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Earth, Planets and Space volume 72 , Article number: 5 Cite this article. Metrics details. Southern Mongolia is part of the Central Asian Orogenic Belt, the origin and evolution of which is not fully known and is often debated. It is composed of several east�west trending lithostratigraphic domains that are attributed to an assemblage of accreted terranes or tectonic zones. This is in contrast to Central Mongolia, which is dominated by a cratonic block in the Hangai region.

Terranes are typically bounded by suture zones that are expected to be deep-reaching, but may be difficult to identify based on observable surface fault traces alone. Thus, attempts to match lithostratigraphic domains to surface faulting have revealed some disagreements in the positions of suspected terranes. Furthermore, the subsurface structure of this region remains relatively unknown. Therefore, high-resolution geophysical data are required to determine the locations of terrane boundaries.

Magnetotelluric data and telluric-only data were acquired across Southern Mongolia on a profile along a longitude of approximately The data were used to generate an electrical resistivity model of the crust and upper mantle, presented here, that can contribute to the understanding of the structure of this region, and of the evolution of the Central Asian Orogenic Belt.

The resistivity model shows a generally resistive upper crust 0�20 km with several anomalously conductive features that are believed to indicate suture zones and the boundaries of tectonic zones.

Moreover, their spatial distribution is coincident with known surface fault segments and active seismicity. The lower crust 30�45 km becomes generally less resistive, but contains an anomalously conductive feature below the Gobi�Altai zone. This potentially agrees with studies that have argued for an allochthonous lower crust below this region that has been relaminated and metamorphosed. Furthermore, there is a large contrast in the electrical properties between identified tectonic zones, due to their unique tectonic histories.

Although penetration to greater depths is limited, the magnetotelluric data indicate a thick lithosphere below Southern Mongolia, in contrast to the previously reported thin lithosphere below Central Mongolia.

The origin and evolution of the CAOB is not well known and remains controversial, however the geological structure is known to be a combination of microcontinents and mobile belts e. Central Mongolia is dominated by the Hangai block, which is part of the Hangai Dome intraplate plateau, and other continental fragments, including the Baydrag block, which are believed to be composed of Precambrian basement rocks Badarch et al.

In contrast, geological studies have revealed that Southern Mongolia is composed of an accretionary collage of many nine or more lithologically and structurally distinct domains Badarch et al. These east�west trending lithostratigraphic provinces consist of back-arcs, fore-arcs, island-arcs, and accretionary wedges that surround the central Hangai nucleus. The distinct lithostratigraphic domains are attributed to separately accreted terranes Badarch et al. The inferred geological history and composition of these regions is summarized in a following section.

The tectonic history of this region is complex, and includes several subduction events Yin ; Jiang et al. Map of survey area. Measurement locations are circles; black are magnetotelluric sites and white are telluric-only sites see text for details ; vertical bars indicate measurements from , horizontal bars from , otherwise from Sites shown in Fig. Blue dashed lines indicate the surface locations of fault zones black text; Styron ; Walker et al.

Local names of mountain ranges are indicated white text; from Bassa The grey star labelled BEq marks the location of the Bogd rupture, an intraplate earthquake of magnitude 8. Mongolia is situated between the Siberian craton and the North China and Tarim cratons dashed grey lines.

Southern Mongolia is assembled from accreted terranes amalgamated against the Hangai microcontinent Badarch et al. The survey location grey box , MT profile red line , Mongolian Altai and Gobi�Altai mountains, political boundary of Mongolia thin black line , and the capital city, Ulaanbaatar UB , are indicated.

Terranes are defined as fault-bounded fragments whose surface geology differs from that of adjacent areas e. However, attempts to match lithostratigraphic domains to surface faulting using geochronology, structural constraints, and aerial potential field measurements have revealed some disagreements in the positions of suspected terranes e. Geophysical potential field data gravity and magnetics are useful to distinguish lithostratigraphic domains because gravity and magnetic signals depend on the specific petrophysical properties of the rock components that is, density and magnetic susceptibility.

However, the main challenge with potential field data is to accurately interpret the depth of each feature. In fact, potential field data have shown close agreement with the four principal tectonic zones Guy et al. Unfortunately, this region lacks seismic data, which could provide new evidence for lithospheric structure.

Instead of identifying terranes by the distinguishable variations in crustal properties between them, due to their unique petrophysical properties and rock types, they can instead be identified by their boundaries, which are rheological weak zones between them.

As mentioned above, if the contrasting lithostratigraphic domains represent distinct terranes they should be partitioned and bounded by faults and suture zones that are suspected to be crustal or lithospheric-scale e. However, due to the extended intracontinental convergent deformation in this region, these faults and suture zones may be very narrow zones, or covered at the surface, and thus difficult to detect e. Hence geophysical methods that can accurately image deep crustal structures are required.

Magnetotelluric MT data image subsurface electrical resistivity using natural electromagnetic signals measured over a broad range of frequencies e. The resistivity of a rock is a unique geophysical signature, which can vary over several orders of magnitude, and is especially sensitive to the quantity and composition of crustal fluids and partial melt. Because faults and suture zones are regions of Batmagnai Chogsom Time fractured, weakened crust, due to past and present deformation, they often have circulating fluids that act to decrease their electrical resistivity e.

Hence the MT method is useful for investigating subsurface fault distributions, and therefore has the potential to identify tectonic zones by imaging their boundaries. Here, we present high-resolution MT measurements across Southern Mongolia. Electrical resistivity models of the lithosphere, in combination with previous geological and geophysical data, provide insights into both the shallow surface and deep structure of this region and help to shed light on the distribution of tectonic blocks and the development of the CAOB.

Apparent resistivity and impedance phase are determined over a range of frequencies, with high frequencies sensitive to shallow structure and low frequencies i. In , a profile of 20 MT sites was completed in Southern Mongolia, along a longitude of approximately Combining these with previously acquired data, a profile was created total range: latitude Both MT instruments and telluric-only data-loggers were deployed. Metronix MFSe magnetic induction coils were used to measure the two horizontal magnetic field components.

The vertical magnetic field was also measured at most MT sites, but is not used in this study. The electric dipole length was typically chosen to be 60 m. The total period range recorded was 0. MT site occupation times were typically less than 3 days. All measurement sites had an average spacing of 8. This survey design ensured fast and efficient field deployment. Typically, there were two MT sites and a few telluric-only sites recording simultaneously.

Some modelling codes are capable of accounting for the independent measurement locations of the electric fields and the magnetic fields e. This is an improvement over simply using nearby magnetic fields for the telluric-only sites because this approach can introduce some error, specifically near strong resistivity contrasts e.

Comeau The MT data were high quality and had a very low noise level due to the remote measurement location. However, the data suffers from large static shifts of up to three orders of magnitude , which are constant, frequency-independent offsets of the apparent resistivity caused by near-surface resistivity structure that occurs at a small spatial length scale e.

To better understand the data and the range of static shifts, the sum of the squared elements of the impedance tensor ssq-average; Rung-Arunwan et al. In addition, their geometric mean was calculated, which represents a regional one-dimensional 1-D average and is assumed to balance a random distribution of static shifts.

This analysis demonstrated the similarities and differences of the data, in the form of apparent resistivity and phase curves. In addition, it can be used to estimate the average penetration depth of electromagnetic signals by computing the real part of the C-response for each period Weidelt Data and penetration depth.

Dimensionality analysis of the data determines if the assumption of a two-dimensional 2-D resistivity model is valid.

If it is not, then a full three-dimensional 3-D analysis may be required to properly model the data. The geo-electric strike direction was estimated for all sites and all periods Becken and Burkhardt Phase tensor and geo-electric strike analysis. The phase tensors indicate 1-D geo-electric structure when circular in shape and 2-D or 3-D structure when elliptical. Dashed grey lines indicate separate tectonic zones. Phase tensor analysis was used to verify this result.

The phase tensors Fig. They will appear as circles for a 1-D subsurface and as ellipses for 2-D or 3-D subsurface conductivity distributions.

Hence, the phase tensor analysis confirmed that a 2-D model is valid, although certain regions displayed distortion or local 3-D resistivity structures. To account for this, data with high phase tensor skew values e. In order to properly account for the effects of galvanic distortion and departures from the 2-D condition, the distortion parameterization of Becken and Burkhardt was employed. This parameterization yields the distortion angles introduced by Smith if the 2-D condition is fulfilled.

In this case, distortion can be partly removed by constructing an inverse distortion matrix. Otherwise, the Batmagnai Gongor Zhu telluric vectors exhibit an elliptical polarization state, an admission of departures from true 2-D conditions, or of a non-optimal principal axis corresponding to the chosen geo-electric strike direction.

However, all data have errors and any 2-D condition can only be confirmed to within the errors of the ellipticities. Non-vanishing ellipticities can be back-propagated into impedance errors, as in Becken et al. Thus these new impedance errors make departures from the 2-D condition indistinguishable, within the errors. This procedure of adjusting the errors corresponds to the down-weighting of 3-D effects i. A 2-D electrical resistivity model Fig.

This algorithm uses a dual-grid approach by computing the forward solution with an adaptive finite-element method that automatically generates and refines unstructured triangular elements. Furthermore, it is capable of properly handling inter-site transfer functions computed for the telluric-only sites. Resistivity model. A combination of full MT sites black triangles and telluric-only sites white triangles was used.

The base site used for inter-site transfer functions with a local site is indicated by the number above each site. Distances are along the profile approximately from north to south along longitude The side panel shows a part of the modelling mesh used. Topography was included in the model and is shown in the upper panel with a vertical exaggeration VE of


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