Annual Report 2000 - WIT

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194 discussion of these problems can be found in (Traub, 1999). Figure 4: Frequency and transmission range of typical survey configurations used in seismic exploration and non-destructive testing as compared to the anticipated scale of measurements in the HIKALISTO experiment. Considering a mean thickness of the ore dyke of about 2 meters, a resolution of less than 1 meter within a granitic environment of about 5 km/s had to be reached. This implied high scattering angles as well as frequencies well above 1 kHz. In this frequency range, limitations are imposed not only by the possible sources and signal transmission, but also by the recording characteristics of available receivers. This situation is depicted in fig. 4, where the scale and frequency range of our experiment is compared with other survey configurations frequently used in exploration and nondestructive testing. Available recording equipment shows a gap in the range between 1 and 10 kHz. Survey Layout The seismic measurements consisted of two parts: firstly, a low-frequency (Û 100 Hz) survey at the surface above the gallery involving groups of 6 geophones with an eigenfrequency of 14 Hz and an airgun-type source. Secondly, a high-frequency survey (up to 5 kHz) within the gallery, mainly concentrating on the testblock shown in fig. 5. In order to resolve the ore dyke with a thickness of about 1 - 3 meters within a granitic host rock, frequencies of up to 5 kHz had to be reached within the gallery. This could be achieved by a combination of high-frequency receivers including geophones with an eigenfrequency of 100 Hz and piezo-accelerometers. The geophones are able to record frequencies up to 3 kHz, whereas the accelerometers are recording in a frequency range of about 1 kHz to 10 kHz. As sources, detonator caps and a HILTI bolt gun were used.
195 Figure 5: The central part of the test site where the gallery system excises a triangular test block of about 50 m length. Figure 6: Overview of the Test site showing the geometry of the geophone spread. Through installation of receivers at the surface and within the gallery, a threedimensional array of receivers could be realized.
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Wave Inversion Technology WIT Annua
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Wave Inversion Technology WIT Wave
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Copyright c 2000 by Karlsruhe Unive
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i TABLE OF CONTENTS Reviews: WIT Re
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Wave Inversion Technology, Report N
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3 theory. It relates properties of
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Imaging 5
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8 two hypothetical eigenwave experi
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7 ¢¥£§¦©¨ ; < calculate sear
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7 7 searches ¡ HNJOL for ¢IHNJML
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14 Trace no. 1000 1500 2000 0.5 1.0
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16 CDP number 3100 3000 2900 2800 2
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18 REFERENCES Höcht, G., de Bazela
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20 INVERSION BY MEANS OF CRS ATTRIB
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22 For synthetic data, it is easy t
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— J J J J J J G J - J J G
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· · v 0 B 0 £ & Ä Ã & v
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31 Dürbaum, H., 1954, Zur Bestimmu
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Ã Ø Ì 0 0 Ì 4 0 Ã 0 G ' 4
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0 0 ˜ ” Z ˜ ” Z 4 4
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39 strategy by combining global and
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41 elled data is presented in Figur
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43 0.2 Distance [m] 1000 1500 2000
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45 In Figure 10 we have the optimiz
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47 Gelchinsky, B., 1989, Homeomorph
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§ ¢ ø ø for a paraxial ray, ref
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Œ § … Z ‹ Z § õ ø \ ø §
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54 As stated in Hubral and Krey, 19
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§ ó § 56 sequence. We made tes
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58 precision of the modeled input d
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60 Cohen, J., Hagin, F., and Bleist
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£ 65 The details of the theory inv
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67 of the figure. On both sides, a
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69 (a) (b) Depth (m) 600 800 Depth
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71 Langenberg, K., 1986, Applied in
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È Û Ñ¿ = ¨ Í Ñ>* = ¿ + ð
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g ý g [ ^ â g [ g g g g g â h [
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g § » ¹ [ƒŽ g 79 We now subst
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ê 81 ing was realized by an implem
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ˆ 83 -0.05 -0.1 Amplitude -0.15 -0
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85 on a second-order approximation.
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88 kinematic (related to traveltime
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¨ º Ý È · § À · Á · Á ¼
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° ´ ´ ã ° ¼ ´ ´ þ Ò Ò ¥
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94 1 taper value ksi1 0 ksi2 Figure
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96 0 1 2 3 4 5 Depth [km] CMP [km]
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98 CONCLUSION As a generalization o
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100 weight during the stacking proc
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102 are not illuminated for every o
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104 obtained from Zoeppritz' equati
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106 PreSDM of Porous layer 0.358 re
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108 REFERENCES Gassmann, F., 1951,
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110 et al., 1992), Hanitzsch (1997)
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112 consecutive wavefronts). Howeve
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114 Numerical example We test the W
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116 Versteeg, R., and Grau, G., 199
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118 indicator. To extract elastic p
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€ b b 120 S where is the position
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É É É É 122 The À constant (da
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124 0 Distance [ m ] 1000 2000 3000
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126 Kosloff, D., Sherwood, J., Kore
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128
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130 penetration distances and a pot
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and » ˆ Ö Ö is the scalar hydra
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Å éÙó ó ».-.‹œì/-jì¨‹
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136 TRIGGERING FRONTS IN HETEROGENE
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Ö ˆ Ö “P£'ˆ é ˆ ó,Lˆ¨
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Ö Ö Ê » Ø Ö » Ö Ê Ê Ê Ö
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142 300 250 200 a) eikonal equation
Page 156 and 157: 144 Shapiro, S. A., and Müller, T.
Page 158 and 159: » i » m ×]Ú ‘Œƒšj'Ÿlk hM
Page 160 and 161: 148 RESULTS Soultz-sous-Forêts Inv
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Page 164 and 165: 152 Figure 5: The cloud of events f
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Page 168 and 169: 156 straightforward. The new approa
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Page 172 and 173: 160 1982). There is also the so-cal
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Page 176 and 177: Ï u u ¬ 164 To summarize, we deri
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Page 180 and 181: ø M ã = ã Ù ø ä Ú ã Ù ø
Page 182 and 183: ã Q c ã ä 170 a=10m; std.dev.=8%
Page 184 and 185: 172 Frankel, A., and Clayton, R. W.
Page 186 and 187: 174 It is well-known that inhomogen
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Page 190 and 191: Kneib, 1995 285-6000 superposition
Page 192 and 193: 180 parameter: Hurst coefficient pa
Page 194 and 195: 182 REFERENCES Bourbié, T., Coussy
Page 196 and 197: 184 1999) in multiple fractured med
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Page 200 and 201: j jÆÅÇ[È”u j jÎÅÇ[È”uw
Page 202 and 203: 190 Davis, P. M., and Knopoff, L.,
Page 204 and 205: 192 properties from the measured se
Page 208 and 209: 196 Altogether, close to 260 shotpo
Page 210 and 211: 198 Time (ms) 0 2 4 6 8 10 12 14 16
Page 212 and 213: 200 of groundwater. ACKNOWLEDGEMENT
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Page 216 and 217: 204 the wavefront curvature matrix
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Page 220 and 221: é 208 Table 1: Median relative err
Page 222 and 223: 210 Table 2: Median relative errors
Page 224 and 225: 212 CONCLUSIONS We have presented a
Page 226 and 227: 214 PUBLICATIONS Previous results c
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Page 230 and 231: 218 weight functions from traveltim
Page 232 and 233: 220 REFERENCES Bleistein, N., 1986,
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Page 240 and 241: 228 In this paper, we present a mor
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Page 244 and 245: 232 Figure 3: The evolution of a WF
Page 246 and 247: 234 Let us analyze next the computa
Page 248 and 249: 236 CONCLUSIONS We have presented a
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Page 252 and 253: ’ Ç r 240 traveltimes, a computa
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“ Ã Æ ³ 244 0 0.5 [km] 0 0.5 1
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î r † Û(Û Ü Œ U Ú Ý Ü Û
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248 Ettrich, N., 1998, FD eikonal s
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ø ü ø ø ý Þ do ø ý Ü
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ø ö ø ú ü ö ü ¡ ü
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‹ 256 transport equation. Neverth
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258 tivalued geometrical spreading
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260 .
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262
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… " ¯ ü ý +- 4=° ü ü +
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ö ô æ º Ò x ¹ v ý ñ
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268 NUMERICAL RESULTS We constructe
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¹ õ ' ' -š' ù ¹ ù ' ' -š
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£ -š' - 272 Ô- —- Figure 6: C
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274 REFERENCES Aldridge, D. F. (199
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276
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278 3. 4. True-amplitude imaging, m
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280 Research Group Hamburg (Gajewsk
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282 Stefan Lüth Robert Patzig Refr
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284 Landmark Graphics Corp. 7409 S.
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286 TotalFinaElf Exploration UK plc
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288 as research assistant at Geoeco
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290 Ingo Koglin is a diploma studen
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292 Matthias Riede received his M.S
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294 Svetlana Soukina received her d
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296 Yonghai Zhang received the Mast
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