P. Schmoldt, PhD - MTNet - DIAS
P. Schmoldt, PhD - MTNet - DIAS P. Schmoldt, PhD - MTNet - DIAS
A. Appendix Anisotropy Resistivity Misfit RMS r xx Depth (km) Depth (km) 100 150 200 250 300 0 rAA 50 Depth (km) -1 0 1 2 3 4 TM -1 0 1 2 3 4 Log 10(periods)-2 S N 0 50 100 150 200 250 300 0 ryy 50 TE Log 10(periods)-2 100 150 200 250 300 synM11 synM11 synH10 0 30 60 90 120 150 180 210 240 270 Distance (km) Apparent resistivity Log10(Wm) Phase degrees synG09 synF08 synE07 synD06 synC01 synH10 synG09 synF08 Log 10(Wm) synE07 synD06 synM11 synH10 synG09 synF08 synE07 synD06 synC01 synC01 Total: Log10(rxx)-Log10(ryy) Log10(Wm) Log10(Wm) 0.22 3.40 2.95 2.50 2.05 1.60 3.2 2.8 2.4 2.0 1.6 degrees Fig. A.17.: Result of anisotropic 2D inversion for the 3D-crust-west profile with stations synM11 - synC01 on top of the synthetic 3D model (cf. Figs. 8.3, 8.4, and 8.5 for synthetic 3D model, station location, and profile location). Station data is decomposed according to the strike direction of the crust (N45W), and inversion is carried out with resistivity laplacian regularisation and an increased smoothing parameter (τ = 6) following the first inversion approach: isotropic inversion of short-period data in the first sequence and anisotropic inversion of long-period data in the second sequence. The less constrained location of the resistivity interface at upper mantle depth in this model is attributed to smoothing constraints of the inversion and the large station spacing in the area. 310
Anisotropy Resistivity Misfit RMS r xx Depth (km) Depth (km) 100 150 200 250 300 0 rAA 50 Depth (km) -1 0 1 2 3 4 TM -1 0 1 2 3 4 Log 10(periods)-2 0 50 100 150 200 250 300 0 ryy 50 TE Log 10(periods)-2 100 150 200 250 300 A.4. Auxiliary figures of the Tajo Basin subsurface investigation S N synN10 synN10 synM05 0 30 60 90 120 150 180 210 240 270 Distance (km) Apparent resistivity Log10(Wm) Phase degrees synL04 synK03 synJ02 synI01 synD00 synM05 synL04 synK03 Log 10(Wm) syn J02 synI01 synN10 synM05 synL04 synK03 synJ02 synI01 synD00 synD00 Log 10(Wm) Log 10(Wm) Log 10(r xx)-Log 10(r yy) Total: 0.50 3.10 2.73 2.35 1.98 1.60 3.10 2.73 2.35 1.98 1.60 degrees Fig. A.18.: Result of anisotropic 2D inversion for the 3D-crust-east profile with stations synN10 - synD00 on top of the synthetic 3D model (cf. Figs. 8.3, 8.4, and 8.5 for synthetic 3D model, station location, and profile location). Station data is decomposed according to the strike direction of the crust (N45W), and inversion is carried out with resistivity gradient regularisation and an increased smoothing parameter (τ = 6) following the first inversion approach: isotropic inversion of short-period data in the first sequence and anisotropic inversion of long-period data in the second sequence. The less constrained location of the resistivity interface at mantle depth in this model is attributed to smoothing constraints of the inversion and the large station spacing in the area. 311
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- Page 315 and 316: 11 Summary and conclusions The key
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- Page 324 and 325: A. Appendix Eocene 54 Ma 42 Ma 36 M
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- Page 330 and 331: A. Appendix A.2.4. Computation time
- Page 332 and 333: 296 3D-mantle profile Inversion res
- Page 334 and 335: 298 07-centre profile The profile 0
- Page 336 and 337: 300 3D-crust profile The profile 3D
- Page 338 and 339: 302 J-centre profile The J-centre p
- Page 340 and 341: A. Appendix Anisotropy Resistivity
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- Page 348 and 349: A. Appendix A.4. Auxiliary figures
- Page 350 and 351: A. Appendix 314 ρ TE(Ω−m) φ T
- Page 352 and 353: A. Appendix 316 ρ TE(Ω−m) φ T
- Page 354 and 355: A. Appendix 318 ρ TE(Ω−m) φ T
- Page 356 and 357: A. Appendix 320 pic003 (off-diagona
- Page 358 and 359: A. Appendix 322 pic013 (off-diagona
- Page 361 and 362: Bibliography Abalos, B., J. Carrera
- Page 363 and 364: Bibliography Artemieva, I. M. (2006
- Page 365 and 366: Bibliography Berdichevsky, M., V. D
- Page 367 and 368: Bibliography Cebriá, J.-M., and J.
- Page 369 and 370: Bibliography de Vicente, G., J. Gin
- Page 371 and 372: Bibliography Egbert, G. D., and J.
- Page 373 and 374: Bibliography Ganapathy, R., and E.
- Page 375 and 376: Bibliography Haak, V., and R. Hutto
- Page 377 and 378: Bibliography Hutton, R. (1972), Som
- Page 379 and 380: Bibliography Jones, A. G., and R. W
- Page 381 and 382: Bibliography Kurtz, R. D., J. A. Cr
- Page 383 and 384: Bibliography Lviv Centre of Institu
- Page 385 and 386: Bibliography Merrill, R. T., and M.
- Page 387 and 388: Bibliography Newman, G., and G. Hoh
- Page 389 and 390: Bibliography Pádua, M. B., A. L. P
- Page 391 and 392: Bibliography Prácser, E., and L. S
- Page 393 and 394: Bibliography Ritter, J. R. R., M. J
- Page 395 and 396: Bibliography Serson, P. H. (1973),
Anisotropy Resistivity<br />
Misfit<br />
RMS<br />
r xx<br />
Depth (km)<br />
Depth (km)<br />
100<br />
150<br />
200<br />
250<br />
300<br />
0<br />
rAA 50<br />
Depth (km)<br />
-1<br />
0<br />
1<br />
2<br />
3<br />
4<br />
TM<br />
-1<br />
0<br />
1<br />
2<br />
3<br />
4<br />
Log 10(periods)-2<br />
0<br />
50<br />
100<br />
150<br />
200<br />
250<br />
300<br />
0<br />
ryy 50<br />
TE<br />
Log 10(periods)-2<br />
100<br />
150<br />
200<br />
250<br />
300<br />
A.4. Auxiliary figures of the Tajo Basin subsurface investigation<br />
S N<br />
synN10<br />
synN10<br />
synM05<br />
0 30 60 90 120 150 180 210 240 270<br />
Distance (km)<br />
Apparent resistivity Log10(Wm) Phase<br />
degrees<br />
synL04<br />
synK03<br />
synJ02<br />
synI01<br />
synD00<br />
synM05<br />
synL04<br />
synK03<br />
Log 10(Wm)<br />
syn J02<br />
synI01<br />
synN10<br />
synM05<br />
synL04<br />
synK03<br />
synJ02<br />
synI01<br />
synD00<br />
synD00<br />
Log 10(Wm)<br />
Log 10(Wm)<br />
Log 10(r xx)-Log 10(r yy)<br />
Total:<br />
0.50<br />
3.10<br />
2.73<br />
2.35<br />
1.98<br />
1.60<br />
3.10<br />
2.73<br />
2.35<br />
1.98<br />
1.60<br />
degrees<br />
Fig. A.18.: Result of anisotropic 2D inversion for the 3D-crust-east profile with stations synN10 - synD00 on top of the synthetic 3D<br />
model (cf. Figs. 8.3, 8.4, and 8.5 for synthetic 3D model, station location, and profile location). Station data is decomposed according<br />
to the strike direction of the crust (N45W), and inversion is carried out with resistivity gradient regularisation and an increased<br />
smoothing parameter (τ = 6) following the first inversion approach: isotropic inversion of short-period data in the first sequence and<br />
anisotropic inversion of long-period data in the second sequence. The less constrained location of the resistivity interface at mantle<br />
depth in this model is attributed to smoothing constraints of the inversion and the large station spacing in the area.<br />
311
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