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

More documents

Recommendations

Info

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

2.1.2 Dykes The Sudbury Region has been intruded by many generations of dyke swarms. The earliest of these is the Matachewan swarm (2.45 Ga; Heaman, 1997; Rousell et al, 1997), which predates rifting of the Archean basement. Quartz-diorite dykes (1.85-1.74 Ga), also known as Offset Dykes, are composed of impact-related melt rock and sulphides that fill impact-induced fractures oriented radially to the Sudbury Igneous Complex (Grant and Bite, 1984). Such dykes constitute important metal resources within the Sudbury Basin. Post-basin dyke intrusions include the ca. 1.4 Ga (Cochrane, 1991) east-west striking hornblende-diabase swarm, known as Trap Dykes (Dressler, 1984), and the northwest striking olivine-diabase Sudbury Dykes (ca. 1.24 Ga; Krogh et al, 1987). All dykes occur in proximity to or in the Creighton Mine. A quartz-diorite Offset Dyke extends from the 800 Level to the 6200 Level where it pinches out (Coulson, 1996). Coulson (1996) also notes that below the 6600 Level hornblende-diabase and olivine-diabase dykes do not constitute important structural elements. At shallower levels and at surface shearing occurs along dykes, as shown in geological mapping (Vale Inco). All dykes are also intersected and offset by late-stage faults and fractures (Cochrane, 1991). 2.1.3 Regional faults The Murray Fault system strikes east-northeast and extends 300 km from Sault Ste. Marie to Sudbury (Fig. 2.1). Zolnai et al. (1984) propose that the Murray Fault System initiated as extensional ductile faults, overprinted by steepening of the faults and brittle thrusting during the Penokean Orogeny, and further reactivated as strike-slip during the Grenville Orogeny. The 8
Murray Fault, the principal fault of the system, shows evidence of right-lateral displacement with a total estimated lateral displacement of 1 kilometer (Cochrane, 1991). The Creighton Fault, part of the Murray Fault System, extends 48 km from Drury Township, west of the Sudbury Basin, east to Coniston where it intersects the Grenville Front (Fig. 2.1; Cochrane, 1991). It trends east to east-northeast and dips steeply north between 75 and 90 degrees (Cochrane, 1991). Previous work by Cochrane (1991) found that the Creighton fault has a net slip of 560 metres. The north side is displaced 540 metres eastward and 150 metres downward relative to the south side. The Creighton fault truncates offset dykes, olivine-diabase dykes, as well as the southern tip of the Creighton embayment, leading Cochrane (1991) to suggest that the Creighton Fault is younger than 1.24 Ga. Akin to Zolnai et al. (1984), Rousell et al. (1997) propose that the cumulative slip of the Creighton fault reflects an early normal movement during the deposition of the Huronian Supergroup, followed by repeated reverse-sense reactivation during the Penokean Orogeny, and dextral-oblique faulting in the Neoproterozoic. The Creighton Fault diverges from the Creighton embayment at depth. Because the fault dips more steeply than the embayment, which dips at 60 degrees, the Creighton Fault does not intersect mine excavations. A splay between Murray and Creighton Faults, termed the Murray-Creighton Splay bounds the eastern margin of the Creighton Embayment and is intersected on levels above the Creighton Deep as the 118 Shear Zone (Hodder, 2002). Parallel features to both the Creighton Fault and Murray Creighton Splay fault are reflected in structures within the Creighton Deep (Tulk, 2001; Hodder, 2002). The Creighton Fault was observed at surface along HWY 144, west of Creighton Mine (Fig. 2.2). Rock in proximity to the Creighton fault is jointed and veined. Brittle jogs in rock in proximity to the fault and offset veins and dykes confirm a dextral sense of motion (Fig. 2.3). 9
Page 1 and 2: THE INFLUENCES OF STRESS AND STRUCT
Page 3 and 4: esulting in increased stress to the
Page 5 and 6: Table of Contents Abstract.........
Page 7 and 8: 4.6.1 Fracture Reactivation........
Page 9 and 10: List of Figures Figure 1.1: Locatio
Page 11 and 12: Figure 3.23: Preliminary stress inv
Page 13 and 14: Figure B11: Events between Jan 1, 2
Page 15 and 16: List of Tables Table 2.1: Geologica
Page 17 and 18: Chapter 1 Introduction 1.1 Backgrou
Page 19 and 20: Figure 1.1: Location of Sudbury and
Page 21 and 22: Chapter 2 Geological Assessment of
Page 23: ack breccia and sediments later dep
Page 27 and 28: 2.2 Local Geology of Creighton Mine
Page 29 and 30: B West East B’ Figure 2.4B: Longi
Page 31 and 32: Table 2.2: Fault systems within the
Page 33 and 34: Table 2.3: Summary of Fault Charact
Page 35 and 36: Figure 2.6: (A) Damage to shotcrete
Page 37 and 38: Figure 2.7: (A) The 1290 Shear Zone
Page 39 and 40: Figure 2.8: Images of (A) the 400-E
Page 41 and 42: Figure 2.9: (A) Photograph of the c
Page 43 and 44: Figure 2.10 (A) Shear foliation, in
Page 45 and 46: Figure 2.11: Thin sections of the F
Page 47 and 48: (Fig. 2.12B). Reduction of quartz g
Page 49 and 50: 2.3.11 Late-Stage Fractures The you
Page 51 and 52: overprinting (Cochrane, 1991; Couls
Page 53 and 54: Table 2.4: Summary of Proterozoic t
Page 55 and 56: Both of these inferred stress direc
Page 57 and 58: are, at this time, in the process o
Page 59 and 60: Microseismic events of this subset
Page 61 and 62: 3.2.1.2 Seismic Energy (E o ) and S
Page 63 and 64: 3.2.1.4 Stress Parameters Stress pa
Page 65 and 66: located events were removed from cl
Page 67 and 68: Figure 3.7: Detected seismicity cor
Page 69 and 70: Table 3.1: Event characteristics in
Page 71 and 72: Table 3.3: Summary of relevant para
Page 73 and 74: ) Damage Zone The rock mass in the
Page 75 and 76:
quadrants of dilatation and compres
Page 77 and 78:
Figure 3.12: Lower hemisphere equal
Page 79 and 80:
mechanism shows that over 57% of th
Page 81 and 82:
Figure 3.16: Classification of prin
Page 83 and 84:
Figure 3.18: Contoured P-axis, B-ax
Page 85 and 86:
Figure 3.20: Distribution of double
Page 87 and 88:
This parameter reflects the magnitu
Page 89 and 90:
Figure 3.23: Preliminary stress inv
Page 91 and 92:
Figure 3.25: Equal area stereonet s
Page 93 and 94:
Figure 3.27: (A) Maximum principal
Page 95 and 96:
4.2 Numerical Methods Phase 2 and U
Page 97 and 98:
Stress-strain relationships are use
Page 99 and 100:
Rock mass failure is governed by th
Page 101 and 102:
Figure 4.5: (A) Model for tectonic
Page 103 and 104:
The zero cohesion and low friction
Page 105 and 106:
Figure 4.9: Model of yielding for C
Page 107 and 108:
Figure 4.11: Model of differential
Page 109 and 110:
Figure 4.14: Model of maximum stres
Page 111 and 112:
stress field model. There is little
Page 113 and 114:
clustering are indications of rock
Page 115 and 116:
Figure 4.23: Contoured domains of s
Page 117 and 118:
Figure 4.24: Fracture initiation th
Page 119 and 120:
seismic Cluster 1, which correspond
Page 121 and 122:
contains energetic events and is no
Page 123 and 124:
preferentially oriented fracture pl
Page 125 and 126:
methodologies employed are of value
Page 127 and 128:
References Alcott, J. M., Kaiser, P
Page 129 and 130:
Galkin, V., Mungall, J. (2005). Str
Page 131 and 132:
Mungall, J. E., & Hanley, J. J. (20
Page 133 and 134:
Appendix A Geological Maps and Samp
Page 135 and 136:
A.2 Level Plans with Sample Locatio
Page 137 and 138:
Figure A3: 7400 Level, modified for
Page 139 and 140:
Figure A5: 7680 Level, modified for
Page 141 and 142:
Figure A7: 7940 Ramp, modified from
Page 143 and 144:
MICROSEISMIC EVENTS Source Radius A
Page 145 and 146:
2006 Event Frequency with Depth 600
Page 147 and 148:
B.2 Spatial Distribution of Seismic
Page 149 and 150:
Figure B11: Events between Jan 1, 2
Page 151 and 152:
Page 153 and 154:
Page 155 and 156:
Cluster 1 Source Radius Asp. Radius
Page 157 and 158:
Seismic Moment 10.0 9.5 9.0 8.5 8.0
Page 159 and 160:
143 Peak Velocity Parameter -2.5 -2
Page 161 and 162:
B.4.2 Temporal Distribution of Clus
Page 163 and 164:
147 Static Stress Drop 5.0 5.5 6.0
Page 165 and 166:
B.4.3 Temporal Distribution of Clus
Page 167 and 168:
151 Static Stress Drop 4.0 4.5 5.0
Page 169 and 170:
Frequency-Magnitude Relation for Cl
Page 171 and 172:
P-axis B-axis T-axis 155 Fault Plan
Page 173 and 174:
P-axis B-axis T-axis Fault Plane 1
Page 175 and 176:
Page 177 and 178:
Page 179 and 180:
D.1.1: Case 1 Models Figure D1: Cas
Page 181 and 182:
Figure D3: Case 1, elastic models s
Page 183 and 184:
A B C D Figure D5: Case 1, plastic
Page 185 and 186:
A B C D Figure D7: Case 1, plastic
Page 187 and 188:
D.1.2: Case 2 Models A B C D Figure
Page 189 and 190:
D.1.3: Case 3 Models A B C Figure D
Page 191 and 192:
D1.4 Tectonic Loading Models Figure
Page 193 and 194:
D.2 Discussion of Phase 2 Models El
Page 195 and 196:
Staged models were created in which
Page 197 and 198:
Figure D17 (A) Elastic model showin
Page 199 and 200:
Figure D19 (A) Elastic model showin
Page 201 and 202:
• Similar damage zones surroundin
Page 203 and 204:
; ;================================
Page 205 and 206:
change jmat=1 range 0,1564.64 0,156
Page 207 and 208:
crack (845.579,718.676) (787.063,57
Page 209 and 210:
;===plum=== crack (0,355.2371429) (
Page 211 and 212:
crack (866.14,726.44) (838.2,737.61
Page 213 and 214:
crack (838.2,737.616) (815.848,771.
Page 215 and 216:
crack (815.848,771.144) (815.848,78
Page 217 and 218:
;===== define sub block ===========
Page 219 and 220:
E.9 S3:S1 Model for fracture reacti
Page 221 and 222:
yval= abs(z_syy(zi)) xyval= abs(z_s
Page 223 and 224:
and rearranged to , (Equation F4) .
Page 225:
Such that , (Equation F19) I is the
show all

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

Create successful ePaper yourself

Delete template?

Save as template?