sgr ms thesis - University of Maine

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Chapter 1 INTRODUCTION Magma chambers are dynamic physical and chemical systems involving multiple processes such as mixing, mingling, convection, recharge and evacuation of magma. At deeper crustal levels, relatively high background temperatures can lead to long-term physical and chemical evolution, obscuring the spatial and temporal relations among individual magmatic events. In contrast, the sequential evolution of magmatic systems high in the crust at the interface between the plutonic and volcanic realms is commonly well preserved. These subvolcanic systems (e.g. Johnson et al., 2002; Metcalf, 2004; Kemp et al., 2006; Marianelli et al., 2006), much like eruptive sequences, can preserve a long and varied history of instantaneous magmatic events. They typically contain a wide variety of intrusive phases (e.g. cone sheets, ring faults and dikes, and massive central intrusions) and are potentially a rich source of information about the evolution of caldera/volcano root zones and the tops of upper-crustal magma chambers. They also commonly preserve genetically related volcanic sequences on their margins. The detailed intrusive relationships in these complexes and the intimate timing relationships between the various intrusions and deformational structures are preserved in part due to rapid quenching of some units, and in part due to the sequential series of intrusions that produce a magmatic stratigraphy. These complexes provide an unusual opportunity to evaluate the evolution of 1
subvolcanic magmatic systems, the links between plutonism and volcanism, and upper-crustal magma plumbing systems in general. In this thesis, I describe a subvolcanic igneous system known as the Cadillac Mountain intrusive complex, emplaced at
Page 1 and 2: FRACTAL ANALYSIS AND THERMAL-ELASTI
Page 3 and 4: LIBRARY RIGHTS STATEMENT In present
Page 5 and 6: emplacement of mafic magma, resulti
Page 7 and 8: © 2011 Samuel Geoffrey Roy All Rig
Page 9 and 10: TABLE OF CONTENTS ACKNOWLEDGEMENTS
Page 11 and 12: 5.3.5. Clast Circularity Analysis .
Page 13 and 14: LIST OF FIGURES Figure 2.1. Figure
Page 15: LIST OF TABLES Table 6.1. Table 7.1
Page 19 and 20: Chapter 2 GEOLOGIC SETTING 2.1. Reg
Page 21 and 22: Somesville granite suite to the wes
Page 23 and 24: Biotite is metamorphic in origin, a
Page 25 and 26: Chapter 3 PHYSICAL DESCRIPTION OF S
Page 27 and 28: thinned lithosphere allows for part
Page 29 and 30: A B C Figure 3.1. Formation of a la
Page 31 and 32: 1997; Branney and Kokelaar, 1998; J
Page 33 and 34: Effusive-Type Eruption max 10 0 - 1
Page 35 and 36: magma quickly intrudes the develope
Page 37 and 38: Piston Downsag Piecemeal Funnel Tra
Page 39 and 40: fragmentation, and thermal energy h
Page 41 and 42: Chapter 4 THERMAL FRAMEWORK FOR CON
Page 43 and 44: contrast, conduction is heat transf
Page 45 and 46: A B Grt C Grt D Crd Crd E 1 mm F Cr
Page 47 and 48: ! ! ! ! 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
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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
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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
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A B Figure 6.6. Brecciation texture
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The final breccia classified in thi
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esolution images of each box were s
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Clast circularity data were produce
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A 1000 Clast Size Distribu on: Type
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diorite dike with D s = 2.62 and R
Page 99 and 100:
6.3.3. Clast Circularity Analysis (
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with decreasing clast size in all T
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possibilities as postulated previou
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Chapter 7 MECHANISMS FOR SECONDARY
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magma. To prove the viability of th
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mesh to better evaluate large therm
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consistent with Type 3 breccias. Th
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A temperature versus time plot was
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Dimensionless time 0 0.05 0.1 0.15
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Figure 7.4 displays model results f
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thermal model ignores advection of
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Zone experienced a relatively weake
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7.4. Thermal-Induced Fracture Field
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Metapelite/hornfels Diorite dike E
Page 127 and 128:
7.4.2. Results and Discussion COMSO
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This thermal fracture model explain
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disaggregation of Bar Harbor clasts
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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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