sgr ms thesis - University of Maine

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4.3.2. Results and Discussion Results (figure 4.5) show temperature versus time curves for 100m interval points from the chamber-wall rock contact, points located at the observed isograds, and a point 400m into the intrusion. The peak metamorphic temperature, 635°C, occurred at the intrusive contact at t = 1.9E11s (~6000 years). Peak temperature 500m from contact was 510°C at t = 3.2E12s (~1E5 years), and 1000m from the contact, peak temperature was 458°C at t = 6.2E12 (~2E5 years). The single intrusion model provides a similar gradient trend within the metamorphosed zone, but the model did not attain the temperatures required to form the observed peak metamorphic facies (figure 4.6a). For this model, Garnet and cordierite are stable at temperatures as low as 460°C, which is possible for low pressure metamorphism (Blatt et al., 2006). This simplified conductive model cannot fully explain the metamorphic pattern seen for pyroxene, however. Metamorphic orthopyroxene requires a temperature of at least 650°C at 1.5 kbar pressure or ~5 km depth (Spear et al., 1999; Blatt et al., 2006). If the pluton contact is not actually vertical, the surface exposures of the metamorphic zones may be oblique from their true thicknesses (figure 4.6b). This could explain the wider than expected thickness of the pyroxene zone and it may provide a constraint on the geometry of the magma reservoir and the Shatter Zone. If the metamorphic aueole dips outward or inward with respect to the chamber by 45 degrees, the “true” thickness of the pyroxene zone is 39
850 750 650 550 450 400m Into Chamber Temperature (°C) 350 Chamber Contact: Pyroxene Zone Cordierite-Garnet Zone: 450m 250 Garnet Zone: 950m Bio te Zone: 1000m 150 100m Intervals from Contact 0 50000 100000 150000 200000 250000 300000 me (years) a er intrusion Figure 4.5. A temperature versus time plot from intrusion model results. Colored curves are for points on the isograd borders. Grey curves are points located on 100m intervals from the reservoir contact. 40
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 and 16: LIST OF TABLES Table 6.1. Table 7.1
Page 17 and 18: subvolcanic magmatic systems, the l
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: t = 0s t = 1E11 t = 1E12s t = 1E13s
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 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
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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
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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
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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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