1. Introduction

OJG

Open Journal of Geology

2161-7570

Scientific Research Publishing

10.4236/ojg.2015.55028

OJG-56350

Articles

Earth&Environmental Sciences

Neotectonics of Boroujerd Area, SW Iran by Index of Active Tectonics

aryam

Omidali

¹Mehran

Arian

¹^*Ali

Sorbi

Department of Geology, Science and Research Branch, Islamic Azad University, Tehran, Iran

Department of Geology, Karaj Branch, Islamic Azad University, Karaj, Iran

* E-mail:mehranarian@yahoo.com(MA);

06052015

050530932414 April 2015accepted 11 May 15 May 2015

2014

This work is licensed under the Creative Commons Attribution International License (CC BY). http://creativecommons.org/licenses/by/4.0/

Boroujerd area has located in the border zone of Zagros mountain and Sanandaj-Sirjan belt in the southwest Iran. Six geomorphic indices were calculated in the study area. Through averaging these indices we obtain index of active tectonics (Iat). The values of the index were divided into classes to define the degree of active tectonics. Therefore, relative tectonic activity was calculated and their values were classified and analyzed in two groups. Regions were identified as low and moderate levels. In analyzing data and combining them with tectonic setting the results were often associated and justified with regional geology. Our results show that the highest value has located along faulted area, which shows 3 classes of relative tectonic activity (moderate level). Also, other values have located along folded area (low level). Therefore, middle part of study area (sub-basin No. 4) is showing the more active uplifting related to surroundings region (sub-basin No. 1, 2 and 3). In other words, sub-basin No. 4 has got the more active uplifting by quaternary movements of several faults such as Doroud fault.

Neotectonics Geomorohic Index Boroujerd Zagros Iran

1. Introduction

The study area is around Boroujerd city in the border zone of Zagros hinterland and Sanandaj-Sirjan belt in the south west Iran (Figure 1). This area is structurally and geographically belonging to Zagros Mountain. Its northeastern margin belongs to Sanandaj-Sirjan zone and its rest belongs to Zagros Mountain. These two zones have no similar geologic history. Sanandaj-Sirjan zone has comprised from some intrusive bodies in this area.

Figure 1 Physiographic-tectonic zoning map of Iran’s sedimentary basins Iran modified from [<xref ref-type="bibr" rid="scirp.56350-ref1">1</xref>] . Numbers in this figure are, 1: Zagros-East Taurus hinterland, 2: Persian Gulf-Mesopotamian foreland basin, 3: Makran accretionary prism, 4: Bashagard Mountains, 5: Jazmorian-Mashkel fore arc basin, 6: Shahsavaran-Soltan magmatic arc, 7: South Lut-South Helmand back arc basin, 8: East Iran Mountain belt, 9: West-Central Alborz and lesser Caucasus hinterland, 10: Great Kavir-Nor-thenUr- mieh lake foreland basin, 11: South Great Kavirfold and thrust belt, 12: South Caspian-Black sea foreland basin, 13: Urmieh- Dokhtar Magmatic Arc, 14: Naien-Kerman retro arc foreland basin, 15: Sanandaj-Sirjanover thrust belts, 16: East Alborz or Binalod hinterland, 17: Torbat-e am-Neyshabour retro arc foreland basin, 18: KopetDagh hinterland, 19: South Caspian remnant basin, 20: Maiamay-Taibad Inverted back arc basin, 21: Khaf-Kavir Plain Magmatic Arc, 22: Lut Plain-Gonabad back arc basin, 23: Tabas hinterland, 24: Yazd-Khour Piggy back basin. The study area is shown in the black rectangle

The southwestern part is a folded mountain belt in which lies the highest parts of the mountain. The boundary of these two different zones is Silakhor plains covered by alluvium.

These two structural zones have structural, metamorphic, magmatic contrasts so that this province can be divided into two contrasting domains: The north-eastern parts of this area are territories defined by magmatic, thermic, metamorphic features and most of the rock sequences are metamorphic. Pellitic metamorphic rocks constitute low lands while marbles are feature forming. The south-western parts of this area are platform sequences of Paleozoic to Triassic that they are composed of sandstone, limestone. Rock sequences younger than Triassic are limited to Plio-Quaternary conglomerates which are formed as post-orogenic deposit. Dominant structural trends in Zagros are NW-SE in this area. From tectonics view, it contains the over thrust and simple fold belts of Zagros that formed on the northeastern part of Arabian plate’s passive margin. Zagros hinterland is external platform (fold and thrust belt) of north margin of Arabian Craton (Figure 1). Vergence of folding in this hinterland is toward south and southwest. But, Sanandaj-Sirjan overthrust belt has been formed by metamorphic rocks of the northeastern part of Arabian plate. Late Cretaceous-Paleogene sequences in this belt have piled up on a wedge top part of Zagros, before regional metamorphism. Recently, pre-Cretaceous deformed and metamorphic rocks have exposed in this province by upthrusting of basement wedges [1] -[3] . In this research, area is divided into 4 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 in active tectonic studies [4] -[7] ; methodology 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 Boroujerd area by using of topographic data and DEM (Figure 2). On the other hand, the area was divided to four sub-basins tructural and for each one, 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 together. The study area is located between longitudes E48˚30' - 49˚ and latitudes N33˚45' - 34˚ in the Louristan province, south west Iran. Based on previous work on the salt diapirism [12] -[21] and neotectonics regime in Iran [22] -[26] , Zagros in south Iran is the most active zone [27] -[36] . Then, Alborz [37] -[69] and Central Iran [70] -[82] have been situated in the next orders.

Altitudes in this area reach to 3645 m on Garin mountain in the western part of Boroujerd, which it have about 2100 m difference respect to the Silakhore plain in the south eastern part of it. Geomorphologically, the ridges and valleys in the area under study are mainly due to the rocks variations in the lithology and assisted by faults presence in the area that offer varying degrees of resistance to the degradation processes. Topographically, the down faulted. Silakhore plain is quaternary alluvium covered (Figure 3).

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 Boroujerd 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 profiles and hydraulic geometrics [83] [84] . [85] 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

Figure 2 Digital elevation model of the Boroujerd areaFigure 3 The Ghaleh Hatam fault (boundary of mountain and plain) in the north eastern part of Boroujerd city, view to the eastFigure 4 Determination of sub-basins in the Boroujerd area based on Digital Elevation model (DEM)

calculated along the four master rivers (Table 1) and then SL graphs have prepared for them (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 in 2 and 3 classes.

3.2. 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:

Figure 5 Graphs of stream length-gradient index for 4 rivers.

Table 1 Values of stream length-gradient index

SL(1)	L	∆L	∆H/∆h	∆h2	∆H
12.06	31.08	4.38	50	1650	1700
8.56	26.21	5.36	50	1700	1750
8.81	21.35	4.36	50	1750	1800
4.99	16.17	6	50	1800	1850
2.62	9.67	7	50	1850	1900
Class 2

SL(2)	L	∆L	∆H/∆h	∆h2	∆H
1.88	21.39	19.30	50	1650	1700
1.30	7.02	9.44	50	1700	1750
Class 3

SL(3)	L	∆L	∆H/∆h	∆h2	∆H
8.92	36.78	7.63	50	1800	1850
8.90	30.36	6.48	50	1850	1900
8.48	24.32	5.59	50	1900	1950
5.6	18.2	6.5	50	1950	2000
5.47	12.6	4.72	50	2000	2050
3.5	7.9	4.7	50	2050	2100
Class 3
SL(4)	L	∆L	∆H/∆h	∆h2	∆H
13.82	78.12	8.76	50	1500	1550
22.25	54.24	3.9	50	1550	1600
7.94	31.47	6.54	50	1600	1650
9.39	25.86	4.68	50	1650	1700
9.79	21.26	3.80	50	1700	1750
6.83	17.42	4.59	50	1750	1800
1.7	13.1	14.06	50	1800	1850
Class 2

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 [84] . [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.

So, we have considered suitable valleys in the study area (Figure 6).

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 2 and 3 classes and show U shape valleys.

3.3. 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- line length of the front. The Mountain fronts of the study area have drawn in Figure 7 by and one of them in sub-basin No. 2 has shown in Figure 8. Smf is commonly less than 3, and approaches 1 where steep mountains rise rapidly along a fault or fold [84] . 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 4sub-basins.

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 between 1.1 to 1.5 (class 2).

3.4. Asymmetry Factor (Aƒ)

This index is related to two tectonic 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), the minimum value belongs to sub-basin No. 4 with 41.96 and the maximum value belongs to sub-basin No. 2 with 61.81 percents. Also, a map has prepared that it shows Asymmetry factor of study area (Figure 9).

Table 2 Values of Vf index

Basin	Sub-Basin	V_fw	E_ld	E_sc	E_rd	V_f	Average	Class
1	1a	150	1930	1750	1930	0.83	8.08	3
	1b	600	2020	1820	1940	3.75
	1c	200	1910	1760	1970	1.11
	1d	800	1920	1810	1848	10.81
	1e	1910	1910	1880	2010	23.88
2	2a	70	2100	1610	2000	0.16	1.64	3
	2b	800	2000	1610	2050	1.93
	2c	800	2600	1620	2400	0.91
	2d	150	1810	1740	1970	1.00
	2e	700	1930	1700	2400	1.51
	2f	200	2050	1650	2300	0.38
	2g	100	2000	1800	2080	0.42
	2h	800	1980	1610	2080	1.90
	2i	400	1810	1680	2040	1.63
	2j	800	1760	1660	1860	5.33
	2k	500	1850	1690	1940	2.44
	2l	500	1850	1680	1980	2.13
3	3a	2000	2100	1810	2040	7.69	2.35	3
	3b	200	2160	2050	2390	0.89
	3c	1500	1980	1880	2350	5.26
	3d	700	2280	2050	2440	2.26
	3e	200	2170	2010	2250	1.00
	3f	200	2250	2000	2400	0.62
4	4a	300	2700	2510	2900	1.03	0.80	2
	4b	100	2100	1750	2000	0.33
	4c	500	1790	1710	1800	5.88
	4d	1000	2050	1650	1850	3.33
	4e	200	1840	1710	2000	0.95
	4f	150	1930	1610	1880	0.51
	4g	800	1690	1960	1900	4.85
	4h	400	2690	1800	2700	0.45
	4i	150	2750	1700	2600	0.15
	4j	100	2400	1720	2150	0.18

Table 3 Values of Smf index

Sub-Basin	L_s	L_mf	S_mf	Class
1	24	26	1.08	1
2	23	26	1.13	2
3	28	34	1.21	2
4	21	30	1.42	2

Table 4 Values of Af index

Sub-Basin	Ar	At	Af	Class
1	233.7	538	43.44	3
2	501.9	812	61.81	2
3	297.2	585	50.8	3
4	1049	2500	41.96	2

Figure 6 Position map for measurement of the valley floor width to valley height ratioFigure 7 Position map for measurement of mountain-front sinuosity indexFigure 8 A Mountain-front in the south western part of Boroujerd city (sub- basin No. 2), view to the SWFigure 9 Asymmetry factor map of study areas3.5. 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:

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 Bl.

To calculate this index in the area, Bl and Bw are obtained using the sub-basins 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 and Table 5). The minimum value belongs to sub-basin No. 1 with 1 and the maximum value belongs to sub- basin No. 2 with 2.4 (Class 3).

3.6. 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. H_max, H_min and H_ave are calculated on DEM. This index is calculated to all sub-basins in the area and the minimum value is 0.19 for sub-basin No. 2 and maximum value is 0.50 for sub-basin No. 3 (Table 6). 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. 3 shows younger topography.

4. Results and Discussion

The average of the six measured geomorphic indices (Vƒ, Smf, SL, Af, Bs and Hi) was used to evaluate the distribution 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. 1, 2 and 3 and moderate relative tectonic activities in sub-basin No. 4 (Figure 11). The sub-basin No. 4 has situated in the middle part of study area and it has got several faults that shown in Figure 12.

Also, based on [23] , this area is a high seismic risk zone with following seismicity parameter: b = 1.06, M max = 7.2. Focal mechanisms of several earthquakes are dextral strike slip in relation to main recent faults of Zagros such as Doroud (Ms = 6.1, 2006).

Figure 10 Basin shape map of study area

Table 5 Values of Bs index

Sub-Basin	B_i	B_w	B_s	Class
1	30.71	30.68	1	3
2	51.86	21.05	2.4	3
3	41.25	19.56	2.1	3
4	74.09	36.24	2.04	3

Table 6 The hypsometric integral (Hi)

Sub-Basin	H_ave	H_max	H_min	H_i	Class
1	2044.54	3036	1609	0.30	3
2	1884.70	2932	1631	0.19	3
3	2131.58	2425	1838	0.50	2
4	1868.98	3250	1440	0.23	3

Table 7 Relative Tectonic activity classification

Sub-Basin	S_mf	V_f	S_l	A_f	B_s	H_i	s/n	IAT
1	1	3	2	3	3	3	2.5	4
2	2	3	3	2	3	3	2.6	4
3	2	3	3	3	3	2	2.6	4
4	2	2	2	2	3	3	2.3	3

Figure 11 Relative Tectonic activity classification map of study area

This area is struck by moderate to high earthquakes with low frequency, long repeat time and 10 - 15 Km focal depth. Intensity of earthquakes is in high levels. Sometimes, focal depths exceed to 70 Km which is an indication of initial stages of thick-skinned tectonics. The most serious seismic hazards in the study area are landslide in high regions, settlement in plain, surface faulting (Figure 13).

Figure 12 Fault map of study areaFigure 13 The Doroud fault, view to the south5. 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 sinuosity (Smf), drainage basin asymmetry (Aƒ), hypsometric integral (Hi) and drainage basin shape (Bs) have been calculated in Boroujerd area.

Therefore, firstly the area was divided to 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 are both low and moderate relative tectonic activities levels.

Low relative tectonic activities level has been found in sub-basin No. 1, 2 and 3 and moderate relative tectonic activities level, has been found in sub-basin No. 4. It means that sub-basin No. 4 has got the more active uplifting by movements of several faults such as Doroud fault.

Acknowledgements

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

NOTES

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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.

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.

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.

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. Journal of Geosciences, 15, 126-133.

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.

Feizi, F., Arian, A. and Rahmani, R. (2007) Seismotectonic Zoning in the Eastern Part of the Central Alborz. Journal of Sciences, 17, 151-164.

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

Arian, M. and Bagha, N. (2012) Active Tectonics of Tehran Area, Iran. Journal of Basic and Applied Scientific Research, 2, 3805-3819.

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

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.

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.

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

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.

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.

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.

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.

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.

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.

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.

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.

Feizi, F. and Arian, M. (2005) Application of Geomorphic Indices to the Assessment of Relative Tectonic Activity Levels in the Alborz-Central Iran Border Zone. Journal of Science, 15,378-403.

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.

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.

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, September 2004, 11-17.

Pourkermani, M. and Arian, M. (2001) Structural Geomorphology of Northeastern Kurdistan. Journal of Humanities, 7, 37-48.

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.

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.

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.

Mousavi, E.J. and Mehran, A. (2015) Tectonic Geomorphology of Atrak River, NE Iran. Open Journal of Geology, 5, 106-114. http://dx.doi.org/10.4236/ojg.2015.53010

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

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

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.

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

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.

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

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.

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.

Mosavi, J.E. 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

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

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, 28-30 August 2001, 556.

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.

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.

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.

Toudeshki, V.H., Pourkermani, M., Arian, M. and Khosrotehrani, K.H. (2011) Influence of Structures on the Ghezel Ozan River. Geosciences, 21, 55-60.

Toudeshki, V.T. and Arian, M. (2011) Morphotectonic Analysis in the Ghezel Ozan River Basin, NW Iran. Journal of Geography and Geology, 3, 258-260.

Pourkermani, M. and Arian, M. (1997) Salt Domes of Central Iran. Journal of Humanities, 3, 29-41.

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.

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.

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.

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