P. Schmoldt, PhD - MTNet - DIAS

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7. Geology of the Iberian Peninsula 134 Fig. 7.1.: Geology of the Iberian Peninsula displaying the main tectonic features and geological units of Spain; modified after Gibbons and Moreno [2002a]. The location of the PICASSO Phase I profile is indicated by the red line.
7.2. Betic Mountain Chain part, represents a thick Palaeozoic shelf sequence of sediments, including Silurian graptolitic black shale [Garcia-Alcalde et al., 2002] and Devonian carbonates [Colmenero et al., 2002], both materials possessing the potential to form good electric conductors (see Section 5 for details about electric conductivities), and extension-related volcanic rocks, with a Proterozoic basement [Gibbons and Moreno, 2002a]. The Iberian Massif also contains the Ossa-Morena Zone (OMZ in Fig. 7.1), located in the south-west of Spain, which originates from the Cadomian orogeny and is therefore pre-Variscan [Gibbons and Moreno, 2002a]. The Cantabrian Mountains were initially formed during Variscan orogeny and underwent post-orogenic deformations during subsequent tectonic processes, whereas the Betics and Pyrenees are due to Alpine orogeny, the result of successive collision of the Iberian continental plate with Eurasia and Africa in Late Mesozoic – Cenozoic times [e.g. Dewey et al., 1989; DeMets et al., 2006; Muñoz, 1992; Abalos et al., 2002; Azanon et al., 2002; Capote et al., 2002; Gibbons and Moreno, 2002a; de Vicente and Vegas, 2009]. The intraplate ranges are compressional mountain belts from Alpine orogeny (Spanish Central System, CR in Fig. 7.1) and Tertiary orogeny (Iberian Ranges), separating the three major Iberian basins, namely Duero, Ebro, and Tajo. Details about geologic settings of these intraplate ranges and the Tajo Basin are given in Section 7.3, describing the regions around the PICASSO Phase I study area more closely. For the central Iberian Peninsula, a lithospheric thickness of around 110 km (±5 km) has been inferred (cf. Sec. 7.3), diminishing towards the boundaries of the peninsula to depths as shallow as 60 km at the Valencia Trough. The crust beneath the stable interior has a typical continental structure with a thickness of 31 – 32 km and increased thickness under the Alpine ranges [e.g. Capote et al., 2002]. Deep structures beneath the peninsula are not well resolved since deep probing seismic studies are complicated due to Iberia’s location on the edge of Europe. Seismic studies in this region, which, besides MT, have the best potential to reveal deep-seated features, are challenged by the need to install and maintain long-term stations in the Atlantic Ocean [e.g. Cloetingh et al., 2009] (cf. Sec. 7.3.2). 7.2. Betic Mountain Chain The Betic Mountain Chain (also Betic Cordillera or Betics) is part of the arc-shaped alpine Betic-Rif Cordilleras, stretching from the southeastern edge of the Iberian Peninsula through the strait of Gibraltar down to the east of Morocco. The Betic-Rif Cordilleras surround the Alboran Basin (also referred to as Alboran Domain and Alboran Microplate), located beneath the western Mediterranean Sea. The Rif and Betic mountains are thrust belts characterised by south-, west-, and north-vergent low angle thrust systems with tectonic transportation directed away from the Alboran Basin [Seber et al., 1996]. The tectonic setting of the Betic Cordillera is reasonably well known, and it is widely accepted that the mountain chain was formed due to the collision of the African and Iberian plates 135
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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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Page 168 and 169: Part II Geology of the study area I
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Page 205 and 206: Recovering a synthetic 3D subsurfac
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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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