Figure 56

Experimentally deformed quartzo-feldspathic rocks

Figure caption

Experimentally deformed quartzo- feldspathic rocks

starting material & regime1 / regime 2 / annealing & melting

56

EA shortened 35% at 725°C, 10-6/sec, and 1200 MPa; dispersed quartz (regime 1) was stronger than matrix feldspar (cataclasis).

EA shortened 35% at 725°C, 10-6/sec, 1200 MPa. At these conditions pure quartz aggregates deform by low temperature (regime 1) dislocation creep and are weaker than pure feldspar aggregates which deform by cataclastic flow. However, the texture in this aplite sample shows that the isolated quartz grains (mostly white grains) were stronger than the feldspar grains (mostly darker grey). The reason for this is that in regime 1 dislocation creep, the recovery process is bulging recrystallization, which can only occur if there are quartz-quartz grain boundaries - and these are rare in the aplite. (W352)

		Experimentally deformed quartzo-feldspathic rocks
		Figure caption

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


56		EA shortened 35% at 725°C, 10-6/sec, and 1200 MPa; dispersed quartz (regime 1) was stronger than matrix feldspar (cataclasis). EA shortened 35% at 725°C, 10-6/sec, 1200 MPa. At these conditions pure quartz aggregates deform by low temperature (regime 1) dislocation creep and are weaker than pure feldspar aggregates which deform by cataclastic flow. However, the texture in this aplite sample shows that the isolated quartz grains (mostly white grains) were stronger than the feldspar grains (mostly darker grey). The reason for this is that in regime 1 dislocation creep, the recovery process is bulging recrystallization, which can only occur if there are quartz-quartz grain boundaries - and these are rare in the aplite. (W352)