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

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

Figure 3.1 (A) Plan view of events related to development blasts (blasts not shown) along the 7810 exploration drift; and (B) production blast-induced events related to blasting in the 4247 Sill. Full waveform recording allows for the calculation of additional seismic event parameters from waveforms recorded in the time domain or from spectra in the frequency domain (Gibowicz and Kijko, 1994; Mendecki, 1997). At Creighton Mine, parameter calculation is often automated but occasionally done manually (by selecting first arrivals). Calculated parameters include source radius, asperity radius, energy released, apparent stress and stress drop. The maximum particle displacement, velocity and acceleration can also be calculated from each waveform. 3.2.1 Seismic Event Parameters A subset of 11,541 microseismic events that occurred between January 1, 2006 and December 31, 2007 and between 7000 and 7600 feet depth was used to establish background seismic parameter values. This depth range eliminates dense activity related to development on deeper levels. Events having location errors greater than 30 feet were filtered from the dataset to avoid intrinsic error in calculated source parameters. Within this block, seismicity pertaining to the 7200 Level, 7400 Level and 7530 Level was examined for spatial and temporal trends. Trends in seismic event parameters were also assessed. 42
Microseismic events of this subset have an average location error of 18 feet. Events were recorded on average by 22 sensors (15 uniaxial and 6 triaxial sensors triggered on average) with the minimum condition of 8 sensors needed for an event to be recorded. Complete population statistics, including those for magnitude events and events identified as blasts can be found in Appendix B. These parameters are automatically calculated by the mine using ESG software, and first arrivals for microseismic events are usually automated. Statistics for macroseismic events that are derived from the underground array may not reflect the true magnitude of the parameters because of waveform clipping for stronger events. 3.2.1.1 Moment Magnitude (M) Three magnitude estimates are made for microseismic events: uniaxial magnitude, as determined from uniaxial sensors, triaxial magnitude and moment magnitude. Magnitudes in this thesis for microseismic events make reference to the moment magnitudes. Detected microseismic events within the study area range in magnitude from M = -2.3 to M = 0.8 with a mean of M = - 1.09. The distribution of magnitudes peaks at M = -1.3 (Fig. 3.2). Below this magnitude a higher proportion of events is expected but events are not recorded due to the detection threshold of the sensors and the minimum sensor requirement for recording events. The magnitude range can also be examined with the frequency-magnitude relation (Fig. 3.3). The shallow slope at low magnitudes demonstrates that events below M = -1.3 are infrequently recorded, though these are expected to occur. Beyond M = 0.4 the relation breaks down due to the relative infrequency of larger events as well as the recording limitations of the sensors. At high magnitudes, sensors become saturated and recorded waveforms clipped. The effective range of microseismic coverage is therefore between M = -1.3 and M = 0.4. Spatially, high-magnitude microseismic events do not show preferential clustering except near blast sites. 43
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THE INFLUENCES OF STRESS AND STRUCT
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esulting in increased stress to the
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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 and 24: ack breccia and sediments later dep
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: are, at this time, in the process o
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
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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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title of the thesis - Department of Geology - Queen's University

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