 FULL PAPER
 Open access
 Published:
Introducing intersite phase tensors to suppress galvanic distortion in the telluric method
Earth, Planets and Space volume 67, Article number: 160 (2015)
Abstract
A common problem when interpreting magnetotelluric (MT) data is that they often are distorted by shallow unresolvable local structures, an effect known as galvanic distortion. We present two transfer functions that are (almost) resistant to galvanic distortion. First, we introduce the electric phase tensor, which is derived from the electric tensor, where the electric tensor relates the horizontal electric fields at a field and base site. The electric phase tensor is only affected by galvanic distortion, if present, at the base site. Second, we introduce the quasielectric phase tensor, which is derived from the quasielectric tensor, where the quasielectric tensor relates the electric field at a field site with the magnetic field at a base site. The quasielectric tensor is not affected by galvanic distortion. Using a synthetic dataset, we show that the sensitivity of the MT phase tensor, the quasielectric phase tensor, and the electric phase tensor is comparable for our model under consideration. Furthermore, we demonstrate that stable (quasi) electric phase tensors can be recovered from a real dataset with the use of existing processing software. In addition, we provide a formalism to propagate the uncertainties from the estimated (quasi) electric and impedance tensors to their respective phase tensors. The uncertainties of the (quasi) electric phase tensors are of the same order of magnitude as the uncertainties of the MT phase tensor. From our study, we conclude that the (quasi) electric phase tensors are an attractive complement to the standard MT responses.
Background
Electromagnetic (EM) studies of the Earth aim to infer its electrical conductivity. In the 1930s, Marcel and Conrad Schlumberger pioneered an EM field survey that relied on naturally occurring telluric currents rather than on the active injection of a direct current by a pair of electrodes (Schlumberger 1939). A telluric current is induced in the Earth by timevarying magnetic fields. These originate in the magnetosphere, ionosphere, and/or atmosphere with sources as far away as the Sun and as close as thunderstorms (Vozoff 1972). The first telluric surveys relied on the simultaneous measurement of one electric field component at a base and a field site. The difference in electric field strength at the base and field site could only qualitatively be interpreted, i.e., information on the relative conductivity difference between the base and field site was obtained.
Two decades later, the magnetotelluric (MT) method was introduced. The MT method is based on measurements of the timevarying (naturally occurring) orthogonal horizontal electric (E) and magnetic (H) field components at the Earth’s surface. The original papers assume that the conductivity distribution of the subsurface is onedimensional (1D), i.e., only varies with depth (Tikhonov 1950; Cagniard 1953). In that case, the ratio of E to H is independent from the measurement coordinate system and depends only on the 1D electrical conductivity distribution of the subsurface. In practice, the conductivity of the subsurface can vary in all three spatial directions and the electric and magnetic field components depend on the measurement coordinates. The E and H field components are related through the 2×2 complexvalued impedance tensor,
where E= [E _{ x },E _{ y }]^{T} and H= [H _{ x },H _{ y }]^{T} indicate the horizontal components of the electric and magnetic field at the field site r _{ f }. The superscript T denotes the transpose of a vector. Hereinafter, the dependence of the responses and EM fields on angular frequency ω is omitted but implied. Z contains information about the subsurface’s conductivity at each field location r _{ f }, see, e.g., Berdichevsky and Dmitriev (2008), Chave and Jones (2012), and Simpson and Bahr (2005) for a detailed description of the MT method.
However, in the 1950s, the magnetic field measurements were characterized by a low signaltonoise (S/N) ratio. The S/N ratio was increased by measuring the magnetic field variations at one site for several weeks and selecting the suitable timewindows. The tedious process of analyzing these long recordings led in the 1960s to the further elaboration of the telluric sounding (TS) method (Berdichevsky 1965; Yungul 1966). In a TS survey, both horizontal components of the electrical field are measured simultaneously at a field site (r _{ f }) and at a base site (r _{ b }) and related through the electric tensor T according to
During the 1970s, TS was often favored above MT because of its relatively low costs and the simplicity of the telluric measurements compared to the magnetic measurements. TS measurements were usually interpreted in terms of the effective electric intensity,
represented as a contour map of equal T _{eff}. Note that the electrical intensity map contained qualitative information of the subsurface’s conductivity (Berdichevsky and Dmitriev 2008; Iliceto and Santaroto 1986). Only with a known 1D conductivity profile beneath the base site, quantitative information on the conductivity of the subsurface could be provided (Yungul 1966).
In the mid1970s, the telluricmagnetotelluric (TMT) method was introduced (Hermance and Thayer 1975). In a TMT survey, the magnetic field at a base site is related with the electric field at a field site according to
We call Q the quasielectric tensor to emphasize that the electric field is measured solely at field sites. The main advantage of the TMT method is that with one magnetic field measurement, almost the same information as contained in the impedance tensor Z (defined in Eq. 1) is obtained (Hermance and Thayer 1975).
In the last couple of decades, the electric and quasielectric tensors have fallen into disuse. The reason for this is twofold. Firstly, increasing technologies improved the quality of the magnetic field measurements such that nowadays, the magnetic field measurements are not a limiting factor anymore in a MT survey. Secondly, it was realized (Bahr 1988; Jiracek 1990) that the measured electric fields can be distorted by charge accumulation at the surface of smallscale heterogeneities in the shallow subsurface. These socalled galvanic distortions can often not be determined adequately to remove their effect in a direct manner. In particular, the TS and the TMT method did not allow for a correction of galvanic distortion. However, it is relevant to remark that recently, a timedomain approach was introduced for a direct estimation of the distortion effect (Püthe et al. 2014).
Here, we extend the TS and the TMT method by introducing two new transfer functions, namely the electric phase tensor (Θ) and the quasielectric phase tensor (Υ). Like the MT phase tensor (Caldwell et al. 2004), the (quasi) electric phase tensors are almost free or completely free from galvanic distortion.
The paper is organized as follows. In “Governing equations” section, we show the derivation of the (quasi) electric phase tensors and we discuss their characteristics in “Multidimensional analysis of the structure of the (quasi) electric phase tensors” section. The behavior of the different phase tensors is discussed in “(Quasi) electric phase tensors predicted by a synthetic model” section using a synthetic dataset. Finally, in “Calculating (quasi) electric phase tensors from a field dataset” section, we demonstrate that stable (quasi) electric phase tensors can be recovered from a real dataset with the use of existing processing software. In the Appendix, we present a formalism to propagate the uncertainties from the estimated MT and (quasi) electric tensors to their respective phase tensors.
Methods
Governing equations
Galvanic distortion is caused by local smallscale heterogeneities in the shallow subsurface which are not the target of the MT survey. At the surface of these heterogeneities, charges accumulate and this affects the direction and magnitude of the electric field but not its phase. Thus, the effect of these local heterogeneities can be represented as a linear function of the electric field that would have been measured in absence of the local heterogeneities, E ^{true}, and a distortion matrix matrix Λ, that is
where Λ is unknown, realvalued, and frequency independent (Bahr 1988). The interested reader is referred to, e.g., Groom and Bailey (1989), Groom and Bahr (1992), and Chave and Smith (1994) for a more detailed explanation of the theory of galvanic distortion.
Following Eq. 5, we can write the electric field at the base and field site as
Eq. 6 implies that the electric tensor T, as defined in Eq. 2, is distorted as well. Indeed, substitution of Eq. 6 into Eq. 2 yields
and thus the true electric tensor, which would be measured in absence of the galvanic distortion, can be written as
and the electric tensor that is measured in presence of galvanic distortions is given by
The electric tensor is affected by galvanic distortion at both the base and the field site. In contrast, the electric phase tensor,
is only affected by galvanic distortion at the base site. Here, the operator ℜ points to the real part of the complexvalued electric tensor T and the operator I to its imaginary part. To prove that Θ is independent of Λ_{ f }, we separate Eq. 9 into its real and imaginary parts
where we used that the distortion matrices Λ_{ f } and Λ_{ b } are realvalued. Inverting the matrix ℜT by using (AB)^{−1}=B^{−1}A^{−1} yields
Substituting Eqs. 11 and 12 into Eq. 10 gives
Here, we used that \(\mathrm {\Lambda }_{f}^{1}\mathrm {\Lambda }_{f} = \mathrm {I}\), where I is the identity matrix. Thus, with the new response Θ, we completely rule out the problem of galvanic distortion at multiple field sites and we only have to account for possible galvanic effects at the base site.
Similarly, we use the quasielectric tensor Q, Eq. 4, to derive the quasielectric phase tensor,
where we have assumed that the horizontal magnetic field is not affected by galvanic effects (H=H ^{true}) (Groom and Bailey 1989). It is seen from Eq. 14 that the quasielectric phase tensor is independent from the distortion matrices Λ_{ f } and Λ_{ b } and is therefore completely free from galvanic distortion. Note that while deriving the (quasi) electric phase tensors, we used the same approach as was used for the derivation of the MT phase tensor (Caldwell et al. 2004).
Multidimensional analysis of the structure of the (quasi) electric phase tensors
The (quasi) electric phase tensors are intersite response functions. It is known that for the intersite horizontal magnetic tensor, the best location for the base site is above a 1D layered half space; otherwise, the effect of inhomogeneities at the base site will be transferred to the entire survey area and the effect of the inhomogeneities at the base site will be superimposed on the effects of the inhomogeneities at the field sites (Leibecker et al. 2002; Varentsov 2005; Habibian Dehkordi and Oskooi 2012). However, we expect that the conductivity profile at the base site does not play a major role if intersite transfer functions are used in a 3D inversion. As long as the conductivity below the base site is part of the inversion domain, the inverse algorithm can solve for both the conductivity below the base and the field sites. But in order to obtain a better understanding of the structure of the (quasi) electric phase tensors, we assume in the following a 1D conductivity section below the base site.
The quasielectric phase tensor
Onedimensional structures The quasielectric tensor Q (Eq. 4) and its phase tensor Υ (Eq. 14) have the same structure as the impedance tensor Z (Eq. 1) and its phase tensor Φ. For a 1D conductivity environment, that is different at the base and the field site, Q reduces to
and Υ reduces to
If the 1D conductivity section at the base site is identical to the 1D conductivity section at the field site, Q ^{1D} in Eq. 15 can be replaced by the 1D impedance Z ^{1D} and Υ^{1D} in Eq. 16 by the phase of impedance Φ^{1D}.
Twodimensional structures For a 2D conductivity distribution, a rotated coordinate system can always be found such that
and
where \(\phi ^{\mathrm {Q}}_{xy}\) and \(\phi ^{\mathrm {Q}}_{yx}\) are the phase angles of the quasielectric tensor elements Q _{ x y } and Q _{ y x }, respectively. The element Q _{ x y } relates E _{ x } with H _{ y } which means that \({\varUpsilon }^{2D}_{yy} {\equiv } \tan \hspace {2pt} \phi ^{\mathrm {Q}}_{xy} \) and \({\varUpsilon }^{2D}_{yy}\) is associated with the Hpolarization of the MT field. Note that wherever a 2D setup is discussed, we assume that the coordinate frame is such that the xaxis is perpendicular to the strike direction of the 2D conductivity structure. Correspondingly, \({\varUpsilon }^{2D}_{xx} {\equiv } \tan \hspace {2pt} \phi ^{\mathrm {Q}}_{yx} \) and \({\varUpsilon }^{2D}_{xx}\) are associated with the Epolarization of the MT field.
Threedimensional structures In 3D conductivity environments, the full quasielectric tensor Q has to be considered. Similar to the normalized skew angle of the MT phase tensor (Booker 2014), we define ψ ^{Υ}
which is a rotational invariant of Υ. As for the MT phase tensor, if the structure is 2D then ψ ^{Υ}= 0. However, ψ ^{Υ}= 0 does not necessarily mean that the structure is 2D as locally 3D symmetry can make ψ ^{Υ} small. A 2D interpretation of MT data is justified if the offdiagonal elements of Υ are one order of magnitude smaller than the diagonal elements of Υ. Applying the aforementioned criterion results into ψ ^{Υ}≥ tan−1(0.1)≥6°, as a practical guideline to decide whether a 3D interpretation of the data is required (Booker 2014).
The electric phase tensor
Onedimensional structures For a lateral uniform conductivity distribution, the horizontal electric field is identical at the field and the base site and the electric tensor T (Eq. 2) equals the identity matrix. If the field and the base site are underlain by different 1D conductivity sections, the electric tensor T is a realvalued diagonal matrix. Since the phase of a realvalued matrix is zero, the electric phase tensor reduces to zero for 1D media. A zerovalued electric phase tensor cannot be used to decide whether the subsurface is a laterally homogeneous 1D medium or consists of different 1D conductivity sections.
Twodimensional structures For 2D structures, T is symmetrical (Iliceto and Santaroto 1986), i.e., T _{ x y }=T _{ y x }. If the measuring axes coincide with the principle directions of T, T reduces to
In this coordinate frame, the electric phase tensor is given by
with \(\phi ^{\mathrm {T}}_{xx}\) and \(\phi ^{T}_{yy}\) the phases of the complexvalued elements T _{ x x } and T _{ y y }, respectively. The element T _{ x x } relates E _{ x }(r _{ b }) with E _{ x }(r _{ f }) (see Eq. 2), which means that Θ _{ x x } is associated with the Hpolarization of the MT field. Similar reasoning results in Θ _{ y y } being associated with the Epolarization of the MT field.
Threedimensional structures In 3D environments, the full electric tensor T has to be considered implying that the same holds for the electric phase tensor Θ. The normalized skew angle of the electric phase tensor can be defined as
However, ψ ^{Θ} cannot be used as an indicator for 3D conductivity structures in the same way as ψ ^{Υ} and ψ ^{Φ}. This can be seen by the fact that ψ ^{Θ} becomes indefinite if the conductivity section is 1D (Θ= 0) and for a 2D conductivity structure ψ ^{Θ} reduces to zero. This makes it impossible to define a workable limit for ψ ^{Θ} from which a 3D interpretation of the data is justified, as can be done for ψ ^{Υ} (“The quasielectric phase tensor” section) and ψ ^{Φ} (Booker 2014).
Results and discussion
(Quasi) electric phase tensors predicted by a synthetic model
We performed a model study to investigate the sensitivity of the (quasi) electric phase tensors compared to the sensitivity of the standard MT phase tensor. Plane and side views of the 3D model are shown in Figs. 1 and 2, respectively. The model mimics a conducting sedimentary basin surrounded by resistive mountains with a conductive fault beneath the left flank of the basin. We expect galvanic coupling between the high conductive sedimentary basin and the deep conducting basement by the downward leakage of electric currents within the fault. We performed two forward model runs, one run in which we have omitted the conductive fault and a second run with a 2000mwide conductive fault. The local structure is 3D at the corner points of the sedimentary basin, 2D around the margins of the basin and 1D away from the margins of the sedimentary basin. The 1D conductivity structure away from the margins continues till infinity. We placed the base site (r _{ b }) approximately 140 km apart from the upper left corner of the fault structure, see Fig. 1. At this location, the condition of one dimensionality is met. The simulations were conducted using the recently developed 3D EM code (Geraskin A, Kruglyakov M, Kuvshinov A: Novel robust and scalable 3D forward solver based on contracting integral equation method and modern programming technologies, submitted to Computers and Geoscienses) based on the contracting integral equation method.
In Fig. 3, the magnitude of the recovered diagonal phase tensor elements (vertical axis) is shown along a profile (horizontal axis) spanning the whole sedimentary basin. The location of the profile is indicated with the dashed horizontal line in Fig. 1. The absolute value of the magnitude of the phase tensor elements is a dimensionless number. For a 2D conductivity structure, the magnitude of Υ_{ x x } equals \(\tan \hspace {2pt} \phi ^{\mathrm {Q}}_{yx}\) and the magnitude of Υ_{ y y } equals \(\tan \hspace {2pt} \phi ^{\mathrm {Q}}_{xy}\) (Eq. 18). Similarly, the magnitudes of the diagonal elements of Φ are related to the phase angles of Z and the magnitudes of the diagonal elements of Θ are related to the phase angles of T. The results are shown for T=30 s. The upper two panels in Fig. 3 present the MT phase tensor elements (Φ _{ x x } and Φ _{ y y }), the middle two panels the quasielectric phase tensor elements (Υ_{ x x } and Υ_{ y y }), and the lower two panels the electric phase tensor elements (Θ _{ x x } and Θ _{ y y }). The red and blackcolored curves indicate the results for the cases with and without fault, respectively. The leftmost vertical line denotes the location of the fault and the rightmost vertical line indicates the border between the sedimentary basin and the surrounding mountains.
From Fig. 3, we see that if no fault is present, the profiles of the phase tensor elements are symmetric around the center of the sedimentary basin, as one would expect. The introduction of the fault results in an asymmetry in the phase tensor elements along the profile. Second, it appears that the location of the fault is most pronounced in the profiles of the yyelement of the MT and the quasielectric phase tensor, corresponding to the xdirected electric field or Hpolarization (see Eq. 18). Similarly, the presence of the fault is most pronounced in the profile of the xxelement of the electric tensor, which also corresponds to the xdirected electric field or Hpolarization (see Eq. 21). The presence of the fault leads to a downward deviation of the xdirected current, which explains why the fault is most pronounced in the Hpolarization. As a result, the effect of the fault is seen at a larger offsets from the fault in Φ _{ y y }, Υ_{ y y }, and Θ _{ x x }. And finally, we observe from Fig. 3 that the behavior of the MT and the quasielectric phase tensor is similar (compare Fig. 3 a, b and c, d), which is expected since both involve horizontal magnetic fields, the MTphase tensor—at each field site and the quasielectric phase tensor—only at the base site, and these fields vary little from site to site for the considered period and considered model.
In Fig. 4, the MT, quasielectric, and electric phase tensor ellipses are shown for the model including the fault and for the same period as the profile shown in Fig. 3, i.e., for T=30 s. We present the phase tensor ellipses along three profiles, namely at the upper and lower border of the sedimentary basin as well as along the profile indicated in Fig. 1. The aim of plotting the phase tensor ellipses is to visualize all four elements of the phase tensor in one plot. Note that if the phase tensor ellipses are circular shaped, the conductivity structure is 1D. Otherwise, the conductivity structure is 2D or 3D (Bibby et al. 2005).
The MT and quasielectric phase tensor ellipses are filled with a color representing their normalized skew angle ψ ^{Υ,Φ}, with ψ ^{Υ} given in Eq. 19 and ψ ^{Φ} is defined in a similar way by replacing ϕ ^{Q} in Eq. 19 with ϕ ^{Z}. The same color is used for the range −6°<ψ ^{Φ,Υ}<6°, indicating the locations where a 2D interpretation is justified. We omitted to fill the electric phase tensor ellipses with a color indicating their normalized skew angle ψ ^{Θ} for reasons discussed in “Multidimensional analysis of the structure of the (quasi) electric phase tensors” section. The gray color of the electric phase tensor ellipses is used for visualization purposes only. As expected, the MT phase tensor ellipses are circular shaped away from the sedimentary basin, thus indicating a 1D conductivity structure. At the upper and lower margin of the sedimentary basin, the ellipses are elongated, indicating either 2D or 3D effects. The value of ψ ^{Φ} is an indicator whether a 2D or 3D conductivity model has to be considered. Around the corner points of the sedimentary basin, the normalized skew angle is larger/smaller than ±6° indicating 3D effects.
The quasielectric phase tensor ellipses show a similar behavior to the phase tensor ellipses. In contrast to the MT and quasielectric phase tensors ellipses, the electric phase tensor ellipses are rapidly vanishing away from the sedimentary basin, which is indicative for a 1D conductivity structure coinciding with the 1D structure beneath the base site.
Calculating (quasi) electric phase tensors from a field dataset
In this section, we investigate how reliably we can calculate the new responses from a field dataset. For this aim, we processed part of our MT data collected during March 2012 on Aluto volcano, situated in the main Ethiopian rift valley (Fig. 5). The ultimate goal of this MT survey was to obtain insight on the geothermal system below the volcano (Samrock et al. 2015).
We estimated the intersite (quasi) electric tensors between an exemplary (field) site, M23, and the remote reference (base) site, RR (shown as blue rhombs in Fig. 5), using the EMTF code (Eisel and Egbert 2001). Site M23 was selected based on its high signaltonoise ratio. Note that due to the strong topography and complicated geology of the fieldwork area, RR is located in non 1D conductivity environment. The estimated (quasi) electric tensor elements are shown in Fig. 6. For comparison, we show as well the elements of the impedance tensor, estimated using a remote reference processing technique (Gamble et al. 1979). One can see that all tensor elements are smooth functions of period. Furthermore, it is seen that the uncertainties of the quasielectric and electric tensor elements are small and comparable to the uncertainties of the impedance tensor elements. From these tensors, we calculated the corresponding phase tensors which are shown in Fig. 7. The uncertainties of the elements of phase tensors were calculated using the delta method (Patro et al. 2013; Booker 2014), which is a standard method for propagating variables’ uncertainties (or errors) to the uncertainties of functions based on them (Ver Hoef 2012). A summary of the mathematics behind the delta method is given in Appendix 1, and in Appendix 2, explicit formulas for the calculation of the uncertainties for the elements of the phase tensors are given. As one would expect—due to the smoothness of the generating tensors—the MT phase tensor, as well as the (quasi) electric phase tensors appeared to be smooth functions of period. Surprisingly enough, the (quasi) electric phase tensors seem to be smoother functions of period than the MT phase tensor, which becomes especially clear at long periods where the MT phase tensor elements show some scatter. In contrast to our model study, for this field dataset, the MT and quasielectric tensors are quite different, most probably due to substantially different conductivity profiles below the field and base site, as 3D inversion revealed (Samrock et al. 2015). Remarkably, the smoothest behavior and the smallest uncertainties are observed in the electric phase tensor.
Conclusions
We introduced two new response functions which can be exploited for the interpretation of MT data. First, we present the electric phase tensor, which is based on the intersite electric tensor. The electric phase tensor requires the simultaneous measurement of the horizontal electric field components at the base and a field site and is only distorted by galvanic effects, if present, at the base site. Second, we present the intersite MT phase tensor, which we called the quasielectric phase tensor. The quasielectric phase tensor requires the simultaneous recording of the horizontal magnetic field components at the base site and the horizontal components of the electric field at a field site. The quasielectric phase tensor is not distorted by galvanic effects. The base site has to be chosen carefully, preferably in a lownoise environment, and where the conductivity section is 1D, to ensure that the (quasi) electric phase tensor is not contaminated by 2D or 3D effects at the base site.
With a synthetic dataset, we showed that the sensitivity of the (quasi) electric phase tensors is comparable to the sensitivity of the MT phase tensor.
We showed for a real dataset that it is possible to estimate stable (quasi) electric tensors using existing processing software. For our real dataset, the calculated (quasi) electric phase tensors appeared to be smoother functions of period than the MT phase tensor. We elaborated formulas to propagate uncertainties of the (quasi) electric tensors to their respective phase tensors. Further, we demonstrated that for our dataset, the uncertainties of the MT phase tensor and the (quasi) electric phase tensors are comparable. Moreover, we observed the smallest uncertainties and the smoothest behavior for the electric phase tensor.
Summing up, we believe that the newly introduced intersite phase tensors could be a useful complement to the standard MT responses. The next natural step is to incorporate the (quasi) electric phase tensors into a 3D inversion scheme. Incorporation of (quasi) electric phase tensors seems rather straightforward, but employing the electric tensor during inversion requires the simultaneous determination of the conductivity distribution and four additional parameters, the realvalued elements of the distortion matrix Λ _{ b } (see Eq. 13) at a base site. Note that recently, Avdeeva et al. (2015) addressed in a similar way the impedance tensor Z inversion by recovering simultaneously the 3D conductivity distribution and the distortion matrix Λ _{ f } at all sites.
Appendix 1
The phase tensor is a nonlinear function of the eight elements of the corresponding tensor, namely the real and imaginary parts of tensor elements. The tensor elements are statistical variables with variances and covariances. We use the delta method (Casella and Berger 2002; Ver Hoef 2012) to propagate the uncertainty from the estimated tensors to their phase tensors. Here, we introduce the delta method and in Appendix 2, explicit formulas for the uncertainties of the electric, quasielectric, and MTphase tensor are given.
The delta method
Consider the Taylor series of a multivariate differentiable function g(m) around μ,
with m=[m _{1},…,m _{ K }]^{T} being a set of random variables and μ=[μ _{1},…,μ _{ K }]^{T} being the corresponding means. The index k runs from 1 to K, with K being the number of elements in vector m, and m _{ k } pointing to the kth element of m. The variance of g(m) is defined as
where E indicates the expected value operator. By substitution of Eq. 23 into Eq. 24 and dropping the remainder, an expression for the variance of g(m) is found as a function of the variances and covariances of m,
where the last equality comes from expanding the square, \(g'_{k}=\frac {\partial g(\mathbf {m})}{\partial m_{k}}\), Var[m _{ k }] is defined as
and Cov[m _{ k },m _{ l }] as
Equation 25 is valid if the covariance matrix is symmetric. However, the covariance matrix of the electric tensor is not symmetric (see Appendix 2) and hence we write Eq. 25 as
Appendix 2
Uncertainties of phase tensors
In this section, we first derive an explicit formula for the uncertainty of the MT phase tensor elements Φ_{ x x },Φ _{ x y },Φ _{ y x }, and Φ_{ y y }, using Eq. 28. The MT phase tensor elements correspond to the function g in Eq. 28 and the vector m in Eq. 28 contains the real and imaginary parts of the impedance tensor Z.
For our derivation, it is convenient to write the phase tensor Φ as
with Φ given by,
Next, we write the vector m as
The introduction of m allows us to write the partial derivatives of the phase tensor as \(\frac {\partial \Phi _{\textit {ij}}}{\partial m_{k}}\) with i,j=x,y. These partial derivatives of the elements of the phase tensor are listed in Table 1.
The impedance tensor elements are complexvalued random vectors. If we assume that the statistical properties of the impedance tensor elements are only described by their covariance matrix, we can write the covariance matrix of m in terms of the covariance matrix of Z (Picinbono 1996) as follows,
Note that the covariance matrix of m is asymmetric and Cov[Z] is the complexvalued 4 by 4 covariance matrix of the electric tensor Z. Combining Eqs. 28 and 32, an expression for the variance of the electric phase tensor elements is obtained,
with \(\frac {\partial \Phi _{\textit {ij}}}{\partial m_{k}}\) given in Table 1, Cov[m _{ k },m _{ l }] given in Eq. 32, and Var[m _{ k }] corresponding to the diagonal elements of Cov[m _{ k },m _{ l }].
In a similar way, we write the quasielectric phase tensor Υ as
where Q is the quasielectric tensor. The uncertainties of Υ are calculated by constructing a vector m containing the elements of R and S, similar to the vector m in Eq. 31 and substitution of Φ = Υ and m into Eq. 33.
For the electric phase tensor Θ, we have
where T indicates the electric tensor. The uncertainties for Θ can be calculated by constructing a vector m containing the elements of U and V and substituting Φ = Θ and m into Eq. 33.
Abbreviations
 MT:

magnetotelluric
 TS:

telluric sounding
 TMT:

telluricmagnetotelluric
References
Avdeeva, A, Moorkamp M, Avdeev D, Jegen M, Miensopust M (2015) Threedimensional inversion of magnetotelluric impedance tensor data and full distortion matrix. Geophys J Int 202: 464–481.
Bahr, K (1988) Interpretation of the magnetotelluric impedance tensor—regional induction and local telluric distortion. J Geophys 62(2): 119–127.
Berdichevsky, MN (1965) Electrical prospecting with the telluric current method. Quart. Colorado School of Mines 60(1): 1–216. English translation of original 1960 Russian book.
Berdichevsky, MN, Dmitriev VI (2008) Models and methods of magnetotellurics. Springer, Berlin Heidelberg.
Bibby, H, Caldwell T, Brown C (2005) Determinable and nondeterminable parameters of galvanic distortion in magnetotellurics. Geophys J Int 163(3): 915–930. doi:10.111/j.1365246X.2005.02779.
Booker, JR (2014) The magnetotelluric phase tensor: a critical review. Surv Geophys 35(1, SI): 7–40. doi:10.1007/s107120139234.
Cagniard, L (1953) Basic theory of the magnetotelluric method of geophysical prospecting. Geophysics 18: 605–635.
Casella, G, Berger RL (2002) Statistical inference. Duxbury, Pacific Grove, CA, USA.
Caldwell, T, Bibby H, Brown C (2004) The magnetotelluric phase tensor. Geophys J Int 158(2): 457–469. doi:10.1111/j.1365246X.2004.02281.
Chave, AD, Smith JT (1994) On electric and magnetic galvanic distortion tensor decompositions. J Geophys Res 99(B3): 4669–doi:10.1029/93JB0336.
Chave, AD, Jones AG (2012) The magnetotelluric method—theory and practice. Cambridge University Press, Cambridge, UK.
Eisel, M, Egbert G (2001) On the stability of magnetotelluric transfer function estimates and the reliability of their variances. Geophys J Int 144(1): 65–82.
Groom, RW, Bailey RC (1989) Decomposition of magnetotelluric impedance tensors in the presence of local 3dimensional galvanic distortion. J Geophys Res Solid Earth Planets 94(B2): 1913–1925. doi:10.1029/JB094iB02p0191.
Groom, R, Bahr K (1992) Corrections for nearsurface effects—decomposition of the magnetotelluric impedance tensor and scaling corrections for regional resitivities—a tutorial. Surv Geophys 13: 341–379. doi:10.1007/BF0190348.
Gamble, T, Clarke J, Goubau W (1979) Magnetotellurics with a remote magnetic reference. Geophysics 44(1): 53–68. doi:10.1190/1.144092.
Habibian Dehkordi, B, Oskooi B (2012) A resolution comparison of horizontal and vertical magnetic transfer functions. Earth Space Phys 40(3): 47–53.
Hermance, J, Thayer R (1975) Telluricmagnetotelluric method. Geophysics 40(4): 664–668. doi:10.1190/1.144055.
Iliceto, V, Santaroto G (1986) On the possibility of the telluric method—some results on faulted structures. Geophys Prospect 34(7): 1082–1098. doi:10.1111/j.13652478.1986.tb00514.
Jiracek, G (1990) Nearsurface and topographic distortions in electromagnetic induction. Survey in Geophysics 11(23): 163–203. doi:10.1007/BF0190165.
Leibecker, J, Gatzemeier A, Honig M, Kuras O, Soyer W (2002) Evidence of electrical anisotropic structures in the lower crust and the upper mantle beneath the Rhenish Shield. Earth Planetary Sci Lett 202(2): 289–302. doi:10.1016/S0012821X(02)00783.
Patro, PK, Uyeshima M, Siripunvaraporn W (2013) Threedimensional inversion of magnetotelluric phase tensor data. Geophys J Int 192(1): 58–66. doi:10.1093/gji/ggs01.
Püthe, C, Manoj C, Kuvshinov A (2014) Reproducing electric field observations during magnetic storms by means of rigorous 3D modelling and distortion matrix coestimation. Earth Planets Space 66: 162–171.
Picinbono, B (1996) Secondorder complex random vectors and normal distributions. IEEE Trans Signal Process 44(10): 2637–2640. doi:10.1109/78.53905.
Samrock, F, Kuvshinov A, Bakker J, Jackson A, Fisseha S (2015) Threedimensional magnetotelluric studies of the AlutoLangano geothermal field, Ethiopia. Geophys J Int 202(3): 1923–1948.
Schlumberger, M (1939) The application of telluric currents to surface prospecting. AGU Trans 3: 271–277.
Simpson, F, Bahr K (2005) Practical magnetotellurics. Cambridge University Press, Cambridge, UK.
Tikhonov, AN (1950) On determining electrical characteristics of the deep layers of the Earth’s crust. Doklady Akademii Nauk.
Varentsov, I (2005) Method of horizontal magnetovariational sounding: techniques and application in the EmteszPomerania project In: 21. Kolloquium Elektromagnetische Tiefenforschung.
Ver Hoef, JM (2012) Who invented the delta method?Am Stat 66(2): 124–127. doi:10.1080/00031305.2012.68749.
Vozoff, K (1972) Magnetotelluric method in exploration of sedimentary basins. Geophysics 37(1): 98. doi:10.1190/1.144025.
Yungul, S (1966) Telluric sounding—a magnetotelluric method without magnetic measurements. Geophysics 31(1): 185. doi:10.1190/1.143973.
Acknowledgements
We thank Stijn Vantieghem and Alexander Grayver for insightful discussions. Furthermore, we thank two anonymous reviewers for their useful comments on the first version of the manuscript. Our research was supported by ETH grant no. ETH30103 and the ETH scholarship for doctoral students.
Author information
Authors and Affiliations
Corresponding author
Additional information
Competing interests
The authors declare that they have no competing interests.
Authors’ contributions
JB and AK drafted the manuscript. JB analyzed the modeled and experimental responses. AG performed the modeling. FS estimated the real data responses. AK and OP initiated the study. All authors read and approved the final manuscript.
Rights and permissions
Open Access This article is distributed under the terms of the Creative Commons Attribution 4.0 International License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made.
About this article
Cite this article
Bakker, J., Kuvshinov, A., Samrock, F. et al. Introducing intersite phase tensors to suppress galvanic distortion in the telluric method. Earth Planet Sp 67, 160 (2015). https://doi.org/10.1186/s4062301503277
Received:
Accepted:
Published:
DOI: https://doi.org/10.1186/s4062301503277