sgr ms thesis - University of Maine

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C p solid 850J/kg °K C p magma 950J/Kg °K L, Latent heat 4E5J/Kg °K T intrusion T clasts 900°C (1173°K) 650°C (923°K) ΔT 250°C T granite solidus T feldspar crystallization T clast solidus 800°C (1073°K) 825°C (1098°K) 720°C (993°K) Thermal conductivity 3W/m °K Density 2650 Kg/m 3 , diffusivity coefficient 1.33E-6 m 2 /s Model area 0.8m 2 % matrix by area 75% Table 7.1. Physical constants for thermal solutions. 95
consistent with Type 3 breccias. The solidus for the Bar Harbor Formation is 720°C, calculated using an optimization algorithm in PerpleX (Connolly, 2009) and the thermodynamic database provided by Holland and Powell (1998). Chemical data required for the thermodynamic calculations came from mineral abundance data from Metzger (1959), and results were compared to melt data from similar metasedimentary and metapelite rocks from the Ballachulish aureole (Pattison and Harte, 1988) and from metapelite P-T-t paths (Spear et al., 1999). I assume a single emplacement event in the Shatter Zone as there is no clear field evidence for multiple injections. Latent heat of granitic magma crystallization must be considered owing to the large percentage of granite matrix in Type 3 Shatter Zone (Nekvasil, 1988; Bowers et al., 1990; Furlong et al., 1991; Petcovic and Dufek, 2005; Huber et el., 2009; Lyubetskaya and Ague, 2009; Dufek and Bachmann, 2010, Bea, 2010). Latent heat correction is obtained by considering the heat of fusion in the calculation of the specific heat (C p ) of a material. For granite, C p liquid is 100 J kg -1 K -1 greater than C p solid , and latent heat (L) is 4x10 5 J kg -1 (Bea, 2010). The correction for latent heat would occur within a temperature range, dT, with the lower limit defined by the solidus. Within dT, the latent-heat corrected C p takes the form (e.g. Bea, 2010) (7.1) For this equation, latent heat is released within the range of dT = 100°C above T granite solidus = 700°C, when most crystallization occurs. Latent heat causes a heightened rate of clast heating when the matrix temperature is within dT and is 96
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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 !
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4.3.1. Model Setup The model is use
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to make a “hockey puck” style g
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t = 0s t = 1E11 t = 1E12s t = 1E13s
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850 750 650 550 450 400m Into Chamb
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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 and 100: 6.3.3. Clast Circularity Analysis (
Page 101 and 102: with decreasing clast size in all T
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: mesh to better evaluate large therm
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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