sgr ms thesis - University of Maine

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structurally anisotropic material is more difficult to constrain because local stresses are produced by thermal gradient, differing thermal expansion coefficients of layered materials, and the presence of materials that have anisotropic expansion and conduction characteristics. These characteristics are beyond the scope of the current thermal stress models, which are therefore most applicable to the homogeneous diorite clasts. 117
REFERENCES Acocella, V. (2007). Understanding caldera structure and development: an overview of analogue models compared to natural calderas. Earth Science Reviews 85: 125-60. Accocella, V.; Porreca, M.; Neri, M.; Mattei, M.; Funicello, R. (2006). Fissure eruptions at Mount Vesuvius (Italy): insights on the shallow propagation of dikes at volcanoes. Geology. 34: 673-676. Aizawa, K.; Acocella, V.; Yoshida, T. (2006). How the development of magma chambers affects collapse calderas: insights from an overview. Mechanisms of Activity and Unrest at Large Calderas 269: 65-81. Allen, M.; Brown, G.; Miles, N. (1995). Measurement of boundary fractal dimensions: review of current techniques. Powder Technology 84: 1-14. Andrle, R. (1996). The west coast of Britain: statistical self-similarity vs. characteristic scales in the landscape. Earth Surface Processes and landforms 21: 955-962. Annen, C.; Scaillet, B.; Sparks, R.S.J. (2006). Thermal constraints on the emplacement rate of a large intrusive complex: the Manaslu Leucogranite, Nepal Himalaya. Journal of Petrology Advance access. Annen, C. and Sparks, R.S.J. (2002). Effects of repetitive emplacement of basaltic intrusions on thermal evolution and melt generation in the crust. Earth and Planetary Science Letters 203: 937-955. Apuani, T. and Corazzato, C. (2009). Numerical model of the Stromboli volcano (Italy) including the effect of magma pressure in the dyke system. Rock Mechanics and Rock Engineering. 42: 53-72. Attoh, K. and Van der Meulen, M. (1984). Metamorphic temperatures in the Michigamme Formation compared with the thermal effect of an intrusion, Northern Michigan. The Journal of Geology 92.4: 417-432. Bachmann, O. and Bergantz, G.W. (2008). The Magma Reservoirs that feed supereruptions. Elements 4: 17-21. Bachman, O.; Miller, C.F.; de Silva, S.L. (2007). The volcanic-plutonic connection as a stage for understanding crustal magmatism. Journal of Volcanology and Geothermal Research 167: 1-23. 118
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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
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Chapter 5 ROCK MECHANICS AND THE FR
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A β δ σ 1 σ 3 σ t c a σ 1 σ
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friction along the closed crack sur
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h h/2 h/4 Figure 5.2. A cube displa
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where N (≥r) is the count of clas
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to place a minimum size limit when
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moment of sudden fracture tip failu
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produced results in a self-similar
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13 ln(area) (pixels) 12 11 10 9 ln(
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eaction processes were involved in
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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 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: disaggregation of Bar Harbor clasts
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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