Fig. 1. Tien Shan – Pamir mountain system (“Pamir”) as a northwest corner of Indo-Asian collision zone and Pamir-Tibet plateau. Note that the shortening in north-south direction in Pamir – Western Tien Shan region absorbs less that 50% of shortening length in the east. Depressions are the regions which are almost not subject to intracontinental shortening. The italisized names show the orogenic belts of Paleozoic and Mesozoic ages reactivated by the growth of plateau.
    Pamir is distinguished from the neighboring Tibet by having (1) the most active areas of seismicity (middle depth) in the world and the most active far seismic zone which is obviously not connected to oceanic subduction; (2) three even-aged active dense belts which are severely deformed by compression; (3) four separate intracontinental magmatic belts.

Fig. 2. The international MT team (Kyrgyzstan, Russia, Tajikistan, Germany). The Research Station RAS has provided the major part of field logistics including transportation. Tajik members of the team were local people from Murgab. MT equipment was provided by the Potsdam Geophysical Equipment Pool.

Fig. 3. МТ data were recorded in summer 2008 at 80 stations (12 combined broadband (BB)/long-period (LMT) stations and 68 broadband stations) in Pamir mountain ranges in Tajikistan with a distance of about 2 km between BB stations and 14 km between BB/LMT stations. These stations form the southern segment (156 km long) of the 430-km profile which goes from Osh in Kyrgyzstan through Sary-Tash, Kyrgyz-Tajik border, Karakul and Murgab to Zorkul Lake in the southern Tajikistan.

Fig. 4. Examples of apparent resistance and phase curves of the four broadband stations in Pamir. The curves were obtained after a three-day registration and processing in the field. The changing form of the curves points to significant changes in deep conductive structure. The distance between sites is about 50 km. For location of stations see Fig.3.

Fig. 5. On the left: Analysis of regional spread (Becken&Burkhard) of all stations in the interval of periods 1-1000s has determined the azimuth of geoelectric spread -17°.
    In the bottom: Maps of induction vectors (Wiese convention) for the periods 1, 32, 128 and 1024s point to the several “reverses” and the complex distribution of the near-surface conductive structure. For location of stations see Fig.3.

Fig. 6. Pseudo-cross-sections of apparent resistance and phases. TE and TM modes were determined according to the results of tensor decomposition presented in fig.5.