Three-dimensional inversion of magnetotelluric data from the Central Andean continental margin
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Magnetotelluric data were collected in the late 1990s in the Central Andes of Chile and Bolivia, with the aim to delineate the electrical conductivity distribution in the subsurface and its relations to subduction processes. In previous studies, these data were interpreted based on 2-D models. The principal result was a vast conductivity zone beneath the Altiplano high plateau at mid and lower crustal depths and a much smaller, though significant conductor associated with the Precordillera Fault System. However, there are some significant 3-D effects in the investigation area, in particular near the coast and on the eastern Altiplano. The aim of this work is to give a reinterpretation based on new 3-D inversion of these data. The 3-D inversion not only provides a better fit to the data compared to 2-D results but furthermore allows to include sites with strong telluric distortion which were ignored in previous studies. We are now able to explain anomalous phases above 90° and induction arrows pointing subparallel to the coast as observed at several sites in the Coastal Cordillera. These strongly distorted data are caused by highly conductive near-surface structures that are partly connected to the Pacific Ocean, forcing currents to flow around the sites. The lower crust beneath the Coastal Cordillera resembles a poorly conductive, nearly homogeneous half-space and is electrically unremarkable. Besides, we can now image the Precordillera conductor as a continuous, elongated feature. The volcanic arc of the Western Cordillera is highly resistive with the exception of a few conductive spots which may be associated with certain individual volcanoes or geothermal resources, respectively. The Altiplano conductor is again the dominant electrical feature in the Central Andes, indicating widespread melting of the middle and lower back-arc crust.
KeywordsMagnetotellurics 3-D inversion Subduction zones Central Andes
The Central Andes developed as a response to the subduction of the oceanic Nazca Plate beneath the continental Southern American plate with a velocity approximately 6.5 cm/year and a dip angle of approximately 25° (Klotz et al.2006). The evolution of the Central Andes is characterized by a systematic eastward migration of the magmatic arc towards the continent (Scheuber et al.1994).
At the surface, we can distinguish five north-south elongated, main morphological units (Figure1) starting with the Coastal Cordillera (CC), the Longitudinal Valley (LC), the Precordillera (PC), the Western Cordillera (WC), the Altiplano, and the Eastern Cordillera (EC). The Coastal Cordillera, located currently in a forearc position, is a relict of the Jurassic-Early Cretaceous magmatic arc. The most prominent structure during this time is the trench-parallel, strike-slip Atacama Fault System that extends for more than 550 km between 21° and 26°S latitude (Scheuber et al.1994). The Longitudinal Valley is a basin filled with Oligocene-Miocene sedimentary and volcanic rocks. The Precordillera developed as a volcanic arc in the Late Cretaceous and Early Paleogene (Scheuber et al.1994). This area is characterized by a large cover of rhyolitic ignimbrites and domes associated with basaltic and andesitic lavas and intruded by granitoid plutons. A large shear zone, the West Fissure or Falla Oeste, is also located here. Along this zone are encountered some of the largest porphyry copper deposits in the world, e.g., Chuquicamata.
The present-day volcanic arc is located in the Western Cordillera. This mountain range reaches mean altitudes of about 4,000 m above sea level with volcanic peaks over 6,000 m. It marks the western border of the Altiplano-Puna plateau, characterized by Miocene to recent stratovolcanoes overlying older ignimbrite sheets of late Miocene eruptions (Baker and Francis1978; De Silva1989).
The basement of the Western Cordillera and western Altiplano is formed by Proterozoic metamorphic rocks of the amphibolite facies and igneous rocks of late Paleozoic that are exposed in the Precordillera (Breitkreuz1986; Wörner et al.2000). The Altiplano represents an intramontane basin with Cenozoic continental sediment fill that reach thicknesses of 7 km. In this area of inland drainage, various large salt flats (salars) developed.
The Uyuni-Kenyani Fault System (UKF) consists of three thrust faults (San Cristobal Fault, Corregidores Fault, Uyuni-Kenyani Fault) located in the central part of the Altiplano, with a NNE strike. Here, Paleozoic units are exposed along this major fault zone (Ege2004). This fault system formed in late Paleogene (28 Ma) and was active again in the Miocene (14 to 10 Ma) and caused an east-vergent thrusting (Elger2003).
To the east, the Altiplano is bordered by the Eastern Cordillera with its bivergent thrust system in Ordovician sedimentary rocks. The syncline is covered by Tertiary rock units (Ege2004; Müller et al.2002).The data used here were collected along two transects and at several intermediate locations between 19.9°S and 21.4°S, crossing the forearc, the Western Cordillera, and the Altiplano high plateau in the backarc. Profile segment A extends 190 km from the Western Cordillera across the Altiplano to the large, obliquely running Uyuni-Kenyani Fault System. Investigation area B includes mainly sites from the Precordillera and area C from the Coastal Cordillera and Longitudinal Valley (see Figure1 (B) and (C)).
Previous studies were based on 2-D models, e.g., (Brasse et al.2002; Schwalenberg et al.2002) and (Echternacht et al.1997). The principal results were a vast zone of partial melts beneath the Altiplano at latitude 21°S at mid and lower crustal depths, and the highly conductive West Fissure Zone beneath the Precordillera, explained by rising saline fluids from the deeper crust or even the downgoing slab (Echternacht et al.1997).
Data and motivation for a 3-D approach
Under ‘normal’ 2-D or even 3-D conditions, the phase of Z xy and Z yx should lie in the first or third quadrants, respectively, assuming an exp(i ω t) dependence of the inducing fields. This can be derived as a result of Kramers-Kronig relations which connect imaginary and real parts of Z. In the presence of strong 3-D current channeling effects (and also on the seafloor if strong bathymetric gradients occur, even in 2-D), this does not hold anymore, and phases may actually leave the original quadrant (Egbert1990; Ichihara and Mogi2009).
is particularly prone to 3-D effects. Induction arrows or vectors are derived from the tipper and point away from high-conductivity zones (in the so-called Wiese convention) in a 2-D environment, but generally not above a 3-D subsoil.
A dimensionality analysis (Brasse et al.2002) described 3-D effects at a number of sites. In particular, some stations on the Eastern Altiplano showed large skew values (as a measure of 2-D vs. 3-D structure) over a large period range. Due to strong distortion with phases above 90°, sites in the Coastal Cordillera were excluded from 2-D interpretation.
Earlier 3-D forward modeling of the forearc by (Lezaeta and Haak2003) showed roughly N-S oriented, conductive structures. It seems that the coast effect is masked by a local anomaly and current channeling. Additionally, a 2-D anisotropic modeling effort by (Beike2001) yielded a narrow, anisotropic conductor comparable to the Atacama Fault which may explain the orientation of the induction arrows, but this model could not explain phases above 90°. In previous studies, these sites were thus excluded from 2-D interpretation (Brasse et al.2002; Schwalenberg et al.2002).
A similar, unexpected deviation of induction arrows is also observed in the Southern Chilean Andes (Brasse et al.2009; Kapinos2011) and in northernmost Chile (Eydam2008; Galindo2010). With the help of 3-D inversion, we are now able to explain these effects and the anomalous phases (see below).
It is thus clear that numerous 3-D effects are characteristic for the Central Andean data set. However, it remains unclear to what degree previous 2-D inversions yielded a reliable image of the subsoil. This will be clarified in the following section.
(a) The WSINV3DMT has been developed on a data-space variant of Occam’s inversion introduced for 1-D setting by (Constable et al.1987) and expanded and implemented for a 3-D case by (Siripunvaraporn et al.2005). Occam’s approach is an algorithm for generating a smooth minimum norm model to an appropriate fit of the data. The computational costs are reduced by transforming from model-space to data-space and allows to invert data sets on a PC in a manageable time. The version used here is a serial code and does not allow to invert tippers. Smoothness of resistivity variation is determined by a model covariance with length scales set to 0.1 as default (see also Additional file6).
(b) The ModEM inversion algorithm employs the non-linear conjugate gradient method (NLCG). The memory-efficient NLCG and hybrid schemes make the program efficient enough to deal with large data sets (Egbert and Kelbert2012). Additionally to the impedance tensor, it allows to invert the magnetic transfer function (tipper).
The program includes a variant of the master-worker parallelization over forward problems following the scheme of (Meqbel2009). This is implemented using calls of the standard Message Passing Interface (MPI), which allows to communicate between different processors and to build a network that is able to use the memories of several processors (Kelbert et al.2014). In contrast to WSINV3DMT, the covariance matrix allows a manual selection of smoothing for each cell, which, e.g., is useful for influences of small-scale near-surface structures (Kelbert et al.2014).
We have implemented the code on Windows Core-i7 PCs in a local area network (LAN). For the inversion results below, we generally used full impedance data (and tipper with ModEM) in the period range 10 to 10,000 s and discarded those of poor quality, i.e., large scatter. We further reduced the data set by only considering every second period, resulting in four periods per decade. If not otherwise mentioned, the error floor was set to the default of 5%. Further information on the used smoothing parameters, number of iterations and resulting root mean square (RMS) are listed in Additional file6. The construction of the initial models was greatly simplified with the Grid3D software, provided by N. Meqbel (personal communication). In the following sections, we will present selected results of both inversion codes.
Profile A: Altiplano
For comparison, the WIN3DINVMT code was applied to this data subset, too. The same initial model was used for the inversion programs. Figure5 shows the resistivity distribution with depth of investigation area A, together with an exemplary data fit of site vad. The left model represents results of the ModEM (root mean square error (RMS) = 1.79) algorithm, the right one of WSINV3DMT (RMS = 1.59) inversion. Both models show mainly similar structures, only the smoothness and depth of the resistivity variations are slightly different. It is not surprising that the RMS is slightly larger for the ModEM result as this implies more data with different resolution capabilities. RMS is more or less equally distributed over the study area (see Additional file7); this holds also for the other areas shown later. Although we invert profile data only, artifact off-line structures are practically absent here and for small-depth (short periods) resistivity distribution looks at least plausible (i.e., correlates with morphology and geology).
Distinct major and minor basins dominate the resistivity image at shallow depths (see Figure4a, A1 to A3). The very low resistivities are caused by saline fluids in the salt pans, the largest being the Salar de Uyuni. A highly resistive structure cuts through the conductors between sites ram and yan (see Figure4a, (B) and Additional file1). We explain this resistor with the Paleozoic uplift of highly resistive rocks along the Uyuni-Kenyani Fault System. Previous studies were not able to constrain this structure more precisely. Contrary to expectation, the Uyuni-Kenyani Fault Zone is not associated with an isolated and elongated conductive zone, neither at small nor large depth.
At depths of more than 20 km, a huge conductivity anomaly (see Figure4b, (C)) can be seen. This Altiplano Conductivity Anomaly is itemized in other scientific studies and explainable as the northern extension of the source region of the Altiplano-Puna Volcanic Complex (De Silva1989). The lower boundary is poorly resolved.
In accordance with Schwalenberg et al. (2002), a sensitivity study (see Additional file8) for the model shown in Figures4 and5 indicates a minimum depth extent of 60 to 80 km. This has been done by setting the lower well-conductive structures to the background resistivity, starting the inversion over, and checking the model response. It is thus possible that this conductor extends through the entire crust.The conductive structure accumulates into two elongated structures north and south of the sites. Probably by adding another transect parallel to the ANCORP profile, the Altiplano Conductivity Anomaly would be seen as a continuous body. The N-S extension of the Altiplano Conductor can be detected in the northern part of the investigation area (Figure1 (B)) but is limited there due to missing sites on the central and eastern parts of the Altiplano.
Concluding, the new 3-D inversions generally confirm the previous 2-D results. These are the Altiplano Conductivity Anomaly beneath the plateau and the generally more resistive volcanic arc.
Area B: Precordillera
Surprisingly, a good conductor can now be detected in the vicinity of the volcanic arc close to stations inc, que, jac, and epu (see Additional files1 and2 for a plot of responses and data fit). This structure becomes clearly visible at a depth of about 2 km and terminates between 5- and 7-km depths (see Figure6a, (E)). Here, fumarolic activity is reported at three potentially active centers: the Irruputuncu, Olca, and Paruma volcanoes (Gonzalez-Ferran1994). This is a new finding compared to earlier 2-D models which could in principal not take the spatial distribution of hydrothermal sources into account. Of course, we cannot resolve the exact location nor the true resistivity of these anomalies as they are slightly offset from the sites. More measurements in Bolivia would be necessary to constrain those potential geothermal resources.The most prominent conductor in this part of the Central Andes runs along the Precordillera and is most likely associated with the West Fissure Fault System (Figure6c, (F) and (G)). It was formerly only modeled as a conductive spot in the upper crust, but we see now that this elongated structure reaches much deeper and may even be electrically connected to the slab, although this cannot be resolved uniquely. In the S-N section of the 3-D model (Figure6c, (F)), it seems that it reaches closer to the surface in the north of the study area. These details, as the exact locations of the anomalies in the volcanic chain, are not really resolvable for the time being due to the lack of sites.
The Precordillera conductor was clearly recognized already by (Brasse et al.2002) and (Schwalenberg et al.2002) and interpreted as an accumulation of aqueous fluids, released from hydrous materials by the subduction process and rising through a conduit provided by the West Fissure Zone. Its location in front of the arc is a common feature of many subduction zones, and there exists a certain correlation with reflection seismological findings along the ANCORP line (see the ‘Discussion’ section). The prominent Altiplano conductor illuminates the eastern margin of the model at depths >30 km but is of course not resolvable with the chosen model block.
Area C: Western Forearc
Inversion of the forearc data, investigation area C (see Figure1), is considerably more demanding due to the proximity of the Pacific Ocean with a trench of nearly 8-km depth which leads to a very significant coast effect. We used the ModEM code to invert all horizontal and vertical components. In the first step, we inverted only T zx and T zy without impedance data. The best resulting model was then taken as a start to invert all data, i.e., tippers and impedances.
The model core of area C (see Figure1) extends laterally 250 km in E-W direction, 100 km in N-S direction, and extends to a depth of 634 km vertically. We discretized this area into 63 × 92 × 34 cells in x, y, and z directions. The thickness of the first layer is around 50 m, increasing with a factor of 1.2 in z to the bottom of the model. In the starting model, a background resistivity of 1,000 Ωm was set here because of the high resistivity beneath the ocean and in the Coastal Cordillera at crustal and mantle depths as derived from previous 2-D studies. Furthermore, the Pacific Ocean was added with simplified bathymetry and a resistivity of 0.3 Ωm. Fourteen periods spaced between 10 and 104 s of 31 stations were used for the inversion, with an error floor of 5% for all elements.
Sites close to the coast are affected by the Pacific Ocean and display a strong coast effect (strong split of TE and TM modes). However and as mentioned above, some sites are significantly influenced by telluric distortion effects (Lezaeta2001). Sites with phases leaving the first quadrant (see Figure7a, black dots) are mainly located in the Coastal Cordillera (see Figure7 (CC)). It seems that near-surface structures are at least partly connected electrically with the Pacific Ocean (see Figure7 (J)). This connection forces the original TE currents to flow around the sites (channeling effects), resulting in those anomalous phases (c.f. Egbert1990; Ichihara and Mogi2009). The model not only explains the phases but also the deviated induction arrows at all sites in the Coastal Cordillera.
Sites glo, pen, and ger are located at the northern segment of the Atacama Fault Zone in the vicinity of the Salar Grande (see Additional files3 and5). These three sites show a similar behavior with respect to phases and apparent resistivities like the exemplary station shown in Figure2. At the surface of this dry, pure halite salar, numerous strike-slip, reverse, normal faults, extensive cracks, and drainage patterns are found (Allmendinger and Gonzales2010; Chong et al.1999) which, if only moderately conductive compared to the salar itself, provide a natural explanation of distortion, together with the observed conductive connection to the Pacific Ocean (see Figure7 (J)). Additionally, conductive near-surface sediments that are younger than the Cordillera basement rocks force current channeling effects.
Site qch located in the Chacarilla gorge at the eastern margin of the Longitudinal Valley shows also phases leaving the quadrant (see Additional file4). The trend of this canyon seems to connect the conductive surface sediments of the Longitudinal Valley with the highly conductive West Fissure Zone (see Figure7a,b (K)). The surrounding igneous rocks display high resistivity. This large conductivity contrast forces currents to flow along the gorge, resulting in anomalous phases. The same behavior is observed at site 685 (see Additional file4) located in a canyon between Longitudinal Valley and Precordillera.Near to the surface in the Longitudinal Valley, highly conductive sediments are modeled (see Figure7 (K)), while more resistive material is dominant at greater depth. Remarkably, induction arrows in the Longitudinal Valley point to the west, away from the conductive West Fissure zone.
In general, the two applied inversion algorithms, when tested, yielded quite similar results. We could usually achieve a good fit of all components of the impedance tensor and, with ModEM, also of the tipper. This is quite remarkable taking the often much larger scatter of main diagonal data into account. Fit of tipper data very close to the coast is not perfect, but this may be attributed to insufficient consideration of true bathymetry and shape of the coastline. Near-surface resistivity distribution often looks chaotic, but we could almost always associate scattered conductors with known structures, e.g., small sub-basins. Although the site density is by no means perfect in many parts of the Central Andes, we believe that the foregoing results are a significant improvement over the older 2-D models. Confidence in the results was also achieved by conducting a number of sensitivity tests; owing to limited computing resources, they were of course less extensive than one usually carries out in 2-D environments. The main findings and the most significant differences compared to previous work are as follows:
Thus, our 3-D model explains the strongly anomalous data in the Coastal Cordillera with purely local effects. Note, however, that the deflection of induction arrows is a regional phenomenon and observable over at least 1,000 km from Arica in the north to Tocopilla in the south of our study area (Brändlein2013; Brasse and Eydam2008). With current computing capacities, it is not possible to include all available North Chilean forearc data into a single 3-D model, and we are unable to decide for the time being if a local or a regional approach is more appropriate for the North Chilean margin. A regional-scale effect is implicitly contained in a 2-D anisotropic model as presented, e.g., by (Galindo2010) for tipper data near Arica and perhaps the truth lies in a synthesis of an anisotropic and a 3-D model.
The deeper forearc beneath the Coastal Cordillera is highly resistive and resembles an almost unstructured half-space. This is similar to older 2-D models and consistent with abundant seismicity in the whole (brittle) crust as discovered very recently (Bloch et al.2014).
Unlike our model, for data farther south, (Brändlein2013) shows a conductor in the mantle wedge above the Nazca plate which he attributes to fluid relocation after the 2007 Mw = 7.7 Tocopilla earthquake. Our study area is located directly where the 2014 Mw = 8.2 Iquique earthquake occurred, and we think it is an interesting speculation that now, in the aftermath of this event, such a conductor might appear, too.
Forearc – Precordillera:
The West Fissure Fault System is now imaged as a continuous lineament and with a larger depth extent than previously deduced. In our new 3-D model, this conductor is seen a little closer to the surface, i.e., commencing at 12-km depth instead of 15 km and even less in the north.
Such a conductive structure some tens of kilometers trenchward of the volcanic front is a common feature of many subduction zones and is interpreted as an accumulation of fluids originating in the downgoing slab (Worzewski et al.2011). A reflection seismological study (Yoon et al.2009) infers a fluid flow from the Nazca slab at this location but with a significantly deeper upper boundary of reflections (approximately 40 km). From there, (Yoon et al.2009) postulate a bifurcation of fluid flow, subvertically towards the surface and laterally along the so-called ‘Quebrada Blanca Reflector’ (a significant seismic bright spot) towards the volcanic arc. As our model experiment are compatible with such a deep reaching conductive structure (even with having in mind the reduced resolution capabilities of MT with respect to lower boundaries of conductive zones), we can for the first time reconcile the seismic and magnetotelluric observations. It remains enigmatic, however, why seismology sees the top of the fluid accumulation zone significantly lower than our MT model. Furthermore, we do not resolve a fluid channel directed towards the arc volcanoes. Thus, a corresponding explanation of the Quebrada Blanca reflector is not consistent with MT observations.
Contrary to earlier expectation, the volcanic arc in the Central Andes is not underlain by large high conductivity zones, neither in the upper nor in the lower crust. This means that a large-volume magma chamber does not exist, at least where our profiles cross the volcanic chain. This even holds for potentially very active volcanoes like Lascar (Díaz et al.2012). The only exception has been the Lazufre complex where rising partial melts lead to an uplift of 3 cm/year over a large area (Budach et al.2013).
This was delineated earlier (Brasse2011) and is now corroborated by our new 3-D modeling efforts. Only north of Olca and east/northeast of Irruputuncu volcanoes near-surface high conductivity spots are detected, which are likely manifestations of hydrothermal resources.
The 3-D model confirms the resistivity image deduced earlier, particularly the Altiplano conductor in the mid to lower crust. It is of enormous dimensions and has recently been detected further south as well (Comeau et al.2013). All geophysical data hint at widespread melting, including a low-velocity zone as inferred from seismic tomography (Heit et al.2008). The upper boundary of the Altiplano Anomaly correlates with the Andean Low-Velocity Zone proposed by (Yuan et al.2000). By inverting gravity data, (Del Potro et al.2013) assume for an area at latitude 21.5°S to 23°S partially molten rocks that ascend diapirically through a strongly weakened crust up to the surface. For further discussion on this unique anomaly, we refer to (Schilling et al.2006).
The weak 3-D effect in the Eastern Altiplano may be explained with a resistive structure that is associated with an uplift of resistive older, Paleozoic rocks along the oblique Uyuni-Kenyani Fault Zone. A conductive fault zone as in the Precordillera is not found here. Thus, the Uyuni-Kenyani Fault Zone cannot be regarded as a fluid conduit nor as a deposit for magmatic hydrothermal ores.
Complex magnetotelluric data at the Central Andean continental margin were successfully analyzed with the help of 3-D inversion algorithms. The most surprising observations near the North Chilean coast (frequent phases above 90° and induction arrows pointing obliquely or even parallel to the coast) are now explained by highly conducting, meandering current pathways rather close to the surface. The West Fissure mega shear zone is imaged as an elongated, deep-reaching conductor promoting fluid flow from the subducted Nazca plate. Modest 3-D effects on the Bolivian Altiplano are explained by thrusting of Paleozoic sediments at the Uyuni-Kenyani Fault. Furthermore, we can now resolve near-surface, moderately conducting features in the volcanic arc, probably associated with geothermal resources.
Our new 3-D inversion efforts are a step forward toward explaining the electrical resistivity structure of the margin. More data are needed to resolve certain features particularly in the forearc; this forms a future task.
We are indebted to W. Siripunvaraporn, A. Kelbert, G. Egbert, and N. Meqbel for providing their inversion algorithms. David Martens wrote some of the Matlab plotting routines to visualize inversion output. We thank two reviewers for their comments and recommendations.
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