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

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$Fayek & Kyser 2000 uraninite fractionations.pdf - Queen's University$

Figure 2.7 Representative structures, rock types and deformation mechanisms of domain V and VI; the high-strain gneissic, and migmatitic Greater Himalayan sequence, respectively. They are from highest to lowest structural levels: (a) Delta-type rotated leucogranite pod indicating dextral shear within domain V. (b) Feldspar (fld) porphyroclasts bordered by micas and dynamically recrystallized quartz, in a core-andmantle sigma-type structure indicating dextral shear, within high-strain gneiss of domain V. (c) Sinistral shear band (red arrows) faulting and drawing into plane sillimanite (sil) and biotite (bt), within pelitic schist of domain V. (d) Quartz (qtz) grains showing interlobate to amoeboid quartz grain boundaries and subgrain extinction (red arrows), within gneissic GHS of domain V. (e) Chessboard-style extinction within quartz of domain VI. (f) Equigranular quartz and feldspar grains of domain VI, exhibiting uniform extinction, and interlobate grain boundaries. 31
pelitic layer and rare throughout the gneiss. Within the pelitic layer, abundant shear bands both fault and draw into plane sillimanite and biotite (Fig. 2.7c). At upper structural levels within the domain, muscovite is common and quartz grains are mildly elongate and inequigranular. Along strike, feldspar porphyroclasts are bordered by recrystallized quartz and feldspar in core-and-mantle type structures (Fig. 2.7b), corresponding to deformation temperatures of ~400-500°C (Tullis and Yund, 1991). At progressively lower structural levels within the domain, muscovite decreases in abundance and quartz grain boundaries transition from interlobate to amoeboid, occasionally exhibiting zones of subgrain extinction (Fig. 2.7d). These textures represent recrystallization dominantly through grain boundary migration, with a considerable component of recrystallization by subgrain rotation. This may correspond to the transition between these two recrystallization mechanisms at ~500°C (Stipp et al., 2002). These trends are consistent with the weakening of high-strain and asymmetric fabric elements with increasing structural depth throughout the entirety of the domain. Despite decreased intensity, tectonic foliations and mineral elongation lineations have a relatively consistent geometry (Fig. 2.3). Elongate quartz, feldspar, and phyllosilicates define a pervasive south-dipping foliation and a shallow to moderately plunging ESE-WNW trending lineation (Fig. 2.3). Minor, broad, upright, open folds with fold axes roughly parallel to the mineral elongation lineation gently warp the domain. Centimeter- to meter-scale isoclinal folds with identical fold axes are also locally observed throughout the high-strain gneiss. Asymmetric fabric elements, including C/S/C’ fabrics, sigma-type feldspar porphyroclasts and delta-type rotated leucogranite pods are best developed within the upper structural section of the domain (Fig. 2.7a,b,c). Shear sense indicators show a near even 32
Page 1 and 2: FROM CESSATION OF SOUTH-DIRECTED MI
Page 3 and 4: Abstract Field mapping and, structu
Page 5 and 6: Co-Authorship This thesis is my own
Page 7 and 8: Table of Contents Abstract ........
Page 9 and 10: 4.1 Introduction ..................
Page 11 and 12: Figure 4.3 Microscale CPO variabili
Page 13 and 14: Abbreviations Mineral Biotite Calci
Page 15 and 16: Figure 1.1 Color relief map of the
Page 17 and 18: 1.2 Evolution of the Himalayan-Tibe
Page 19 and 20: Figure 1.3 Structures in the Himala
Page 21 and 22: the various models. However, this a
Page 23 and 24: of shear (Murphy and Copeland, 2005
Page 25 and 26: Chapter 4 outlines proposed future
Page 27 and 28: indicated by symmetric high-tempera
Page 29 and 30: The second phase of middle Miocene
Page 31 and 32: 2.3 Geologic Setting 2.3.1 Himalaya
Page 33 and 34: 2.4 Geology of the upper Karnali Va
Page 36 and 37: Figure 2.3 Lithotectonic map and si
Page 38 and 39: the main shear zone fabric. The lit
Page 40 and 41: South of the interface, the TSS is
Page 42 and 43: WNW Figure 2.6 Representative struc
Page 46 and 47: distribution of dextral and sinistr
Page 48 and 49: al., 1986; Mainprice et al., 1986).
Page 50 and 51: Figure 2.9 Summary of CPO post-acqu
Page 52: a c a c Figure 2.10 Summary of quar
Page 56 and 57: Sample HK131A is a high-strain quar
Page 58 and 59: constriction, where rhomb slip domi
Page 60 and 61: ± 50°C (Law et al., 2004). Furthe
Page 62 and 63: Figure 2.14 (a) Photomicrograph of
Page 64 and 65: Figure 2.15 Summary of lithotectoni
Page 66 and 67: elationships, these data constrain
Page 68 and 69: primary reference material, “4409
Page 70 and 71: Figure 2.16 - continued. 57
Page 72: monazite grains are aligned paralle
Page 75 and 76: Analysis Position Pb U Th Th/U 207
Page 79 and 80: Analysis Position HK117A Pb U Th Th
Page 83 and 84: are derived from intensely deformed
Page 85 and 86: Samples KH10, HK102a, HK105, HK115,
Page 87 and 88: the intralaboratory standard (MAC-8
Page 89 and 90: Figure 2.18 - continued. 76
Page 91 and 92: espectively. Note that the plateaus
Page 93 and 94: Figure 2.19 Plots of muscovite cool
Page 95 and 96:
Figure 2.20 Summary of results from
Page 97 and 98:
(2) Previously published chronologi
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Figs. 2.7b,d, 2.15) is locally over
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Thermochronology of muscovite grain
Page 103 and 104:
Figure 2.21 - continued - Box (3) r
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92 Figure 2.22 (a) Location of stud
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is little data to support both afor
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Figure 2.23 Numerical model of modi
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The second phase is associated with
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yr Figure 3.1 Numerical model of Co
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phenomena are consistent with ongoi
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towards the topographic front of th
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Chapter 4 Microstructural analyses:
Page 121 and 122:
a c a c Figure 4.1 Summary of quart
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Figure 4.2 Results of study by Toy
Page 125 and 126:
factors on the formation of differe
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1987; Simpson and De Paor, 1993, 19
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2009). Furthermore, there is rising
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Figure 4.5 Simplified set up of ana
Page 133 and 134:
Appendix A Station locations and st
Page 135 and 136:
Station Latitude Longitude Elevatio
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Station Latitude Longitude KH019 KH
Page 139 and 140:
HK 140 - Non-processed EBSD data 12
Page 141 and 142:
HK 131A - U-Stage data 128
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HK 131A - Non-processed EBSD data 1
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HK 139D - Non-processed EBSD data 1
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HK 105A - U-Stage data 134
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HK 105A - Processed EBSD data (e.g.
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HK 125 - Processed EBSD data (e.g.
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Page 159 and 160:
Page 161 and 162:
HK 124B2 - Processed EBSD data (e.g
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KH18a - Monazite 1 150
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HK109 - Thin section * For HK109_mo
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U Th 4 3 2 1 5 10 9 11 7 8 6 Nd Y 1
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HK109 - Monazite 3 170
Page 185 and 186:
U SL CP 172
Page 187 and 188:
U Th SL 174
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Page 191 and 192:
U Nd CP 178
Page 193 and 194:
U Nd Th 180
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Page 197 and 198:
Y Nd U Th 184
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U Th SL 186
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CP Nd 2 3 4 6 5 1 Y P 190
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U Th SL 192
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CP Nd Y P 196
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U Th SL 198
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HK117a - Thin section 200
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11 12 10 8 9 13 14 15 7 6 4 2 5 3 1
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4 1 5 9 10 2 11 6 16 3 7 17 14 8 18
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9 8 7 10 6 5 4 3 2 1 206
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7 6 8 9 13 14 15 4 5 1 2 3 10 11 12
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210
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5 4 9 6 7 8 3 2 1 10 212
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Holdsworth, R.E., McCaffrey, K.J.W.
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Cottle, J. M., Jessup, M. J., Newel
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Ghosh, S.K., and Ramberg, H. 1976.
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Hodges, K.V., and Silverberg, D.S.
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Kohn, M.J. 2008. P-T-t data from ce
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Means, W. D., Hobbs, B. E., Lister,
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Prior, D.J. 2009. EBSD in the earth
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Caledonides. In, S. Sengupta (Ed.),
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Yakymchuck, C., 2010. Tectonometamo
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