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Article

Erosive Wind Characteristics and Aeolian Sediment Transport and Dune Formation in Makran Region of Baluchistan, Iran

by
Hamidreza Abbasi
1,*,
Azadeh Gohardoust
1,
Fazeh Mohammadpour
2,
Mohammad Khosroshahi
1,
Michael Groll
3 and
Christian Opp
4,*
1
Desert Division, Research Institute of Forests and Rangelands, Agricultural Research Education and Extension Organization (AREEO), Tehran 13165-116, Iran
2
Faculty of Natural Resources, University of Tehran, Karaj 31587-11167, Iran
3
EUPeace Curriculum Officer, Philipps-Universität Marburg, 35037 Marburg, Germany
4
Department of Geography, Philipps-Universität Marburg, 35037 Marburg, Germany
*
Authors to whom correspondence should be addressed.
Atmosphere 2025, 16(6), 650; https://doi.org/10.3390/atmos16060650
Submission received: 1 April 2025 / Revised: 5 May 2025 / Accepted: 15 May 2025 / Published: 27 May 2025
(This article belongs to the Topic Natural Hazards and Environmental Challenges in the Anthropocene Age, 2nd Edition)
Browse Figures
Versions Notes

Abstract

:
Understanding aeolian sediment transport and wind erosion enhances our knowledge of desert dune formation and sand migration. The Makran region of southern Sistan and Baluchistan is prone to wind-driven erosion alongside frequent sand and dust storms (SDSs). Hourly wind data from two meteorological stations spanning 1994–2020 were analyzed to study erosive winds and sand transport. Wind energy analysis using drift potential (DP) indicated low energy (DP < 200 in vector unit) and minimal spatial variation across the Makran dune fields. The effective winds transporting sand particles were towards the east from November to May, and in the northwestern direction from June to October. The DP showed a gradual decline in the study area from 1990 to 2022, with no significant temporal trends. The sand dune morphology analysis indicates that bimodal wind regimes primarily form linear dunes and sand sheets, while crescentic, transverse, and topographic dunes are also present.

1. Introduction

Wind plays a crucial role in shaping desert landscapes and coastal environments, influencing the erosion and deposition of sand [1,2]. Wind regimes are characterized by their speed, direction, and variability. Studies show that the strength and persistence of wind significantly affect the rate and pattern of sand transport [3]. Sand transport occurs primarily through three mechanisms: creep, saltation, and suspension [4]. Creep involves the movement of larger particles along the surface, while saltation refers to the bouncing motion of smaller grains lifted by wind [5]. Suspension occurs when fine particles are lifted high into the atmosphere and can be transported over great distances [6,7]. Wind direction plays a crucial role in shaping the patterns and movements of sand dunes. Variations in wind regimes exert significant influence over dune morphology, orientation, and dynamics [8,9,10].
Various methods are employed to study erosive winds related to sand transport and dune morphology, with the Fryberger and Dena method being well-suited for desert environments [11]. This method primarily involves the calculation of the sand drift potential (DP), resultant drift direction (RDD), resultant drift potential (RDP), and the RDP/DP ratio, all derived from wind speed and direction data. These indices also characterize the wind energy environment (Table 1). DP refers to the wind’s potential to transport sand particles in a specific direction. As a key driver of sand abrasion from land surfaces, it serves as a useful indicator for classifying environmental energy classes and understanding dune formation. DP represents the portion of wind force exceeding the threshold needed to erode sand particles. The resultant drift potential (RDP) reflects the net potential for sand transport influenced by winds from multiple directions, while resultant drift direction (RDD) indicates the predominant sand drift direction impacted by those winds [3]. In fact, these indices indicate erosive winds characteristics—power, intensity, direction, and blow angle—that can transport sand particles, as well as the formation and shifting of sand dunes.
In addition, sand dune types can be categorized according to the wind regime which are classified as unimodal, bimodal, or complex, with unimodal wind regimes usually forming crescentic and transverse dunes, while bimodal regimes are suitable for the formation of linear dunes, and complex wind regimes form star dunes [3,5].
Previous studies have examined the link between erosive wind regimes, wind–sediment transport, and dune formation in various deserts globally, including those in the U.S.A [12,13,14,15,16,17,18], in China [19,20,21,22,23,24,25,26], Africa [3,27,28], Kuwait [29], Saudi Arabia [3], Bahrain [3], Israel [30,31,32], and South America [33,34]. In Iran, there are several studies focused on surface wind characteristics, aeolian sediment transport, and dune activity in different deserts of Iran [35,36,37,38,39,40,41,42,43,44,45,46,47,48,49,50,51]. These studies show considerable spatial variability in erosive wind energy across Iranian deserts, with most areas exhibiting medium to high wind energy environments.
The Sistan and Baluchistan province, located in southeastern Iran, borders Pakistan to the east, the Hormozgan province to the west, the Kerman and South Khorasan provinces to the north and northeast, and the Gulf of Oman to the south. Its capital is Zahedan, covering an area of 181,785 km2 with a population of 3.3 million. The Makran coast along the Gulf of Oman in the southern part of the province stretches approximately 1000 km from Jask in the west to near Karachi in Pakistan.
Some studies have highlighted the significant economic damage from aeolian SDSs on agricultural productivity, public health, and infrastructure [52,53]. Wind erosion caused an estimated $1.9 billion in damage nationwide in 2017 [54]. The dust storm and shifting sand dunes in Baluchistan’s coastal deserts pose significant challenges for local inhabitants [36,55]. This phenomenon has led to the formation of transverse and compound crescentic, as well as sand sheets, impacting air quality and sea transport on the coast of the Oman Sea in Iran [56].
A previous study found no significant correlation between wind speed and average annual mean wave power at the Oman Sea Coast from 1992 to 2002 [57]. Conversely, some studies predict sand dune expansion along the Makran coast, potentially reaching 592 km2 by 2035 due to increased sea storm frequency if unmanaged. A remote sensing survey in western Zarabad revealed a sand dune area increase from 561 km2 in 1990 to 578 km2 in 2014, representing a 17 km2 expansion [58].
This paper investigates surface erosive wind features and aeolian sediment characteristics in the Makran region of southern Baluchistan, addressing a knowledge gap in this area of the country.

2. Materials and Methods

2.1. Study Area

The study area covers the Makran region, spanning about 1000 km from the Strait of Hormuz in southeastern Iran to near Karachi in southern Pakistan [59]. The study area is a coastal near-shore zone formed during the Quaternary surrounded by mountain ranges in the north of the study area with marls and calcareous sandstone formations dating back to the Upper Miocene. It is located between 25.9–25.26° N and 59.13–61.3° E, and the elevation ranges between 0 and 58 m in sand dunes near Chabahar in the Ramin erg (Figure 1). The study area is in the political–administrative territory of the four counties Dashtiari, Chabahar, Konarak, and Zarabad. Chabahar, Konarak, Kahir, Zarabad, Darak, Beris, Pasabandar, and Tis are among the most important communities. In total, about 55 settlements with a total population of 391,216 are suffering from SDSs.
Topographically, the study area consists of coastal flood plains, sand dunes, and the Sarbaz, Kahiri, Kacho, Sargan, Bir, Torjak, Rabaj, Kashi, and Biask rivers. The sediments of these rivers are the source of the sand dunes. The sand dunes are a habitat of several turtle species (like: Chelonia mydas, Linnaeus, 1758) that are listed as endangered species by the IUCN and CITES and are protected from exploitation in most countries [60].
This region is influenced by the northern mountains, and the air flows originating from the Gulf of Oman and the Indian Ocean (monsoons). The range of rainfall fluctuations in Chabahar varies from 114 mm to 185 mm per year and its average temperature is 26.4 degrees Celsius.
The average of dusty day frequency during 1951–2016 varied between 81–160 days [55], which is one of the highest classifications of dusty days in 15 weather stations in East Iran.

2.2. Data

This study utilized hourly wind speed and direction data collected from 2 meteorological stations, with 1 to 3 measurements taken every 24 h at a height of 10 m from the Iran Meteorological Organization (IMO, https://data.irimo.ir/, accessed on 25 June 2023) provided in the period of 1994 to 2022 for the Chabahar and Konarak weather stations (Table 2). The meteorological data were processed using WD Converter software 2.0, developed by Yazd University in Iran [61], and the wind speed frequencies in various directions were extracted using WRPLOT 8.0.2 software, developed by Lakes Software Co. (Ontario, Canada). We also used results analyzed from the Rask, Nik-shahr, and Bahookalat stations [35]. When the wind speed was zero and there was no direction, it was considered a calm period, expressed as a percentage.

2.3. Methodology

The analysis of sand transport, sand drift potential (DP), resultant drift direction (RDD), resultant drift potential (RDP), and the unidirectional index (UDI = RDP/DP) in relation to erosive winds was conducted using wind data and calculated as follows:
DP = V2(V − Vt) t
Here, DP represents the annual total sand drift across all wind directions, measured in vector units (VU). V denotes the mean recorded wind velocity at a height of 10 m above the ground, while Vt signifies the impact threshold wind velocity, set at 6 m/s. t is the time the wind blew expressed as a percentage. A vector unit refers to a spatial vector of length 1, as illustrated in a sand rose diagram. DP is expressed in knots to facilitate comparison with Fryberger and Dean’s classification system.
The RDP quantifies the overall DP resulting from the interaction of winds blowing from multiple directions, determined using Formula (2).
RDP = (C2 − D2)0.5
C = ∑(VU) Sin(θ)
D = ∑(VU) Cos(θ)
θ denotes the angle (in degrees) corresponding to the central point of each wind direction category, measured clockwise from either 0° or 360° (indicating north). In this study, wind data were classified into eight directional groups: N, NE, E, SE, S, SW, W, and NW.
The RDD represents the dominant pattern of sand movement, indicating the direction in which sand is most likely to be transported due to winds from multiple directions [3]. It was calculated using Formula (3) as shown below:
RDD = Arctan (C/D)
RDD represents the angular direction in degrees, measured clockwise from geographic north (0°).
UDI = RDP/DP
The unidirectional index (UDI) quantifies directional variability by expressing the ratio of resultant drift potential (RDP in VU) to drift potential (DP in VU). A UDI value close to 1 indicates a dominant wind regime with a single prevailing drift direction, whereas a value near 0 signifies a multidirectional wind regime with several significant drift directions. Table 1 categorizes wind energy environments and directional variability based on the Fryberger and Dean method [3].
Sand dune morphology was surveyed using 7 May 2023 Landsat 8–9 imagery (1:25,000 scale).

3. Results and Discussion

3.1. Wind Velocity

The average annual wind velocity increased from 3 to 4.5 m/s−1 from East to West across the study area (Figure 1). It was 3.8 m/s in Chabahar and 3.1 m/s at the Konarak weather station. Wind velocity in the Makran region exhibited minimal seasonal variation, with lows from October to December and peaks in July and August. Dust storm frequency, which also peaked in July and August, corroborated these findings [55,62].
Mean wind velocities exceeding 6 m/s (the threshold for sand particle movement) were 9 m/s in Chabahar and 7 m/s in Konarak, both from the southeast. Southeast winds were prevalent in the study area, occurring 15% of the time in Chabahar and 11% in Konarak. Furthermore, southeast winds exceeding the threshold velocity were most frequent, with 41% observed in Chabahar and 60% in Konarak (Table 3).

3.2. Wind Direction

An analysis of weather systems and air masses revealed that four distinct winds influence the northern coastline of the Oman Sea:
(I)
The Shamal wind with northwestern and western directions in winter was a salient feature of the surface wind peaking in December and February [63];
(II)
The summer monsoon wind with southern to southeastern direction, prevalent from June to September [64,65,66,67];
(III)
The winter monsoon with southwestern direction peaking in March and April [66,68,69];
(IV)
The Levar wind, originating in Central Asia, flowed toward the northern coast of the Arabian Sea. Commonly referred to as the “120-day wind”, it is characterized by its sustained presence throughout the summer season [36,63,69].
The wind rose diagrams from meteorological stations revealed that the study areas predominantly experience a complex wind pattern (Figure 1). The most frequent wind direction was from the southeast (13.1%), followed by the south and southwest (both at 12.5%). Other notable directions include west (8.1%), east (8.5%), northeast (5.2%), northwest (3.5%), and north (2%) (Table 4)
In Chabahar, the primary wind direction was SE (112.5–157.5°), with an average occurrence of 15.5%. The secondary wind direction was S (157.5–202.5°), averaging 13.6%, followed by SW (202.5–247.5°) with an average frequency of 13.5%. In Konarak, the predominant wind direction was SE (112.5–157.5°), appearing with an average frequency of 10.7%. The secondary wind directions, S (157.5–202.5°) and SW (202.5–247.5°), each had an average occurrence of 11.4%.
A monthly wind analysis indicated that low-intensity southwestern and western winds dominated the Gulf of Oman from February to April. With the arrival of the summer monsoon in June, southeastern winds took over, peaking in intensity during July and August, and continuing until September. As autumn approached, wind intensity declined, with varying directions including southwest, west, northeast, and southeast (Figure 2). This calm persisted from October to early January, marking a transition phase with weak and complex wind directions between the summer and winter monsoons, as noted by some studies [66,68,69].

3.3. Erosive Wind Characteristics and Sand Transport

3.3.1. Spatial Variations

Spatial analysis of drift potential at selected weather stations indicated that wind energy conditions across the study area exhibited minimal variation (Figure 3). The entire area was classified as a low wind energy environment according to the Fryberger and Dena method [3].
Table 5 shows that the DP was consistently below 200 (VU) at all meteorological stations, indicating a region characterized by low wind energy potential environment. Chabahar and Konarak experienced the highest DP values at 111 and 194, respectively, compared to other stations in the study area. The DP value at the Jask station, located in the western part of the study area, was 401 (VU) in the period of 1985 to 2005 [40]. This shows that while the study area had a low risk for erosive winds, the wind energy environment increased to a high risk toward the west in the Hormozgan province.
The spatial distribution of the RDP exhibited a pattern similar to that of the DP in the Makran dune fields. The RDP value was determined in Chabahar and Konarak, at 47 and 104, respectively. The lowest resultant drift potential (RDP) values were recorded in Rask and Nik-Shahr, measuring 14 and 29, respectively.
The annual directional sand transport index (RDD) showed moderate spatial variation in the study area (Table 4), with values typically ranging from 12 to 82 (Figure 4). This indicates that sand was transported northeast across the dune fields, leading to the formation of some dunes from mountainous regions.
The annual unidirectional index (UDI = RDP/DP) in the study area was classified as intermediate, ranging from 0.4 to 0.6, indicating a transition from an obtuse to an acute bimodal wind regime. The sand roses, shown in Figure 4, are derived from hourly wind data using the eight-compass-directions method at the Chabahar meteorological stations [3].
For seven months of the year, from November to May, effective winds drive sand particles towards the East. These winds are coming from the northwestern direction from June to October. The highest value of DP is about 13 VU in March and July. This approximately aligns with the summer monsoon and the Levar wind. The region experienced its highest frequency of monthly dust events in July, aligning with the seasonal occurrence of the Levar wind [63].

3.3.2. Temporal Variations

The analysis of the DP at the Chabahar meteorological station revealed minimal variation between 1990 and 2020 (Figure 5). The highest recorded DP was 154 VU in 2002, while the lowest value was 68 VU in 2020. Overall, the trend in wind energy, based on the DP, gradually declined during this period. Throughout these years, the DP remained below 200 VU, indicating a low-energy wind environment based on Fryberger and Dean’s classification.

3.4. Sand Dune Geomorphology

Dune shapes are influenced by wind regimes, sand availability, and sediment grain size [1,5]. Dunes are categorized into crescentic, linear, reversing, star, parabolic, and anchored types, each of which can be further classified as simple, compound, or complex forms [9,10,70,71]. In the Makran erg, dune morphology was analyzed using visual interpretation of Landsat 8–9 (7 May 2023) imagery. Based on this classification, the study area contains sand sheets, transverse dunes, linear dunes, and topographic dunes (Figure 6).
Sand dunes along the coast of the Gulf of Oman originate from the alluvial fans of local rivers. Satellite images of dust storms and ground surveys revealed seven sand and dust sources in the study area (Figure 3).
The analysis of grain size distribution of sand dunes revealed that the sand particles originated from the Makran Marl Formation. The material was transported by water from upland regions and was deposited in alluvial fans of local rivers [72,73]. Destructive and sudden floods quickly transport sediments, providing aeolian particles for wind erosion in source areas. The sheet erosion in the upland valleys and gully erosion on the edges of main streams are universal in the Sarbaz and local rivers. The sediment granulometry and mineralogy of Baluchistan’s sand dunes showed that approximately 71.43% of sediments are transported and deposited by aeolian processes, 21.42% by fluvial processes, and 7.15% by a combination of both [74].
Linear dunes have slip faces on both sides of a central crest line, with only one side active at a time, alternating seasonally or, less commonly, daily. They can be categorized into sharp-crested and rounded sand ridges. Here, ‘linear dune’ generically refers to all dunes known as seif, longitudinal, or ridge [71]. In the study area, linear dunes are found in northern Chabahar, northeast of Konarak, and south of Zarabad, Kahir, and Jahliyan (Figure 6). The southeastern and southwestern winds, blowing at an acute angle, significantly contribute to their formation. Overall, these dunes are shifting towards the northeast. Some parts of these dunes climb from uplands and form topographic dunes in the northern part of flood plains and alluvial fans. In addition, the compound linear and sand sheets are usually the most common forms.
Transvers and crescentic dunes are distributed around Darak and Zarabad. It seems that the southwestern wind is more dominant than other winds along the west coast of the Makran region, leading to the spread of crescentic dunes in this area.

4. Conclusions

Wind regimes from two meteorological stations in the northern Gulf of Oman were analyzed to improve the understanding of sand transport, dune activity, wind erosion, and sand stabilization in the Makran region of Baluchistan. Although this region is classified as a low-energy wind environment [3], the presence of active dunes [35,73] and its designation as a significant dust-generating area in Iran [62] suggest otherwise. This discrepancy is attributed to the intense storms caused by monsoon effects and the Levar wind phenomenon, as well as the sudden and short-duration strong storms that current models struggle to accurately capture. The high percentage of winds exceeding the threshold speed—41% at Chabahar and 60% at Konarak—indicates storm-like conditions.
Seasonal variations in wind speed indicate that the strongest wind energy occurs in spring and summer, while autumn in Makran is generally calm. The prevailing winds carry sand particles eastward from November to May, while the sand moves from southwest to northeast from June to October. The interaction of these two wind directions at an acute angle has led to the annual formation of linear sand dunes in the region. In addition, other types of sand dunes, such as transverse, crescent, sheet, and topographic sand dunes, also exist.
Analysis of temporal changes in drift potential (DP) at the Chabahar meteorological station shows a gradual decrease in wind energy between 1990 and 2020. This trend is consistent with global studies that predict a decrease in DP and dune activity in two-thirds of the world’s dune areas by the end of the century. However, approximately one-third of the dune areas are expected to experience an increase in DP due to the effects of the SSP5-8.5 emission scenario and global warming [74]. Given the limitations of existing models in estimating DP values during severe storms that occur suddenly and for short periods, future studies should include instantaneous wind speeds instead of average wind speeds in calculations to more accurately reflect these short-term changes in wind erosion processes.

Author Contributions

Conceptualization, M.K. and C.O.; Methodology, H.A.; Software, A.G.; Formal analysis, A.G. and F.M.; Investigation, M.G.; Data curation, A.G. and F.M.; Writing—original draft, H.A.; Writing—review & editing, M.G. and C.O.; Supervision, M.K. and C.O.; Project administration, H.A. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the Research Institute of Forests and Rangelands Iran basic research program, research project number: 01-100-170000-04-000-84026.

Institutional Review Board Statement

Not applicable.

Informed Consent Statement

Not applicable.

Data Availability Statement

The original contributions presented in this study are included in the article. Further inquiries can be directed to the corresponding author.

Acknowledgments

This work has benefited from access to the Iran Meteorological Organization database.

Conflicts of Interest

The authors declare that they have no known competing financial interests or personal relationships that could have appeared to influence the work reported in this paper.

Abbreviations

The following abbreviations are used in this manuscript:
DPDrift Potential
RDPResultant drift potential
RDDResultant drift direction
UDIUnidirectional index
SDSSand and dust storms
IMOIranian meteorological organization

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Figure 1. Location of study area within Sistan and Baluchistan province. Sand and dust sources and dunes, the annual mean wind velocity (in m/s), and annual wind roses of the Makran region, Iran. The data of wind for IMO.
Figure 1. Location of study area within Sistan and Baluchistan province. Sand and dust sources and dunes, the annual mean wind velocity (in m/s), and annual wind roses of the Makran region, Iran. The data of wind for IMO.
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Figure 2. The monthly wind roses in Chabahar weather station for the period of 1994–2022. The data of wind for IMO.
Figure 2. The monthly wind roses in Chabahar weather station for the period of 1994–2022. The data of wind for IMO.
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Figure 3. The spatial variation of sand drift potential (DP in VU) in the study area. Sand drift potential (DP in VU) varied spatially within the study area. Wind data from IMO were analyzed for the periods 1990–2022 (Chabahar and Konarak), 2006–2013 (Rask and Nik-Shahr), and 1986–1996 (Bahookalat).
Figure 3. The spatial variation of sand drift potential (DP in VU) in the study area. Sand drift potential (DP in VU) varied spatially within the study area. Wind data from IMO were analyzed for the periods 1990–2022 (Chabahar and Konarak), 2006–2013 (Rask and Nik-Shahr), and 1986–1996 (Bahookalat).
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Figure 4. The monthly and yearly sand roses at Chabahar weather station in the period of 1994–2022. The data of wind for IMO.
Figure 4. The monthly and yearly sand roses at Chabahar weather station in the period of 1994–2022. The data of wind for IMO.
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Figure 5. The trend of DP in Chabahar weather station in the period of 1990 to 2020.
Figure 5. The trend of DP in Chabahar weather station in the period of 1990 to 2020.
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Figure 6. Map of dune types (morphology) in the Makran region (Landsat 8–9, 6 June 2023).
Figure 6. Map of dune types (morphology) in the Makran region (Landsat 8–9, 6 June 2023).
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Table 1. The classification of wind energy environments using drift potential (DP) and directional variability [3].
Table 1. The classification of wind energy environments using drift potential (DP) and directional variability [3].
DP
(Vector Unit)		Wind Energy
Environment		RDP/DPDirectional
Variability		Directional Category
(Probability Distribution)
<200Low<0.3HighComplex or obtuse bimodal
200–400Intermediate0.3–0.8IntermediateObtuse to acute bimodal
>400High>0.8LowWide to narrow unimodal
Table 2. Statistical summary of wind data and weather stations in the study area and around.
Table 2. Statistical summary of wind data and weather stations in the study area and around.
StationsDurationRecordsCalm %
Chabahar2022–1994161,45333
Konarak2022–1994158,56431
Rask *2013–200651,34817
Nik-shahr *2013–200651,26318
Bahookalat *1996–198662,24515
*: The data of these stations are adopted from [35]. The data of wind for IMO.
Table 3. Statistical summary of the wind velocity parameters in weather stations for the period of 1994–2022. The data of wind for IMO.
Table 3. Statistical summary of the wind velocity parameters in weather stations for the period of 1994–2022. The data of wind for IMO.
StationParameters Wind Velocity Upper 6 (m/s)Annual Mean Wind Velocity (m/s)
Mean±SDPrevailing Wind MaxMinMean±SDPrevailing Wind
DirectionFreq.
%		DirectionFreq.
%
Chabahar93.74Southeast411603.83.56Southeast15
Konarak71.5Southeast602003.12.97Southeast11
Table 4. The percentage of wind directions at selected weather stations (Chabahar and Konarak) for the period of 1994–2022. The data of wind for IMO.
Table 4. The percentage of wind directions at selected weather stations (Chabahar and Konarak) for the period of 1994–2022. The data of wind for IMO.
DirectionYearlySpringSummerFallWinter
North2.00.850.465.775.19
Northeast5.23.083.8110.369.62
East8.57.1415.996.206.06
Southeast13.114.5831.876.918.04
South12.514.0121.9610.018.09
Southwest12.516.747.814.7414.84
West8.114.82.6512.9417.76
Northwest3.54.60.588.129.65
Calm Wind34.626.314.8724.9420.75
Table 5. Summary of erosive winds for meteorological stations of study area and around.
Table 5. Summary of erosive winds for meteorological stations of study area and around.
StationsDurationDP
(VU)		RDPRDD°RDP/DPWind Energy Environment
Chabahar1994–202211147120.4Low
Konarak1994–2022180104140.6Low
Rask *2006–20133114610.5Low
Nik-shahr *2006–20135529820.5Low
Bahookalat *1986–1996194109510.5Low
*: The data of these stations are adopted from [36]. The data of wind for IMO.
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Abbasi, H.; Gohardoust, A.; Mohammadpour, F.; Khosroshahi, M.; Groll, M.; Opp, C. Erosive Wind Characteristics and Aeolian Sediment Transport and Dune Formation in Makran Region of Baluchistan, Iran. Atmosphere 2025, 16, 650. https://doi.org/10.3390/atmos16060650

AMA Style

Abbasi H, Gohardoust A, Mohammadpour F, Khosroshahi M, Groll M, Opp C. Erosive Wind Characteristics and Aeolian Sediment Transport and Dune Formation in Makran Region of Baluchistan, Iran. Atmosphere. 2025; 16(6):650. https://doi.org/10.3390/atmos16060650

Chicago/Turabian Style

Abbasi, Hamidreza, Azadeh Gohardoust, Fazeh Mohammadpour, Mohammad Khosroshahi, Michael Groll, and Christian Opp. 2025. "Erosive Wind Characteristics and Aeolian Sediment Transport and Dune Formation in Makran Region of Baluchistan, Iran" Atmosphere 16, no. 6: 650. https://doi.org/10.3390/atmos16060650

APA Style

Abbasi, H., Gohardoust, A., Mohammadpour, F., Khosroshahi, M., Groll, M., & Opp, C. (2025). Erosive Wind Characteristics and Aeolian Sediment Transport and Dune Formation in Makran Region of Baluchistan, Iran. Atmosphere, 16(6), 650. https://doi.org/10.3390/atmos16060650

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