Active Tectonics of Kangavar Area, West Iran

Abstract

Kangavar area is located in the Sanandaj-Sirjan belt in the west Iran. Geomorphic indices of active tectonics are useful tools to analyze the influence of active tectonics. These indices have the advantage of being calculated from Arc GIS and remote sensing packages over large area as a reconnaissance tool to identify geomorphic anomalies possibly related to active tectonics. This is particularly valuable that relatively little work on active tectonics based on this method is done, so this method is new and useful. Six geomorphic indices are calculated in the study area. Then, based on index of active tectonics values that calculated by average of six geomorphic indices, two relative tectonic activities levels are revealed. The low class of Iat is mainly in the sub-basins of 3, 4, 15, 16, 17, 19 & 22 while the rest of the study area has moderate active tectonics in the other sub-basins. Our results show that the moderate value is located on faulted area, which shows 3 class of relative tectonic activity.

Share and Cite:

Gholamhosein Fard, N. , Sorbi, A. and Arian, M. (2015) Active Tectonics of Kangavar Area, West Iran. Open Journal of Geology, 5, 422-441. doi: 10.4236/ojg.2015.56040.

1. Introduction

The study area is around of Kangavar city in the Sanandaj-Sirjan belt in the west Iran (Figure 1). Sanandaj-Sir- jan overthrust belts have formed by metamorphic rocks of the northeastern part of Arabian plate. This province has continued to the north part of Dead Sea fault in the south Turkey. Late Cretaceous-Paleogene sequences in this belt have piled up on a wedge top part of Zagros proforeland basin, before regional metamorphism. Recently, pre-Cretaceous deformed and metamorphic rocks have exposed in this province by upthrusting of basement

Figure 1. Physiographic-tectonic zoning map of Iran’s sedimentary basins Iran modified from [1] . The study area is shown in the black rectangle.

wedges.

Kabodarahang depression on the north margin of this area with Urmieh-Dokhtar is an index cases from Supra-Arc troughs. This basin is significant in marking loss of the fore-arc basin beneath back―thrusts antithetic to the subduction direction and can explain the presence of younger molasses in a setting referred to as a suture zone [1] -[3] .

In this research, area is divided into 24 sub-basins and the following indices are calculated: stream-gradient index (Sl), valley floor width-valley height ratio (Vƒ), and mountain-front sinuosity (Smf), drainage basin asymmetry (Aƒ), hypsometric integral (Hi) and drainage basin shape (Bs). We use geomorphic indices of active tectonics, known to be useful for assessment of relative tectonic activities. Methodology for active tectonic studies [4] -[7] has been previously tested as a valuable tool in different tectonically active areas, namely SW USA [8] the Pacific coast of Costa Rica [9] , central Zagros, Iran [10] .

2. Materials and Methods

The calculated geomorphic indices are suitable for assessment of tectonic activity of the study area. The geomorphic indices such as: stream-gradient index (Sl), valley floor width-valley height ratio (Vƒ), mountain-front sinuosity (Smf), drainage basin asymmetry (Aƒ), hypsometric integral (Hi) and drainage basin shape (Bs) are calculated in Kangavararea by using of topographic data and DEM (Figure 2 and Figure 3). On the other hand, the area was divided into 24 sub-basins, and for each one, above indices were calculated, then all of the indices were combined to obtain index of active tectonics (Iat) by new method [11] . Therefore, sub-basins can be compared

Figure 2. Digital Elevation model of the Kangavar area.

Figure 3. Shaded Relief of the Kangavar area for identification of drainage pattern based on digital elevation model.

together. The study area is located between longitudes 47˚30'E - 48˚30'E and latitudes 34˚N - 35˚N in the Kermanshah province, west Iran. Based on previous work on the salt and mud diapirism [12] -[22] and neotectonics regime in Iran [23] -[28] , Zagros in south Iran is the most active zone [29] -[41] . Then, Alborz [42] -[75] and Central Iran [76] -[88] have been situated in the next orders.

3. Results and Discussion

To study the indices, there is a formula which we turn to describe each one of indices; It is necessary to have some primary maps to calculate the indices, and the most important of which are: Digital Elevation Model (DEM), the drainage network and the sub-basins map of the Kangavar area that have been extracted from DEM (Figure 4). DEM extracted from a digitized topographic map (with 10 m intervals).

3.1. The Stream-Gradient Index (SL)

The rivers flowing over rocks and soils of various strengths tend to reach equilibrium with specific longitudinal

Figure 4. Determination of sub-basins in the Kangavar area based on Digital Elevation model (DEM).

profiles and hydraulic geometrics [89] -[91] defined the stream-gradient index (SL) to discuss influences of environmental variables on longitudinal stream profiles, and to test whether streams has reached equilibrium. The calculation formula is in this manner:

where (∆H/∆L) is local slope of the channel segment that is located between two contours and L is the channel length from the division to the midpoint of the channel reaches for which the index is calculated. This index is calculated along the master streams of 13 measurable sub-basins (Table 1, Figure 5). The SL index can be used to evaluate relative tectonic activity. An area on soft rocks with high SL values can be indicated for active tectonics. Based on our results, there are two classes (Figure 6).

Valley floor width-valley height ratio (Vƒ):

Another index sensitive to tectonic uplift is the valley floor width to valley height ratio (Vƒ). This index can separate v-shaped valleys with small amounts from u-shaped valleys with greater amounts. The calculation formula is in this manner:

Table 1. Values of stream length-gradient index.

where Vƒw is the width of the valley floor, and Eld, Erd and Esc are the altitudes of the left and right divisions (looking downstream) and the stream channel, respectively [90] . [4] found significant differences in Vƒ between tectonically active and inactive mountain fronts. Also, they found significant differences in Vƒ between tectonically active and inactive mountain fronts, because a valley floor is narrowed due to rapid stream down cutting.

Vƒw value is obtained by measuring the length of a line which cuts the river and limits to two sides of a contour through which the river crosses (Table 2). Based on [11] , Vƒ values are divided into 3 classes: 1 (Vƒ < 0.3), 2 (0.3 < Vƒ < 1), and 3 (Vƒ > 1). Therefore, all of the valleys are in 1 class and show V-shape valleys (Figure 7).

Mountain-front sinuosity index (Smf):

This index represents a balance between stream erosion processes tending to cut some parts of a mountain front and active vertical tectonics that tend to produce straight mountain fronts. Index of mountain front sinuosity [3] is defined by:

where Lj is the planimetric length of the mountain along the mountain-piedmont junction, and Ls is the straight-

Table 2. Values of Vf index.

Figure 5. Stream length-gradient values along the master streams.

Figure 6. Classification of sub-basins based on stream length-gradient index.

Figure 7. Classification map for the valley floor width to valley height ratio.

line length of the front. The Mountain fronts sinuosity classification map of the study area has been drawn in Figure 8. Smf is commonly less than 3, and approaches 1 where steep mountains rise rapidly along a fault or fold [90] . Therefore, this index can play an important role in tectonic activity. Considering that mountain fronts sites are independent from basins places, chances are some of them have various fronts (Table 3). Values of Smf are readily calculated from topographic maps for sub-basins.

Figure 8. Classification map for Mountain-front sinuosity index.

Table 3. Values of Smf index.

Based on [11] , Smf values are divided into 3 classes: 1 (Smf < 1.1), 2 (1.1 < Smf < 1.5), and 3 (Smf > 1.5) and in the study area most of the obtained values are in 3 classes.

Asymmetry factor (Aƒ):

This index is related to two tectonics and none tectonic factors. None tectonic factors may relate to lithology and rock fabrics. It is a way to evaluate the existence of tectonic tilting at the scale of a drainage basin. The index is defined as follows:

where Ar is the right side area of the master stream basin (looking downstream) and At is the total area of the basin that can be measured by GIS software. To calculate this index in the area At and Ar are obtained using the sub-basins and the master river maps. Aƒ is close to 50 if there is no or little tilting perpendicular to the direction of the master stream. Aƒ is significantly greater or smaller than 50 under the effects of active tectonics or strong lithologic control. The values of this index are divided into three categories. 1: (Aƒ < 35 or Aƒ > 63) 2: (57 < Aƒ < 65) or (35 < Aƒ < 43) and 3: (43 < Aƒ < 57), based on [11] .

Among the obtained values (Table 4), a map has prepared that it shows Asymmetry factor of study area (Figure 9).

Basin shape index (Bs):

Relatively young drainage basins in active tectonic areas tend to be more elongated than their normal shape to the topographic slope of a mountain. The elongated shape tends to evolve into a more circular shape [4] . The horizontal projection of the basin shape may be described by the basin shape index or the elongation ratio, Bs [7] . The calculation formula is:

Figure 9. Classification map for Asymmetry factor index.

Table 4. Values of Af index.

where Bl is the length of the basin measured from the headwater to the mount, and Bw is basin width in the widest point of the basin.

To calculate this index in the area, Bl and Bw are obtained using the sub-basins (Table 5) and the master river maps then the values are divided into 3 classes. 1: (Bs > 4) 2: (3 < Bs < 4) 3: (Bs < 3), based on [11] . According to Figure 10 the maximum value belongs to sub-basin No. 4 (Class 3).

Hypsometric integral index (Hi):

The hypsometric integral (Hi) describes the relative distribution of elevation in a given area of a landscape particularly a drainage basin. The index is defined as the relative area below the hypsometric curve and it is an important indicator for topographic maturity. Hmax, Hmin and Have are calculated on DEM. This index is calculated to all sub-basins in the area. The hypsometric integral reveals the maturity stages of topography that can, indirectly, be an indicator of active tectonics.

In general, high values of the hypsometric integral are convex, and these values are generally >0.5. Intermediate values tend to be more concave-convex or straight, and generally have values between 0.4 and 0.5. Finally, lower values (<0.4) tend to have concave shapes [11] . We can consider class 1 for Hi > 0.5, class 2 for Hi between 0.4 and 0.5 and class 3 for Hi < 0.4 and so, sub-basin No.18 shows younger topography (Table 6, Figure 11).

4. Results and Discussion

The average of the six measured geomorphic indices (Vƒ, Smf, SL, Af, Bs and Hi) was used to evaluate the dis-

Figure 10. Classification map for Basin shapeindex.

Figure 11. The hypsometric integral classification map for study area.

Table 5. Values of Bs index.

tribution of relative tectonic activity. Through averaging these six indices (Table 7), we obtain one index that is known index of active tectonics (Iat). The values of the index were divided into four classes to define the degree of active tectonics: 1-very high (1 < Iat < 1.5), 2-high (1.5 < Iat < 2), 3-moderate (2 < Iat < 2.5), 4-low (2.5 < Iat) [11] .

Thus, there are low relative tectonic activities in sub-basin No. 3, 4, 15, 16, 17, 19 & 22 and moderate relative tectonic activities in the other sub-basins (Figure 12).

Also, based on [25] , this area is a moderate seismic risk zone with following seismicity parameter: b = 0.82, Mmax = 7.1. Focal mechanisms of several earthquakes are reversed and thrusted such as Changureh (Ms = 6.4, 2002)

This area is struck by low to moderate earthquakes with low frequency, medium repeat time and down to 10 Km focal depth. Intensity of earthquakes is in high levels in which there are cold igneous rocks. Sometimes, focal depths exceed to 70 Km that it is indicator for initial stages of thick-skinned tectonics. The most serious seismic hazards in Kangavar area, are settlement in Qorveh plainand surface faulting.

5. Conclusions

The calculated geomorphic indices are suitable for assessment of tectonic activity of the study area. The six geomorphic indices; stream-gradient index (Sl), valley floor width-valley height ratio (Vƒ) and mountain-front

Figure 12. Relative tectonic activity classification and fault map of study area.

Table 6. Values of Hi index.

Table 7. Relative tectonic activity classification.

sinuosity (Smf), drainage basin asymmetry (Aƒ), hypsometric integral (Hi) and drainage basin shape (Bs) have calculated in Kangavararea.

Therefore, firstly the area was divided into 24 sub-basins and for each one, indices were calculated, then all of the indices were divided into relative tectonic activity classes. Afterwards, the six measured indices for each sub-basin were compounded and a unit index obtained as index of active tectonics (Iat). According to this index, there were low and moderate relative tectonic activities levels.

Low relative tectonic activities level has been found in sub-basin No. 3, 4, 15, 16, 17, 19 & 22 and moderate relative tectonic activities level, has been found in the other sub-basins. It means that sub-basin No. 3, 4, 15, 16, 17, 19 & 22 have got the more active uplifting by Arabian-Eurasian convergent movements.

Acknowledgements

This work has funded by the Department of geology, Science and Research branch, Islamic Azad University, Tehran, Iran. Also, Special thanks to vice-president for the research in Science and Research branch, Tehran.

NOTES

*Corresponding author.

Conflicts of Interest

The authors declare no conflicts of interest.

References

[1] Arian, M. (2013) Physiographic-Tectonic Zoning of Iran’s Sedimentary Basins. Open Journal of Geology, 3, 169-177. http://dx.doi.org/10.4236/ojg.2013.33020
[2] Qorashi, M. and Arian, M. (2011) Tectonics of Iran. Geologic Survey of Iran, Tehran, 336 p.
[3] Arian, M. (2011) Basement Tectonics and Geology of Iran. AsarNafis Press, Qum, 300 p.
[4] Bull, W.B. and McFadden, L.D. (1977) Tectonic Geomorphology North and South of the Garlock Fault, California. In: Doehring, D.O., Ed., Geomorphology in Arid Regions, Proceedings of the 8th Annual Geomorphology Symposium, State University of New York, Binghamton, 115-138.
[5] Molin, P., Pazzaglia, F.J. and Dramis, F. (2004) Geomorphic Expression of Active Tectonics in a Rapidly-Deforming Forearc, Sila Massif, Calabria, Southern Italy. American Journal of Science, 304, 559-589.
http://dx.doi.org/10.2475/ajs.304.7.559
[6] Silva, P.G., Goy, J.L., Zazo, C. and Bardajm, T. (2003) Fault Generated Mountain Fronts in Southeast Spain: Geomorphologic Assessment of Tectonic and Earthquake Activity. Geomorphology, 250, 203-226.
http://dx.doi.org/10.1016/S0169-555X(02)00215-5
[7] Keller, EA. and Pinter, N. (2002) Active Tectonics: Earthquakes, Uplift, and Landscape. Prentice Hall, Upper Saddle River, 432.
[8] Rockwell, T.K., Keller, E.A. and Jonson, D.L. (1985) Tectonic Geomorphology of Alluvial Fans and Mountain Fronts near Ventura, California. In: Morisawa, M., Ed., Tectonic Geomorphology, Proceedings of the 15th Annual Geomorphology Symposium, Allen and Unwin Publishers, Boston, 183-207.
[9] Wells, S.G., Bullard, T.F., Menges, T.M., Drake, P.G., Karas, P.A., Kelson, K.I., Ritter, J.B. and Wesling, J.R. (1988) Regional Variations in Tectonic Geomorphology along Segmented Convergent Plate Boundary. Geomorphology, 1, 239-265. http://dx.doi.org/10.1016/0169-555X(88)90016-5
[10] Dehbozorgi, M., Pourkermani, M., Arian, M., Matkan, A.A., Motamedi, H. and Hosseiniasl, A. (2010) Quantitative Analysis of Relative Tectonic Activity in the Sarvestan Area, Central Zagros, Iran. Geomorphology, 121, 329-341. http://dx.doi.org/10.1016/j.geomorph.2010.05.002
[11] El Hamdouni, R., Irigaray, C., Fernandez, T., Chacon, J. and Keller, E.A. (2008) Assessment of Relative Active Tectonics, Southwest Border of Sierra Nevada (Southern Spain). Geomorphology, 96, 150-173. http://dx.doi.org/10.1016/j.geomorph.2007.08.004
[12] Arian, M. (2011) A Preface on Salt Diapirism of Iran. AsarNafis Press, Qum, 309 p.
[13] Arian, M. and Noroozpour, H. (2015) The Biggest Salt-Tongue Canopy of Central Iran. Open Journal of Geology, 5, 55-60. http://dx.doi.org/10.4236/ojg.2015.52005
[14] Asadian, F., Pourkermani, M. and Arian, M. (2007) Tectonic Geomorphology of Salt Structures in the Garmsar-Lasjerd Area. Geographical Research, 39, 75-84.
[15] Pourkermani, M. and Arian, M. (1997) Salt Domes of Central Iran. Journal of Humanities, 3, 29-41.
[16] Arian, M. (2012) Salt Diapirism and Tectonics. 2nd Edition, AsarNafis Press, Qum, 319 p.
[17] Arian, M. and Noroozpour, H. (2015) Tectonic Geomorphology of Iran’s Salt Structures. Open Journal of Geology, 5, 61-72. http://dx.doi.org/10.4236/ojg.2015.52006
[18] Asadian, F. and Arian, M. (2009) Identification of Diapiric Provinces of Central Iran through Geological and Geographical Analysis. International Journal of Agriculture Environment & Biotechnology, 2, 3443-3451.
[19] Arian, M. (2012) Clustering of Diapiric Provinces in the Central Iran Basin. Carbonates and Evaporites, 27, 9-18. http://dx.doi.org/10.1007/s13146-011-0079-9
[20] Pourkermani, M. and Arian, M. (1998) Tectonic Geomorphology of Salt Domes in West of Zanjan Province, Iran. Geographical Research, 47 , 44-53.
[21] Arian, M. and Feizi, F. (2010) The Significance of Faulting on the Surficial Spreading of Evaporitic Deposits in the Varamin-Semnan Area. Journal of Earth and Resources, 3, 1-20.
[22] Feizi, F., Arian, M. and Arian, A. (2015) Mud Diapirism on the Makran, Iran: Case Study on the Napag Mud Volcano. Open Journal of Geology, 5, 300-308. http://dx.doi.org/10.4236/ojg.2015.55027
[23] Arian, M. and Khodabakhshnezhad, A. (2015) Sedimentary Environments Can Be Changed by Geotechnology (Case Study: A Morphotectonic Idea for Design of Extensive Artificial Bay on the Iranian Plateau). International Journal of Geosciences, 6, 487-496. http://dx.doi.org/10.4236/ijg.2015.65039
[24] Arian, M. (2011) Middle East Tectonics. AsarNafis Press, Qum, 236 p.
[25] Arian, M. (2010) Applied Seismotectonics. Farazamin Press, Tehran, 304 p.
[26] Arian, M. and Maleki, R. (2008) Neotectonics. Farazamin Research Center, Tehran, 150.
[27] Pourkermani, M. and Arian, M. (1998) Seismicity of Iran. Shahid Beheshti University Press, Tehran, 212.
[28] Pourkermani, M. and Arian, M. (1997) Seismotectonics. Dez Ab Consulting Engineers Company Press, Tehran, 270.
[29] Arian, M. and Aram, Z. (2014) Relative Tectonic Activity Classification in the Kermanshah Area, Western Iran. Solid Earth, 5, 1277-1291. http://dx.doi.org/10.5194/se-5-1277-2014
[30] Mashal, M., PourKermani, M., Charchi, A., Almasian, M. and Arian, M. (2013) Pattern of Structural Geology Underground in Eastern of North Dezfol Embayment. Advances in Environmental Biology, 7, 260-268.
[31] Pazhoohan, M., Arian, M., Ghorashi, M. and Khosrotehrani, K. (2014) A Study of Drainage Pattern Responses to Active Tectonics in Tadvan Region? SW Iran. Geodynamics, 1, 36-41.
[32] Rahimi, N. and Arian, M. (2014) Tectonic Geomorphplogy of Kangavar-Sosangerd Region, West Iran. Advances in Environmental Biology, 8, 119-124.
[33] Arian, M. and Hashemi, A. (2008) Seismotectonic Zoning in the Zagros. Journal of Sciences, 18, 63-76.
[34] Arian, M., Ahmadnia, A., Qorashi, M. and Pourkermani, M. (2002) Structural Analysis of Mengharak Transcurrent Fault System in Zagros, Iran. Special Geo 2002 Conference Issue Geoarabia, 7, 209-210.
[35] Arian, M., Qorashi, M., Pourkermani, M. and Ahmadnia, A. (2003) Fractal Analysis of Mengharak Transcurrent Fault System in Zagros, Iran. Abstracts of 4th International Conference on Seismology and Earthquake Engineering, Tehran, 12-14 May 2003, 23.
[36] Baharvand, S., Pourkermani, M., Ajalloian, R., Arian, M. and Nouryazdan, A.R. (2010) Seymareh Landslide and Its Role in Environmental and Geomorphologic Changes of the Pole-Dokhtar Area. Journal of the Earth, 4, 13-24.
[37] Abdideh, M., Qorashi, M., Rangzan, K. and Arian, M. (2011) Assessment of Relative Active Tectonics Using Morphometric Analysis, Case Study of Dez River (Southwestern, Iran). Geosciences, 20, 33-46.
[38] Arian, M., Qorashi, M., Pourkermani, M. and Ahmadnia, A. (2006) The Structural Significance Kareh Bas Transcurrent Fault System in the Zagros Fold and Thrust Belt. Geosciences, 15, 126-133.
[39] Arian, M. and Noroozpour, H. (2015) Seismic Activity and Fractal Geometry of Kareh Bas Fault System in Zagros, South of Iran. Open Journal of Geology, 5, 291-299. http://dx.doi.org/10.4236/ojg.2015.55026
[40] Ehsani, J. and Arian, M. (2015) Quantitative Analysis of Relative Tectonic Activity in the Jarahi-Hendijan Basin Area, Zagros Iran. Geosciences Journal, 19, 1-15. http://dx.doi.org/10.1007/s12303-015-0016-3
[41] Omidali, M., Arian, M. and Sorbi, A. (2015) Neotectonics of Boroujerd Area, SW Iran by Index of Active Tectonics. Open Journal of Geology, 5, 309-324. http://dx.doi.org/10.4236/ojg.2015.55028
[42] Noroozpour, H., Arian, M. and Sorbi, A. (2015) Fault Movement Potentials in the Tehran-Semnan Region (North Iran). Open Journal of Geology, 5, 281-290. http://dx.doi.org/10.4236/ojg.2015.55025
[43] Arian, M., Maleki, Z. and Noroozpour, H. (2011) Cenozoic Diastrophism and Deformational Events in the East Central Alborz. Journal of Basic and Applied Scientific Research, 1, 2394-2400.
[44] Feizi, F., Arian, A. and Rahmani, R. (2007) Seismotectonic Zoning in the Eastern Part of the Central Alborz. Journal of Sciences, 17, 151-164.
[45] Khavari, R., Arian, M. and Ghorashi, M. (2009) Neotectonics of the South Central Alborz Drainage Basin, in NW Tehran, N Iran. Journal of Applied Sciences, 9, 4115-4126.
http://dx.doi.org/10.3923/jas.2009.4115.4126
[46] Arian, M. and Bagha, N. (2012) Active Tectonics of Tehran Area, Iran. Journal of Basic and Applied Scientific Research, 2, 3805-3819.
[47] Bagha, N., Arian, M., Ghorashi, M., Pourkermani, M., El Hamdouni, R. and Solgi, A. (2014) Evaluation of Relative Tectonic Activity in the Tehran Basin, Central Alborz, Northern Iran. Geomorphology, 213, 66-87. http://dx.doi.org/10.1016/j.geomorph.2013.12.041
[48] Arian, M. and Feizi, F. (2005) Application of Geomorphic Indices to the Assessment of Relative Tectonic Activity Levels in the Alborz-Central Iran Border Zone. Journal of Sciences, 15, 378-403.
[49] Arian, M., Bagha, N., Khavari, R. and Noroozpour, H. (2012) Seismic Sources and Neo-Tectonics of Tehran Area (North Iran). Indian Journal of Science and Technology, 5, 2379-2383.
[50] Moghimi, H., Arian, M. and Sorbi, A. (2015) Fault Movement Potential of Marzanabad Area, North Alborz, Iran. Open Journal of Geology, 5, 126-135. http://dx.doi.org/10.4236/ojg.2015.53012
[51] Arian, M. and Pourkermani, M. (2004) Tectonic Elements of South Flank in the East-Central Alborz Mountain. Journal of Sciences (Teacher Training University), 4, 359-368.
[52] Arian, M. and Qorashi, M. (2006) The Movement Potential Evaluation of the Major Quaternary Faults in Alborz-Central Iran Border Zone, from the East of Tehran to the East of Semnan. Journal of Geosciences, Geological Survey of Iran, 15, 184-188.
[53] Poroohan, N., Pourkermani, M. and Arian, M. (2013) An Assessment of Relationship in F-Parameter and Paleostress Fields in Heterogeneous Lithologies: Roudbar Area (Northwest of Iran). Australian Journal of Basic & Applied Sciences, 7, 933-942.
[54] Poroohan, N., Poukermani, M. and Arian, M. (2009) An Assessment on Correlations of Seismotectonic Parameters Preceding and Following Roudbar-Manjil Earthquake (Gilan, North of Iran). Australian Journal of Basic & Applied Sciences, 3, 2643-2652.
[55] Farrokhnia, A.R., Pirasteh, S., Pourkermani, M. and Arian, M. (2011). Geo-Information Technology for Mass Wasting Hazard Zonation: Central-West Alborz-Iran. Disaster Advances, 4, 24-33.
[56] Khavari, R., Ghorashi, M. and Arian, M. (2009) Assessment of Relative Active Tectonics, South Central Alborz (North Iran). EGU General Assembly Conference Abstracts, 11, 1137.
[57] Sorbi, A., Arian, M. and Pourkermani,M.,(2009) The Movement Potential Evaluation of the Major Quaternary Faults in Tehran Quadrangle. Journal of the Earth, 19, 176-182.
[58] Feizi, F. and Arian, M. (2006) The Classification of Thrust Fronts in the Alborz-Central Iran Border Zone from the East of Varamin to the East of Semnan. Journal of Sciences, 16, 75-87.
[59] Arian, M. and Feizi, F. (2005) Application of Geomorphic Indices to the Assessment of Relative Tectonic Activity Levels in the Alborz-Central Iran Border Zone the Alborz-Central Iran Border Zone. Journal of Science, 15, 378-403.
[60] Arian, M. and Pourkermani, M. (2004) Structural Significance of North Semnan and Attary Faults in Alborz-Central Iran Border Zone. Journal of Science, 14, 4551-4569.
[61] Arian, M. and Pourkermani, M. (2005) Cenozoic Diastrophism and Deformational Events in the Southern Flank of Central-East Alborz. Journal of Faculty Earth Sciences, 10, 43-51.
[62] Arian, M., Pourkermani, M., Qorashi, M. and Ghasemi, M.R. (2003) North Semnan Fault System and Its Role on Basin Division. 8th Symposium of Geological Society of Iran, Shahrood University of Technology, 4-6 September 2003, 11-17.
[63] Pourkermani, M. and Arian, M. (2001) Structural Geomorphology of Northeastern Kurdistan. Journal of Humanities, 7, 37-48.
[64] Mardani, Z., Ghorashi, M. and Arian, M. (2011) Geomorphic Signatures of Active Tectonics in the Talaghan Rud, Shah Rud and Sefidrud Drainage Basins in Central Alborz, N Iran. Geosciences, 20, 159-166.
[65] Sorbi, A., Arian, M. and Pourkermani, M. (2011) The Application of Geomorphic Indices to the Assessment of Relative Tectonic Activity Levels in Tehran Quadrangle. Journal of the Earth, 6, 1-9.
[66] Khavari, R., Ghorashi, M., Arian, M. and Khosrotehrani, K. (2010) Geomorphic Signatures of Active Tectonics in the Karaj Drainage Basin in South Central Alborz, N Iran. Geosciences, 19, 67-74.
[67] Mousavi, E.J. and Arian, M. (2015) Tectonic Geomorphology of Atrak River, NE Iran. Open Journal of Geology, 5, 106-114. http://dx.doi.org/10.4236/ojg.2015.53010
[68] Nouri, R., Jafari, M.R., Arian, M., Feizi, F. and Afzal, P. (2013) Correlation between Cu Mineralization and Major Faults Using Multifractal Modelling in the Tarom Area (NW Iran). Geologica Carpathica, 64, 409-416. http://dx.doi.org/10.2478/geoca-2013-0028
[69] Nouri, R., Jafari, M.R., Arian, M., Feizi, F. and Afzal, P. (2013) Prospection for Copper Mineralization with Contribution of Remote Sensing, Geochemical and Mineralographical Data in Abhar 1:100,000 Sheet, NW Iran. Archives of Mining Sciences, 58, 1071-1084. http://dx.doi.org/10.2478/amsc-2013-0074
[70] Nouri, R., Afzal, P., Arian, M., Jafari, M. and Feizi, F. (2013) Reconnaissance of Copper and Gold Mineralization Using Analytical Hierarchy Process in the Rudbar 1: 100,000 Map Sheet, Northwest Iran. Journal of Mining and Metallurgy, 49, 9-19.
[71] Arian, M. and Nouri, R. (2015) Lineament Tectonics and Mineralization in Tarom Area, North Iran. Open Journal of Geology, 5, 115-124. http://dx.doi.org/10.4236/ojg.2015.53011
[72] Feizi, F. and Arian, M. (2011) The Role of Structural Controllers in Geneses of Copper Deposits in 1:50000 Map of Saiin Qaleh. Journal of Sciences, 21, 1-10.
[73] Khavari, R., Ghorashi, M. and Arian, M. (2009) Assessment of Relative Active Tectonics, South Central Alborz (North Iran). EGU General Assembly Conference Abstracts, 11, 1137.
[74] Bahiraee, S., Arian, M., Qorashi, M. and Solgi, M. (2015) The Movement Potential Evaluation of the Mosha Fault (the West of Firoozkuh to the Shahrestanak). Geosciences, 24, 123-126.
[75] Bagha, N., Ghorashi, M., Arian, M., Pourkermani, M. and Solgi, A. (2015) Neotectonic Analysis of Mosha-North Tehran Fault Zone, Based on Morphotectonic Features, Central Alborz, Northern Iran. Geosciences, 24, 41-52.
[76] Mosavi, E.J. and Arian, M. (2015) Neotectonics of Tabas Area, Central Iran by Index of Active Tectonics (IAT). Open Journal of Geology, 5, 209-223. http://dx.doi.org/10.4236/ojg.2015.54019
[77] Daryani, N.J., Arian, M. and Omran, N.R. (2015) Tectonics and Mineralization of Copper in the Ardestan-Kahang Area, Central Iran by Remote Sensing. Open Journal of Geology, 5, 188-196.
http://dx.doi.org/10.4236/ojg.2015.54017
[78] Arian, M. and Pourkermani, M. (2001) Rivers Morphology and Active Tectonic (Reviewing the Current Status of Ghezel Ozon River in the Province of Zanjan). 5th Conference of Geological Society of Iran, Tehran, 28-23 August 2001, 556.
[79] Eshghi, Z., Arian, M. and Pourkermani, M. (2012) Structural Investigation on the Lak Mining Area (Bueen Zahra) Based on Remote Sensing, Used for Its Mineralization. Journal of the Earth, 6, 145-155.
[80] Arian, M., Toudeshki, V.H. and Noroozpour, H. (2011) Active Tectonics of Qezel Ozan River Basin, NW Iran. Journal of Applied Environmental and Biological Sciences, 1, 291-295.
[81] Alizadeh, H., Arian, M., Lotfi, M., Ghorashi, M. and Ghorbani, M. (2015) Determination of Porphyry Copper Deposit Locations Using Photo Lineament Factor in Northern Parts of the Dehaj-Sardoiyeh Belt. Geosciences, 24, 247-252.
[82] Toudeshki, V.H., Pourkermani, M., Arian, M. and Khosrotehrani, K.H. (2011) Influence of Structures on the Ghezel Ozan River. Geosciences, 21, 55-60.
[83] Toudeshki, V.H. and Arian, M. (2011) Morphotectonic Analysis in the GhezelOzan River Basin, NW Iran. Journal of Geography and Geology, 3, 258-260.
[84] Pourkermani, M. and Arian, M. (1997) Salt Domes of Central Iran. Journal of Humanities, 3, 29-41.
[85] Arian, M., Pourkermani, M., Sistanipour, A. and Noroozpour, H. (2011) Kinematic Significance of Fold- and Fault-Related Fracture Systems in the Rafsanjan’s Northeast Highlands (Central Iran). Journal of Basic and Applied Scientific Research, 1, 3398-3406.
[86] Arian, M., Pourkermani, M., Sistanipour, A. and Noroozpour, H. (2011) Seismicity and Fault Segmentation of Bafq-Baghin Fault System (Central Iran). Journal of Applied Environmental and Biological Sciences, 1, 382-396.
[87] Mosavi, E.J., Arian, M., Ghorashi, M. and Nazemi, M. (2012) Measurments of Geomorphic Indices in Tabas Area. Journal of the Earth, 7, 213-225.
[88] Arian, M. (2010) Earthquake-Fault Hazard Investigations in the Kerman Quadrangle. Journal of Sciences, 19, 176-182.
[89] Bronnimann, P., Zaninetti, L., Bozorgnia, F., Dashti, G.R. and Moshtaghian, A. (1971) Lithostratigraphy and foraminifera of the Upper Triassic Naiband Formation, Iran. Revue de Micropaléontologie, 14, 7-16.
[90] Bull, W.B. (2007) Tectonic Geomorphology of Mountains: A New Approach to Paleoseismology. Blackwell, Malden. http://dx.doi.org/10.1002/9780470692318
[91] Hack, J.T. (1973) Stream-Profiles Analysis and Stream-Gradient Index. Journal of Research of the U.S. Geological Survey, 1, 421-429.

Copyright © 2024 by authors and Scientific Research Publishing Inc.

Creative Commons License

This work and the related PDF file are licensed under a Creative Commons Attribution 4.0 International License.