The magnetotelluric method is a frequency domain electromagnetic (EM) tool which utilizes natural variations in the Earth’s magnetic and electrical field as a source. Variations in the Earth’s natural fields supply information, providing the ability to study the electric substructure of the Earth in great depths. The large frequency range of the EM signals eradicates the problematic presence of conductive overburden or sampling frequencies, thereby allowing a deep penetration. Natural magnetotelluric (MT) signals arise from a variety of natural currents, including thunderstorms and solar winds. Total frequency range of the MT data can be from 40 kHz to less than 1^-4 Hz. Data is acquired in a passive mode using a combination of electric sensors and induction coil magnetometers, and can detect changes of resistivity in great depths (Simpson and Bahr, 2005).
Cagniard (1953) and Tikhonov (1950) developed a theory underlying the
magnetotelluric method independent of each other in the 1950’s. They both observed that the electric and magnetic fields associated with telluric currents that flow in the Earth as a result of variations in the Earth’s natural electromagnetic field, should relate to each other in a certain way depending on the electrical characteristics of the Earth. The ratio of the horizontal electric field to the orthogonal horizontal magnetic field gives the electromagnetic impedance. The major advantage of the MT method is that it simultaneously measures the electric and magnetic fields in two perpendicular directions. The electric sensors are used to determine the electric field, which is derived from measurements of the voltage difference between electrode pairs of E_x and E_y. Induction coils are used to measure the magnetic field components in 3 orthogonal directions. The ratio of the recorded electric and magnetic fields gives an estimate of the apparent resistivity of the Earth at any given depth.
The elements of the 2x2 impedance (Z) tensor are derived from complex ratios of the orthogonal components of the horizontal electric and magnetic fields in the frequency domain. As all the measurement stations are located over a line in our case, the data only permit the application of a two-dimensional interpretation process that requires the  identification of the TE and the TM modes corresponding to electric and magnetic fields parallel to the geologic strike, respectively. As the geological strikes are not known in advance, the components of electromagnetic fields are measured in geomagnetic (or arbitrary) directions and the impedance tensor is rotated to principal axes. The strike direction often changes with depth in the field, accordingly, the rotational angle varies at each frequency. For two-dimensional structures, there are many conditions and consequently many possible schemes to determine the rotational angle (Simpson and Bahr, 2005). Here, we minimized the diagonal elements of the impedance tensor. There are two possible strike directions for a certain frequency and the interpreter identifies the TE and the TM modes using geological and geophysical information.
Volcanic activities of Sabalan started in Eocene and resumed in Pliocence by the eruption of trachy-andesitic lava flow through the main caldera. Four major lithostratigraphic units were defined in the studied area in the following order: Dizu formation (Quaternary alluvium and terrace), Kasra formation (post-caldera, latepliostocene), Taos formation (syn-caldera, early Plistocene) and Volhazir formation (pre caldera, Pliocence). The Sabalan fault complex, structurally consists of linear faulting trending NE-SW, N-S and WNW-ESE and arcuate structures forming inner and outer fractures to the caldera (Sahabi, 1378). The MT data were obtained using three sets of MTU-5A equipment, two roving sites within Mt. Sabalan and one remote reference site. The raw time series data were processed using the Phoenix Geophysics, Ltd. SSMT 2000 software, and the resulting EDI files were edited, analyzed and modeled using the Geosystem’s WinGlink software. Overall, the obtained MT data were in good quality down to 10^-2 Hz. However, some MT obtained data were of poor quality despite being retested mainly because of bad weather conditions (i.e. snowy, windy) or becuase the site was situated along the steep and rocky flanks of Mt. Sabalan. Along the profile MM (on Figure 5) a distinct feature is an almost continuous conductive anomaly (