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10. Data inversion Group velocity map 10s 20s 10s 20s Villarseñor et al. 2007 high conductivity – low velocity anomaly < pic020 < pic019 < pic017 < pic015 < pic013 < pic011 < pic009 < pic007
10.1. Inversion for crustal structures Fig. 10.12.: Real induction vectors (Parkinson convention) for 64 s periods at PICASSO Phase I station in proximity of the high conductivity – low velocity anomaly within the Iberian Massif (labelled ‘f’ in Figure 10.6, cf. Figure 10.11); location of the region on display shown in the inset. The dashed white ellipse indicates the location of the low velocity anomaly derived by seismic tomography [Villaseñor et al., 2007] (cf. Fig. 7.21). Thin black lines denote the location of DC train lines in the area. Additional insight about this feature are given by the 3D inversion result (Fig. 10.34) by characteristics of the induction arrows for station pic019 (in Parkinson convention) which point directly towards the anomaly, thus indicating higher conductivity in this area (cf. Fig. 10.12). Stations to the north exhibit different behaviour, pointing in NE (pic017) and NW (pic013, pic015) direction, i.e. not towards the anomaly. However, the DC train line, intersecting the PICASSO Phase I profile in between stations pic013 and pic015, may distort magnetic transfer functions of these nearby stations; see Section 9.8 for an analysis of magnetic transfer functions of PICASSO Phase I stations in the Tajo Basin and their distortion. For station pic017, on the contrary, no straightforward explanation can be devised for the fact that its induction arrows point away from the low velocity anomaly. Thus, induction arrow data do not yield a strong support for a highly conductive region to the west of stations pic017 and pic019 unless future geological or geophysical investigations provide plausible reasons for the diverging induction arrow at station pic017, e.g. an additional conductor to the northeast of station pic017. Given their similarity in location, anomaly ‘f’ is most likely related to the low velocity region within the Central Iberian Zone (CIZ) derived in the tomography study by Villaseñor et al. [2007]; the anomaly is situated close to the PICASSO Phase I profile at the southern edge of the Tajo Basin (cf. Fig. 10.11). The seismic anomaly comprises a velocity reduction of up to 4% within the relatively faster region associated with the Iberian Massif. Thus, the anomalous region is inferred, based on results of the PICASSO Phase I processing, to possess high conductivity and low velocity characteristic. This rules out most cases of ore bodies as cause of the conductive anomaly, because they exhibit a higher density which would produce an increase in seismic velocity instead. The increased con- 243
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Multidimensional isotropic and anis
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Contents 2.3. Deviation from plane
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Contents 8.3. Inversion of 3D model
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List of Figures 2.1. Amplitude of t
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List of Figures 4.17. Visual repres
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List of Figures 8.2. Ambient noise
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List of Figures 10.10.RMS misfit va
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List of Figures A.15.Result of anis
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List of Tables xviii 5.5. Parameter
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List of Acronyms FE finite element
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List of Symbols Below is a list of
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Symbol SI unit Denotation φ · pha
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Abstract The Tajo Basin and Betic C
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Publications Poster presentations x
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Acknowledgements Team, namely Colin
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Introduction 1 The Iberian Peninsul
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ections from enhanced one-dimension
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Part I Theoretical background of ma
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2. Sources for magnetotelluric reco
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Mathematical description of electro
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yields 3.2. Deriving magnetotelluri
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3.2. Deriving magnetotelluric param
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3.3. Magnetotelluric induction area
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Depth d s d 1 d 2 d n-2 d n-1 t 1 t
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3.4. Boundary conditions materials
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3.5. The influence of electric perm
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Distortion of magnetotelluric data
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4.1. Types of distortion Fig. 4.1.:
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J s 0 s 0 4.1. Types of distortion
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Scale Type Terminology Example Atom
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4.1. Types of distortion the use of
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4.2. Dimensionality Fig. 4.12.: The
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1D 2D local 3D/1D 3D/2D regional 4.
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4.3. General mathematical represent
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4.4. Removal of distortion effects
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Parameter Geoelectrical application
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4.4.5. Caldwell-Bibby-Brown phase t
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Method Applicability Swift angle 2D
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5. Earth’s properties observable
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6. Using magnetotellurics to gain i
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Part II Geology of the study area I
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7. Geology of the Iberian Peninsula
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Recovering a synthetic 3D subsurfac
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direction direction Depth: 12 - 30
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8.2. Generating synthetic 3D model
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Distance from the centre of the mes
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3D N45W 3D-crust TE Rho TE Phi Peri
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8.3. Inversion of 3D model data sch
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Model variation RMS misfit Optimal
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Profile: 3D-crust (TM-only) Depth (
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Parameter Value 8.3. Inversion of 3
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Depth (km) 10 -2 10 -1 10 0 10 1 10
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Depth (km) 10 -2 10 -1 10 0 10 1 10
Page 227 and 228: Step 1: Isotropic 2D inversion Step
Page 229 and 230: 8.3. Inversion of 3D model data par
Page 231 and 232: 8.4. Summary and conclusions bution
Page 233 and 234: Regularisation order Smoothing para
Page 235 and 236: S N 1% 0 Depth (km) 3% Depth (km) 1
Page 237 and 238: 9.1. Profile location Data collecti
Page 239 and 240: Location (degrees) Recording period
Page 241 and 242: Geological region Stations Geologic
Page 243 and 244: 9.4. Segregation of data acquired w
Page 245 and 246: Phase (degrees) 135 90 45 0 Z xy -4
Page 247 and 248: 0 km 10 km 30 km 100 km 300 km Dept
Page 255 and 256: Pseudo-sections crustal strike dire
Page 257 and 258: 9.8. Analysis of vertical magnetic
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Page 262 and 263: 10. Data inversion WinGLink softwar
Page 264 and 265: a (horizontal smoothing) 10. Data i
Page 266 and 267: 10. Data inversion Short period ran
Page 268 and 269: 10. Data inversion TM+TE Depth (km)
Page 270 and 271: 10. Data inversion (a) Constrained
Page 272 and 273: 10. Data inversion the model into u
Page 274 and 275: 10. Data inversion Depth (km) S N 0
Page 276 and 277: Depth (km) 10. Data inversion S N 0
Page 280 and 281: 10. Data inversion ductivity of thi
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Page 290 and 291: 10. Data inversion isotropic 2D lay
Page 292 and 293: 10. Data inversion Depth (km) Depth
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Page 300 and 301: Depth (km) Depth (km) 10. Data inve
Page 302 and 303: Modelled Observed Modelled Observed
Page 304 and 305: Depth (km) 10. Data inversion 0 30
Page 306 and 307: 10. Data inversion Depth off LAB (k
Page 308 and 309: 10. Data inversion Depth (km) S 0 5
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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
Page 326 and 327: A. Appendix A.2. Auxiliary informat
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A. Appendix 292 Fig. A.3.: Issues i
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A. Appendix A.2.4. Computation time
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296 3D-mantle profile Inversion res
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298 07-centre profile The profile 0
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300 3D-crust profile The profile 3D
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302 J-centre profile The J-centre p
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A. Appendix Anisotropy Resistivity
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A. Appendix A.4. Auxiliary figures
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A. Appendix 314 ρ TE(Ω−m) φ T
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A. Appendix 320 pic003 (off-diagona
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A. Appendix 322 pic013 (off-diagona
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Bibliography Abalos, B., J. Carrera
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Bibliography Artemieva, I. M. (2006
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Bibliography Berdichevsky, M., V. D
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Bibliography Cebriá, J.-M., and J.
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Bibliography de Vicente, G., J. Gin
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Bibliography Egbert, G. D., and J.
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Bibliography Ganapathy, R., and E.
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Bibliography Haak, V., and R. Hutto
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Bibliography Hutton, R. (1972), Som
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Bibliography Jones, A. G., and R. W
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Bibliography Kurtz, R. D., J. A. Cr
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Bibliography Lviv Centre of Institu
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Bibliography Merrill, R. T., and M.
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Bibliography Newman, G., and G. Hoh
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Bibliography Pádua, M. B., A. L. P
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Bibliography Prácser, E., and L. S
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Bibliography Ritter, J. R. R., M. J
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Bibliography Serson, P. H. (1973),
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Bibliography Spitzer, K. (2006), Ma
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Bibliography Tikhonov, A. N., and V
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Bibliography Wanamaker, B. J., and
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Bibliography Xu, Y., C. McCammon, a
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