Active tectonics is one of the fastest growing disciplines among the earth sciences considering the recent developments of new geochronological tools and mapping that assist to obtain uplift rate, shear rate, erosion rate, fault slip rate and… in variable time scale (10,001,000,000 years) [1] [2] [3] .

Tectonic geomorphology is a relatively new field in active tectonic that provides a valuable tool for assessing the tectonic activity of structures with low to medium deformation rate, especially when there is a lack of Quaternary age [4] . The results of regional studies in tectonic active area are important for natural hazards assessment, planning and management of land use in densely populated [2] [3] . That in addition to its social and economic benefits, active tectonic study is a multidisciplinary approach that structural geology, geomorphology, stratigraphy, archeology, geology, earthquake and mapping are directed toward it with data integration [3] .

With obtaining simpler data from DEM with high precision and remote sensing, a growing number of achievements in response to faults morphology and active folds that have been created over the past three decades [3] [5] guide us to understand active tectonics of the region and remote areas covered by Quaternary deposits and clear signs [6] .

These studies to understand the movement and the mechanical development of regional active tectonic are useful. The active tectonic is the main cause of uplift of mountains stone blocks, and the presence of their new topography is because of difference between the tectonic and attrition processes [2] [3] .

Topography, drainage pattern analysis and morphometric indices can be used for evaluation of recent tectonic activity [1] [3] [6] [7] . Drainage pattern in active tectonic areas is sensitive to active processes such as folds and faults, channels incision, asymmetry of basin, diversion of canals and other effects can be considered as the results of these processes [3] . Numerical and surface data of morphology or new sediments are used to obtain the rate of tectonics (faults, folds, etc.) and morphological processes (incision of channels etc.) [3] [7] .

The analysis of the catchment is a powerful tool for identification of recent tectonic activities and uplift, for example, river channels are very sensitive to changes in the parameters, which control their shape and slope [4] .

The morphometry index assesses the situation and prevalence of tectonic activities. El Hamdouni et al. (2008) divided six indices to 4 categories using calculation of IRAT along the southwestern of Sri Nevada in southern of Spain and tectonic activity. IRAT classified. This study showed that the proportion of high potential of continues tectonic activity associated with IRAT values. Mahmood and Gloguen (2012) calculated seven morphometry indices using calculation of values of IRAT using GIS in the Hindu Kush, Karakoram and Himalayas. The values of IRAT index are in accordance with the rate of uplift, geomorphological and geological characteristics. Gao et al. (2013) used the morphometry indices such as hypsometric curve and longitudinal gradient of river to find the tectonic activity and assess recent uplift the northeast margin of the Tibetan plateau. Alipoor et al. (2011) evaluated morphometry indices around the dam of Rudbar, Lorestan, in high Zagros belt (the southwestern of Iran). In this way, strong tectonic thus can be developed the morphologies of the remaining streams. In this study, we studied a large area of Bashagard mountain in the south of Jazmurian subsidence (northern Makran, south and south-eastern of Iran) using morphometry indices and pattern morphometry analysis of the catchment. The technique involves the extraction of drainage basins of DEM, calculation of morphometry index, estimating IRAT, classification of IRAT levels and determination of relationship between the IRAT level and distribution of tectonic activity in the drainage basin.

Bashagard Mountains are located in northern Makran (south of Jazmurian subsidence). Northern Makran is the most northern part of Makran incremental prism (the largest incremental prism in the world), which is located in south- eastern of Iran and southern of Pakistan with the length of 850 km from the Strait of Hormuz in the West to near Karachi in the East. Prism width is from 300 to 350 km from deformation in front of the coast to Jazmurian subsidence in Iran and Meshkel in Pakistan (Figure 1). The subduction probably began during the Paleocene that led to start accretion during the Eocene and new accretionary prism from the end of Miocene [11] [12] . The active convergence rate between the Arabian plate and Makran coast that measured in Muscat of Oman and Cha- bahar coast of Iran, is 1.9 cm per year. Today the convergence rate between the Makran coast (Chabahar GPS) and Eurasian shield is 8 mm per year (Figure 2) [12] [13] .

Northern Makran includes Bashagard thrust sheet and imbricate zone includes Bande Ziarat complex, Ganj, Rameshk, Mokhtarabad and Kamsafid of Cretaceous and Eocene sediments determined with basic to high basic rocks (Figure 1(A) and Figure 1(B)). The upper cretaceous rocks have been resulted from the southern parts and have been covered by olistostrome. Moreover, it includes weak folds with long wavelength with low amplitude and the general trend of eastern-western [15] [16] . Usually, thrust faults have the slope direction towards north-northeast. Imbricate zone, which is mainly located at the eastern edge of Jazmurian dredged, is highly faulted and includes left-lateral strike-slip and is in connection with conjugate faults right-lateral strike-slip with northwest-southeast direction and reverse and normal faults directing northwest- southeast to north-south.

The geological study area has a very complex structure that this complexity is in terms of its instability, lithology compounds of different rocks and tectonic situation.

Connection between Jazmurian in north of Makran accretionary prism to south is generally fault [15] [16] . The southeast border of Jazmurian is continued towards east-west that has the maximum number of normal and reverse faults such as Karang that separates southern border of the Jazmurian subsidence from the mountain with reverse function and is continued from Esfand towards the east with approximate length of 60 km with directions of N45W, W-E"N-S and N70E (Figure 3). The Jazmurian fault is located following the Karang fault with east-west direction and the thrust type and approximate length of 42 km (Figure 3), as the southern border Jazmurian is almost eastern-western of and is continued from Beijing to southeast with the Ganj fault with almost length of 49 Km with the length of N65W. The same time northern border of that load unit is located with Cretaceous and its Rameshk unit southern boundary is with Eocene. The load unit trusted on Rameshk unit. The function of the mentioned fault is the thrust type (Figure 3).

West border of Bashagard mountain forms the Jiroft fault with a length of about 130 km with northern-southern and northwestern-southeastern directions. This fault system caused a separation in alluvial deposits in past 22 and 42 thousand years with the values of 49 and 132 meters, respectively. The average movement rate of this fault has been calculated about 2.7 ± 0.7 mm per year (Figure 3 and Figure 4).

The mentioned fault with approximate direction of northern-southern is finished with direction of northwest-southeast at the end with the right-lateral strike-slip function. One of other structures of the west is Ghale Ganj fault with a length of almost 90 km from Shadab in north after passing through the town of Ghale Ganj to Dadkhoda well in the south with the northern-southern trend to N15W parallel to the Jiroft fault that separated Ganj unit from the Quaternary sediments (Figure 3).

We obtained five morphometric indices of mountain front sinuosity (Smf), index of basin shape, valley floor width to height (Vf), basin asymmetry (Af), basin shape (Bs) and watersheds of Bashagard mountain with respect to the resistance of rock area (Figure 5) and erosion map of area (Figure 6). Then, they were divided into three categories based on division of digital morphometry [8] [19] [20] .