P. Schmoldt, PhD - MTNet - DIAS

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9. Data collection and processing 0 km 10 km 30 km 100 km 300 km Depth range Depth: 12 – 30 km (intermediate and lower crust) 90 75 60 45 30 15 0 pic041 pic040 pic037 pic035 pic033 pic031 Betic Cordillera pic029 pic027 pic025 pic023 CIZ pic022 pic020 pic019 pic017 pic015 Multi-strike (Av. RMS-misfit in brackets) pic013 pic011 pic009 pic007 Tajo Basin pic006 All stations Tajo Basin 19.3 (1.0) 49.1 (0.8) Fig. 9.9.: RMS misfit for different geoelectric strike directions of stations recorded during PICASSO Phase I, using data in the Niblett- Bostick depth range 12 – 30 km; shown in the inset. Empty spaces are due to lack of data for this depth range at the respective station. Also shown in the top right corner is the optimal common geoelectric strike direction clockwise from North calculated for all stations and for stations in the Tajo Basin only; indicated by dashed and dotted white lines in the main plot, respectively. Assignment of stations to the different geological regions, displayed on the bottom of the plot, is based on their location in respect to geological units of the USGS EnVision map for Europe (Fig. 9.1), CIZ: Central Iberian Zone, part of the Iberian Massif. See text for further details. pic009, and pic013. Note that the geoelectric strike estimate has a 90 degrees ambiguity; therefore calculated values of N50.5E and N47.8E imply that geoelectric strike directions of N140.5E and N137.5E fit the data equally well. However, unlike station pic005, stations pic009 and pic013 do not exhibit a strong 2D behaviour, indicating that the two respective faults do not result in a significant vertical geoelectric interface. Comparing RMS misfits of the Tajo Basin intermediate and lower crust with the region associated with the Betic Cordillera reveals the different subsurface structures present along the profile, i.e. no distinct strike direction observable for the Betic Cordillera. This circumstance can be explained by the complex 3D structures below the mountain chain originating from its intricate origin (cf. Sec. 7). This difference in dimensionality for Tajo Basin and Betics region of the profile, also observed at mantle depth (shown in the next paragraphs), suggests separate investigation of the two regions. Strike analysis results for other depth ranges, shown in the following figures, support the concept of the complex structure of the southern region. Combined intermediate and lower crust Given the similarities in optimal strike direction, as well as overall directional variation of RMS misfit for intermediate and lower crust, strike analysis is conducted for the combined depth range as well. Analysis for the combined depth range yields a directional RMS misfit distribution that is similar to distributions of the individual depth ranges and a multi-strike direction of N49.1E (0.8 av. RMS misfit) for the Tajo Basin region (Fig. 9.9). Northern-most stations (pic001 – 004) agree well with this strike direction, whereas central stations (pic006 - 020) exhibit a considerable 1D structure. Results from seismic studies in the Tajo Basin, indicating a geologic strike direction with an NW-SE orientation (cf. Section 7.3.2), are used to solve the 90 degrees ambiguity. Accordingly, the geoelectric strike direction chosen for this region is N40.9W (or N139.1E). RMS misfits for stations associated with the Betic Cordillera is generally higher and no optimal strike direction is observable. 214 pic005 pic004 pic003 pic002 pic001 RMS misfit 4 3 2 1 0
0 km 10 km 30 km 100 km 300 km Depth range Depth: 35 – 100 km (lithospheric-mantle) 90 75 60 45 30 15 0 pic041 pic040 pic037 pic035 pic033 pic031 9.6. Compensating for distortion of the impedance tensor pic029 pic027 pic025 pic023 pic022 Depth: 35 – 120 km (lithospheric-mantle) 90 75 60 45 30 15 0 pic041 pic040 pic037 pic035 pic033 pic031 pic029 pic027 pic025 pic023 Depth: 140 – 300 km (asthenosphere) 90 75 60 45 30 15 0 pic041 pic040 pic037 pic035 pic033 pic031 Betic Cordillera pic029 pic027 pic025 pic023 CIZ pic022 pic022 pic020 pic020 pic020 pic019 pic019 pic019 pic017 pic017 pic017 pic015 pic015 pic015 Multi-strike (Av. RMS-misfit in brackets) pic013 pic013 pic011 pic011 pic009 pic009 pic007 Multi-strike (Av. RMS-misfit in brackets) pic013 pic011 pic009 pic007 Multi-strike (Av. RMS-misfit in brackets) pic007 Tajo Basin pic006 pic006 pic006 All stations Tajo Basin 11.6 (1.0) 30.0 (0.8) pic005 pic005 pic004 pic004 pic003 pic003 pic002 All stations Tajo Basin 12.4 (1.0) 29.4 (0.8) pic005 pic004 pic003 pic002 All stations Tajo Basin 14.1 (0.7) 20.2 (0.7) Fig. 9.10.: RMS misfit for different geoelectric strike directions of stations recorded during PICASSO Phase I, using data in the Niblett-Bostick depth ranges 35 – 100, 35 – 120, and 140 – 300 km; shown in the inset. Empty spaces are due to lack of data for this depth range at the respective station. Also shown in the top right corner is the optimal common geoelectric strike direction clockwise from North calculated for all stations and for stations in the Tajo Basin only; indicated by dashed and dotted white lines in the main plot, respectively. Assignment of stations to the different geological regions, displayed on the bottom of the plot, is based on their location in respect to geological units of the USGS EnVision map for Europe (Fig. 9.1), CIZ: Central Iberian Zone, part of the Iberian Massif. See text for further details. Intra-mantle depth As for the crust, directional distribution of the RMS misfit is investigated in more detail for regions within the mantle by subdividing the respective depth range into layers related to lithospheric-mantle and asthenosphere. No detailed information is available about the lithosphere–asthenosphere boundary (LAB) depth in this region, but from seismic data it can be inferred, that the LAB is likely to be found within the depth range 110 – 130 km (Sec. 7.3.2). Therefore, one section spanning from 140 km to 300 km, representing the asthenosphere, and two sections related to the lithospheric-mantle, extending down to 100 km and 120 km, are investigated (Fig. 9.10). Similar to the crust, the Tajo Basin exhibits an overall lower RMS misfit and an apparent optimal direction. Of those stations, the RMS misfit is in general higher for the odd-numbered stations, equipped with broadband and long-period systems, than for the data from even-numbered stations, recorded by broadband systems only. The difference in behaviour is due to the fact that data from sites with broadband stations only are less pic002 pic001 pic001 pic001 RMS misfit 4 3 2 1 0 RMS misfit 4 3 2 1 0 RMS misfit 4 3 2 1 0 215
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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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Page 200 and 201: 7. Geology of the Iberian Peninsula
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Page 205 and 206: Recovering a synthetic 3D subsurfac
Page 207 and 208: direction direction Depth: 12 - 30
Page 209 and 210: 8.2. Generating synthetic 3D model
Page 211 and 212: Distance from the centre of the mes
Page 213 and 214: 3D N45W 3D-crust TE Rho TE Phi Peri
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Page 217 and 218: Model variation RMS misfit Optimal
Page 219 and 220: Profile: 3D-crust (TM-only) Depth (
Page 221 and 222: Parameter Value 8.3. Inversion of 3
Page 223 and 224: Depth (km) 10 -2 10 -1 10 0 10 1 10
Page 225 and 226: 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
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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
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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
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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 278 and 279: 10. Data inversion Group velocity m
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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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Depth (km) Depth (km) 10. Data inve
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Modelled Observed Modelled Observed
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Depth (km) 10. Data inversion 0 30
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10. Data inversion Depth off LAB (k
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10. Data inversion Depth (km) S 0 5
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10. Data inversion 10.3. Summary an
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10. Data inversion owing to availab
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11 Summary and conclusions The key
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11.2. PICASSO Phase I investigation
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A. Appendix Eocene 54 Ma 42 Ma 36 M
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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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P. Schmoldt, PhD - MTNet - DIAS

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