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

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

2.1.1 Evolution of the Sudbury Basin The Sudbury Basin has been shaped by numerous tectonic events since the early Paleoproterozoic. Events that have affected the Sudbury region are listed in Table 2.1. The Archean hinterland of the Superior Province rifted at ca. 2.46 Ga, leading to the establishment of a passive margin at the southern edge of the Superior Craton (Mungall and Hanley, 2004). Passive margin rocks comprise the Southern Province. In the Sudbury area, Southern Province rocks include metasedimentary and metavolcanic rocks of the Huronian Supergroup. The proposed 2.40-2.20 Ga Blezardian Orogeny (Stockwell, 1982) may represent the first Proterozoic compressional deformation event affecting the Sudbury area. Blezardian deformation is thought to be responsible for the development of an early tectonic foliation in Huronian rocks and large-wavelength, non-cylindrical thick-skinned folds (Riller et al., 1999). The Penokean Orogeny (Van Schmus, 1976) initiated at ca. 1.88 Ga with the oblique collision of an island arc system with the Superior Craton (Schulz and Cannon, 2007). Before the bulk of the Penokean deformation terminated, the Sudbury region was impacted by a meteorite (Dietz, 1964) at 1.85 Ga (Krogh et al, 1984). Impact melting and impact induced-melting formed the Sudbury Igneous Complex (SIC), characterized by a differentiated pool of norite, gabbro and granophyre, lined by a Sublayer Norite, which hosts the bulk of the basin’s rich ore deposits (Dressler and Reimold, 2001; Jones, 2005). Post-impact deformation features during the Penokean Orogeny are restricted to the southern margin of the Sudbury Basin and include folds, faults and shear zones (Cochrane, 1991), which are responsible for offsetting and folding the Sudbury Igneous Complex into a doubly plunging synform (Brocoum and Dalziel, 1974; Mungall and Hanley, 2004). The Sudbury Igneous Complex is filled by the Whitewater Group, which consists of impact-related rocks such as fall- 6
ack breccia and sediments later deposited in the Penokean foreland basin (Dressler and Reimold, 2001; Long, 2004). The impact culminated in the emplacement of rich nickel and copper sulfides and platinum group metals. Table 2.1: Geological Events in the Sudbury Area Event Age Reference Grenville Orogeny 1.30-.1.00 Ga Van Breemen and Davidson, 1988 Intrusion of olivine-diabase Sudbury Dykes 1.238 Ga Krogh et al, 1987 Intrusion of hornblende-diabase Trap Dykes 1.4 Ga Dressler, 1984 Cochrane, 1991 Deposition of Whitewater Group 1.85- 1.7 Ga Hemming et al., 1996 Intrusion of quartz-diorite aplitic dykes (Offset dykes) Sudbury Event meteorite impact and SIC emplacement 1.850 Ga Krogh et al, 1984 1.850 Ga Dietz, 1964 Krogh et al, 1984 Penokean Orogeny 1.88-1.83 Ga Van Schmus, 1976 Schulz and Cannon, 2007 Intrusion of Nipissing Gabbro dykes and sills 2.22 Ga Corfu and Andrews, 1986 Blezardian Orogeny 2.40-2.20 Ga Stockwell, 1982 Riller et. al, 1999 Deposition of Huronian Supergroup 2.45-2.42 Ga Mungall and Hanley, 2004 Rifting of Superior Province 2.46 Ga Mungall and Hanley, 2004 Matachewan Dyke Swarm 2.476 Ga Heaman, 1997 7
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: Chapter 2 Geological Assessment of
Page 25 and 26: Murray Fault, the principal fault o
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
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) Damage Zone The rock mass in the
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quadrants of dilatation and compres
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Figure 3.12: Lower hemisphere equal
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mechanism shows that over 57% of th
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Figure 3.16: Classification of prin
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Figure 3.18: Contoured P-axis, B-ax
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Figure 3.20: Distribution of double
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This parameter reflects the magnitu
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Figure 3.23: Preliminary stress inv
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Figure 3.25: Equal area stereonet s
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Figure 3.27: (A) Maximum principal
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4.2 Numerical Methods Phase 2 and U
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Stress-strain relationships are use
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Rock mass failure is governed by th
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Figure 4.5: (A) Model for tectonic
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The zero cohesion and low friction
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Figure 4.9: Model of yielding for C
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Figure 4.11: Model of differential
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Figure 4.14: Model of maximum stres
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stress field model. There is little
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clustering are indications of rock
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Figure 4.23: Contoured domains of s
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Figure 4.24: Fracture initiation th
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seismic Cluster 1, which correspond
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contains energetic events and is no
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preferentially oriented fracture pl
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methodologies employed are of value
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References Alcott, J. M., Kaiser, P
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Galkin, V., Mungall, J. (2005). Str
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Mungall, J. E., & Hanley, J. J. (20
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Appendix A Geological Maps and Samp
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A.2 Level Plans with Sample Locatio
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Figure A3: 7400 Level, modified for
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Figure A5: 7680 Level, modified for
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Figure A7: 7940 Ramp, modified from
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MICROSEISMIC EVENTS Source Radius A
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2006 Event Frequency with Depth 600
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B.2 Spatial Distribution of Seismic
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Figure B11: Events between Jan 1, 2
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Cluster 1 Source Radius Asp. Radius
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Seismic Moment 10.0 9.5 9.0 8.5 8.0
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143 Peak Velocity Parameter -2.5 -2
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B.4.2 Temporal Distribution of Clus
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147 Static Stress Drop 5.0 5.5 6.0
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B.4.3 Temporal Distribution of Clus
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151 Static Stress Drop 4.0 4.5 5.0
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Frequency-Magnitude Relation for Cl
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P-axis B-axis T-axis 155 Fault Plan
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P-axis B-axis T-axis Fault Plane 1
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D.1.1: Case 1 Models Figure D1: Cas
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Figure D3: Case 1, elastic models s
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A B C D Figure D5: Case 1, plastic
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A B C D Figure D7: Case 1, plastic
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D.1.2: Case 2 Models A B C D Figure
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D.1.3: Case 3 Models A B C Figure D
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D1.4 Tectonic Loading Models Figure
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D.2 Discussion of Phase 2 Models El
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Staged models were created in which
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Figure D17 (A) Elastic model showin
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Figure D19 (A) Elastic model showin
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• Similar damage zones surroundin
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; ;================================
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change jmat=1 range 0,1564.64 0,156
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crack (845.579,718.676) (787.063,57
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;===plum=== crack (0,355.2371429) (
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crack (866.14,726.44) (838.2,737.61
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crack (838.2,737.616) (815.848,771.
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crack (815.848,771.144) (815.848,78
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;===== define sub block ===========
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E.9 S3:S1 Model for fracture reacti
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yval= abs(z_syy(zi)) xyval= abs(z_s
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and rearranged to , (Equation F4) .
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Such that , (Equation F19) I is the
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