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$Fayek & Kyser 2000 uraninite fractionations.pdf - Queen's University$

5.7 a) A representative common source gather from the crosshole data collected at the Imperial College test site. The signal to noise ratio is high, and the rst arrival waveforms are clear and coherent. At late times, incoherent, large amplitude arrivals dominate. b) Predicted common source data using acoustic forward modelling in the velocity structure shown in Figure 5.6. The rst arrival traveltimes and waveforms match well with the observed data, but the large amplitude, late arrivals are not predicted with the acoustic method. . . . . . . . 144 5.8 Predicted common source data using the new visco-elastic modelling results. a) Horizontal displacement component. b) Vertical displacement component. The horizontal component shows rst arrival times and waveforms that are similar to the acoustic modelling results, and some high amplitude arrivals at late times. The vertical component shows high amplitude arrivals similar to those observed on the real data. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 145 15
Chapter 1 Introduction Modelling the propagation of seismic waves, and thereby predicting the response at seismic receivers is a crucial step in the interpretion, or the formal inversion of data from seismic experiments. Seismic modelling is thus an important tool in geological hypothesis testing. As seismic experiments become increasingly more sophisticated and complete, we naturally seek to model the seismic response of increasingly realistic media. To model complete, wide band, seismic wave behaviour, in a heterogeneous, porous, and visco-elastic medium, numerical modeling of the full visco-elastic wave equation would seem desirable. Ideally one would like to include, if possible, 3 dimensions (3-D), general anisotropy and arbitrary visco-elasticity. While formulations for 3-D anisotropic media are possible (Mora, 1989a; Carcione et al., 1992), the memory and cpu time requirements for realistic model sizes currently still prevents the production use of such methods, especially for multi-source problems. Nevertheless, there has been a historical progression toward the practical use of ever more general methods (Alterman and Karal Jr, 1968; Kelly et al., 1975; Gazdag, 1981; Dablain, 1986; Holdberg, 1987; Virieux, 1986a; Dai et al., 1995), both for one-dimensional (1-D) two-dimensional (2-D) earth models. There are two major approaches used in seismic modelling: The rst of these is asymptotic ray theory (e.g. Cerveny et al. (1982) or Chapman (1985)), a technique that can oer insight into the nature of various arrivals in the seismic record but 16
Page 1 and 2: Frequency domain seismic forward mo
Page 3 and 4: Acknowledgements I would like to gr
Page 5 and 6: 2.5 Nested dissection ordering . .
Page 7 and 8: 6.1.4 Waveeld inversion . . . . . .
Page 9 and 10: 2.3 Two waydissected matrix S ~ = L
Page 11 and 12: 4.3 Two representative source gathe
Page 13 and 14: 4.15 Frequency domain modelled (pre
Page 15: 5.3 Numerical dispersion of the new
Page 19 and 20: Pratt (1995) and Song (1995) showed
Page 21 and 22: parameters is a daunting task. Extr
Page 23 and 24: element methods. 1.2 The signicance
Page 25 and 26: this sparsity. As in time domain me
Page 27 and 28: where the complex \impedance" matri
Page 29 and 30: 1.4 Fourier transforms and frequenc
Page 31 and 32: in order to unambiguously reconstru
Page 33 and 34: If the forward Fourier transform is
Page 35 and 36: ased on data setfrom an underground
Page 37 and 38: therefore one of the main applicati
Page 39 and 40: 2.3 Solving linear equation systems
Page 41 and 42: are always calculated by the time t
Page 43 and 44: Case 2 2 S = ~ 6 4 4 0 0 0 .5 0 .79
Page 45 and 46: Figure 2.2: Two-way dissected nite
Page 47 and 48: (n/2*n/2)/2 L 55 (n/2*n/2)/2 n*n/2
Page 49 and 50: (to within anorder of magnitude) ne
Page 51 and 52: D 4 (n; 0) (2n) 2 =2 + 2(2n=2) 2 =
Page 53 and 54: The memory required to perform LU d
Page 55 and 56: are of theorder of hundereds of kil
Page 57 and 58: 10000 1000 Time (s) Sequential orde
Page 59 and 60: Chapter 3 Visco-acoustic frequency
Page 61 and 62: Figure 3.1: Finite dierence operato
Page 63 and 64: However, analytical solutions do no
Page 65 and 66: 3.2.4 Lumped and consistent matrix
Page 67 and 68:
+4c=1 (3.9) which makes the minimiz
Page 69 and 70:
that the required memory is afuncti
Page 71 and 72:
1996). However quantitativeevaluati
Page 73 and 74:
(1991). The low velocity regions (1
Page 75 and 76:
a) Time slice at 5s b) Time slice a
Page 77 and 78:
domain approach would have to gener
Page 79 and 80:
1988). Reviews have been provided b
Page 81 and 82:
Figure 4.1: Grimsel Pass areal phot
Page 83 and 84:
5 10 15 20 25 30 35 40 45 50 55 60
Page 85 and 86:
160m BOUS 85.003 BOBK 85.004 BOBK 8
Page 87 and 88:
will assume that rst n r n x n z (
Page 89 and 90:
where jxj represents represents the
Page 91 and 92:
or c J~ = S ~ ,1 G ~ (4.13) where F
Page 93 and 94:
Figure 4.6: Comparison of the trave
Page 95 and 96:
In order to initialize the waveeld
Page 97 and 98:
the trace-to-trace amplitude variat
Page 99 and 100:
manner these groups were identied.
Page 101 and 102:
km/s 4.80 4.85 4.90 4.95 5.00 5.05
Page 103 and 104:
4.6.2 Regularization tests From thi
Page 105 and 106:
RMS Roughness 0.8 0.7 0.6 0.5 5 10
Page 107 and 108:
Figure 4.15: Frequency domain model
Page 109 and 110:
y the best isotropic results. In al
Page 111 and 112:
a) b) c) Figure 4.19: Data residual
Page 113 and 114:
Figure 4.20: Anisotropic full wavee
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km/s 4.80 4.85 4.90 4.95 5.00 5.05
Page 117 and 118:
Figure 4.24: Final waveeld inversio
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can eect theimages (the wrong theor
Page 121 and 122:
In essence, our new scheme is the e
Page 123 and 124:
where ! = 2f is the angular frequen
Page 125 and 126:
dicult to formulate direct solvers
Page 127 and 128:
! 2 u 0 + v 0 + ( +2) + ( + ) @ u
Page 129 and 130:
\stars": ! @ 2 1 0 0 1 0 -2 0 @x 0
Page 131 and 132:
free to vary from one node point to
Page 133 and 134:
(see equations 5.24 and 5.25), exce
Page 135 and 136:
1 1 0.8 0.8 a 0.6 0.4 b 0.6 0.4 0.2
Page 137 and 138:
Numerical dispersion curves for σ=
Page 139 and 140:
Ifollow closely the dispersion anal
Page 141 and 142:
the opposite results. The fraction
Page 143 and 144:
identied; it is also possible to id
Page 145 and 146:
Real data Acoustic modelling result
Page 147 and 148:
observed data. However, even with t
Page 149 and 150:
Chapter 6 Conclusions and further w
Page 151 and 152:
compensated for by the accuracy gai
Page 153 and 154:
(1992)). I have also shown how sens
Page 155 and 156:
Extensions to more complex cases Th
Page 157 and 158:
Although waveeld inversions have be
Page 159 and 160:
to nd more dicult targets. An incre
Page 161 and 162:
Bathe, K. J., and Wilson, E. L., 19
Page 163 and 164:
Cole, J. B., 1994, A nearly exact s
Page 165 and 166:
Lailly, P., 1984, Migration methods
Page 167 and 168:
Peng, C., Cheng, C. H., and Toksoz,
Page 169 and 170:
Smith, W. D., 1974, The application
Page 171 and 172:
Appendix A Dispersion analysis for
Page 173:
and 2 = ( 1 R 2 + 2 )( 1 + 2 R 2
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