Geology, mineralogy, and isotope (Sr, S) geochemistry of the Likak celestite deposit, SW Iran
Abstract Celestite mineralization in the Likak deposit is hosted by Early to Middle Miocene Gachsaran evaporitic formation. The celestite-bearing layers are composed of medium- to coarse-grained celestite crystals with different morphologies in a carbonate groundmass. The presence of carbonate and g...
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| Autor*in: |
Ehya, Farhad [verfasserIn] |
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| Format: |
E-Artikel |
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| Sprache: |
Englisch |
| Erschienen: |
2013 |
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| Schlagwörter: |
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| Anmerkung: |
© Springer-Verlag Berlin Heidelberg 2013 |
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| Übergeordnetes Werk: |
Enthalten in: Carbonates and evaporites - [Dordrecht [u.a.]] : Springer Netherlands, 1986, 28(2013), 4 vom: 12. Feb., Seite 419-431 |
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| Übergeordnetes Werk: |
volume:28 ; year:2013 ; number:4 ; day:12 ; month:02 ; pages:419-431 |
| Links: |
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| DOI / URN: |
10.1007/s13146-013-0137-6 |
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SPR030658462 |
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| 245 | 1 | 0 | |a Geology, mineralogy, and isotope (Sr, S) geochemistry of the Likak celestite deposit, SW Iran |
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| 520 | |a Abstract Celestite mineralization in the Likak deposit is hosted by Early to Middle Miocene Gachsaran evaporitic formation. The celestite-bearing layers are composed of medium- to coarse-grained celestite crystals with different morphologies in a carbonate groundmass. The presence of carbonate and gypsum inclusions within celestite crystals as well as the pseudomorphic habits of some crystals suggests that celestite replaced preexisting carbonate and gypsum. The lithofacies features and faunal assemblage of the host rocks indicate subtidal–supratidal environments of deposition for country rocks. Strontium isotope analyses indicate that Sr originated from Middle Miocene seawater. Sulfur isotopic ratios indicate higher $ δ^{34} $S values in analyzed samples than those of Middle Miocene seawater. These higher values were probably resulted by bacterial reduction of sulfate. Based on petrographic evidences and Sr-isotope ages, it is revealed that mineralization occurred as a late-diagenetic process during deposition of Gachsaran Formation. Taking into account the available data, it can be suggested that precursors of the mineralizing fluids were probably produced by evaporation of seawater in a coastal sabkha setting. As these brines entered into underlying sediments, they leached considerable amounts of Sr from host sediments. Once these Sr-enriched fluids discharged back up into overlying beds containing gypsum and carbonate materials, celestite precipitation took place by replacement of the preexisting minerals as well as by mixing of the mineralizing fluids with sulfate-enriched brines entrapped within the beds. | ||
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| 650 | 4 | |a Strontium isotopes |7 (dpeaa)DE-He213 | |
| 650 | 4 | |a Sulfur isotopes |7 (dpeaa)DE-He213 | |
| 650 | 4 | |a Iran |7 (dpeaa)DE-He213 | |
| 700 | 1 | |a Shakouri, Behnaz |4 aut | |
| 700 | 1 | |a Rafi, Mehrdad |4 aut | |
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10.1007/s13146-013-0137-6 doi (DE-627)SPR030658462 (SPR)s13146-013-0137-6-e DE-627 ger DE-627 rakwb eng Ehya, Farhad verfasserin aut Geology, mineralogy, and isotope (Sr, S) geochemistry of the Likak celestite deposit, SW Iran 2013 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Springer-Verlag Berlin Heidelberg 2013 Abstract Celestite mineralization in the Likak deposit is hosted by Early to Middle Miocene Gachsaran evaporitic formation. The celestite-bearing layers are composed of medium- to coarse-grained celestite crystals with different morphologies in a carbonate groundmass. The presence of carbonate and gypsum inclusions within celestite crystals as well as the pseudomorphic habits of some crystals suggests that celestite replaced preexisting carbonate and gypsum. The lithofacies features and faunal assemblage of the host rocks indicate subtidal–supratidal environments of deposition for country rocks. Strontium isotope analyses indicate that Sr originated from Middle Miocene seawater. Sulfur isotopic ratios indicate higher $ δ^{34} $S values in analyzed samples than those of Middle Miocene seawater. These higher values were probably resulted by bacterial reduction of sulfate. Based on petrographic evidences and Sr-isotope ages, it is revealed that mineralization occurred as a late-diagenetic process during deposition of Gachsaran Formation. Taking into account the available data, it can be suggested that precursors of the mineralizing fluids were probably produced by evaporation of seawater in a coastal sabkha setting. As these brines entered into underlying sediments, they leached considerable amounts of Sr from host sediments. Once these Sr-enriched fluids discharged back up into overlying beds containing gypsum and carbonate materials, celestite precipitation took place by replacement of the preexisting minerals as well as by mixing of the mineralizing fluids with sulfate-enriched brines entrapped within the beds. Celestite (dpeaa)DE-He213 Gachsaran Formation (dpeaa)DE-He213 Strontium isotopes (dpeaa)DE-He213 Sulfur isotopes (dpeaa)DE-He213 Iran (dpeaa)DE-He213 Shakouri, Behnaz aut Rafi, Mehrdad aut Enthalten in Carbonates and evaporites [Dordrecht [u.a.]] : Springer Netherlands, 1986 28(2013), 4 vom: 12. Feb., Seite 419-431 (DE-627)617505799 (DE-600)2533885-7 1878-5212 nnns volume:28 year:2013 number:4 day:12 month:02 pages:419-431 https://dx.doi.org/10.1007/s13146-013-0137-6 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4326 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 AR 28 2013 4 12 02 419-431 |
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10.1007/s13146-013-0137-6 doi (DE-627)SPR030658462 (SPR)s13146-013-0137-6-e DE-627 ger DE-627 rakwb eng Ehya, Farhad verfasserin aut Geology, mineralogy, and isotope (Sr, S) geochemistry of the Likak celestite deposit, SW Iran 2013 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Springer-Verlag Berlin Heidelberg 2013 Abstract Celestite mineralization in the Likak deposit is hosted by Early to Middle Miocene Gachsaran evaporitic formation. The celestite-bearing layers are composed of medium- to coarse-grained celestite crystals with different morphologies in a carbonate groundmass. The presence of carbonate and gypsum inclusions within celestite crystals as well as the pseudomorphic habits of some crystals suggests that celestite replaced preexisting carbonate and gypsum. The lithofacies features and faunal assemblage of the host rocks indicate subtidal–supratidal environments of deposition for country rocks. Strontium isotope analyses indicate that Sr originated from Middle Miocene seawater. Sulfur isotopic ratios indicate higher $ δ^{34} $S values in analyzed samples than those of Middle Miocene seawater. These higher values were probably resulted by bacterial reduction of sulfate. Based on petrographic evidences and Sr-isotope ages, it is revealed that mineralization occurred as a late-diagenetic process during deposition of Gachsaran Formation. Taking into account the available data, it can be suggested that precursors of the mineralizing fluids were probably produced by evaporation of seawater in a coastal sabkha setting. As these brines entered into underlying sediments, they leached considerable amounts of Sr from host sediments. Once these Sr-enriched fluids discharged back up into overlying beds containing gypsum and carbonate materials, celestite precipitation took place by replacement of the preexisting minerals as well as by mixing of the mineralizing fluids with sulfate-enriched brines entrapped within the beds. Celestite (dpeaa)DE-He213 Gachsaran Formation (dpeaa)DE-He213 Strontium isotopes (dpeaa)DE-He213 Sulfur isotopes (dpeaa)DE-He213 Iran (dpeaa)DE-He213 Shakouri, Behnaz aut Rafi, Mehrdad aut Enthalten in Carbonates and evaporites [Dordrecht [u.a.]] : Springer Netherlands, 1986 28(2013), 4 vom: 12. Feb., Seite 419-431 (DE-627)617505799 (DE-600)2533885-7 1878-5212 nnns volume:28 year:2013 number:4 day:12 month:02 pages:419-431 https://dx.doi.org/10.1007/s13146-013-0137-6 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4326 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 AR 28 2013 4 12 02 419-431 |
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10.1007/s13146-013-0137-6 doi (DE-627)SPR030658462 (SPR)s13146-013-0137-6-e DE-627 ger DE-627 rakwb eng Ehya, Farhad verfasserin aut Geology, mineralogy, and isotope (Sr, S) geochemistry of the Likak celestite deposit, SW Iran 2013 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Springer-Verlag Berlin Heidelberg 2013 Abstract Celestite mineralization in the Likak deposit is hosted by Early to Middle Miocene Gachsaran evaporitic formation. The celestite-bearing layers are composed of medium- to coarse-grained celestite crystals with different morphologies in a carbonate groundmass. The presence of carbonate and gypsum inclusions within celestite crystals as well as the pseudomorphic habits of some crystals suggests that celestite replaced preexisting carbonate and gypsum. The lithofacies features and faunal assemblage of the host rocks indicate subtidal–supratidal environments of deposition for country rocks. Strontium isotope analyses indicate that Sr originated from Middle Miocene seawater. Sulfur isotopic ratios indicate higher $ δ^{34} $S values in analyzed samples than those of Middle Miocene seawater. These higher values were probably resulted by bacterial reduction of sulfate. Based on petrographic evidences and Sr-isotope ages, it is revealed that mineralization occurred as a late-diagenetic process during deposition of Gachsaran Formation. Taking into account the available data, it can be suggested that precursors of the mineralizing fluids were probably produced by evaporation of seawater in a coastal sabkha setting. As these brines entered into underlying sediments, they leached considerable amounts of Sr from host sediments. Once these Sr-enriched fluids discharged back up into overlying beds containing gypsum and carbonate materials, celestite precipitation took place by replacement of the preexisting minerals as well as by mixing of the mineralizing fluids with sulfate-enriched brines entrapped within the beds. Celestite (dpeaa)DE-He213 Gachsaran Formation (dpeaa)DE-He213 Strontium isotopes (dpeaa)DE-He213 Sulfur isotopes (dpeaa)DE-He213 Iran (dpeaa)DE-He213 Shakouri, Behnaz aut Rafi, Mehrdad aut Enthalten in Carbonates and evaporites [Dordrecht [u.a.]] : Springer Netherlands, 1986 28(2013), 4 vom: 12. Feb., Seite 419-431 (DE-627)617505799 (DE-600)2533885-7 1878-5212 nnns volume:28 year:2013 number:4 day:12 month:02 pages:419-431 https://dx.doi.org/10.1007/s13146-013-0137-6 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4326 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 AR 28 2013 4 12 02 419-431 |
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10.1007/s13146-013-0137-6 doi (DE-627)SPR030658462 (SPR)s13146-013-0137-6-e DE-627 ger DE-627 rakwb eng Ehya, Farhad verfasserin aut Geology, mineralogy, and isotope (Sr, S) geochemistry of the Likak celestite deposit, SW Iran 2013 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Springer-Verlag Berlin Heidelberg 2013 Abstract Celestite mineralization in the Likak deposit is hosted by Early to Middle Miocene Gachsaran evaporitic formation. The celestite-bearing layers are composed of medium- to coarse-grained celestite crystals with different morphologies in a carbonate groundmass. The presence of carbonate and gypsum inclusions within celestite crystals as well as the pseudomorphic habits of some crystals suggests that celestite replaced preexisting carbonate and gypsum. The lithofacies features and faunal assemblage of the host rocks indicate subtidal–supratidal environments of deposition for country rocks. Strontium isotope analyses indicate that Sr originated from Middle Miocene seawater. Sulfur isotopic ratios indicate higher $ δ^{34} $S values in analyzed samples than those of Middle Miocene seawater. These higher values were probably resulted by bacterial reduction of sulfate. Based on petrographic evidences and Sr-isotope ages, it is revealed that mineralization occurred as a late-diagenetic process during deposition of Gachsaran Formation. Taking into account the available data, it can be suggested that precursors of the mineralizing fluids were probably produced by evaporation of seawater in a coastal sabkha setting. As these brines entered into underlying sediments, they leached considerable amounts of Sr from host sediments. Once these Sr-enriched fluids discharged back up into overlying beds containing gypsum and carbonate materials, celestite precipitation took place by replacement of the preexisting minerals as well as by mixing of the mineralizing fluids with sulfate-enriched brines entrapped within the beds. Celestite (dpeaa)DE-He213 Gachsaran Formation (dpeaa)DE-He213 Strontium isotopes (dpeaa)DE-He213 Sulfur isotopes (dpeaa)DE-He213 Iran (dpeaa)DE-He213 Shakouri, Behnaz aut Rafi, Mehrdad aut Enthalten in Carbonates and evaporites [Dordrecht [u.a.]] : Springer Netherlands, 1986 28(2013), 4 vom: 12. Feb., Seite 419-431 (DE-627)617505799 (DE-600)2533885-7 1878-5212 nnns volume:28 year:2013 number:4 day:12 month:02 pages:419-431 https://dx.doi.org/10.1007/s13146-013-0137-6 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4326 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 AR 28 2013 4 12 02 419-431 |
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10.1007/s13146-013-0137-6 doi (DE-627)SPR030658462 (SPR)s13146-013-0137-6-e DE-627 ger DE-627 rakwb eng Ehya, Farhad verfasserin aut Geology, mineralogy, and isotope (Sr, S) geochemistry of the Likak celestite deposit, SW Iran 2013 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Springer-Verlag Berlin Heidelberg 2013 Abstract Celestite mineralization in the Likak deposit is hosted by Early to Middle Miocene Gachsaran evaporitic formation. The celestite-bearing layers are composed of medium- to coarse-grained celestite crystals with different morphologies in a carbonate groundmass. The presence of carbonate and gypsum inclusions within celestite crystals as well as the pseudomorphic habits of some crystals suggests that celestite replaced preexisting carbonate and gypsum. The lithofacies features and faunal assemblage of the host rocks indicate subtidal–supratidal environments of deposition for country rocks. Strontium isotope analyses indicate that Sr originated from Middle Miocene seawater. Sulfur isotopic ratios indicate higher $ δ^{34} $S values in analyzed samples than those of Middle Miocene seawater. These higher values were probably resulted by bacterial reduction of sulfate. Based on petrographic evidences and Sr-isotope ages, it is revealed that mineralization occurred as a late-diagenetic process during deposition of Gachsaran Formation. Taking into account the available data, it can be suggested that precursors of the mineralizing fluids were probably produced by evaporation of seawater in a coastal sabkha setting. As these brines entered into underlying sediments, they leached considerable amounts of Sr from host sediments. Once these Sr-enriched fluids discharged back up into overlying beds containing gypsum and carbonate materials, celestite precipitation took place by replacement of the preexisting minerals as well as by mixing of the mineralizing fluids with sulfate-enriched brines entrapped within the beds. Celestite (dpeaa)DE-He213 Gachsaran Formation (dpeaa)DE-He213 Strontium isotopes (dpeaa)DE-He213 Sulfur isotopes (dpeaa)DE-He213 Iran (dpeaa)DE-He213 Shakouri, Behnaz aut Rafi, Mehrdad aut Enthalten in Carbonates and evaporites [Dordrecht [u.a.]] : Springer Netherlands, 1986 28(2013), 4 vom: 12. Feb., Seite 419-431 (DE-627)617505799 (DE-600)2533885-7 1878-5212 nnns volume:28 year:2013 number:4 day:12 month:02 pages:419-431 https://dx.doi.org/10.1007/s13146-013-0137-6 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4326 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 AR 28 2013 4 12 02 419-431 |
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Enthalten in Carbonates and evaporites 28(2013), 4 vom: 12. Feb., Seite 419-431 volume:28 year:2013 number:4 day:12 month:02 pages:419-431 |
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Ehya, Farhad @@aut@@ Shakouri, Behnaz @@aut@@ Rafi, Mehrdad @@aut@@ |
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The celestite-bearing layers are composed of medium- to coarse-grained celestite crystals with different morphologies in a carbonate groundmass. The presence of carbonate and gypsum inclusions within celestite crystals as well as the pseudomorphic habits of some crystals suggests that celestite replaced preexisting carbonate and gypsum. The lithofacies features and faunal assemblage of the host rocks indicate subtidal–supratidal environments of deposition for country rocks. Strontium isotope analyses indicate that Sr originated from Middle Miocene seawater. Sulfur isotopic ratios indicate higher $ δ^{34} $S values in analyzed samples than those of Middle Miocene seawater. These higher values were probably resulted by bacterial reduction of sulfate. Based on petrographic evidences and Sr-isotope ages, it is revealed that mineralization occurred as a late-diagenetic process during deposition of Gachsaran Formation. 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Ehya, Farhad |
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Ehya, Farhad misc Celestite misc Gachsaran Formation misc Strontium isotopes misc Sulfur isotopes misc Iran Geology, mineralogy, and isotope (Sr, S) geochemistry of the Likak celestite deposit, SW Iran |
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Geology, mineralogy, and isotope (Sr, S) geochemistry of the Likak celestite deposit, SW Iran Celestite (dpeaa)DE-He213 Gachsaran Formation (dpeaa)DE-He213 Strontium isotopes (dpeaa)DE-He213 Sulfur isotopes (dpeaa)DE-He213 Iran (dpeaa)DE-He213 |
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geology, mineralogy, and isotope (sr, s) geochemistry of the likak celestite deposit, sw iran |
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Geology, mineralogy, and isotope (Sr, S) geochemistry of the Likak celestite deposit, SW Iran |
| abstract |
Abstract Celestite mineralization in the Likak deposit is hosted by Early to Middle Miocene Gachsaran evaporitic formation. The celestite-bearing layers are composed of medium- to coarse-grained celestite crystals with different morphologies in a carbonate groundmass. The presence of carbonate and gypsum inclusions within celestite crystals as well as the pseudomorphic habits of some crystals suggests that celestite replaced preexisting carbonate and gypsum. The lithofacies features and faunal assemblage of the host rocks indicate subtidal–supratidal environments of deposition for country rocks. Strontium isotope analyses indicate that Sr originated from Middle Miocene seawater. Sulfur isotopic ratios indicate higher $ δ^{34} $S values in analyzed samples than those of Middle Miocene seawater. These higher values were probably resulted by bacterial reduction of sulfate. Based on petrographic evidences and Sr-isotope ages, it is revealed that mineralization occurred as a late-diagenetic process during deposition of Gachsaran Formation. Taking into account the available data, it can be suggested that precursors of the mineralizing fluids were probably produced by evaporation of seawater in a coastal sabkha setting. As these brines entered into underlying sediments, they leached considerable amounts of Sr from host sediments. Once these Sr-enriched fluids discharged back up into overlying beds containing gypsum and carbonate materials, celestite precipitation took place by replacement of the preexisting minerals as well as by mixing of the mineralizing fluids with sulfate-enriched brines entrapped within the beds. © Springer-Verlag Berlin Heidelberg 2013 |
| abstractGer |
Abstract Celestite mineralization in the Likak deposit is hosted by Early to Middle Miocene Gachsaran evaporitic formation. The celestite-bearing layers are composed of medium- to coarse-grained celestite crystals with different morphologies in a carbonate groundmass. The presence of carbonate and gypsum inclusions within celestite crystals as well as the pseudomorphic habits of some crystals suggests that celestite replaced preexisting carbonate and gypsum. The lithofacies features and faunal assemblage of the host rocks indicate subtidal–supratidal environments of deposition for country rocks. Strontium isotope analyses indicate that Sr originated from Middle Miocene seawater. Sulfur isotopic ratios indicate higher $ δ^{34} $S values in analyzed samples than those of Middle Miocene seawater. These higher values were probably resulted by bacterial reduction of sulfate. Based on petrographic evidences and Sr-isotope ages, it is revealed that mineralization occurred as a late-diagenetic process during deposition of Gachsaran Formation. Taking into account the available data, it can be suggested that precursors of the mineralizing fluids were probably produced by evaporation of seawater in a coastal sabkha setting. As these brines entered into underlying sediments, they leached considerable amounts of Sr from host sediments. Once these Sr-enriched fluids discharged back up into overlying beds containing gypsum and carbonate materials, celestite precipitation took place by replacement of the preexisting minerals as well as by mixing of the mineralizing fluids with sulfate-enriched brines entrapped within the beds. © Springer-Verlag Berlin Heidelberg 2013 |
| abstract_unstemmed |
Abstract Celestite mineralization in the Likak deposit is hosted by Early to Middle Miocene Gachsaran evaporitic formation. The celestite-bearing layers are composed of medium- to coarse-grained celestite crystals with different morphologies in a carbonate groundmass. The presence of carbonate and gypsum inclusions within celestite crystals as well as the pseudomorphic habits of some crystals suggests that celestite replaced preexisting carbonate and gypsum. The lithofacies features and faunal assemblage of the host rocks indicate subtidal–supratidal environments of deposition for country rocks. Strontium isotope analyses indicate that Sr originated from Middle Miocene seawater. Sulfur isotopic ratios indicate higher $ δ^{34} $S values in analyzed samples than those of Middle Miocene seawater. These higher values were probably resulted by bacterial reduction of sulfate. Based on petrographic evidences and Sr-isotope ages, it is revealed that mineralization occurred as a late-diagenetic process during deposition of Gachsaran Formation. Taking into account the available data, it can be suggested that precursors of the mineralizing fluids were probably produced by evaporation of seawater in a coastal sabkha setting. As these brines entered into underlying sediments, they leached considerable amounts of Sr from host sediments. Once these Sr-enriched fluids discharged back up into overlying beds containing gypsum and carbonate materials, celestite precipitation took place by replacement of the preexisting minerals as well as by mixing of the mineralizing fluids with sulfate-enriched brines entrapped within the beds. © Springer-Verlag Berlin Heidelberg 2013 |
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Geology, mineralogy, and isotope (Sr, S) geochemistry of the Likak celestite deposit, SW Iran |
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https://dx.doi.org/10.1007/s13146-013-0137-6 |
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Shakouri, Behnaz Rafi, Mehrdad |
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10.1007/s13146-013-0137-6 |
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2024-07-03T19:23:07.654Z |
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| score |
7.401597 |