P. Schmoldt, PhD - MTNet - DIAS

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List of Symbols Symbol SI unit Denotation Z Ω = V Zxx, Zxy, Zyx, Zyy A Ω complex impedance tensor elements of Z in Cartesian coordinates z m (or km) depth êx unity vector with respect to x-coordinate ı complex number Re real part of a complex number Im imaginary part of a complex number ∂x partial derivative with respect to x-coordinate ∂t partial derivative with respect to time ∇ Nabla operator ∆ = ∇2 Laplace operator J Jacobian H Hessian Ξ linear operator used in the error function ∞ infinite | · | absolute value || · || norm 〈·〉 estimate x vector x X, X T matrix X, transpose matrix X X, X ∗ matrix X, complex conjugated matrix X I identity matrix Cl Chlorine Cu Copper CuSO4 Copper sulfate Nd Neodymium Pb Lead (Plumbum) PbCl2 Lead chloride Sr Strontium U Uranium xxvi
Abstract The Tajo Basin and Betic Cordillera are the areas investigated by the first phase of the PICASSO (Program to Investigate the Convective Alboran Sea System Overturn) project in south-central Spain. The magnetotelluric (MT) component of PICASSO Phase I provides information about the electric conductivity distribution in previously unprobed subsurface regions, as well as enhancing results of prior geological and geophysical investigations, thereby enabling the devise of a petrological subsurface model and a comprehensive understanding about the tectonic setting. During analysis of the MT data, oblique geoelectric strike directions were determined for the Tajo Basin subsurface, which causes severe artefacts in models from commonly applied isotropic two-dimensional (2D) inversion, or requires computationally expensive three-dimensional (3D) inversion. A novel approach is developed in this thesis, which utilises electric anisotropy in one-dimensional (1D) and 2D inversions to image oblique 2D subsurface structures. Computational expense of this approach is considerably lower and its performance is successfully tested in a synthetic model study and subsequently employed to derive a model of the Tajo Basin subsurface. In addition to the novel anisotropic approach, isotropic 2D and 3D inversions are used to obtain enhanced insight into Iberian subsurface geology. The most striking features of the model are (i) a distinct vertical interface in the centre of the Tajo Basin that is associated with the “Alpine Spain” – “Variscan Spain” boundary; (ii) a mid- to lower crustal anomaly that is related to remnants of asthenospheric intrusion in connection with Pliocene volcanic events in the Calatrava Volcanic Province; (iii) a low resistivity – low velocity feature in the Tajo Basin lithospheric-mantle, related to the extensive reservoir responsible for volcanic events throughout Europe and Morocco. For the latter two, effects of hydrous phases are inferred that may originate from dehydration processes at the subducting slab beneath Alboran Domain and Betics Cordillera. xxvii
Page 1: Multidimensional isotropic and anis
Page 4 and 5: Contents 2.3. Deviation from plane
Page 6 and 7: Contents 8.3. Inversion of 3D model
Page 9 and 10: List of Figures 2.1. Amplitude of t
Page 11 and 12: List of Figures 4.17. Visual repres
Page 13 and 14: List of Figures 8.2. Ambient noise
Page 15 and 16: List of Figures 10.10.RMS misfit va
Page 17: List of Figures A.15.Result of anis
Page 20 and 21: List of Tables xviii 5.5. Parameter
Page 22 and 23: List of Acronyms FE finite element
Page 25 and 26: List of Symbols Below is a list of
Page 27: Symbol SI unit Denotation φ · pha
Page 32 and 33: Publications Poster presentations x
Page 34 and 35: Acknowledgements Team, namely Colin
Page 37 and 38: Introduction 1 The Iberian Peninsul
Page 39 and 40: ections from enhanced one-dimension
Page 41: Part I Theoretical background of ma
Page 44 and 45: 2. Sources for magnetotelluric reco
Page 67 and 68: Mathematical description of electro
Page 69 and 70: yields 3.2. Deriving magnetotelluri
Page 71 and 72: 3.2. Deriving magnetotelluric param
Page 73 and 74: 3.3. Magnetotelluric induction area
Page 75 and 76: Depth d s d 1 d 2 d n-2 d n-1 t 1 t
Page 77 and 78: 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
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Step 1: Isotropic 2D inversion Step
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8.3. Inversion of 3D model data par
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8.4. Summary and conclusions bution
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Regularisation order Smoothing para
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S N 1% 0 Depth (km) 3% Depth (km) 1
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9.1. Profile location Data collecti
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Location (degrees) Recording period
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Geological region Stations Geologic
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9.4. Segregation of data acquired w
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Phase (degrees) 135 90 45 0 Z xy -4
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0 km 10 km 30 km 100 km 300 km Dept
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Pseudo-sections crustal strike dire
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9.8. Analysis of vertical magnetic
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9.8. Analysis of vertical magnetic
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10. Data inversion WinGLink softwar
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a (horizontal smoothing) 10. Data i
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10. Data inversion Short period ran
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10. Data inversion TM+TE Depth (km)
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10. Data inversion (a) Constrained
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10. Data inversion the model into u
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10. Data inversion Depth (km) S N 0
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Depth (km) 10. Data inversion S N 0
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10. Data inversion Group velocity m
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10. Data inversion ductivity of thi
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10. Data inversion Shtrikman upper
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10. Data inversion in the lithosphe
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10. Data inversion isotropic 2D lay
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10. Data inversion Depth (km) Depth
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10. Data inversion tigation is usua
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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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