6/sec, 1200 MPa. At these conditions the quartz deforms by intermediate temperature (regime 2) dislocation creep and the feldspars deform by low temperature (regime 1) dislocation creep. Because dislocation climb is easy in the quartz grains, they can undergo homogeneous grain flattening; some grains show sub-basal deformation lamellae, and recrystallized grains formed by progressive subgrain misorientation are observed especially along some grain boundaries. The feldspars are stronger and deform less homogeneously; they tend to undergo micro-boudinage, although that is not obvious in this photo. (W314)