title of the thesis - Department of Geology - Queen's University

trending lineation (Fig. 2.3). Discrete pods and rare crosscutting to semi-concordant leucogranite
dykes constitute < 10 vol% of the domain.
Strongly flattened quartz grains exhibit core and mantle structures, recrystallized
subgrains, and subgrain extinction (Fig. 2.6d), indicating deformation temperatures of ~400-
500°C (Stipp et al., 2002). Garnets are inclusion-rich, intensely fractured and pulled apart parallel
to the mineral elongation lineation (Fig. 2.6c).
Asymmetric fabric elements, including C/S/C’ fabrics and sigma-type feldspar
porphyroclasts, are abundant and well developed within high-strain quartzite and pelitic schist
(Fig. 2.6a,b). Shear sense indicators show a near even distribution of dextral and sinistral senses
of motion.
2.4.2.5 Domain V – High-strain gneissic GHS
High-strain gneiss of the GHS is exposed approximately 1 to 6 km structurally below the
GHS-TSS interface, and spans ESE-WNW across the extent of the field area (Figs. 2.3, 2.7).
Rocks within the structurally uppermost section of this domain are highly strained, and
progressively decrease in strain and increase in volume percent of melt with increasing structural
depth. The high-strain gneiss (Fsp + Qtz ± Bt ± Ms ± Grt ± Tur ± Sil) contains up to 30 vol%
leucosome and is fairly homogeneous, with the exception of rare meter sized quartz/quartzite
layers and a ~100 m thick layer of pelitic schist (Qtz + Bt + Ms + Sil + Grt).
Structurally above this pelitic schist, to east of the village of Yangar, a mesoscale low
strain zone exposes augen gneiss of a similar mineralogy to the dominant high-strain gneiss. This
may suggest that the augen gneiss is the protolith to the high-strain gneissic GHS.
Garnets are inclusion-rich and intensely fractured but not consistently stretched parallel
to the mineral elongation lineation. Sillimanite in the form of fibrolite is abundant within the
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