@2024 Afarand., IRAN
ISSN: 2538-4384 Geographical Researches 2020;35(4):343-354
ISSN: 2538-4384 Geographical Researches 2020;35(4):343-354
Reconstruction of the Least Phase Quaternary Climate Condition in Shahdad River Basin
ARTICLE INFO
Article Type
Original ResearchAuthors
Ghazanfarpour H. (*1)Pourkhosravani M. (1)
Sheykhshariati Kermani B. (1)
(*1) Department of Geography and Urban Planning, Faculty of Literature and Humanities, Shahid Bahonar University of Kerman, Kerman, Iran
Correspondence
Address: Department of Geography and Urban Planning, Faculty of Literature and Humanities, Sha-hid Bahonar University of Ker-man, Kerman, Iran. Postal Code: 7616913439.Phone: +98 (34) 31322409
Fax: +98 (34) 33257165
Ma1380@uk.ac.ir
Article History
Received: August 3, 2020Accepted: September 12, 2020
ePublished: December 12, 2020
ABSTRACT
Aims & Backgrounds
Climate changes are the most dominant characters in quaternary period. The aim of this research was to reconstruct the least phase quaternary climate condition in Shahdad basin.
Methodology At first the Wright and Porter method were used to access the last temperature and rainfall, and then the cirques and terraces were recognized based on the topography maps 1:50000 and digital elevation model of 30m.
Findings The maximum and minimum of temperature and rainfall were 25°C and 5°C and 210 and 60 ml in the present time, as well as, 20°C and -20°C and 450 and 150 ml in the last time. The altitude of perpetual snow line was 2908 m in the Wright method by passing the line of 60% of the location of glacial circuses of Shahdad basin, 2849 m in the cirque-floor altitude method, 3018 m in the altitude ratio method, and finally 2850 m in the Accumulation-area ratio method. The average of these four methods was 2906 altitude. 104 circuses were identified, with the highest frequency of circuses at an altitude of 2700 to 2900 meters. Also, by reconstructing the lake terraces and establishing a connection between the co-altitude terraces, 5 terraces were identified, which were located at altitudes of 1000, 800, 550, 400, and 250 meters.
Conclusion Although, today Shahdad basin has located in the dry climate area, but evidence has shown that this basin has glacial signs including glacial terraces, cirques and etc., and had lower temperature and more rainfall in the past. Therefore using the geomorphologic signs is a suitable method for reconstructing the old environment and climate during the last period of the maximum Expansion of glaciers.
Methodology At first the Wright and Porter method were used to access the last temperature and rainfall, and then the cirques and terraces were recognized based on the topography maps 1:50000 and digital elevation model of 30m.
Findings The maximum and minimum of temperature and rainfall were 25°C and 5°C and 210 and 60 ml in the present time, as well as, 20°C and -20°C and 450 and 150 ml in the last time. The altitude of perpetual snow line was 2908 m in the Wright method by passing the line of 60% of the location of glacial circuses of Shahdad basin, 2849 m in the cirque-floor altitude method, 3018 m in the altitude ratio method, and finally 2850 m in the Accumulation-area ratio method. The average of these four methods was 2906 altitude. 104 circuses were identified, with the highest frequency of circuses at an altitude of 2700 to 2900 meters. Also, by reconstructing the lake terraces and establishing a connection between the co-altitude terraces, 5 terraces were identified, which were located at altitudes of 1000, 800, 550, 400, and 250 meters.
Conclusion Although, today Shahdad basin has located in the dry climate area, but evidence has shown that this basin has glacial signs including glacial terraces, cirques and etc., and had lower temperature and more rainfall in the past. Therefore using the geomorphologic signs is a suitable method for reconstructing the old environment and climate during the last period of the maximum Expansion of glaciers.
CITATION LINKS
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[15]Ramesht M, Seyf A, Shahzeydi S, Entezari M (2009). Effect of juniper tectonics on the cone morphology of arboreal alluvium in Shahdad region of Kerman. Geography and Develoment Iranian Journal. 7(16):29-46.
[16]Rahdanmofrad M, Servati M, Seif A (2015). Snow reconstruction of the final Quaternary boundaries within the Rig site. Geographical Research. 30(116):193-208.
[17]Shahzeydi S (2016). Lut hole formation developments in the Quaternary (with emphasis on the reconstruction of lake barracks). Geography and Environmental Planning .27(2):119-131.
[18]Sharifi M, Taherinezhad K, Zare F (2016). Evaluation of climate change between present and pleistocene and reconstruction of past climatic conditions using geomorphic Indicators, case study: Ebrahimabad-Yazd Plain Basin). Quantitative Geomorphological Researches. 5(1):110-128.
[19]Sharifi M, Farahbakhsh Z (2015) Investigation of thermal and humidity anomalies between the present and Pleistocene and reconstruction of conditions climatic using geomorphic evidence (case study: Khezrabad Basin - Yazd). Physical Geography Research. 47(4):583-605.
[20]Sharma R, N Shakya M (2006). Hydrological changes and its impact on water resources of Bagmati watershed, Nepal. Journal of Hydrology. 327(3-4):315-322.
[21]Sarıkaya M, Marek Zreda A, Christopher Z, Ciner A (2008). Cold and Wet last glacial maximum on mount Sandıras, SW Turkey, inferred from cosmogenic dating and glacier modeling. Quaternary Science Reviews. 27(7-8):769-780.
[22]Tahouni P (2004). Geomorphological evidences of Pleistocene glacial erosion in Talesh heights. Physical Geography Research. 36(47):31-55.
[23]Yamani M (2002). Geomorphology of mountain Alam glaciers. Physical Geography Research. 34(42):1-18.
[24]Yamani M (2010). Snow reconstruction of Pleistocene boundaries in Jajroud basin. Physical Geography Research. (76):35-50
[2]Asghari Moghadam M (1999). Natural geography of the city (Geomorphology). 1st ed. Tehran: Mosee Publiction. pp. 202.
[3]Almodaresi A (2005). Hydrogeomorphology of Sakhvid basin (Yazd Province). Geographical Space. 19.
[4]Condom T, Coudrain A, Sicart JE, Thery S (2007). Computation of the space and time evolution of equilibrium-line altitudes on Andean glaciers (10°N–55°S). Global and Planetary change. 59(1-4):189-202.
[5]Foundation AG, Lewis KJ, Doran PT (1999). Spatial climatic variation and its control on glacier equilibrium line altitude in Taylor Valley, Antarctica. Global and Planetary change. 22(1-4):1-10.
[6]Glacier B (2010). Using glacier models to reconstruct climate change over the last 13,000 Years [dissertation]. Canada: University of Wellington.
[7]Ghahroudi Tali M, Nosrati K, Abdoli I (2015). Estimation of snow in the last glacial period in Daalkhani basin. Geography and Environmental Planning. 6(2):9-16.
[8]Jafari G, Barati Z (2018). Reconstruction of climatic conditions of Alivand Pleistocene glacial periods of Hamedan based on geomorphological evidences. Natural Geography Quarterly. 11(40):121-139. [Persian]
[9]Jafari Gh, Avaji M (2016). Investigation of snow effects of the permanent boundary of Quaternary glaciers of Qorveh mountain range. Quaternary Journal of Iran. 2(4):379-391.
[10]Khosravi O, Ghorbani A, Nourmohammadi A (2016). Investigation of geomorphological evidence of Quaternary Glacier in the northeastern Highlands of Iran. Quantitative Geomorphological Researches. 5(1):1-13.
[11]Liu K, Liu Y, Han B, Xu B, Zhu L, Ju J, et al (2019). Bacterial community changes in a glacial-fed Tibetan lake are correlated with glacial melting. Science of the Total Environment. 651:2059-2067.
[12]Lea D W (2004). The 100 000-yr cycle in tropical SST, greenhouse forcing, and cimate sensitivity. Journal of Climate. 17(11):2170-2179.
[13]Pedrami M (1988). The absolute age of Quaternary's underlying border is about 600,000 years old. Journal of Science, University of Tehran. 17(3-4):88-14.
[14]Paasche O, Dahl SO, Bakke J, Lovlie R, Nesje A (2007). Cirque glacier activity in arctic Norway during the last deglaciation. Quaternary Research. 68(3):387-399.
[15]Ramesht M, Seyf A, Shahzeydi S, Entezari M (2009). Effect of juniper tectonics on the cone morphology of arboreal alluvium in Shahdad region of Kerman. Geography and Develoment Iranian Journal. 7(16):29-46.
[16]Rahdanmofrad M, Servati M, Seif A (2015). Snow reconstruction of the final Quaternary boundaries within the Rig site. Geographical Research. 30(116):193-208.
[17]Shahzeydi S (2016). Lut hole formation developments in the Quaternary (with emphasis on the reconstruction of lake barracks). Geography and Environmental Planning .27(2):119-131.
[18]Sharifi M, Taherinezhad K, Zare F (2016). Evaluation of climate change between present and pleistocene and reconstruction of past climatic conditions using geomorphic Indicators, case study: Ebrahimabad-Yazd Plain Basin). Quantitative Geomorphological Researches. 5(1):110-128.
[19]Sharifi M, Farahbakhsh Z (2015) Investigation of thermal and humidity anomalies between the present and Pleistocene and reconstruction of conditions climatic using geomorphic evidence (case study: Khezrabad Basin - Yazd). Physical Geography Research. 47(4):583-605.
[20]Sharma R, N Shakya M (2006). Hydrological changes and its impact on water resources of Bagmati watershed, Nepal. Journal of Hydrology. 327(3-4):315-322.
[21]Sarıkaya M, Marek Zreda A, Christopher Z, Ciner A (2008). Cold and Wet last glacial maximum on mount Sandıras, SW Turkey, inferred from cosmogenic dating and glacier modeling. Quaternary Science Reviews. 27(7-8):769-780.
[22]Tahouni P (2004). Geomorphological evidences of Pleistocene glacial erosion in Talesh heights. Physical Geography Research. 36(47):31-55.
[23]Yamani M (2002). Geomorphology of mountain Alam glaciers. Physical Geography Research. 34(42):1-18.
[24]Yamani M (2010). Snow reconstruction of Pleistocene boundaries in Jajroud basin. Physical Geography Research. (76):35-50