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Bazman

Coordinates: 28°07′N 60°00′E / 28.117°N 60.000°E / 28.117; 60.000
From Wikipedia, the free encyclopedia
For the city in Iran, see Bazman, Iran. For the administrative subdivision of Iran, see Bazman District.
Bazman
Bazman is located in Iran
Bazman
Bazman
Iran
Highest point
Elevation3,490 m (11,450 ft)[1]
Prominence2,400 m (7,900 ft)[2]
ListingUltra
Coordinates28°07′N 60°00′E / 28.117°N 60.000°E / 28.117; 60.000[1]
Geography
LocationSistan and Baluchestan Province, Iran
Geology
Mountain typeStratovolcano
Last eruptionc. 41,000 years ago

Bazman (Persian: بزمان, also known as Kuh-e Bazman) is a dormant stratovolcano in a remote desert region of Sistan and Baluchestan Province in southeastern Iran. A 500-m-wide crater caps the summit of the dominantly andesitic-dacitic volcano, the flanks of which are covered by monogenetic centres especially to the northwest. Bazman is a geologically young volcano which formed mainly in the Quaternary, with the oldest dated rocks being 11.7 million years old and the youngest 0.6 million years. Although no historic eruptions have been reported from Bazman, it does contain fumaroles. Thus Bazman may be regarded as dormant, rather than extinct, volcano. Its satellite cones have been the source of basaltic lava flows.

Bazman volcano is part of a volcanic arc in southeastern Iran, the Makran volcanic arc. At this arc, shallow subduction has generated an arc of volcanic activity which includes Bazman, Taftan and Koh-i-Sultan volcanoes. Bazman has been affected by heavy erosion. The flanks of the volcano are covered with debris coming from the volcano. A Cretaceous pluton is also associated with Bazman and has been investigated for the possibility of mining.

Bazman volcano ISS

Geography and geology

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Bazman is also known as Kuh-i-Zindeh ("Mountain of the Living One"), after a saint, Khizr-as-Sallam.[3] Yet another name is Kuh-i-Naushada,[4] although they are sometimes considered to be separate mountains.[5] The mountain was climbed in 1896 by Percy Sykes and Brazier Creagh;[6] by 1906 its volcanic nature was known to geologists.[7] It is located 420 kilometres (260 mi) away from the Arabian Sea,[8] and 120 kilometres (75 mi) north-northwest of Bampur.[7]

Regional setting

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Iran contains two major mountain ranges, the Alborz in northern Iran and Zagros in western Iran.[9] Each range is associated with a major suture zone, the Alborz-Kopeh Dag and the Bitlis-Zagros sutures respectively.[10] These mountain chains surround Central Iran, in whose southern part lies the Lut block and Bazman. Tectonically, southern central Iran does not follow the typical Alpide geological patterns insofar as faults are rare and the folds in the crust are broad. The Bazman area is covered by volcanic rocks of Tertiary age.[9] The foreland of the mountain massifs such as the Bazman massif are affected by tectonic subsidence.[11] A major Tertiary volcanic belt, analogous to the Indonesian volcanic arc, crosses Iran behind the Zagros.[12] South of Bazman volcano lies the broad Jaz Murian depression. To the south of this depression the Makran area separates the Arabian Sea from inner Iran. The Makran area is geologically subdivided into the Inner Makran series which includes ophiolitic melange and the Coastal Makran Series.[13] A phase of subduction commenced in the Cretaceous[14] or Plio-Pleistocene, probably after earlier phases of subduction. This subduction has resulted in the formation of a volcanic complex including Bazman that stretches 150 kilometres (93 mi) east-west and reaches a width of 100 kilometres (62 mi),[15] and is known as the Makran-Chagai magmatic arc.[16] There is also earthquake activity including the 1945 Makran earthquake,[15] but overall earthquake activity in the Makran is low,[17] probably due to the effect of sediments in the trench.[18] A large accretionary prism formed directly behind the trench,[19] in the trench the subduction occurs at a pace of 2 centimetres per year (0.79 in/year).[10] There is no evidence of a Wadati–Benioff zone beneath the Makran[12] and subduction occurs at a shallow angle.[20] Bazman has been grouped with Taftan volcano also in Iran and Koh-i-Sultan in Pakistan, of which only Taftan is considered active,[21] Kuh-e-Nader is another volcanic field in this arc.[14] This arc is over 600 kilometres (370 mi) away from the trench, indicating that the subduction is very shallow.[22] Within this arc, Bazman is located at the edge between the actual subduction and the continental collision zone.[23] Bazman is also considered part of a 1,700 kilometres (1,100 mi) long volcanic belt named the Urumieh-Dokhtar or Sahand-Bazman belt that extends from northwest to southeast and is accompanied by Cenozoic volcanic rocks and plutons.[24][25] Bazman is sometimes considered to be part of a volcanic complex with the neighbouring Shahsavaran volcanic field.[26]

Local setting

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Bazman is one among about nine volcanic centres in Iran that have had Quaternary eruptions. Other volcanoes are Damavand which is also Asia's highest volcano, Taftan, Qal'eh Hasan Ali, Sabalan and Sahand volcanoes. Most of these volcanoes are part of a volcanic belt named Dokhtar-Urmiah. With the exception of reports of possible lava flows at Taftan, none of these volcanoes have been reportedly active during historical times.[27] Older volcanic activity within this belt has generated a number of copper porphyry deposits.[28]

Bazman volcano is 3,500 metres (11,500 ft) high, rising high above the surrounding terrain, and has steep slopes.[3] At the top of the volcano lies a summit crater. This crater is well conserved and it has a diameter of 500 metres (1,600 ft). On the north flank, a northbound lava flow with prominent levees that eventually splits into a northwestern and northeastern arm was discharged by a steep lava cone[29][1] that is known as Bazman Bacheh ("Bazman's Child") and lies 3 kilometres (1.9 mi) northeast of the summit.[30] Other viscous lava flows have been erupted from satellite cones,[29] which occur mainly at distances of 10–20 kilometres (6.2–12.4 mi) northeast from the summit. In total the volcano covers an area of about 300 square kilometres (120 sq mi).[30] The volcano is constructed on top of the Lut block, which reaches a thickness of 40 kilometres (25 mi).[31] Quaternary sediments are buried beneath Bazman's eruption products.[8] The Moho beneath Bazman is approximately 48–50 kilometres (30–31 mi) deep.[32] The area around Bazman is remote.[1]

A field of monogenetic volcanoes is found northwest of Bazman.[12] These include broad and shallow craters with diameters of 800 metres (2,600 ft) with pyroclastic rocks,[33] cryptodomes with diameters of up to 3 kilometres (1.9 mi) and heights of 75 metres (246 ft), scoria cones reaching a height of 300 metres (980 ft) with lava flow fields and individual lava flows. The varying state of erosion of these volcanoes indicates they formed over many millennia; some have been worn down to their feeding dykes.[12]

Bazman has no recorded historical eruptions but fumarolic activity has been reported,[1] as well as ongoing surface deformation.[34] Bazman is considered to be occasionally smoking.[4] Hot springs containing iron and sulfur are other signs of ongoing volcanism;[35] Bazman has been considered a potential site for development of geothermal energy, with a surface area of 8,356 square kilometres (3,226 sq mi).[36] In 1960, Bazman together with Taftan was considered a volcano with sporadic historic activity,[37] while a different report in 1975 considered the volcano extinct.[38] Potassium-argon dating of basalts from the volcano has yielded ages of 4.6 and 0.6 million years ago.[31] These dates were obtained on the monogenetic cones; zircons directly from Bazman rocks are dated 7.5 ± 0.1 and 5.9 ± 0.2 million years ago by uranium-lead dating, along with other ages of 8–6 million years ago from other zircons around Bazman.[39] A third date is of 11.7 million years ago.[18] Another report in 1981 suggested that isotopic ages also indicate historic activity.[40] Latest research indicates that the main Bazman volcano formed between 1.4 and 0.63 million years ago, with a preceding stage of regional volcanism between 8.6 and 4.1 million years ago.[41] Later ignimbritic volcanism took place between 590,000 and 470,000 years ago; the final volcanic activity around the summit of the volcano continued until less than 41,000 years ago.[42] An important geothermal field is associated with Bazman[43] and hot springs occur south of the volcano;[44] they might derive their heat source from it[45] but the volcano features no fumaroles.[46] Towns and in particular roads around the volcano could be threatened by lava flows, ash falls and nuee ardente emission, in case of renewed eruptions.[47]

Bazman volcano is constructed by dacite,[3] but andesite has also been mentioned.[21] Minor amounts of rhyolite have also been reported.[39] Overall rock samples range from basalt to rhyolite in composition and are mostly of calc-alkaline composition.[48] The satellite cones have erupted olivine-containing basalts.[1] The mountain's flanks are covered by a layer of detritus,[3] burying most of the flanks to over 2,135 metres (7,005 ft) of altitude. Most of this detritus is erosional in nature, but pyroclastic rocks created by explosive activity and hot avalanches of extruded lava also contribute.[12] 120 metres (390 ft) thick olivine basalt found in the Jaz Murian depression may also come from Bazman.[49] Basalt has also been found at one cryptodome.[12] North of Bazman, andesites of Miocene-Eocene age are partly buried beneath the volcano[50] and there are also andesitic to dacitic intrusions.[30] Carboniferous and Permian metamorphic rocks form the oldest basement at Bazman.[39]

Petrological analysis at the monogenetic volcanoes around Bazman has indicated porphyritic basalts containing clinopyroxene, hornblende, olivine and plagioclase, and titanite and zircon as accessories.[51][52] The rocks have medium potassium content, lower than that of Taftan and Koh-i-Sultan. This may reflect differences in the subduction beneath Bazman and the other two volcanoes.[53] Composition data are typical of volcanic island arc rocks,[40] with some samples have element ratios more akin to ocean island basalts.[52][54] Lithosphere modified by the subduction may be the origin of the magmas that formed the monogenetic cones.[23] On the basis of its composition, the environmental conditions under which one of the samples formed have been estimated, the temperature being c. 1,400 °C (2,550 °F) and a minimum depth of about 76 kilometres (47 mi).[55] The magmas ultimately originate through partial melting from a stable heat source.[56]

A mining area is associated with Bazman and more precisely with Paleozoic-Mesozoic rocks including a c. 70 million years old granite pluton.[50] This late Cretaceous pluton is localized south of Bazman volcano.[57] According to other reports its rocks are also exposed on the northern side of Bazman.[58] The granite complex is partly buried by Bazman volcano.[44] Various hydrothermal and skarn alterations have generated mineral deposits that include silver, gold, copper, lead, magnesium, molybdenum, and zinc, and minor amounts of tungsten and possibly of vanadium.[50] The Chahnali epithermal gold deposit is close to the volcano.[23]

The area of Bazman is affected by rain erosion. Sheet floods such as those that occurred in 1976 are principal agents. Together with other kinds of erosion such as frost and salt weathering, these have formed a pediplain terrain with inselbergs being left, especially where harder rocks are found.[59] Pebbles eroded from Bazman have been transported to the terrains of the Jaz Murian depression south of Bazman.[60] The effects of this erosion have mantled the volcano with debris locally known as "dasht", reaching distances of over 30 kilometres (19 mi) from the vent.[12] With the exception of the Ziyarat valley on Bazman's southern flank, the area around Bazman is arid and uninhabited.[3]

Climate and environment

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The 3,246.88 square kilometres (1,253.63 sq mi) Bazman protected area encompasses part of the volcano.[61] Animal species recorded there include the Asian black bear, bustard, chinkara and sand cat.[62]

See also

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Citations

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  1. ^ a b c d e f "Bazman". Global Volcanism Program. Smithsonian Institution.
  2. ^ Peaklist.org: Iran Mountain Ultra-Prominence
  3. ^ a b c d e Gabriel, Alfons (September 1938). "The Southern Lut and Iranian Baluchistan". The Geographical Journal. 92 (3): 193–208. doi:10.2307/1788828. JSTOR 1788828.
  4. ^ a b CLAPP, F. G. (1 January 1940). "Geology of Eastern Iran". Geological Society of America Bulletin. 51 (1): 87. Bibcode:1940GSAB...51....1C. doi:10.1130/GSAB-51-1.
  5. ^ Geological Survey of Pakistan. Records. Manager of Publications.
  6. ^ "Mitteilungen der Österreichischen Mineralogischen Gesellsehaft". Tschermaks Mineralogische und Petrographische Mitteilungen (in German). 5 (4): 412. 1956. Bibcode:1956MinPe...5..406.. doi:10.1007/BF01127700.
  7. ^ a b Reclus, Elisée (1906). Les volcans de la terre (in French). Société belge d 'astronomie, de météorologie et de physique du globe. pp. 22–23. Retrieved 2 August 2016.
  8. ^ a b Jafarian, Abdolreza (2011). "Geochemical Signatures of Bazman Volcano: Evidence from Makran Subduction Zone, Southeast Iran" (PDF). EGU General Assembly 201. Retrieved 17 August 2016.
  9. ^ a b Weise 1978, p. 452
  10. ^ a b Pang et al. 2014, p. 2152
  11. ^ Weise 1978, p. 453
  12. ^ a b c d e f g Shearman et al. 1976, p. 405
  13. ^ Shearman et al. 1976, p. 395
  14. ^ a b Ghalamghash et al. 2018, p.2
  15. ^ a b Shearman et al. 1976, p. 403
  16. ^ Ghalamghash et al. 2018, p.1
  17. ^ Pang et al. 2014, p. 2153
  18. ^ a b Pang et al. 2014, p. 2154
  19. ^ Saadat et al. 2011, p. 608
  20. ^ Delavari et al. 2022, p.2
  21. ^ a b Skrine, C. P. (October 1931). "The Highlands of Persian Baluchistan". The Geographical Journal. 78 (4): 321–338. doi:10.2307/1784749. JSTOR 1784749.
  22. ^ McCall, G.J.H (December 1997). "The geotectonic history of the Makran and adjacent areas of southern Iran". Journal of Asian Earth Sciences. 15 (6): 523–524. Bibcode:1997JAESc..15..517M. doi:10.1016/S0743-9547(97)00032-9.
  23. ^ a b c Richards, Jeremy P. (October 2015). "Tectonic, magmatic, and metallogenic evolution of the Tethyan orogen: From subduction to collision". Ore Geology Reviews. 70: 332. doi:10.1016/j.oregeorev.2014.11.009.
  24. ^ Ghannadpour, Seyyed Saeed; Hezarkhani, Ardeshir (1 September 2018). "Providing the bivariate anomaly map of Cu–Mo and Pb–Zn using combination of statistic methods in Parkam district, Iran". Carbonates and Evaporites. 33 (3): 2. doi:10.1007/s13146-017-0349-2. ISSN 1878-5212. S2CID 131858482.
  25. ^ Arjmandzadeh, R.; Karimpour, M.H.; Mazaheri, S.A.; Santos, J.F.; Medina, J.M.; Homam, S.M. (May 2011). "Sr–Nd isotope geochemistry and petrogenesis of the Chah-Shaljami granitoids (Lut Block, Eastern Iran)". Journal of Asian Earth Sciences. 41 (3): 283–284. Bibcode:2011JAESc..41..283A. doi:10.1016/j.jseaes.2011.02.014.
  26. ^ Mirnejad, H.; Blourian, G. H.; Kheirkhah, M.; Akrami, M. A.; Tutti, F. (22 July 2008). "Garnet-bearing rhyolite from Deh-Salm area, Lut block, Eastern Iran: anatexis of deep crustal rocks". Mineralogy and Petrology. 94 (3–4): 260. Bibcode:2008MinPe..94..259M. doi:10.1007/s00710-008-0015-4. S2CID 128568108.
  27. ^ Eshaghpour, Masoud; Saloomahalleh, Hasan Alizadeh (April 2015). "Relationship Between Thermal Springs of Western Alborz Mountains and Regional Tectonics" (PDF). pangea.stanford.edu. Melbourne: Proceedings World Geothermal Congress. p. 2. Retrieved 17 August 2016.
  28. ^ Hezarkhani, Ardeshir (July 2008). "Hydrothermal Evolution of the Miduk Porphyry Copper System, Kerman, Iran: A Fluid Inclusion Investigation". International Geology Review. 50 (7): 665–684. Bibcode:2008IGRv...50..665H. doi:10.2747/0020-6814.50.7.665. S2CID 129645979.
  29. ^ a b Global Volcanism Program, Photo Gallery
  30. ^ a b c Ghalamghash et al. 2018, p.4
  31. ^ a b Saadat et al. 2011, p. 609
  32. ^ Abdetedal, M.; Shomali, Z. H.; Gheitanchi, M. R. (2 January 2014). "Crust and upper mantle structures of the Makran subduction zone in south-east Iran by seismic ambient noise tomography". Solid Earth Discussions. 6 (1): 12. Bibcode:2014SolED...6....1A. doi:10.5194/sed-6-1-2014.
  33. ^ Shearman et al. 1976, p. 406
  34. ^ Shirzaei, M. (2012). "A satellite geodetic survey of spatiotemporal deformation of Iranian volcanos". EGU General Assembly 2012. 14: 13789. Bibcode:2012EGUGA..1413789S.
  35. ^ Bazin, Dominique; Hübner, Helmuth (July 1969). "La règion cuprifère à gisements porphyriques de Kerman (Iran)". Mineralium Deposita (in French). 4 (2): 202. Bibcode:1969MinDe...4..200B. doi:10.1007/BF00208052. S2CID 128623436.
  36. ^ Nejat, Payam; Morsoni, Abdul Kasir; Jomehzadeh, Fatemeh; Behzad, Hamid; Saeed Vesali, Mohamad; Majid, M.Z.Abd. (June 2013). "Iran's achievements in renewable energy during fourth development program in comparison with global trend". Renewable and Sustainable Energy Reviews. 22: 569. doi:10.1016/j.rser.2013.01.042.
  37. ^ Walther, Hansjust W. (December 1960). "Orogen-struktur und Metallverteilung Im östlichen Zagros (Südost-Iran)". Geologische Rundschau (in German). 50 (1): 359. Bibcode:1960GeoRu..50..353W. doi:10.1007/BF01786851. S2CID 128826381.
  38. ^ Frs, N. L. Falcon (March 1975). "From Musandam to the Iranian Makran". The Geographical Journal. 141 (1): 55–58. doi:10.2307/1796945. JSTOR 1796945.
  39. ^ a b c Sholeh et al. 2016, p. 621
  40. ^ a b Berberian, Manuel; King, G. C. P. (February 1981). "Towards a paleogeography and tectonic evolution of Iran". Canadian Journal of Earth Sciences. 18 (2): 255. Bibcode:1981CaJES..18..210B. doi:10.1139/e81-019.
  41. ^ Ghalamghash et al. 2018, p.11
  42. ^ Ghalamghash et al. 2018, p.13
  43. ^ Deshaee et al. 2020, p.1
  44. ^ a b Deshaee et al. 2020, p.2
  45. ^ Deshaee et al. 2020, p.10
  46. ^ Delavari et al. 2022, p.3
  47. ^ Khaiatzadeh, Ahmad; Abbasnejad, Ahmad; Ranjbar, Hojjatolah; Ahmadipour, Hamid; Abbasnejad, Behnam (24 December 2022). "Tephra, Lava flow and Nuee Ardente Hazard Assessment and Zoning of Bazman Volcano, SE Iran". Advanced Applied Geology. 13 (2): 455–468. doi:10.22055/aag.2022.40960.2299. ISSN 2251-7057.
  48. ^ Pang et al. 2014, p. 2157
  49. ^ Falcon, N. L. (June 1974). "An Outline of the Geology of the Iranian Makran". The Geographical Journal. 140 (2): 284–291. doi:10.2307/1797086. JSTOR 1797086.
  50. ^ a b c Ghorbani, Mansour (2013). "Metallogenic and Mining Provinces, Belts and Zones of Iran". The economic geology of Iran mineral deposits and natural resources. Springer Geology. Dordrecht: Springer. pp. 290–291. doi:10.1007/978-94-007-5625-0_6. ISBN 978-94-007-5625-0.
  51. ^ Ghalamghash et al. 2018, p.5
  52. ^ a b Saadat et al. 2011, p. 610
  53. ^ Saadat et al. 2011, p. 617
  54. ^ Saadat et al. 2011, p. 611
  55. ^ Pang et al. 2014, p. 2162
  56. ^ Ghalamghash et al. 2018, p.15
  57. ^ Sholeh et al. 2016, p. 620
  58. ^ Mokhtari, Zahra; Boomeri, Mohammad; Bagheri, Sasan (18 January 2015). "Digital Image Processing and Analysis Techniques for Detection of Hydrothermal Alteration Zones: A Case Study in Siah-Jangal Area, North of Taftan Volcano, Southeastern Iran". Journal of the Indian Society of Remote Sensing. 43 (2): 363–377. doi:10.1007/s12524-014-0422-4. S2CID 129620054. Retrieved 17 August 2016.
  59. ^ Weise 1978, p. 458
  60. ^ Weise 1978, p. 459
  61. ^ Morovati, Karami and Amjas 2020, pp.5-6
  62. ^ Morovati, Karami and Amjas 2020, p.16

Sources

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