04.08.2013
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7. Geology of the Iberian Peninsula crystalline rocks, whereas seismic and xenolith studies indicate that the middle and lower crust consist of felsic intrusives and granulites, respectively. Since no seismic activity was recorded below the middle crust, it is likely that the lower crust, is an incompetent, ductile layer between the mantle and the other crustal layers. Faults with an approximately N45W direction intersect the PICASSO Phase I profile in the proximity of stations pic005, pic009, and pic013, potentially yielding a respective geoelectric strike direction in MT data of shorter periods. Material interfaces at crustal depth below the Tajo Basin, as interred from seismic studies, coincide with the borders of the Betic Cordillera and the Iberian Range. The respective ENE-WSW and NW-SE orientation of the interfaces indicate different geoelectric strike directions for the northern and southern parts of the PICASSO Phase I profile (cf. Sec. 9.6.1). Furthermore, since the low velocity feature, occurring slightly north of the Betic Cordillera, reaches down to at least 200 km, whereas the anomaly associated with the Iberian Range cannot be observed at depths greater than 53 km, it is likely that the geoelectric strike direction in the Tajo Basin below the PICASSO Phase I profile will also change with depth. Seismic tomography studies further derive low velocity structures at crustal depth beneath Betic Cordillera and Alboran Sea, in the mid- and lower crust beneath in the Campo de Montiel region, and an extensive low velocity region located approximately 50 km to 350 km beneath the Tajo Basin. Different settings could explain such decreases of velocity, e.g. increased temperature, different chemistry, and the presence of partial melt or fluids. Investigation of the electric conductivity distribution in this region will add further constraints on this issue and might help to better understand the geological setting and the related tectonic evolution. In addition, results of the PICASSO Phase I investigation can help to reassess the stratigraphy of Tajo Basin and Betic Cordillera as deduced from seismic reflection and refraction studies. Formation of proposed Miocene folding and the depth extend of faults in the Tajo Basin may also be evaluated using results of this study. Further, the currently unknown eastward extent of the Iberian Massif beneath the Tajo Basin, in the region of the Manchega Plain, can be investigated given the significantly higher resistivity of the Iberian Massif. At deeper regions, it can be tested whether an uppermost electric asthenosphere layer with values of approximately 10 Ωm (proposed for the Betics region) is observable beneath central Iberia, or whether a more resistive upper mantle (as suggested by laboratory studies) satisfies the responses. If the location of the eLAB can be derived for the study area, its relative position in respect to the estimates for sLAB and tLAB in the region can be used to enhance knowledge about the local geological processes. Furthermore, by contrasting results of MT, seismic, and thermal studies conclusions can be drawn about composition and condition of the south-central Iberian Peninsula subsurface. 166
Part III A novel inversion approach for oblique geoelectric strike directions in crust and mantle The most exciting phrase to hear in science, the one that heralds new dis- coveries, is not “Eureka!” (I found it!) but “That’s funny” – Isaac Asimov
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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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2. Sources for magnetotelluric reco
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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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3.5. The influence of electric perm
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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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4.1. Types of distortion Fig. 4.3.:
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J s 0 s 0 4.1. Types of distortion
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4.1. Types of distortion Fig. 4.7.:
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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. Removal of distortion effects
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4.4.5. Caldwell-Bibby-Brown phase t
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4.4. Removal of distortion effects
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Method Applicability Swift angle 2D
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5. Earth’s properties observable
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5. Earth’s properties observable
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5. Earth’s properties observable
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5. Earth’s properties observable
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5. Earth’s properties observable
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5. Earth’s properties observable
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5. Earth’s properties observable
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5. Earth’s properties observable
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5. Earth’s properties observable
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5. Earth’s properties observable
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5. Earth’s properties observable
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5. Earth’s properties observable
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6. Using magnetotellurics to gain i
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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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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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0 km 10 km 30 km 100 km 300 km Dept
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0 km 10 km 30 km 100 km 300 km Dept
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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 TM+TE Depth (km)
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10. Data inversion TM+TE Depth (km)
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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 Depth (km) Depth
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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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11.2. PICASSO Phase I investigation
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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 Anisotropy Resistivity
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A. Appendix Anisotropy Resistivity
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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 316 ρ TE(Ω−m) φ T
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A. Appendix 318 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