sgr ms thesis - University of Maine

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% of clasts 40 35 30 25 20 15 10 Type 1 0.1-1cm radius clasts 1-10cm radius clasts 10+ radius clasts Total mean 1- 10cm radius, 431 0.1- 1cm radius, 925 10+cm radius, 6 5 % of clasts 0 40 35 30 25 20 15 10 5 0 35 30 0 0.2 0.4 0.6 0.8 1 Circularity Type 2 0 0.2 0.4 0.6 0.8 1 Circularity 40 Type 3 1-10cm radius, 644 10+cm radius, 14 1- 10cm radius, 595 0.1- 1cm radius, 2155 10+cm radius, 9 Circularity 1 0.9 0.8 0.7 0.6 0.5 0.4 0.3 0.2 0.1 0 Clast Circularity Analysis 0.1-1cm 1-10cm 10+cm Type 1 Type 2 Type 3 % of clasts 25 20 15 0.1-1cm radius, 3945 10 5 0 0 0.2 0.4 0.6 0.8 1 Circularity Figure 6.13. Circularity data ordered by Shatter Zone type. Percent of clasts with respect to circularity with slast radius bin sizes of 0.1-1, 1-10, and 10+cm represented by red, green, and blue, respectively. Mean circularity values are given by the bar graph to the right, and the pie charts display clast bin size populations. The circularity interval is 0.05. 85
with decreasing clast size in all Types. CBS decreases with proximity to the intrusive contact (Hawkins and Johnson 2004). 6.4. Discussion 6.4.1. Bifractal Distributions for Type 1 and 2 The change in slope for Types 1 and 2 represent some scale dependent factor that limits the self-similar nature of rock fragmentation to a finite size range. In this case, there are two clast size distributions with the slope change at clast radius of approximately 1.5cm. Although the data are variable, bifractal distributions with breakpoints at 1.25cm for Type 1 and 1.52cm for Type 2 best represent these size distribution data trends. Two possible factors affecting a rock’s fractal properties include scale dependent rock heterogeneity (e.g. Clarke et al., 1998) and individual mechanisms that are limited to a finite size range (Barnett, 2004, Farris and Paterson, 2007). Interests lie in the mechanism or condition that produces a relatively large D s for the coarse scale and a small D s for the fine scale. This would imply greater fragmentation intensity forming the coarse clasts. One possibility worth consideration involves the secondary modification of small clasts entrained along previously formed fracture paths during intrusion. Soon after fractures formed, volatile rich magma travelled up the fracture network. With the introduction of a water-rich heat source, small clasts entrained in these fracture networks would be highly susceptible to thermal disaggregation. This is a mechanism dependent on clast melt and magmatic flow that produces bifractal 86
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FRACTAL ANALYSIS AND THERMAL-ELASTI
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LIBRARY RIGHTS STATEMENT In present
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emplacement of mafic magma, resulti
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© 2011 Samuel Geoffrey Roy All Rig
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TABLE OF CONTENTS ACKNOWLEDGEMENTS
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5.3.5. Clast Circularity Analysis .
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LIST OF FIGURES Figure 2.1. Figure
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LIST OF TABLES Table 6.1. Table 7.1
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subvolcanic magmatic systems, the l
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Chapter 2 GEOLOGIC SETTING 2.1. Reg
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Somesville granite suite to the wes
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Biotite is metamorphic in origin, a
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Chapter 3 PHYSICAL DESCRIPTION OF S
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thinned lithosphere allows for part
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A B C Figure 3.1. Formation of a la
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1997; Branney and Kokelaar, 1998; J
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Effusive-Type Eruption max 10 0 - 1
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magma quickly intrudes the develope
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Piston Downsag Piecemeal Funnel Tra
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fragmentation, and thermal energy h
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Chapter 4 THERMAL FRAMEWORK FOR CON
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contrast, conduction is heat transf
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A B Grt C Grt D Crd Crd E 1 mm F Cr
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! ! ! ! Biotite Zone Garnet Zone !
Page 49 and 50: 4.3.1. Model Setup The model is use
Page 51 and 52: to make a “hockey puck” style g
Page 53 and 54: t = 0s t = 1E11 t = 1E12s t = 1E13s
Page 55 and 56: 850 750 650 550 450 400m Into Chamb
Page 57 and 58: approximately 140m thinner. The Sha
Page 59 and 60: Chapter 5 ROCK MECHANICS AND THE FR
Page 61 and 62: A β δ σ 1 σ 3 σ t c a σ 1 σ
Page 63 and 64: friction along the closed crack sur
Page 65 and 66: h h/2 h/4 Figure 5.2. A cube displa
Page 67 and 68: where N (≥r) is the count of clas
Page 69 and 70: to place a minimum size limit when
Page 71 and 72: moment of sudden fracture tip failu
Page 73 and 74: produced results in a self-similar
Page 75 and 76: 13 ln(area) (pixels) 12 11 10 9 ln(
Page 77 and 78: eaction processes were involved in
Page 79 and 80: Chapter 6 ANALYSIS AND RESULTS The
Page 81 and 82: Type 1 Type 2 500 m N Type 1 Type 2
Page 83 and 84: A B Figure 6.3. Type 2 Shatter Zone
Page 85 and 86: A B Figure 6.5. Centimeter-scale bo
Page 87 and 88: A B Figure 6.6. Brecciation texture
Page 89 and 90: The final breccia classified in thi
Page 91 and 92: esolution images of each box were s
Page 93 and 94: Clast circularity data were produce
Page 95 and 96: A 1000 Clast Size Distribu on: Type
Page 97 and 98: diorite dike with D s = 2.62 and R
Page 99: 6.3.3. Clast Circularity Analysis (
Page 103 and 104: possibilities as postulated previou
Page 105 and 106: Chapter 7 MECHANISMS FOR SECONDARY
Page 107 and 108: magma. To prove the viability of th
Page 109 and 110: mesh to better evaluate large therm
Page 111 and 112: consistent with Type 3 breccias. Th
Page 113 and 114: A temperature versus time plot was
Page 115 and 116: Dimensionless time 0 0.05 0.1 0.15
Page 117 and 118: Figure 7.4 displays model results f
Page 119 and 120: thermal model ignores advection of
Page 121 and 122: Zone experienced a relatively weake
Page 123 and 124: 7.4. Thermal-Induced Fracture Field
Page 125 and 126: Metapelite/hornfels Diorite dike E
Page 127 and 128: 7.4.2. Results and Discussion COMSO
Page 129 and 130: This thermal fracture model explain
Page 131 and 132: disaggregation of Bar Harbor clasts
Page 133 and 134: REFERENCES Acocella, V. (2007). Und
Page 135 and 136: Billen, M.I. and Gurnis, M. (2001).
Page 137 and 138: Clarke, D. B. (2007). Assimilation
Page 139 and 140: Fisher, R.V. (1960). Classification
Page 141 and 142: Hartmann, W.K. (1969). Terrestrial,
Page 143 and 144: Johnson, S.E.; Paterson, S.R.; Tate
Page 145 and 146: Mandelbrot, B.B. (1967). How long i
Page 147 and 148: Oliver, N.H.S.; Rubenach, M.J.; Fu,
Page 149 and 150: Schoutens, J.E. (1979). Empirical A
Page 151 and 152:
Wiebe, R.; Holden, J.; Coombs, M.;
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