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Invariant TE and TM magnetotelluric impedances: application to the BC87 dataset
Earth, Planets and Space volume 70, Article number: 133 (2018)
Abstract
Invariants under rotation of the magnetotelluric impedance tensor relax the directional requirements when fitting data using twodimensional (2D) models. This happens, for instance, when using the familiar impedance derived from the determinant of the tensor. In this work, we use two particular invariants that reduce in 2D to the traditional transverse electric (TE) and transverse magnetic (TM) impedances. They are obtained as the missing first link of an infinite chain of invariants that are computed iteratively without any reference to a strike direction. We challenge the current view that the TE and TM impedances are not invariant. We argue in favor of the invariance. We apply our approach to the wellknown and difficult BC87 dataset. These data present (1) electrogalvanic distortions, (2) static shifts and (3) inconsistent strikes. To remove the electrogalvanic distortions, we use recent developments that combine the phase tensor with the quadratic equation. To handle statics, we use a mimic of the electromagnetic array profiling (EMAP) method; the property of the TE mode of acting as a natural filter for static effects, as reported recently in the literature. Finally, the multiple strikes are handled by the invariant character of the TE and TM impedances. The processed TE responses are interpreted as onedimensional models to construct a 2D resistivity image of the subsurface, which is accompanied by the complementary image of the multiple strikes. Our model correlates very well with an independent EMAP survey over the Nelson Batholith and with seismic reflection and refraction lines.
Introduction
The magnetotelluric (MT) method of geophysical exploration as originally proposed assumed scalar data in the form of impedances defined as ratios of orthogonal electric and magnetic fields (Tikhonov 1950; Rikitake 1950; Cagniard 1953). The assumptions of a plane wave and of an electrical resistivity that varies only with depth imply that the fields can be measured in any direction as long as they are orthogonal. The impedance is said to be invariant under rotation of coordinates. On the other hand, when the resistivity distribution varies laterally this azimuthally symmetric model breaks down. The data are no longer a scalar but a 2 × 2 tensor whose elements depend on the coordinate system. However, it is still possible to compute scalars that are invariant under rotation and that may benefit the interpretation process. The effective impedance of Berdichevsky and Dmitriev (1976) obtained from the determinant of the tensor is the archetypical that exemplifies the incentives of using invariants in the interpretation of twodimensional (2D) data. These assets have been illustrated by Pedersen and Engels (2005), who remarks as the most important asset that the sounding curves are the same regardless of the assumed azimuth. In fact, the sounding curves are the same regardless of the variations of azimuths from site to site and from frequency to frequency.
This work was motivated by the possibility of extending the assets of invariants to the 2D classical transverse electric (TE) and transverse magnetic (TM) induction modes. The former is associated with the current flow along strike and the latter to the flow across strike. The traditional view of the TE and TM impedances is that they depend on the strike direction, since one needs to evaluate the impedances at a given predetermined angle, either using traditional formulae as that of Swift (1967) or by fitting a distortion model to the data as in the approach of Groom and Bailey (1989). In both cases, the calculated impedances seem to depend on the chosen strike direction. Because of this dependence on direction the current view is that the TE and TM impedances are not invariant under rotation. However, recent developments seem to indicate that this dependence is only apparent and that it originates in the way strike and impedances are traditionally computed, either finding the strike first and then rotating accordingly, or doing it simultaneously as when using a distortion model. The fact is that strike and impedances can be decoupled from each other. Muñíz et al. (2017) combine the phase tensor of Caldwell et al. (2004) and the quadratic equation of GómezTreviño et al. (2014a) to obtain, independently from each other, the strike direction and the TE and TM impedances. The question is (a) how should this decoupling of the two quantities be understood and (b) how to use it in practice to improve 2D inversions of data.
The wellknown BC87 dataset has several features that make it adequate for the present problem because it presents inconsistent strikes from site to site and from frequency to frequency. The dataset was acquired across the Nelson Batholith in British Colombia in 1987 using thethen stateoftheart commercial MT equipment, was presented by Jones et al. (1988) and further processed and interpreted by Jones et al. (1993), among others. The product of a workshop, the pertinent papers were published in a special issue of Journal of Geomagnetism and Geoelectricity with an introductory paper by Jones (1993). The dataset is available at the MTNet site. It is recommended for testing ideas and advances in tools for processing and inverting MT soundings. The data are distorted by (1) electrogalvanic effects, (2) static shifts and (3) inconsistent strike directions from site to site and from frequency to frequency. In this work we deal with the distortions and the static shifts using recent developments describe in GómezTreviño et al. (2014a, b) and Muñíz et al. (2017). For the third problem, that of inconsistent strikes, we first provide a general proof unrelated to any angular reference to show that the TE and TM impedances must be considered invariants. We then proceed to interpret the data.
Theory
The basic unit of any MT survey is a secondorder complex impedance tensor \(\varvec{Z}\), such that \(\varvec{E} = \varvec{ZH}\), where \(\varvec{E }\) and \(\varvec{H}\) stand for the horizontal electric and magnetic fields, respectively. Explicitly
Following Romo et al. (2005) we define two complex resistivities as
and
Here ω stands angular frequency, μ_{0} for the magnetic permeability of free space, Z ^{2}_{s} is the trace of \(\varvec{Z}^{\text{T}} \varvec{Z}\) and Y ^{−2}_{s} is the reciprocal of the trace of \(\varvec{Y}^{\text{T}} \varvec{Y}\), where \(\varvec{Y} = \varvec{Z}^{  1}\) is the admittance tensor. We call \(\varrho_{\text{s}}\) and ϱ_{p} the series and parallel resistivities, respectively. These resistivities are complex but their magnitudes are the same as those of the classical formulas. However, the phases of the complex resistivities are double those of the corresponding impedances because of the squared complex impedance. Both \(\varrho_{s}\) and ϱ_{p} are invariant under rotation of coordinates because this is a property of the trace of \(\varvec{Z}^{\text{T}} \varvec{Z}\) and \(\varvec{Y}^{\text{T}} \varvec{Y}\).
Following GómezTreviño et al. (2013) we define a sequence of invariants as
and
The sequence starts with \(i = 1\) so that \(\varrho_{{{\text{s}}1}} = \varrho_{\text{s}}\) and ϱ_{p1} = ϱ_{s} are the original resistivities. As iterations proceed the new resistivities are averages of the ones computed at the previous cycle. The elementary units from which all averages come from are of course \(\varrho_{\text{s}}\) and \(\varrho_{\text{p}}\). We now ask whether there are invariants more elementary than ϱ_{s} and ϱ_{p}. In other words: what is iteration zero? Mathematically, this can be stated as finding \(\gamma \;{\text{and}}\;\lambda\) such that
and
At this point it is important to realize that \(\gamma \;{\text{and}}\;\lambda\) are not part of the chain of invariants defined by Eqs. 4 and 5. We are taking a step backward. It is a working hypothesis that \(\gamma \;{\text{and}}\;\lambda\) do actually exist and that they might be meaningful, but there is no warrantee.
Solving for γ there results
We call the solutions ϱ_{±} and are given as
In Eqs. 6 and 7, the variables \(\gamma \;{\text{and}}\;\lambda\) can’t be distinguished from each other so the solutions for γ are the same as those for \(\lambda\). Equation 9 attracts and resolves the duality with the ± signs. On the other hand, multiplying \(\varrho_{ + } \;{\text{by}}\;\varrho_{  }\) it follows that \(\varrho_{ + } \varrho_{  } = \varrho_{\text{s}} \varrho_{\text{p}}\). Also, combining Eqs. 4 and 5 it follows that \(\varrho_{{{\text{s}}i}} \varrho_{{{\text{p}}i}} = \varrho_{{{\text{s}}\left( {i + 1} \right)}} \varrho_{{{\text{p}}\left( {i + 1} \right)}}\). The product ϱ_{+}ϱ_{−} is then equal to the product \(\varrho_{{{\text{s}}i}} \varrho_{{{\text{p}}i}}\) for any iteration. In fact, the sequence converges to \(\sqrt {\varrho_{\text{s}} \varrho_{\text{p}} }\), the geometric mean of ϱ_{s} and \(\varrho_{\text{p}}\), which in turn is equal to \(\varrho_{\text{d}}\), the determinant resistivity (GómezTreviño et al. 2013). Figure 1 illustrates the sequence and its convergence after a few iterations for site 31 of Varentsov (1998) synthetic COPROD2S1 dataset. To denote the amplitude of the complex resistivities we use ρ = ϱ with the corresponding subscripts. For the phases of ϱ_{±} we use \(\phi_{ \pm }\).
The analysis above demonstrates that \(\varrho_{ \pm }\) are invariant under rotation and that they are the first members of an infinite family of pairs of invariants whose geometric average is the resistivity derived from the determinant. So far there has been no restriction as to the dimensionality of the data. The derivation of the quadratic Eq. 8 is completely general in the sense that it applies to any dimension. An earlier derivation of the equation in GómezTreviño et al. (2014a) relied on 2D analyses and extrapolation of its solution to three dimensions. In the present work we proceed from the general to the particular. In 2D the invariants ϱ_{s} and ϱ_{p} can be written as ϱ_{s} = (ϱ_{TE} + ϱ_{TM})/2 and \(\varrho_{\text{p}}^{  1} = \left( {\varrho_{\text{TE}}^{  1} + \varrho_{\text{TM}}^{  1} } \right) /2)\). Substituting these expressions into Eq. 9 we obtain ρ_{+} = ρ_{TE} and ρ_{−} = ρ_{TM} or ρ_{+} = ρ_{TM} and ρ_{−} = ρ_{TE}. It is unfortunate that this result is not unique, in the sense that the modes cannot be differentiated. However, this is how things should be. This ambiguity is consistent with the original assumption in Eqs. 6 and 7 about \(\gamma \;{\text{and}}\;\lambda\), which can also exchange places, and also with the traditional ambiguity of 90°. Beyond this uncertainty, the invariants \(\varrho_{ + } \;{\text{and}}\;\varrho_{  }\) are the same as \(\varrho_{\text{TE}} \;{\text{and}}\;\varrho_{\text{TM}}\). The outer curves in Fig. 1 illustrate this correspondence.
The elements of the impedance tensor are not invariant under rotation. This is illustrated in Fig. 2 using polar diagrams for the element Z_{xy} expressed as resistivity ρ_{xy} for the period of 1000 s of the sounding curve used in Fig. 1. We also plot the series and parallel resistivities as well as ρ_{+} and \(\rho_{  }\), all of which describe circles as the coordinates are rotated from 0 to 360°. The resistivity ρ_{xy} plots into the characteristic peanut shape for 2D data. We present polar diagrams for the two strikes of 0 (90) and 30 (60) degrees. Regardless of the strike, ρ_{+} and \(\rho_{  }\) always intersect ρ_{xy} when this attains the main resistivities ρ_{TE} and \(\rho_{\text{TM}}\). Thus, ρ_{+} and \(\rho_{  }\) predict the resistivities of the two orthogonal modes regardless of strike.
Applications: BC87 dataset
Fit to data and predicted TE impedances
Figure 3 shows the location of the MT sites that comprise the BC87 dataset. We selected 16 soundings to make a profile 110 km long between sites 902 and 022. Also shown is the location of an EMAP line over the Nelson Batholith and three nearby sites. They will be compared below after the final analysis of the dataset. There are three issues posed by this dataset: (1) electrogalvanic distortions; (2) static shifts and (3) variable strikes. We don’t deal explicitly with the first here. It was reported in Muñíz et al. (2017) using a combination of the phase tensor and the quadratic equation. We take it from there and proceed to the issue of static shifts. For this we follow GómezTreviño et al. (2014b) by inverting the apparent resistivity of the TM mode and the phases of both modes, and considering the TE apparent resistivity as output in the inversion process. We focus here on the third issue of variable strikes. For comparison, we also consider fixed strikes, and to be unbiased about the classical ambiguity of 90° in the strike determination we analyze all possibilities.
Figures 4 and 5 present the results for the case of fixed strikes. The choices of strikes determined by Jones et al.(1993) are − 30° (N30°W) or 60° (N60°E). They chose N30°W for their interpretation because that is the regional geological strike of the Canadian Cordillera. On the other hand Eisel and Bahr (1993) determine a strike of 45° (N45°E). In our case we decided to keep the ambiguity of East or West and consider both options until the end of the analysis. The option of the East is backed by the existence of deep transverse basement structural control of mineral systems at a more local level in the area as reported by McMechan (2012). The impedances were computed using the STRIKE algorithm based on the work of McNeice and Jones (2001). This algorithm also removes any electrogalvanic distortions that may be present in the data so that they are ready for the second step, that of correcting for the static shifts. Figure 4 summarizes the case of strike N30°W. The upper part shows the data and the lower part the responses of the resistivity model obtained by inverting the data. For now let us center our attention around the fit to the data and on the inversion process. The input to the inverse routine is the amplitude of the TM apparent resistivity and the phases of both modes. Any static shifts of the amplitude of the TM apparent resistivity can be accommodated by electric charges placed on the walls of small cells around the electric dipoles. This is not the case for the TE mode, so we leave the apparent resistivity out of the inversion process. Details of this approach are given in GómezTreviño et al. (2014b). The result is a very good fit to the inverted data but not so good for those left out. In fact, the pseudosections for the TE apparent resistivity don’t look alike at all for the strike of N30°W in Fig. 4, although they resemble each other better for the strike of N60°E in Fig. 5. Another difference worth noting is that the characteristic anomalous phases larger than 90° of this dataset fall in the TM mode for the strike N30°W and in the TE mode for the case of N60°E. The former contradicts the results of Weidelt and Kaikkonen (1994) who showed that TM phase responses of 2D models lie in the range 0–90°, and the latter coincides with Parker (2010) who proves that 2D models exist whose TE mode phase responses are outside 0–90°. This reinforces the likelihood of a strike N60°E as suggested by the dominance of local transverse structures of McMechan (2012).
We now turn to the invariants \(\rho_{ \pm }\). The result of identifying ρ_{−} as TM (\(\rho_{  } \leftrightarrow {\text{TM}})\) is shown in Fig. 6 and that of ρ_{+} with TM (\(\rho_{ + } \leftrightarrow {\text{TM}})\) in Fig. 7. We proceeded likewise as for the case of fixed angles. Again, the result is a very good fit to the data involved in the inversion and not so good for those left out. The pseudosections for the TE apparent resistivity don’t look alike at all for \(\rho_{  } \leftrightarrow {\text{TM}}\) in Fig. 6, but they resemble each other very much for \(\rho_{ + } \leftrightarrow {\text{TM}}\) as shown in Fig. 7. On the other hand, by inspection one can relate N30°W with \(\rho_{  } \leftrightarrow {\text{TM}}\) and N60°E with \(\rho_{ + } \leftrightarrow {\text{TM}}\). This means that ρ_{−} refers to free strikes around N30°W and \(\rho_{ + }\) to free strikes around N60°E. In relation to whether the strike should be toward the NW or NE we can only add at this point that the best prediction of the TE apparent resistivity data is that of \(\rho_{ + } \leftrightarrow {\text{TM}}\) which we have associated with N60°E. This is a second clue in favor of the transverse strike to the Canadian Cordillera. Before proceeding with this analysis we must explain the origin of all the computed pseudosections. That is, the models behind them and how they were obtained.
Roughest models
The computed pseudosections in the four previous figures were obtained from the corresponding four models shown in Fig. 8. The input data were the measured apparent resistivity of the TM mode and the phases of both modes. Rather than considering these models as the output in the inversion process we use them as stepping stones to obtain the TE apparent resistivity which is free from static effects (GómezTreviño et al. 2014b). We monitor the geometric average of each sounding and choose the model for which there is convergence for all sites. This is illustrated in Fig. 9 where the variable tau is the regularization parameter in the inverse routine of Rodi and Mackie (2001). Traditionally, a compromise is sought between roughness of the model and fitness to the data, in such a way that the final model is smooth following Occam’s philosophy (Constable et al. 1987). Instead, we seek the roughest model with the maximum possible of the larger wave numbers. The idea is to mimic Bostick’s (1984, 1986) EMAP method. The roughest models are difficult to interpret visually because they would correspond to the unprocessed EMAP data.
Static shifts
Proceeding with the analysis of the computed TE apparent resistivity pseudosections of Figs. 4, 5, 6 and 7, we need to explain why they do look or do not look alike those of the field data, depending on the case. It is difficult to infer what is behind the discrepancies by comparing the images because they present different shapes. To illustrate the differences we chose three sites from the worst and the best resemblances. The worst is ρ_{−} ↔ TM and the best is ρ_{+} ↔ TM. Figure 10 shows the comparison between the computed sounding curves and the field data. It can be observed that the TM data in both cases are well fitted by the corresponding responses of their roughest models and that the TE computed and field curves are parallel to each other. The degree of shift, measured by the ratio of the field curve to the computed response, defines the staticshift factor. The factors for all the sites are shown in Fig. 11 for both ρ_{−} ↔ TM and ρ_{+} ↔ TM. The average factor for the first case is of about two orders of magnitude and always greater than unity. The values of unity at the extremes of the profile were not fixed, that is how they come out in the calculations. On the other hand, the average factor for the second case is of less than an order of magnitude and presents values larger and smaller than unity. These factors for ρ_{+} ↔ TM seem more likely than the too large and consistently larger than unity of ρ_{−} ↔ TM. This is a third and extra point in favor of the NE strike.
It is possible with this dataset to make a classical hypothesis testing exercise. What we did was to take three soundings from each of the pseudosections and used them as predictors of how a staticfree sounding would look like over the Nelson Batholith. The predictions are then compared with actual EMAP observations. Figure 12 shows the predictions of the four options contrasted with an EMAP line reported by Jones et al. (1989) whose location is shown in Fig. 3 as lying over the Nelson Batholith. The line is 10 km long and runs with an azimuth N30°W, so that the measured electric fields have the same azimuth as those of the TE mode. It can be observed that the cases of strike N30°W and its associated ρ_{−} ↔ TM stand as the worst predictions. Next comes N60°E and the best match is its associated ρ_{+} ↔ TM. Then there is no doubt, what the hypothesis testing exercise is telling us is that the model behind the ρ_{+} ↔ TM option is the best choice. Notice that we are not using the EMAP line to correct the data as it is customary. We are using it as an external agent to help us decide which hypothesis makes the correct prediction. The result supports the hypothesis that the invariant TE and TM impedances associated with ρ_{+} ↔ TM should be the best choice. Before proceeding to compare the corresponding models we still have a final point to clarify. The electric fields of the EMAP line have the direction N30°W. That is, the electric dipoles are aligned along the EMAP line. If we assume a strike N60°E the TM mode corresponds also to electric dipoles in the direction N30°W. The same goes for the associated ρ_{+} ↔ TM; the electric fields are predominantly NW. Let us now turn to the models or predicted images of the subsurface. They can be contrasted directly with other geophysical methods and with the geology of the area.
Models
We need to convert the staticfree pseudosections into true sections, in order to compare them with other geophysical models and to make possible geological inferences. To do this we also follow Bostick (1984, 1986) who uses the 1D approximate formulae known as the Nibblet–Bostick transformation (Jones 1983). We use a stable version that estimates depth averages of electrical conductivity by combining data for any two periods (GómezTreviño 1996). Expressed in terms of resistivities the formula is
where
and
The average ρ_{HA} is the harmonic average over depth z of the underground vertical resistivity distribution ρ(z). The average is over a depth window defined by \(h_{2} \;{\text{and}}\;h_{1}\).The widths of the depth windows are h_{2} − h_{1}, where \(h_{2} \;{\text{and}}\;h_{1}\) are fractions of the skin depths \(\delta_{1} \;{\text{and}}\;\delta_{2}\), respectively. The apparent resistivity ρ_{a1} corresponds to the period T_{1} and \(\rho_{a2}\) to T_{2}, where it is assumed that \(T_{1 } < T_{2}\). The values of ρ_{HA} are plotted at the geometric mean \(h_{m} = \sqrt {h_{1} h_{2} }\).
The sections of resistivity versus depth are shown in Fig. 13 in the same order as those of Fig. 12. As expected, the images for N30°W and ρ_{−} ↔ TM on the left side provide somewhat similar pictures of the subsurface. The same can be said about the images for N60°E and ρ_{+} ↔ TM on the right side. However, contrasting left and right sides it is clear that they offer qualitatively different pictures of the subsurface. It is also clear that the choice of N30°W or N60°E is crucial for a correct interpretation. The same applies for the choice between \(\rho_{  } \leftrightarrow {\text{TM }}\) or \(\rho_{ + } \leftrightarrow {\text{TM}}\). We spent quite some time working with the pair (N30°W, ρ_{−} ↔ TM) trying to make sense of the models on the left side of Fig. 13. Then we found out about the existence of the deep transverse basement structural control of mineral systems in the area reported by McMechan (2012), and became fully aware of the results of Eisel and Bahr (1993) for the complementary angle of strike. This motivated the exercise of predicting the EMAP line with the pair (N60°E,\(\rho_{ + } \leftrightarrow {\text{TM}}\)). The corresponding resistivity image assuming \(\rho_{ + } \leftrightarrow {\text{TM}}\) is shown in Fig. 13d. Basically, this image reveals a large resistive body below the surface expression of the Nelson Batholith. Notice that the image for the fixed angle N60°E is a hesitant disclosure of the resistive body.
In addition to the concordance shown in Fig. 12 in relation with the EMAP line, the image for \(\rho_{ + } \leftrightarrow {\text{TM}}\) clearly delineates the Nelson Batholith which is the prominent geological feature of the profile. This is further confirmed in Fig. 14 by contrasting the resistivity image with the seismic refraction model of Clowes et al. (1995). In the same figure, we include a seismic reflection model from Zelt and White (1995). It can be observed that the resistivity image correlates very well with the two seismic models, and particularly in relation to the location of the Slocan Lake Fault (SLF in the figure).On the other hand, the highly conductive regions below the whole profile and particularly at shallow depths below the Purcell Anticlinorium, are most likely extensions of those detected at also shallow depths by Gupta and Jones (1995) in a more extensive survey of the anticlinorium. They associate the enhanced conductivity to the presence of mineralization (copper, etc.), rather than other geophysical causes. In any case, the depth of penetration is severely damped at the base of the resistivity image because of this enhanced conductivity. It can be observed that the assigned depths for the longest periods all cluster together above the largest penetration. Along the profile they define a kind of envelope or halo that embraces the Nelson Batholith, the Kootenay Arc and the Purcell Anticlinorium. Very little else can be said about this halo beyond its uppermost topography because of the severely damped depths of penetration. This also prevents the detection of an anisotropic layer below 30 km reported by both Jones et al. (1993) and Eisel and Bahr (1993). In any case, even with enough depth of penetration we wouldn’t be able to judge about the anisotropic nature of the layer because we are using invariants. Aside from this, our model resembles a lot more that of Eisel and Bahr (1993) who assume a N45°E strike, than that of Jones et al. (1993) who assume a N30°W strike.
The invariant character of the TE and TM impedances relaxes the rigidity of a single strike direction. However, using invariants does not save us from the classical problem of having to choose between two possible strikes. The question is transferred to decide between ρ_{+} and \(\rho_{  }\). In the present case all \(\rho_{  }\) curves have the same shape and also do all ρ_{+} curves (see Fig. 10 for a sample). The question is to decide which shape corresponds to which mode. One way is to use the STRIKE algorithm to couple the impedances with a strike direction as we did and then associate by shape the resulting TE and TM modes with the ρ_{+} and \(\rho_{  }\) resistivities. In this way, we were able to associate the strike N60°E with \(\rho_{ + } \leftrightarrow {\text{TM}}\). Our approach still relies on the STRIKE algorithm for this geographical connection with the geology.
We show in Fig. 15 the resistivity image together with estimates of the strike directions using the phase tensor as reported in Muñíz et al. (2017). Of the two complementary angles, we chose only the positive values in view of the mentioned choice of \(\rho_{ + } \leftrightarrow {\text{TM}}\) and its relation with N60°E. Geologically, the strikes correspond to the local transversal structures reported by McMechan (2012). The strikes are plotted using the same vertical scales as for the resistivities. Figure 15 summarizes the results of relaxing the directionality constraints in 2D inversions. On one side we have a resistivity model that complies with a strict requirement as an EMAP line much better than assuming a fixed strike, and on the other we have a detailed strike model of the subsurface. The largest strikes in red around the eastern edge of the Nelson Batholith correspond very well with the newly discovered transversal structures described by McMechan (2012). This may be a chance coincidence but we cannot but mention it because they are the features that stand out in both the strikes image below and the geological map of McMechan (2012).
A final remark about how to view Fig. 15 is worthwhile. The resistivity image comes directly from the TE response of a model with zero strike. However, this model comes from inverting data that may have different strikes. Thus, the resistivity image cannot be viewed as a normal cross section whose properties don’t change in the direction perpendicular to the profile, which corresponds to strike zero. It is still a cross section, but now we have to specify the related azimuths. The fit to the data was done assuming a model with azimuth zero, but because the impedances are invariant this model can accommodate perfectly well other azimuths. The model is then incompletely characterized by the resistivity distribution, and requires to be fully differentiated to specify the corresponding distribution of strikes.
Conclusion
The recognition that TE and TM impedances can be treated in theory and in practice as invariants opens a new possibility for treating MT profiles that present inconsistent strikes. The current approach is to fix the strike and modify the impedances accordingly. The new option keeps the invariant impedances untouched in spite of multiple strikes. With the present computing power, there is no reason for not working with both options in routine 2D interpretations. The present work completes earlier developments for removing 1) electrogalvanic distortions using the same quadratic equation as for the present problem, and 2) the static effects using a mimic of the EMAP method. The conclusion that the strikefree impedances are valuable assets for 2D interpretations is presented in three progressive steps using the BC87 dataset. First, they lead to more reasonable static factors than those of fixed strikes. Second, they predict much better an independent EMAP line over the Nelson Batholith. And third, their predicted image of the subsurface correlates very well with seismic refraction and reflection surveys, particularly in relation to the Slocan Lake Fault and the delineation of the Nelson Batholith. We conclude that this is because a model with strike zero can accommodate impedances with other strikes. The resulting resistivity image of the subsurface is no longer a normal cross section. It is still a cross section, but it requires the corresponding strikes to be specified because otherwise the resistivity image is strike ignorant. We hope that he gives a lift to the survival of 2D MT profiles which come so naturally in many matteroffact applications.
Abbreviations
 MT:

magnetotelluric
 TE:

transverse electric
 TM:

transverse magnetic
 EMAP:

electromagnetic array profiling
 2D:

twodimensional
 1D:

onedimensional
 SLF:

Slocan Lake Fault
 NB:

Nelson Batholith
 KA:

Kootenay Arc
 PA:

Purcell Anticlinorium
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Authors’ contributions
YM performed part of the inversions for the first half of the manuscript. MC run the STRIKE algorithm for the fixed angle strikes and the corresponding inversions and her work led to the comparison with the EMAP line. The earlier work of AC with other invariants led to the comparison with the seismic reflection and refraction surveys. EGT developed the theory, drafted the manuscript and coordinated the different steps. All authors read and approved the final manuscript.
Acknowledgements
We would like to thank Alan Jones for providing the BC87 dataset and the new version of the STRIKE algorithm. Thanks also to J.M. Romo, F.J. Esparza and C. Flores for fruitful discussions, and to the anonymous reviewers for helpful comments to shorten and improve the manuscript. Y.M., M.C. and A.CM acknowledge scholarships from CONACYT. Y. M. and A.CM. also acknowledge terminal scholarship from CeMIEGeo through CONACYT Project Number 207032. Thanks also to CeMIEGeo for the use of the Lamb Cluster for running inversions.
Competing interests
The authors declare that they have no competing interests.
Availability of data and materials
The BC87 dataset is available at the MTNet site (http://www.completemtsolutions.com/mtnet/main).
Funding
CICESE, CONACYT and CeMIEGeo (CONACYT Project Number 207032).
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GómezTreviño, E., Muñiz, Y., Cuellar, M. et al. Invariant TE and TM magnetotelluric impedances: application to the BC87 dataset. Earth Planets Space 70, 133 (2018). https://doi.org/10.1186/s406230180900y
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DOI: https://doi.org/10.1186/s406230180900y