western quebec and southern ontario - Department of Geology

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

waveform (Pn, Pg, Sn, Sg, PmP, SmS, pPg, pPmP. sPg, sPmP, etc.) and polarity of firstarrival times of P-waves and to manually assign weights for the picks. The waveformdata in SEED format for each event were initially obtained with duration of 600 secondsand various sample rates (40, 50 or 100 samples-per-second (sps)). These files wereconverted into SAC files using rdseed program (IRIS) and subsequently to a specialUWO format used in the PLTSEK program. Data were analysed using a sample rate of50 sps. The two data sets for each event (one from the Canadian and one from the USstations) were combined to form one UWO file for each event. These files were then usedin PLTSEK for visualization and analysis of the waveforms and for picking the arrivaltimes (Pn, Pg, Sn, and Sg, etc.) and the polarities of P-waves (Pg, Pn).The weights of the arrival times were assigned manually based on the quality offirst arrival: sharp and clear or unclear. Numbers 0, 1, 2, 3, 4 (0 for best and 4 for poorarrivals) were assigned corresponding to the weighting scheme in the HYPOCENTERprogram. The accurate arrival time is important for finding the exact location of theevent. The smallest uncertainties for P- and S arrival picks for all stations are 0.02 sec,but in many cases they are up to 0.06 sec because of the presence of noise. Usually the P-arrivals (Pg or Pn) can be picked with better accuracy than the subsequent arrival (Sn, Sg,etc.) because they have to be distinguished only from the background ambient noise. Thesecondary arrivals come at the coda of the P-waves and it is much more difficult todistinguish because of the presence of P-coda and lower signal to noise ratio. Figure 3.6shows examples of the arrival time picks for P- and S-waves. On Figure 3.6a the signal tonoise ratio is large and P g and S g are clear. In cases where the signal to noise ratio issmall, picking the first arrival times is comparatively difficult (Fig. 3.6b, top left).33
The amplitudes of the seismic waves decrease with distance. For thecomparatively strong seismic events studied here (m N > 3.5) it was possible to pickarrival times for stations at epicentral distances up to 900 km. An example of seismicrecords for one of the studied events aligned by the distance is shown in Figure 3.7.Figure 3.6a: Example of arrival times picking for Pg and Sg –waves for station CRLO atepicentral distance 133 km from m N 4.5 earthquake NW from Maniwaki.When possible, the polarity (compression or dilatation) of the first arrivals on thevertical component was defined. In some cases it was possible to define the polarities ofboth Pn and Pg waves on the same waveform (Figure 3.6). No filter was used when thepolarities were picked to avoid distortion of the signal and change of the original polarity34
Page 1 and 2: FOCAL MECHANISMS AND VARIATIONS IN
Page 3: Acknowledgements:I would like to ex
Page 9 and 10: Figure 5.12: Summary of the focal m
Page 11 and 12: AbbreviationsCNSN: Canadian Nationa
Page 13 and 14: Earthquakes in western Quebec and s
Page 15 and 16: 1.2 Organization of ThesisChapter 1
Page 17 and 18: eastern Canada each year, of which
Page 19 and 20: Metasedimentary Belt boundary tecto
Page 21 and 22: The Grenville Front tectonic zone (
Page 23 and 24: Figure 2.3: Seismicity in the study
Page 25 and 26: oadly similar continent-continent c
Page 27 and 28: Figure 2.4: Historical earthquakes
Page 29 and 30: earthquakes have occurred within th
Page 31 and 32: cluster, which is considered part o
Page 33 and 34: 2001. All events seemed to occur in
Page 35 and 36: CHAPTER 3DATA SET AND METHODS3.1 In
Page 37 and 38: Fig. 3.1: Locations of seismic stat
Page 39 and 40: Figure 3.2: Number of stations used
Page 41 and 42: the strongest recorded event in the
Page 43: Figure 3.5: Earthquake source param
Page 47 and 48: Figure 3.7: Vertical component wave
Page 49 and 50: HYPOCENTER programThe HYPOCENTER pr
Page 51 and 52: wave - e.g. Pg or Pn, Sg or Sn), th
Page 53 and 54: model for P-wave velocity with mult
Page 55 and 56: CHAPTER 4RESULTSIn this chapter the
Page 57 and 58: Figure 4.1: Distribution of RMS of
Page 59 and 60: Table 4.2: Earthquake parameters (h
Page 61 and 62: The focal depth calculated here is
Page 63 and 64: focal mechanism beach-ball diagrams
Page 65 and 66: some spatial variability of the ori
Page 67 and 68: 22 20001006 50 ±3 134 ±10 90 ±0
Page 69 and 70: a)b)c)d)Western QuebecSouthern Onta
Page 71 and 72: esults from other similar studies,
Page 73 and 74: source region (e.g. Chen and Molnar
Page 75 and 76: estimate using a stress inversion t
Page 77 and 78: Figure 5.3: Stress pattern for all
Page 79 and 80: oundaries of the Central Metasedime
Page 81 and 82: In Western Quebec Seizmic Zone (WQS
Page 83 and 84: deeper than 20 km (20 km to 26 km).
Page 85 and 86: Figure 5.7: Geologic features of WQ
Page 87 and 88: 2009). The Mont-Laurier earthquake
Page 89 and 90: a) b)c) d)Figure 5.9: Summary of th
Page 91 and 92: 5.4.3 Adirondack Clusters (WQ4 and
Page 93 and 94: WQ5 is located in the southern part
Page 95 and 96:
Figure 5.13: Geological features of
Page 97 and 98:
consistent with regional fault map
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WQ8 is locatedin the north-western
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5.4.5 Timiskaming Cluster (WQ9)The
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The known faults in WQ9 cluster are
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a) b)c) d)Figure 5.19: Summary of t
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ecorded within this cluster. As it
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Figure 5.22: Nodal plane strike for
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estricted to western Lake Ontario o
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More detailed look at the relations
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Baird, W.A. F., and McKinnon, S. D.
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Easton, R. M. (1986). Geochronology
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Havskov, J., and Ottemöller, L. (2
Page 121 and 122:
Ma, S., and Adams, J. (2002). Estim
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Rimando, R. E., and Benn, K. (2005)
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Wahlstrom, R. (1987) Focal mechanis
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APPENDIX A: Examples of Input and O
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SUNO BZ SN 3 141 15.29SADO BZ SG 4
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EEO BZ SG 4 140 48.02 91 0.09 0 315
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PAL BZ PN 2 D 140 33.20 53 -0.21 1
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APPENDIX C: Faults Plane Solutions
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Appendix D: Focal Mechanisms From P
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19810707 -74.6 45.1 13.0 1.9 304.0
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19950603 -76.4 47.1 18.0 3.9 100.1
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20060225 -75.2 45.7 18.7 4.5 125.8
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western quebec and southern ontario - Department of Geology

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