An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts

Abstract Fluorine and chlorine affect phase stabilities in magmatic rocks. We present phase equilibrium experiments investigating a peralkaline and iron-rich phonolitic composition with variable F and Cl contents. The starting composition represents a dyke rock, which is a possible parental melt to the peralkaline Ilímaussaq plutonic complex (South Greenland). Experiments were performed at 100 MPa, 1,000–650 °C and low oxygen fugacity adjusted with graphite-lined gold capsules in an internally heated argon pressure vessel and rapid quench cold seal pressure vessels. To cover this large T interval, we applied a two-step fractional crystallization strategy where glasses representing residual melt compositions at 800 °C were synthesized as starting material for consecutive experiments at lower T. In these experiments, oxidized starting glasses allocate oxygen by reduction of ferric iron and up to 1.2 wt% dissolved OH form through reaction with hydrogen provided by the pressure medium ($ H_{2} $O) in initially dry experiments. For OH determination, hydrated super-liquidus experiments in Au capsules were performed to calibrate the extinction coefficient for the fundamental OH stretching vibration using infrared spectroscopy (ε3,415 = 48 ± 3 L $ mol^{−1} $ $ cm^{−1} $). Observed mineral phases in our experiments are titanomagnetite, fayalitic olivine, clinopyroxene, aenigmatite ($ Na_{2} %$ Fe_{5} %$ TiSi_{6} %$ O_{20} $), alkali feldspar and nepheline (±native iron) coexisting with residual melt. Above 1.5 wt% $ F_{melt} $ concentrations, fluorite ($ CaF_{2} $) and hiortdahlite ($ Ca_{6} %$ Zr_{2} %$ Si_{4} %$ O_{16} %$ F_{4} $) are stable in favor of Ca-rich clinopyroxene. Sodalite ($ Na_{8} %$ Al_{6} %$ Si_{6} %$ O_{24} %$ Cl_{2} $) and eudialyte ($ Na_{15} %$ Ca_{6} %$ Fe_{3} %$ Zr_{3} %$ Si_{26} %$ O_{73} $(OH)3$ Cl_{2} $) form at $ Cl_{melt} $ concentrations of 0.2–0.5 wt% (depending on T) and $ ZrO_{2 melt} $ concentrations >0.7 wt% are additionally needed to stabilize eudialyte and hiortdahlite. Therefore, F and Cl may become compatible in such systems and have the potential to influence F/Cl melt ratios in evolving magmas. Ausführliche Beschreibung

Gespeichert in:

Autor*in:	Giehl, Christopher [verfasserIn] Marks, Michael A. W. [verfasserIn] Nowak, Marcus [verfasserIn]

Format:	E-Artikel
Sprache:	Englisch

Erschienen:	2014

Schlagwörter:	Phase equilibrium experiment Liquid line of descent Halogens Phonolite Ilímaussaq Agpaitic Eudialyte Infrared spectroscopy Extinction coefficient

Übergeordnetes Werk:	Enthalten in: Contributions to mineralogy and petrology - Berlin : Springer, 1947, 167(2014), 3 vom: 25. Feb.
Übergeordnetes Werk:	volume:167 ; year:2014 ; number:3 ; day:25 ; month:02

Links:	Volltext

DOI / URN:	10.1007/s00410-014-0977-7

Katalog-ID:	SPR005254256

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245	1	3	\|a An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts
264		1	\|c 2014
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520			\|a Abstract Fluorine and chlorine affect phase stabilities in magmatic rocks. We present phase equilibrium experiments investigating a peralkaline and iron-rich phonolitic composition with variable F and Cl contents. The starting composition represents a dyke rock, which is a possible parental melt to the peralkaline Ilímaussaq plutonic complex (South Greenland). Experiments were performed at 100 MPa, 1,000–650 °C and low oxygen fugacity adjusted with graphite-lined gold capsules in an internally heated argon pressure vessel and rapid quench cold seal pressure vessels. To cover this large T interval, we applied a two-step fractional crystallization strategy where glasses representing residual melt compositions at 800 °C were synthesized as starting material for consecutive experiments at lower T. In these experiments, oxidized starting glasses allocate oxygen by reduction of ferric iron and up to 1.2 wt% dissolved OH form through reaction with hydrogen provided by the pressure medium ($ H_{2} $O) in initially dry experiments. For OH determination, hydrated super-liquidus experiments in Au capsules were performed to calibrate the extinction coefficient for the fundamental OH stretching vibration using infrared spectroscopy (ε3,415 = 48 ± 3 L $ mol^{−1} $ $ cm^{−1} $). Observed mineral phases in our experiments are titanomagnetite, fayalitic olivine, clinopyroxene, aenigmatite ($ Na_{2} %$ Fe_{5} %$ TiSi_{6} %$ O_{20} $), alkali feldspar and nepheline (±native iron) coexisting with residual melt. Above 1.5 wt% $ F_{melt} $ concentrations, fluorite ($ CaF_{2} $) and hiortdahlite ($ Ca_{6} %$ Zr_{2} %$ Si_{4} %$ O_{16} %$ F_{4} $) are stable in favor of Ca-rich clinopyroxene. Sodalite ($ Na_{8} %$ Al_{6} %$ Si_{6} %$ O_{24} %$ Cl_{2} $) and eudialyte ($ Na_{15} %$ Ca_{6} %$ Fe_{3} %$ Zr_{3} %$ Si_{26} %$ O_{73} $(OH)3$ Cl_{2} $) form at $ Cl_{melt} $ concentrations of 0.2–0.5 wt% (depending on T) and $ ZrO_{2 melt} $ concentrations >0.7 wt% are additionally needed to stabilize eudialyte and hiortdahlite. Therefore, F and Cl may become compatible in such systems and have the potential to influence F/Cl melt ratios in evolving magmas.
650		4	\|a Phase equilibrium experiment \|7 (dpeaa)DE-He213
650		4	\|a Liquid line of descent \|7 (dpeaa)DE-He213
650		4	\|a Halogens \|7 (dpeaa)DE-He213
650		4	\|a Phonolite \|7 (dpeaa)DE-He213
650		4	\|a Ilímaussaq \|7 (dpeaa)DE-He213
650		4	\|a Agpaitic \|7 (dpeaa)DE-He213
650		4	\|a Eudialyte \|7 (dpeaa)DE-He213
650		4	\|a Infrared spectroscopy \|7 (dpeaa)DE-He213
650		4	\|a Extinction coefficient \|7 (dpeaa)DE-He213
700	1		\|a Marks, Michael A. W. \|e verfasserin \|4 aut
700	1		\|a Nowak, Marcus \|e verfasserin \|4 aut
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publishDate	2014
allfields	10.1007/s00410-014-0977-7 doi (DE-627)SPR005254256 (SPR)s00410-014-0977-7-e DE-627 ger DE-627 rakwb eng 550 ASE 38.25 bkl 38.30 bkl Giehl, Christopher verfasserin aut An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts 2014 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Fluorine and chlorine affect phase stabilities in magmatic rocks. We present phase equilibrium experiments investigating a peralkaline and iron-rich phonolitic composition with variable F and Cl contents. The starting composition represents a dyke rock, which is a possible parental melt to the peralkaline Ilímaussaq plutonic complex (South Greenland). Experiments were performed at 100 MPa, 1,000–650 °C and low oxygen fugacity adjusted with graphite-lined gold capsules in an internally heated argon pressure vessel and rapid quench cold seal pressure vessels. To cover this large T interval, we applied a two-step fractional crystallization strategy where glasses representing residual melt compositions at 800 °C were synthesized as starting material for consecutive experiments at lower T. In these experiments, oxidized starting glasses allocate oxygen by reduction of ferric iron and up to 1.2 wt% dissolved OH form through reaction with hydrogen provided by the pressure medium ($ H_{2} $O) in initially dry experiments. For OH determination, hydrated super-liquidus experiments in Au capsules were performed to calibrate the extinction coefficient for the fundamental OH stretching vibration using infrared spectroscopy (ε3,415 = 48 ± 3 L $ mol^{−1} $ $ cm^{−1} $). Observed mineral phases in our experiments are titanomagnetite, fayalitic olivine, clinopyroxene, aenigmatite ($ Na_{2} %$ Fe_{5} %$ TiSi_{6} %$ O_{20} $), alkali feldspar and nepheline (±native iron) coexisting with residual melt. Above 1.5 wt% $ F_{melt} $ concentrations, fluorite ($ CaF_{2} $) and hiortdahlite ($ Ca_{6} %$ Zr_{2} %$ Si_{4} %$ O_{16} %$ F_{4} $) are stable in favor of Ca-rich clinopyroxene. Sodalite ($ Na_{8} %$ Al_{6} %$ Si_{6} %$ O_{24} %$ Cl_{2} $) and eudialyte ($ Na_{15} %$ Ca_{6} %$ Fe_{3} %$ Zr_{3} %$ Si_{26} %$ O_{73} $(OH)3$ Cl_{2} $) form at $ Cl_{melt} $ concentrations of 0.2–0.5 wt% (depending on T) and $ ZrO_{2 melt} $ concentrations >0.7 wt% are additionally needed to stabilize eudialyte and hiortdahlite. Therefore, F and Cl may become compatible in such systems and have the potential to influence F/Cl melt ratios in evolving magmas. Phase equilibrium experiment (dpeaa)DE-He213 Liquid line of descent (dpeaa)DE-He213 Halogens (dpeaa)DE-He213 Phonolite (dpeaa)DE-He213 Ilímaussaq (dpeaa)DE-He213 Agpaitic (dpeaa)DE-He213 Eudialyte (dpeaa)DE-He213 Infrared spectroscopy (dpeaa)DE-He213 Extinction coefficient (dpeaa)DE-He213 Marks, Michael A. W. verfasserin aut Nowak, Marcus verfasserin aut Enthalten in Contributions to mineralogy and petrology Berlin : Springer, 1947 167(2014), 3 vom: 25. Feb. (DE-627)25372208X (DE-600)1458979-5 1432-0967 nnns volume:167 year:2014 number:3 day:25 month:02 https://dx.doi.org/10.1007/s00410-014-0977-7 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE 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_267 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_2056 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_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 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_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.25 ASE 38.30 ASE AR 167 2014 3 25 02
spelling	10.1007/s00410-014-0977-7 doi (DE-627)SPR005254256 (SPR)s00410-014-0977-7-e DE-627 ger DE-627 rakwb eng 550 ASE 38.25 bkl 38.30 bkl Giehl, Christopher verfasserin aut An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts 2014 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Fluorine and chlorine affect phase stabilities in magmatic rocks. We present phase equilibrium experiments investigating a peralkaline and iron-rich phonolitic composition with variable F and Cl contents. The starting composition represents a dyke rock, which is a possible parental melt to the peralkaline Ilímaussaq plutonic complex (South Greenland). Experiments were performed at 100 MPa, 1,000–650 °C and low oxygen fugacity adjusted with graphite-lined gold capsules in an internally heated argon pressure vessel and rapid quench cold seal pressure vessels. To cover this large T interval, we applied a two-step fractional crystallization strategy where glasses representing residual melt compositions at 800 °C were synthesized as starting material for consecutive experiments at lower T. In these experiments, oxidized starting glasses allocate oxygen by reduction of ferric iron and up to 1.2 wt% dissolved OH form through reaction with hydrogen provided by the pressure medium ($ H_{2} $O) in initially dry experiments. For OH determination, hydrated super-liquidus experiments in Au capsules were performed to calibrate the extinction coefficient for the fundamental OH stretching vibration using infrared spectroscopy (ε3,415 = 48 ± 3 L $ mol^{−1} $ $ cm^{−1} $). Observed mineral phases in our experiments are titanomagnetite, fayalitic olivine, clinopyroxene, aenigmatite ($ Na_{2} %$ Fe_{5} %$ TiSi_{6} %$ O_{20} $), alkali feldspar and nepheline (±native iron) coexisting with residual melt. Above 1.5 wt% $ F_{melt} $ concentrations, fluorite ($ CaF_{2} $) and hiortdahlite ($ Ca_{6} %$ Zr_{2} %$ Si_{4} %$ O_{16} %$ F_{4} $) are stable in favor of Ca-rich clinopyroxene. Sodalite ($ Na_{8} %$ Al_{6} %$ Si_{6} %$ O_{24} %$ Cl_{2} $) and eudialyte ($ Na_{15} %$ Ca_{6} %$ Fe_{3} %$ Zr_{3} %$ Si_{26} %$ O_{73} $(OH)3$ Cl_{2} $) form at $ Cl_{melt} $ concentrations of 0.2–0.5 wt% (depending on T) and $ ZrO_{2 melt} $ concentrations >0.7 wt% are additionally needed to stabilize eudialyte and hiortdahlite. Therefore, F and Cl may become compatible in such systems and have the potential to influence F/Cl melt ratios in evolving magmas. Phase equilibrium experiment (dpeaa)DE-He213 Liquid line of descent (dpeaa)DE-He213 Halogens (dpeaa)DE-He213 Phonolite (dpeaa)DE-He213 Ilímaussaq (dpeaa)DE-He213 Agpaitic (dpeaa)DE-He213 Eudialyte (dpeaa)DE-He213 Infrared spectroscopy (dpeaa)DE-He213 Extinction coefficient (dpeaa)DE-He213 Marks, Michael A. W. verfasserin aut Nowak, Marcus verfasserin aut Enthalten in Contributions to mineralogy and petrology Berlin : Springer, 1947 167(2014), 3 vom: 25. Feb. (DE-627)25372208X (DE-600)1458979-5 1432-0967 nnns volume:167 year:2014 number:3 day:25 month:02 https://dx.doi.org/10.1007/s00410-014-0977-7 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE 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_267 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_2056 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_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 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_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.25 ASE 38.30 ASE AR 167 2014 3 25 02
allfields_unstemmed	10.1007/s00410-014-0977-7 doi (DE-627)SPR005254256 (SPR)s00410-014-0977-7-e DE-627 ger DE-627 rakwb eng 550 ASE 38.25 bkl 38.30 bkl Giehl, Christopher verfasserin aut An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts 2014 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Fluorine and chlorine affect phase stabilities in magmatic rocks. We present phase equilibrium experiments investigating a peralkaline and iron-rich phonolitic composition with variable F and Cl contents. The starting composition represents a dyke rock, which is a possible parental melt to the peralkaline Ilímaussaq plutonic complex (South Greenland). Experiments were performed at 100 MPa, 1,000–650 °C and low oxygen fugacity adjusted with graphite-lined gold capsules in an internally heated argon pressure vessel and rapid quench cold seal pressure vessels. To cover this large T interval, we applied a two-step fractional crystallization strategy where glasses representing residual melt compositions at 800 °C were synthesized as starting material for consecutive experiments at lower T. In these experiments, oxidized starting glasses allocate oxygen by reduction of ferric iron and up to 1.2 wt% dissolved OH form through reaction with hydrogen provided by the pressure medium ($ H_{2} $O) in initially dry experiments. For OH determination, hydrated super-liquidus experiments in Au capsules were performed to calibrate the extinction coefficient for the fundamental OH stretching vibration using infrared spectroscopy (ε3,415 = 48 ± 3 L $ mol^{−1} $ $ cm^{−1} $). Observed mineral phases in our experiments are titanomagnetite, fayalitic olivine, clinopyroxene, aenigmatite ($ Na_{2} %$ Fe_{5} %$ TiSi_{6} %$ O_{20} $), alkali feldspar and nepheline (±native iron) coexisting with residual melt. Above 1.5 wt% $ F_{melt} $ concentrations, fluorite ($ CaF_{2} $) and hiortdahlite ($ Ca_{6} %$ Zr_{2} %$ Si_{4} %$ O_{16} %$ F_{4} $) are stable in favor of Ca-rich clinopyroxene. Sodalite ($ Na_{8} %$ Al_{6} %$ Si_{6} %$ O_{24} %$ Cl_{2} $) and eudialyte ($ Na_{15} %$ Ca_{6} %$ Fe_{3} %$ Zr_{3} %$ Si_{26} %$ O_{73} $(OH)3$ Cl_{2} $) form at $ Cl_{melt} $ concentrations of 0.2–0.5 wt% (depending on T) and $ ZrO_{2 melt} $ concentrations >0.7 wt% are additionally needed to stabilize eudialyte and hiortdahlite. Therefore, F and Cl may become compatible in such systems and have the potential to influence F/Cl melt ratios in evolving magmas. Phase equilibrium experiment (dpeaa)DE-He213 Liquid line of descent (dpeaa)DE-He213 Halogens (dpeaa)DE-He213 Phonolite (dpeaa)DE-He213 Ilímaussaq (dpeaa)DE-He213 Agpaitic (dpeaa)DE-He213 Eudialyte (dpeaa)DE-He213 Infrared spectroscopy (dpeaa)DE-He213 Extinction coefficient (dpeaa)DE-He213 Marks, Michael A. W. verfasserin aut Nowak, Marcus verfasserin aut Enthalten in Contributions to mineralogy and petrology Berlin : Springer, 1947 167(2014), 3 vom: 25. Feb. (DE-627)25372208X (DE-600)1458979-5 1432-0967 nnns volume:167 year:2014 number:3 day:25 month:02 https://dx.doi.org/10.1007/s00410-014-0977-7 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE 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_267 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_2056 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_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 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_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.25 ASE 38.30 ASE AR 167 2014 3 25 02
allfieldsGer	10.1007/s00410-014-0977-7 doi (DE-627)SPR005254256 (SPR)s00410-014-0977-7-e DE-627 ger DE-627 rakwb eng 550 ASE 38.25 bkl 38.30 bkl Giehl, Christopher verfasserin aut An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts 2014 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Fluorine and chlorine affect phase stabilities in magmatic rocks. We present phase equilibrium experiments investigating a peralkaline and iron-rich phonolitic composition with variable F and Cl contents. The starting composition represents a dyke rock, which is a possible parental melt to the peralkaline Ilímaussaq plutonic complex (South Greenland). Experiments were performed at 100 MPa, 1,000–650 °C and low oxygen fugacity adjusted with graphite-lined gold capsules in an internally heated argon pressure vessel and rapid quench cold seal pressure vessels. To cover this large T interval, we applied a two-step fractional crystallization strategy where glasses representing residual melt compositions at 800 °C were synthesized as starting material for consecutive experiments at lower T. In these experiments, oxidized starting glasses allocate oxygen by reduction of ferric iron and up to 1.2 wt% dissolved OH form through reaction with hydrogen provided by the pressure medium ($ H_{2} $O) in initially dry experiments. For OH determination, hydrated super-liquidus experiments in Au capsules were performed to calibrate the extinction coefficient for the fundamental OH stretching vibration using infrared spectroscopy (ε3,415 = 48 ± 3 L $ mol^{−1} $ $ cm^{−1} $). Observed mineral phases in our experiments are titanomagnetite, fayalitic olivine, clinopyroxene, aenigmatite ($ Na_{2} %$ Fe_{5} %$ TiSi_{6} %$ O_{20} $), alkali feldspar and nepheline (±native iron) coexisting with residual melt. Above 1.5 wt% $ F_{melt} $ concentrations, fluorite ($ CaF_{2} $) and hiortdahlite ($ Ca_{6} %$ Zr_{2} %$ Si_{4} %$ O_{16} %$ F_{4} $) are stable in favor of Ca-rich clinopyroxene. Sodalite ($ Na_{8} %$ Al_{6} %$ Si_{6} %$ O_{24} %$ Cl_{2} $) and eudialyte ($ Na_{15} %$ Ca_{6} %$ Fe_{3} %$ Zr_{3} %$ Si_{26} %$ O_{73} $(OH)3$ Cl_{2} $) form at $ Cl_{melt} $ concentrations of 0.2–0.5 wt% (depending on T) and $ ZrO_{2 melt} $ concentrations >0.7 wt% are additionally needed to stabilize eudialyte and hiortdahlite. Therefore, F and Cl may become compatible in such systems and have the potential to influence F/Cl melt ratios in evolving magmas. Phase equilibrium experiment (dpeaa)DE-He213 Liquid line of descent (dpeaa)DE-He213 Halogens (dpeaa)DE-He213 Phonolite (dpeaa)DE-He213 Ilímaussaq (dpeaa)DE-He213 Agpaitic (dpeaa)DE-He213 Eudialyte (dpeaa)DE-He213 Infrared spectroscopy (dpeaa)DE-He213 Extinction coefficient (dpeaa)DE-He213 Marks, Michael A. W. verfasserin aut Nowak, Marcus verfasserin aut Enthalten in Contributions to mineralogy and petrology Berlin : Springer, 1947 167(2014), 3 vom: 25. Feb. (DE-627)25372208X (DE-600)1458979-5 1432-0967 nnns volume:167 year:2014 number:3 day:25 month:02 https://dx.doi.org/10.1007/s00410-014-0977-7 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE 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_267 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_2056 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_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 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_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.25 ASE 38.30 ASE AR 167 2014 3 25 02
allfieldsSound	10.1007/s00410-014-0977-7 doi (DE-627)SPR005254256 (SPR)s00410-014-0977-7-e DE-627 ger DE-627 rakwb eng 550 ASE 38.25 bkl 38.30 bkl Giehl, Christopher verfasserin aut An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts 2014 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Fluorine and chlorine affect phase stabilities in magmatic rocks. We present phase equilibrium experiments investigating a peralkaline and iron-rich phonolitic composition with variable F and Cl contents. The starting composition represents a dyke rock, which is a possible parental melt to the peralkaline Ilímaussaq plutonic complex (South Greenland). Experiments were performed at 100 MPa, 1,000–650 °C and low oxygen fugacity adjusted with graphite-lined gold capsules in an internally heated argon pressure vessel and rapid quench cold seal pressure vessels. To cover this large T interval, we applied a two-step fractional crystallization strategy where glasses representing residual melt compositions at 800 °C were synthesized as starting material for consecutive experiments at lower T. In these experiments, oxidized starting glasses allocate oxygen by reduction of ferric iron and up to 1.2 wt% dissolved OH form through reaction with hydrogen provided by the pressure medium ($ H_{2} $O) in initially dry experiments. For OH determination, hydrated super-liquidus experiments in Au capsules were performed to calibrate the extinction coefficient for the fundamental OH stretching vibration using infrared spectroscopy (ε3,415 = 48 ± 3 L $ mol^{−1} $ $ cm^{−1} $). Observed mineral phases in our experiments are titanomagnetite, fayalitic olivine, clinopyroxene, aenigmatite ($ Na_{2} %$ Fe_{5} %$ TiSi_{6} %$ O_{20} $), alkali feldspar and nepheline (±native iron) coexisting with residual melt. Above 1.5 wt% $ F_{melt} $ concentrations, fluorite ($ CaF_{2} $) and hiortdahlite ($ Ca_{6} %$ Zr_{2} %$ Si_{4} %$ O_{16} %$ F_{4} $) are stable in favor of Ca-rich clinopyroxene. Sodalite ($ Na_{8} %$ Al_{6} %$ Si_{6} %$ O_{24} %$ Cl_{2} $) and eudialyte ($ Na_{15} %$ Ca_{6} %$ Fe_{3} %$ Zr_{3} %$ Si_{26} %$ O_{73} $(OH)3$ Cl_{2} $) form at $ Cl_{melt} $ concentrations of 0.2–0.5 wt% (depending on T) and $ ZrO_{2 melt} $ concentrations >0.7 wt% are additionally needed to stabilize eudialyte and hiortdahlite. Therefore, F and Cl may become compatible in such systems and have the potential to influence F/Cl melt ratios in evolving magmas. Phase equilibrium experiment (dpeaa)DE-He213 Liquid line of descent (dpeaa)DE-He213 Halogens (dpeaa)DE-He213 Phonolite (dpeaa)DE-He213 Ilímaussaq (dpeaa)DE-He213 Agpaitic (dpeaa)DE-He213 Eudialyte (dpeaa)DE-He213 Infrared spectroscopy (dpeaa)DE-He213 Extinction coefficient (dpeaa)DE-He213 Marks, Michael A. W. verfasserin aut Nowak, Marcus verfasserin aut Enthalten in Contributions to mineralogy and petrology Berlin : Springer, 1947 167(2014), 3 vom: 25. Feb. (DE-627)25372208X (DE-600)1458979-5 1432-0967 nnns volume:167 year:2014 number:3 day:25 month:02 https://dx.doi.org/10.1007/s00410-014-0977-7 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE 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_267 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_2056 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_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 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_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.25 ASE 38.30 ASE AR 167 2014 3 25 02
language	English
source	Enthalten in Contributions to mineralogy and petrology 167(2014), 3 vom: 25. Feb. volume:167 year:2014 number:3 day:25 month:02
sourceStr	Enthalten in Contributions to mineralogy and petrology 167(2014), 3 vom: 25. Feb. volume:167 year:2014 number:3 day:25 month:02
format_phy_str_mv	Article
institution	findex.gbv.de
topic_facet	Phase equilibrium experiment Liquid line of descent Halogens Phonolite Ilímaussaq Agpaitic Eudialyte Infrared spectroscopy Extinction coefficient
dewey-raw	550
isfreeaccess_bool	false
container_title	Contributions to mineralogy and petrology
authorswithroles_txt_mv	Giehl, Christopher @@aut@@ Marks, Michael A. W. @@aut@@ Nowak, Marcus @@aut@@
publishDateDaySort_date	2014-02-25T00:00:00Z
hierarchy_top_id	25372208X
dewey-sort	3550
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We present phase equilibrium experiments investigating a peralkaline and iron-rich phonolitic composition with variable F and Cl contents. The starting composition represents a dyke rock, which is a possible parental melt to the peralkaline Ilímaussaq plutonic complex (South Greenland). Experiments were performed at 100 MPa, 1,000–650 °C and low oxygen fugacity adjusted with graphite-lined gold capsules in an internally heated argon pressure vessel and rapid quench cold seal pressure vessels. To cover this large T interval, we applied a two-step fractional crystallization strategy where glasses representing residual melt compositions at 800 °C were synthesized as starting material for consecutive experiments at lower T. In these experiments, oxidized starting glasses allocate oxygen by reduction of ferric iron and up to 1.2 wt% dissolved OH form through reaction with hydrogen provided by the pressure medium ($ H_{2} $O) in initially dry experiments. For OH determination, hydrated super-liquidus experiments in Au capsules were performed to calibrate the extinction coefficient for the fundamental OH stretching vibration using infrared spectroscopy (ε3,415 = 48 ± 3 L $ mol^{−1} $ $ cm^{−1} $). Observed mineral phases in our experiments are titanomagnetite, fayalitic olivine, clinopyroxene, aenigmatite ($ Na_{2} %$ Fe_{5} %$ TiSi_{6} %$ O_{20} $), alkali feldspar and nepheline (±native iron) coexisting with residual melt. Above 1.5 wt% $ F_{melt} $ concentrations, fluorite ($ CaF_{2} $) and hiortdahlite ($ Ca_{6} %$ Zr_{2} %$ Si_{4} %$ O_{16} %$ F_{4} $) are stable in favor of Ca-rich clinopyroxene. Sodalite ($ Na_{8} %$ Al_{6} %$ Si_{6} %$ O_{24} %$ Cl_{2} $) and eudialyte ($ Na_{15} %$ Ca_{6} %$ Fe_{3} %$ Zr_{3} %$ Si_{26} %$ O_{73} $(OH)3$ Cl_{2} $) form at $ Cl_{melt} $ concentrations of 0.2–0.5 wt% (depending on T) and $ ZrO_{2 melt} $ concentrations >0.7 wt% are additionally needed to stabilize eudialyte and hiortdahlite. 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author	Giehl, Christopher
spellingShingle	Giehl, Christopher ddc 550 bkl 38.25 bkl 38.30 misc Phase equilibrium experiment misc Liquid line of descent misc Halogens misc Phonolite misc Ilímaussaq misc Agpaitic misc Eudialyte misc Infrared spectroscopy misc Extinction coefficient An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts
authorStr	Giehl, Christopher
ppnlink_with_tag_str_mv	@@773@@(DE-627)25372208X
format	electronic Article
dewey-ones	550 - Earth sciences
delete_txt_mv	keep
author_role	aut aut aut
collection	springer
remote_str	true
illustrated	Not Illustrated
issn	1432-0967
topic_title	550 ASE 38.25 bkl 38.30 bkl An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts Phase equilibrium experiment (dpeaa)DE-He213 Liquid line of descent (dpeaa)DE-He213 Halogens (dpeaa)DE-He213 Phonolite (dpeaa)DE-He213 Ilímaussaq (dpeaa)DE-He213 Agpaitic (dpeaa)DE-He213 Eudialyte (dpeaa)DE-He213 Infrared spectroscopy (dpeaa)DE-He213 Extinction coefficient (dpeaa)DE-He213
topic	ddc 550 bkl 38.25 bkl 38.30 misc Phase equilibrium experiment misc Liquid line of descent misc Halogens misc Phonolite misc Ilímaussaq misc Agpaitic misc Eudialyte misc Infrared spectroscopy misc Extinction coefficient
topic_unstemmed	ddc 550 bkl 38.25 bkl 38.30 misc Phase equilibrium experiment misc Liquid line of descent misc Halogens misc Phonolite misc Ilímaussaq misc Agpaitic misc Eudialyte misc Infrared spectroscopy misc Extinction coefficient
topic_browse	ddc 550 bkl 38.25 bkl 38.30 misc Phase equilibrium experiment misc Liquid line of descent misc Halogens misc Phonolite misc Ilímaussaq misc Agpaitic misc Eudialyte misc Infrared spectroscopy misc Extinction coefficient
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hierarchy_parent_title	Contributions to mineralogy and petrology
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title	An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts
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title_full	An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts
author_sort	Giehl, Christopher
journal	Contributions to mineralogy and petrology
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author_browse	Giehl, Christopher Marks, Michael A. W. Nowak, Marcus
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author-letter	Giehl, Christopher
doi_str_mv	10.1007/s00410-014-0977-7
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title_sort	experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts
title_auth	An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts
abstract	Abstract Fluorine and chlorine affect phase stabilities in magmatic rocks. We present phase equilibrium experiments investigating a peralkaline and iron-rich phonolitic composition with variable F and Cl contents. The starting composition represents a dyke rock, which is a possible parental melt to the peralkaline Ilímaussaq plutonic complex (South Greenland). Experiments were performed at 100 MPa, 1,000–650 °C and low oxygen fugacity adjusted with graphite-lined gold capsules in an internally heated argon pressure vessel and rapid quench cold seal pressure vessels. To cover this large T interval, we applied a two-step fractional crystallization strategy where glasses representing residual melt compositions at 800 °C were synthesized as starting material for consecutive experiments at lower T. In these experiments, oxidized starting glasses allocate oxygen by reduction of ferric iron and up to 1.2 wt% dissolved OH form through reaction with hydrogen provided by the pressure medium ($ H_{2} $O) in initially dry experiments. For OH determination, hydrated super-liquidus experiments in Au capsules were performed to calibrate the extinction coefficient for the fundamental OH stretching vibration using infrared spectroscopy (ε3,415 = 48 ± 3 L $ mol^{−1} $ $ cm^{−1} $). Observed mineral phases in our experiments are titanomagnetite, fayalitic olivine, clinopyroxene, aenigmatite ($ Na_{2} %$ Fe_{5} %$ TiSi_{6} %$ O_{20} $), alkali feldspar and nepheline (±native iron) coexisting with residual melt. Above 1.5 wt% $ F_{melt} $ concentrations, fluorite ($ CaF_{2} $) and hiortdahlite ($ Ca_{6} %$ Zr_{2} %$ Si_{4} %$ O_{16} %$ F_{4} $) are stable in favor of Ca-rich clinopyroxene. Sodalite ($ Na_{8} %$ Al_{6} %$ Si_{6} %$ O_{24} %$ Cl_{2} $) and eudialyte ($ Na_{15} %$ Ca_{6} %$ Fe_{3} %$ Zr_{3} %$ Si_{26} %$ O_{73} $(OH)3$ Cl_{2} $) form at $ Cl_{melt} $ concentrations of 0.2–0.5 wt% (depending on T) and $ ZrO_{2 melt} $ concentrations >0.7 wt% are additionally needed to stabilize eudialyte and hiortdahlite. Therefore, F and Cl may become compatible in such systems and have the potential to influence F/Cl melt ratios in evolving magmas.
abstractGer	Abstract Fluorine and chlorine affect phase stabilities in magmatic rocks. We present phase equilibrium experiments investigating a peralkaline and iron-rich phonolitic composition with variable F and Cl contents. The starting composition represents a dyke rock, which is a possible parental melt to the peralkaline Ilímaussaq plutonic complex (South Greenland). Experiments were performed at 100 MPa, 1,000–650 °C and low oxygen fugacity adjusted with graphite-lined gold capsules in an internally heated argon pressure vessel and rapid quench cold seal pressure vessels. To cover this large T interval, we applied a two-step fractional crystallization strategy where glasses representing residual melt compositions at 800 °C were synthesized as starting material for consecutive experiments at lower T. In these experiments, oxidized starting glasses allocate oxygen by reduction of ferric iron and up to 1.2 wt% dissolved OH form through reaction with hydrogen provided by the pressure medium ($ H_{2} $O) in initially dry experiments. For OH determination, hydrated super-liquidus experiments in Au capsules were performed to calibrate the extinction coefficient for the fundamental OH stretching vibration using infrared spectroscopy (ε3,415 = 48 ± 3 L $ mol^{−1} $ $ cm^{−1} $). Observed mineral phases in our experiments are titanomagnetite, fayalitic olivine, clinopyroxene, aenigmatite ($ Na_{2} %$ Fe_{5} %$ TiSi_{6} %$ O_{20} $), alkali feldspar and nepheline (±native iron) coexisting with residual melt. Above 1.5 wt% $ F_{melt} $ concentrations, fluorite ($ CaF_{2} $) and hiortdahlite ($ Ca_{6} %$ Zr_{2} %$ Si_{4} %$ O_{16} %$ F_{4} $) are stable in favor of Ca-rich clinopyroxene. Sodalite ($ Na_{8} %$ Al_{6} %$ Si_{6} %$ O_{24} %$ Cl_{2} $) and eudialyte ($ Na_{15} %$ Ca_{6} %$ Fe_{3} %$ Zr_{3} %$ Si_{26} %$ O_{73} $(OH)3$ Cl_{2} $) form at $ Cl_{melt} $ concentrations of 0.2–0.5 wt% (depending on T) and $ ZrO_{2 melt} $ concentrations >0.7 wt% are additionally needed to stabilize eudialyte and hiortdahlite. Therefore, F and Cl may become compatible in such systems and have the potential to influence F/Cl melt ratios in evolving magmas.
abstract_unstemmed	Abstract Fluorine and chlorine affect phase stabilities in magmatic rocks. We present phase equilibrium experiments investigating a peralkaline and iron-rich phonolitic composition with variable F and Cl contents. The starting composition represents a dyke rock, which is a possible parental melt to the peralkaline Ilímaussaq plutonic complex (South Greenland). Experiments were performed at 100 MPa, 1,000–650 °C and low oxygen fugacity adjusted with graphite-lined gold capsules in an internally heated argon pressure vessel and rapid quench cold seal pressure vessels. To cover this large T interval, we applied a two-step fractional crystallization strategy where glasses representing residual melt compositions at 800 °C were synthesized as starting material for consecutive experiments at lower T. In these experiments, oxidized starting glasses allocate oxygen by reduction of ferric iron and up to 1.2 wt% dissolved OH form through reaction with hydrogen provided by the pressure medium ($ H_{2} $O) in initially dry experiments. For OH determination, hydrated super-liquidus experiments in Au capsules were performed to calibrate the extinction coefficient for the fundamental OH stretching vibration using infrared spectroscopy (ε3,415 = 48 ± 3 L $ mol^{−1} $ $ cm^{−1} $). Observed mineral phases in our experiments are titanomagnetite, fayalitic olivine, clinopyroxene, aenigmatite ($ Na_{2} %$ Fe_{5} %$ TiSi_{6} %$ O_{20} $), alkali feldspar and nepheline (±native iron) coexisting with residual melt. Above 1.5 wt% $ F_{melt} $ concentrations, fluorite ($ CaF_{2} $) and hiortdahlite ($ Ca_{6} %$ Zr_{2} %$ Si_{4} %$ O_{16} %$ F_{4} $) are stable in favor of Ca-rich clinopyroxene. Sodalite ($ Na_{8} %$ Al_{6} %$ Si_{6} %$ O_{24} %$ Cl_{2} $) and eudialyte ($ Na_{15} %$ Ca_{6} %$ Fe_{3} %$ Zr_{3} %$ Si_{26} %$ O_{73} $(OH)3$ Cl_{2} $) form at $ Cl_{melt} $ concentrations of 0.2–0.5 wt% (depending on T) and $ ZrO_{2 melt} $ concentrations >0.7 wt% are additionally needed to stabilize eudialyte and hiortdahlite. Therefore, F and Cl may become compatible in such systems and have the potential to influence F/Cl melt ratios in evolving magmas.
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title_short	An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts
url	https://dx.doi.org/10.1007/s00410-014-0977-7
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up_date	2024-07-03T15:04:02.823Z
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An experimental study on the influence of fluorine and chlorine on phase relations in peralkaline phonolitic melts

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