Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia

Abstract The Haldzan-Buregtey group of alkali granitoid massifs with an age of 391–395 Ma is located among the Early Caledonides of the Ozernaya zone of western Mongolia and consists of seven intrusive phases, including two rare-metal phases with Zr, Mn, Y, and REE mineralization. In order to identify the magma sources of the massifs, the abundances and canonical ratios of incompatible trace elements in the rocks of various intrusive phases are analyzed and compared with those in the volcanic rocks of Pantelleria island. The latter rocks were taken as the reference association of rocks linked through crystallization differentiation. The rocks of the Haldzan-Buregtey Complex were formed by mixing an OIB source (with participation of MORB) and host ophiolites, while alkali granitoids of phase 2 originated via mixting these sources with the host non-alkaline granitoids. Practically all rocks have mixed sources, with all transitional varieties from OIB, MORB to ophiolites. OIB was the main source for the rocks, while the host ophiolites could serve as sources for anatectic magmas or contaminants of the magmas of other considered rocks. The rare-metal granitoids were produced from the same sources as the barren magmatic rocks of the Haldzan-Buregtey Complex. The rocks of the Haldzan-Buregtey Complex show a bimodal distribution, with the practically complete absence of intermediate varieties between basite dikes and syenite-granite rocks. This seems to be related to the formation of the least differentiated sialic rocks (nordmarkites, pantellerites, some alkali granites) by anatexis of their own parental basite rocks (dolerites and basites), their cumulates, or ophiolites. Most of the phase-2 alkali granites likely resulted from the differentiation of the phase-1 nordmarkites coupled with assimilation of the host ophiolites. Ekerites are geochemically similar to the nordmarkites and can be interpreted as their residual in situ melts or their anatectic melts. Ausführliche Beschreibung

Gespeichert in:

Autor*in:	Kovalenko, V. I. [verfasserIn] Kozlovsky, A. M. Yarmolyuk, V. V.

Format:	E-Artikel
Sprache:	Englisch

Erschienen:	2009

Schlagwörter:	Magmatic Rock Incompatible Trace Element Alkali Granite Trace Element Ratio MORB Source

Anmerkung:	© Pleiades Publishing, Ltd. 2009

Übergeordnetes Werk:	Enthalten in: Petrology - Moscow : MAIK Nauka/Interperiodica Publ. [u.a.], 1996, 17(2009), 2 vom: 28. März
Übergeordnetes Werk:	volume:17 ; year:2009 ; number:2 ; day:28 ; month:03

Links:	Volltext

DOI / URN:	10.1134/S0869591109020040

Katalog-ID:	SPR020201060

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245	1	0	\|a Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia
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520			\|a Abstract The Haldzan-Buregtey group of alkali granitoid massifs with an age of 391–395 Ma is located among the Early Caledonides of the Ozernaya zone of western Mongolia and consists of seven intrusive phases, including two rare-metal phases with Zr, Mn, Y, and REE mineralization. In order to identify the magma sources of the massifs, the abundances and canonical ratios of incompatible trace elements in the rocks of various intrusive phases are analyzed and compared with those in the volcanic rocks of Pantelleria island. The latter rocks were taken as the reference association of rocks linked through crystallization differentiation. The rocks of the Haldzan-Buregtey Complex were formed by mixing an OIB source (with participation of MORB) and host ophiolites, while alkali granitoids of phase 2 originated via mixting these sources with the host non-alkaline granitoids. Practically all rocks have mixed sources, with all transitional varieties from OIB, MORB to ophiolites. OIB was the main source for the rocks, while the host ophiolites could serve as sources for anatectic magmas or contaminants of the magmas of other considered rocks. The rare-metal granitoids were produced from the same sources as the barren magmatic rocks of the Haldzan-Buregtey Complex. The rocks of the Haldzan-Buregtey Complex show a bimodal distribution, with the practically complete absence of intermediate varieties between basite dikes and syenite-granite rocks. This seems to be related to the formation of the least differentiated sialic rocks (nordmarkites, pantellerites, some alkali granites) by anatexis of their own parental basite rocks (dolerites and basites), their cumulates, or ophiolites. Most of the phase-2 alkali granites likely resulted from the differentiation of the phase-1 nordmarkites coupled with assimilation of the host ophiolites. Ekerites are geochemically similar to the nordmarkites and can be interpreted as their residual in situ melts or their anatectic melts.
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700	1		\|a Kozlovsky, A. M. \|4 aut
700	1		\|a Yarmolyuk, V. V. \|4 aut
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912			\|a GBV_ILN_31
912			\|a GBV_ILN_32
912			\|a GBV_ILN_39
912			\|a GBV_ILN_40
912			\|a GBV_ILN_60
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912			\|a GBV_ILN_63
912			\|a GBV_ILN_65
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912			\|a GBV_ILN_70
912			\|a GBV_ILN_73
912			\|a GBV_ILN_74
912			\|a GBV_ILN_90
912			\|a GBV_ILN_95
912			\|a GBV_ILN_100
912			\|a GBV_ILN_105
912			\|a GBV_ILN_110
912			\|a GBV_ILN_120
912			\|a GBV_ILN_138
912			\|a GBV_ILN_150
912			\|a GBV_ILN_151
912			\|a GBV_ILN_152
912			\|a GBV_ILN_161
912			\|a GBV_ILN_170
912			\|a GBV_ILN_171
912			\|a GBV_ILN_187
912			\|a GBV_ILN_213
912			\|a GBV_ILN_224
912			\|a GBV_ILN_230
912			\|a GBV_ILN_250
912			\|a GBV_ILN_281
912			\|a GBV_ILN_285
912			\|a GBV_ILN_293
912			\|a GBV_ILN_370
912			\|a GBV_ILN_602
912			\|a GBV_ILN_636
912			\|a GBV_ILN_702
912			\|a GBV_ILN_2001
912			\|a GBV_ILN_2003
912			\|a GBV_ILN_2004
912			\|a GBV_ILN_2005
912			\|a GBV_ILN_2006
912			\|a GBV_ILN_2007
912			\|a GBV_ILN_2008
912			\|a GBV_ILN_2009
912			\|a GBV_ILN_2010
912			\|a GBV_ILN_2011
912			\|a GBV_ILN_2014
912			\|a GBV_ILN_2015
912			\|a GBV_ILN_2020
912			\|a GBV_ILN_2021
912			\|a GBV_ILN_2025
912			\|a GBV_ILN_2026
912			\|a GBV_ILN_2027
912			\|a GBV_ILN_2031
912			\|a GBV_ILN_2034
912			\|a GBV_ILN_2037
912			\|a GBV_ILN_2038
912			\|a GBV_ILN_2039
912			\|a GBV_ILN_2044
912			\|a GBV_ILN_2048
912			\|a GBV_ILN_2049
912			\|a GBV_ILN_2050
912			\|a GBV_ILN_2055
912			\|a GBV_ILN_2057
912			\|a GBV_ILN_2059
912			\|a GBV_ILN_2061
912			\|a GBV_ILN_2064
912			\|a GBV_ILN_2065
912			\|a GBV_ILN_2068
912			\|a GBV_ILN_2070
912			\|a GBV_ILN_2086
912			\|a GBV_ILN_2088
912			\|a GBV_ILN_2093
912			\|a GBV_ILN_2106
912			\|a GBV_ILN_2107
912			\|a GBV_ILN_2108
912			\|a GBV_ILN_2110
912			\|a GBV_ILN_2111
912			\|a GBV_ILN_2112
912			\|a GBV_ILN_2113
912			\|a GBV_ILN_2116
912			\|a GBV_ILN_2118
912			\|a GBV_ILN_2119
912			\|a GBV_ILN_2122
912			\|a GBV_ILN_2129
912			\|a GBV_ILN_2143
912			\|a GBV_ILN_2144
912			\|a GBV_ILN_2147
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912			\|a GBV_ILN_2152
912			\|a GBV_ILN_2153
912			\|a GBV_ILN_2188
912			\|a GBV_ILN_2190
912			\|a GBV_ILN_2232
912			\|a GBV_ILN_2336
912			\|a GBV_ILN_2446
912			\|a GBV_ILN_2470
912			\|a GBV_ILN_2472
912			\|a GBV_ILN_2507
912			\|a GBV_ILN_2522
912			\|a GBV_ILN_2548
912			\|a GBV_ILN_4035
912			\|a GBV_ILN_4037
912			\|a GBV_ILN_4046
912			\|a GBV_ILN_4112
912			\|a GBV_ILN_4125
912			\|a GBV_ILN_4242
912			\|a GBV_ILN_4246
912			\|a GBV_ILN_4249
912			\|a GBV_ILN_4251
912			\|a GBV_ILN_4305
912			\|a GBV_ILN_4306
912			\|a GBV_ILN_4307
912			\|a GBV_ILN_4313
912			\|a GBV_ILN_4322
912			\|a GBV_ILN_4323
912			\|a GBV_ILN_4324
912			\|a GBV_ILN_4325
912			\|a GBV_ILN_4326
912			\|a GBV_ILN_4333
912			\|a GBV_ILN_4334
912			\|a GBV_ILN_4335
912			\|a GBV_ILN_4336
912			\|a GBV_ILN_4338
912			\|a GBV_ILN_4393
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951			\|a AR
952			\|d 17 \|j 2009 \|e 2 \|b 28 \|c 03

Indexfelder

author_variant	v i k vi vik a m k am amk v v y vv vvy
matchkey_str	article:15562085:2009----::rceeetaissniaosforeiignmgaifrnitooaklgaiodadaieoteadabrgemsiadhh
hierarchy_sort_str	2009
publishDate	2009
allfields	10.1134/S0869591109020040 doi (DE-627)SPR020201060 (SPR)S0869591109020040-e DE-627 ger DE-627 rakwb eng Kovalenko, V. I. verfasserin aut Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia 2009 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Pleiades Publishing, Ltd. 2009 Abstract The Haldzan-Buregtey group of alkali granitoid massifs with an age of 391–395 Ma is located among the Early Caledonides of the Ozernaya zone of western Mongolia and consists of seven intrusive phases, including two rare-metal phases with Zr, Mn, Y, and REE mineralization. In order to identify the magma sources of the massifs, the abundances and canonical ratios of incompatible trace elements in the rocks of various intrusive phases are analyzed and compared with those in the volcanic rocks of Pantelleria island. The latter rocks were taken as the reference association of rocks linked through crystallization differentiation. The rocks of the Haldzan-Buregtey Complex were formed by mixing an OIB source (with participation of MORB) and host ophiolites, while alkali granitoids of phase 2 originated via mixting these sources with the host non-alkaline granitoids. Practically all rocks have mixed sources, with all transitional varieties from OIB, MORB to ophiolites. OIB was the main source for the rocks, while the host ophiolites could serve as sources for anatectic magmas or contaminants of the magmas of other considered rocks. The rare-metal granitoids were produced from the same sources as the barren magmatic rocks of the Haldzan-Buregtey Complex. The rocks of the Haldzan-Buregtey Complex show a bimodal distribution, with the practically complete absence of intermediate varieties between basite dikes and syenite-granite rocks. This seems to be related to the formation of the least differentiated sialic rocks (nordmarkites, pantellerites, some alkali granites) by anatexis of their own parental basite rocks (dolerites and basites), their cumulates, or ophiolites. Most of the phase-2 alkali granites likely resulted from the differentiation of the phase-1 nordmarkites coupled with assimilation of the host ophiolites. Ekerites are geochemically similar to the nordmarkites and can be interpreted as their residual in situ melts or their anatectic melts. Magmatic Rock (dpeaa)DE-He213 Incompatible Trace Element (dpeaa)DE-He213 Alkali Granite (dpeaa)DE-He213 Trace Element Ratio (dpeaa)DE-He213 MORB Source (dpeaa)DE-He213 Kozlovsky, A. M. aut Yarmolyuk, V. V. aut Enthalten in Petrology Moscow : MAIK Nauka/Interperiodica Publ. [u.a.], 1996 17(2009), 2 vom: 28. März (DE-627)511882602 (DE-600)2235750-6 1556-2085 nnns volume:17 year:2009 number:2 day:28 month:03 https://dx.doi.org/10.1134/S0869591109020040 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_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 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 17 2009 2 28 03
spelling	10.1134/S0869591109020040 doi (DE-627)SPR020201060 (SPR)S0869591109020040-e DE-627 ger DE-627 rakwb eng Kovalenko, V. I. verfasserin aut Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia 2009 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Pleiades Publishing, Ltd. 2009 Abstract The Haldzan-Buregtey group of alkali granitoid massifs with an age of 391–395 Ma is located among the Early Caledonides of the Ozernaya zone of western Mongolia and consists of seven intrusive phases, including two rare-metal phases with Zr, Mn, Y, and REE mineralization. In order to identify the magma sources of the massifs, the abundances and canonical ratios of incompatible trace elements in the rocks of various intrusive phases are analyzed and compared with those in the volcanic rocks of Pantelleria island. The latter rocks were taken as the reference association of rocks linked through crystallization differentiation. The rocks of the Haldzan-Buregtey Complex were formed by mixing an OIB source (with participation of MORB) and host ophiolites, while alkali granitoids of phase 2 originated via mixting these sources with the host non-alkaline granitoids. Practically all rocks have mixed sources, with all transitional varieties from OIB, MORB to ophiolites. OIB was the main source for the rocks, while the host ophiolites could serve as sources for anatectic magmas or contaminants of the magmas of other considered rocks. The rare-metal granitoids were produced from the same sources as the barren magmatic rocks of the Haldzan-Buregtey Complex. The rocks of the Haldzan-Buregtey Complex show a bimodal distribution, with the practically complete absence of intermediate varieties between basite dikes and syenite-granite rocks. This seems to be related to the formation of the least differentiated sialic rocks (nordmarkites, pantellerites, some alkali granites) by anatexis of their own parental basite rocks (dolerites and basites), their cumulates, or ophiolites. Most of the phase-2 alkali granites likely resulted from the differentiation of the phase-1 nordmarkites coupled with assimilation of the host ophiolites. Ekerites are geochemically similar to the nordmarkites and can be interpreted as their residual in situ melts or their anatectic melts. Magmatic Rock (dpeaa)DE-He213 Incompatible Trace Element (dpeaa)DE-He213 Alkali Granite (dpeaa)DE-He213 Trace Element Ratio (dpeaa)DE-He213 MORB Source (dpeaa)DE-He213 Kozlovsky, A. M. aut Yarmolyuk, V. V. aut Enthalten in Petrology Moscow : MAIK Nauka/Interperiodica Publ. [u.a.], 1996 17(2009), 2 vom: 28. März (DE-627)511882602 (DE-600)2235750-6 1556-2085 nnns volume:17 year:2009 number:2 day:28 month:03 https://dx.doi.org/10.1134/S0869591109020040 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_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 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 17 2009 2 28 03
allfields_unstemmed	10.1134/S0869591109020040 doi (DE-627)SPR020201060 (SPR)S0869591109020040-e DE-627 ger DE-627 rakwb eng Kovalenko, V. I. verfasserin aut Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia 2009 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Pleiades Publishing, Ltd. 2009 Abstract The Haldzan-Buregtey group of alkali granitoid massifs with an age of 391–395 Ma is located among the Early Caledonides of the Ozernaya zone of western Mongolia and consists of seven intrusive phases, including two rare-metal phases with Zr, Mn, Y, and REE mineralization. In order to identify the magma sources of the massifs, the abundances and canonical ratios of incompatible trace elements in the rocks of various intrusive phases are analyzed and compared with those in the volcanic rocks of Pantelleria island. The latter rocks were taken as the reference association of rocks linked through crystallization differentiation. The rocks of the Haldzan-Buregtey Complex were formed by mixing an OIB source (with participation of MORB) and host ophiolites, while alkali granitoids of phase 2 originated via mixting these sources with the host non-alkaline granitoids. Practically all rocks have mixed sources, with all transitional varieties from OIB, MORB to ophiolites. OIB was the main source for the rocks, while the host ophiolites could serve as sources for anatectic magmas or contaminants of the magmas of other considered rocks. The rare-metal granitoids were produced from the same sources as the barren magmatic rocks of the Haldzan-Buregtey Complex. The rocks of the Haldzan-Buregtey Complex show a bimodal distribution, with the practically complete absence of intermediate varieties between basite dikes and syenite-granite rocks. This seems to be related to the formation of the least differentiated sialic rocks (nordmarkites, pantellerites, some alkali granites) by anatexis of their own parental basite rocks (dolerites and basites), their cumulates, or ophiolites. Most of the phase-2 alkali granites likely resulted from the differentiation of the phase-1 nordmarkites coupled with assimilation of the host ophiolites. Ekerites are geochemically similar to the nordmarkites and can be interpreted as their residual in situ melts or their anatectic melts. Magmatic Rock (dpeaa)DE-He213 Incompatible Trace Element (dpeaa)DE-He213 Alkali Granite (dpeaa)DE-He213 Trace Element Ratio (dpeaa)DE-He213 MORB Source (dpeaa)DE-He213 Kozlovsky, A. M. aut Yarmolyuk, V. V. aut Enthalten in Petrology Moscow : MAIK Nauka/Interperiodica Publ. [u.a.], 1996 17(2009), 2 vom: 28. März (DE-627)511882602 (DE-600)2235750-6 1556-2085 nnns volume:17 year:2009 number:2 day:28 month:03 https://dx.doi.org/10.1134/S0869591109020040 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_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 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 17 2009 2 28 03
allfieldsGer	10.1134/S0869591109020040 doi (DE-627)SPR020201060 (SPR)S0869591109020040-e DE-627 ger DE-627 rakwb eng Kovalenko, V. I. verfasserin aut Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia 2009 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Pleiades Publishing, Ltd. 2009 Abstract The Haldzan-Buregtey group of alkali granitoid massifs with an age of 391–395 Ma is located among the Early Caledonides of the Ozernaya zone of western Mongolia and consists of seven intrusive phases, including two rare-metal phases with Zr, Mn, Y, and REE mineralization. In order to identify the magma sources of the massifs, the abundances and canonical ratios of incompatible trace elements in the rocks of various intrusive phases are analyzed and compared with those in the volcanic rocks of Pantelleria island. The latter rocks were taken as the reference association of rocks linked through crystallization differentiation. The rocks of the Haldzan-Buregtey Complex were formed by mixing an OIB source (with participation of MORB) and host ophiolites, while alkali granitoids of phase 2 originated via mixting these sources with the host non-alkaline granitoids. Practically all rocks have mixed sources, with all transitional varieties from OIB, MORB to ophiolites. OIB was the main source for the rocks, while the host ophiolites could serve as sources for anatectic magmas or contaminants of the magmas of other considered rocks. The rare-metal granitoids were produced from the same sources as the barren magmatic rocks of the Haldzan-Buregtey Complex. The rocks of the Haldzan-Buregtey Complex show a bimodal distribution, with the practically complete absence of intermediate varieties between basite dikes and syenite-granite rocks. This seems to be related to the formation of the least differentiated sialic rocks (nordmarkites, pantellerites, some alkali granites) by anatexis of their own parental basite rocks (dolerites and basites), their cumulates, or ophiolites. Most of the phase-2 alkali granites likely resulted from the differentiation of the phase-1 nordmarkites coupled with assimilation of the host ophiolites. Ekerites are geochemically similar to the nordmarkites and can be interpreted as their residual in situ melts or their anatectic melts. Magmatic Rock (dpeaa)DE-He213 Incompatible Trace Element (dpeaa)DE-He213 Alkali Granite (dpeaa)DE-He213 Trace Element Ratio (dpeaa)DE-He213 MORB Source (dpeaa)DE-He213 Kozlovsky, A. M. aut Yarmolyuk, V. V. aut Enthalten in Petrology Moscow : MAIK Nauka/Interperiodica Publ. [u.a.], 1996 17(2009), 2 vom: 28. März (DE-627)511882602 (DE-600)2235750-6 1556-2085 nnns volume:17 year:2009 number:2 day:28 month:03 https://dx.doi.org/10.1134/S0869591109020040 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_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 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 17 2009 2 28 03
allfieldsSound	10.1134/S0869591109020040 doi (DE-627)SPR020201060 (SPR)S0869591109020040-e DE-627 ger DE-627 rakwb eng Kovalenko, V. I. verfasserin aut Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia 2009 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Pleiades Publishing, Ltd. 2009 Abstract The Haldzan-Buregtey group of alkali granitoid massifs with an age of 391–395 Ma is located among the Early Caledonides of the Ozernaya zone of western Mongolia and consists of seven intrusive phases, including two rare-metal phases with Zr, Mn, Y, and REE mineralization. In order to identify the magma sources of the massifs, the abundances and canonical ratios of incompatible trace elements in the rocks of various intrusive phases are analyzed and compared with those in the volcanic rocks of Pantelleria island. The latter rocks were taken as the reference association of rocks linked through crystallization differentiation. The rocks of the Haldzan-Buregtey Complex were formed by mixing an OIB source (with participation of MORB) and host ophiolites, while alkali granitoids of phase 2 originated via mixting these sources with the host non-alkaline granitoids. Practically all rocks have mixed sources, with all transitional varieties from OIB, MORB to ophiolites. OIB was the main source for the rocks, while the host ophiolites could serve as sources for anatectic magmas or contaminants of the magmas of other considered rocks. The rare-metal granitoids were produced from the same sources as the barren magmatic rocks of the Haldzan-Buregtey Complex. The rocks of the Haldzan-Buregtey Complex show a bimodal distribution, with the practically complete absence of intermediate varieties between basite dikes and syenite-granite rocks. This seems to be related to the formation of the least differentiated sialic rocks (nordmarkites, pantellerites, some alkali granites) by anatexis of their own parental basite rocks (dolerites and basites), their cumulates, or ophiolites. Most of the phase-2 alkali granites likely resulted from the differentiation of the phase-1 nordmarkites coupled with assimilation of the host ophiolites. Ekerites are geochemically similar to the nordmarkites and can be interpreted as their residual in situ melts or their anatectic melts. Magmatic Rock (dpeaa)DE-He213 Incompatible Trace Element (dpeaa)DE-He213 Alkali Granite (dpeaa)DE-He213 Trace Element Ratio (dpeaa)DE-He213 MORB Source (dpeaa)DE-He213 Kozlovsky, A. M. aut Yarmolyuk, V. V. aut Enthalten in Petrology Moscow : MAIK Nauka/Interperiodica Publ. [u.a.], 1996 17(2009), 2 vom: 28. März (DE-627)511882602 (DE-600)2235750-6 1556-2085 nnns volume:17 year:2009 number:2 day:28 month:03 https://dx.doi.org/10.1134/S0869591109020040 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_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 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 17 2009 2 28 03
language	English
source	Enthalten in Petrology 17(2009), 2 vom: 28. März volume:17 year:2009 number:2 day:28 month:03
sourceStr	Enthalten in Petrology 17(2009), 2 vom: 28. März volume:17 year:2009 number:2 day:28 month:03
format_phy_str_mv	Article
institution	findex.gbv.de
topic_facet	Magmatic Rock Incompatible Trace Element Alkali Granite Trace Element Ratio MORB Source
isfreeaccess_bool	false
container_title	Petrology
authorswithroles_txt_mv	Kovalenko, V. I. @@aut@@ Kozlovsky, A. M. @@aut@@ Yarmolyuk, V. V. @@aut@@
publishDateDaySort_date	2009-03-28T00:00:00Z
hierarchy_top_id	511882602
id	SPR020201060
language_de	englisch
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author	Kovalenko, V. I.
spellingShingle	Kovalenko, V. I. misc Magmatic Rock misc Incompatible Trace Element misc Alkali Granite misc Trace Element Ratio misc MORB Source Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia
authorStr	Kovalenko, V. I.
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topic_title	Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia Magmatic Rock (dpeaa)DE-He213 Incompatible Trace Element (dpeaa)DE-He213 Alkali Granite (dpeaa)DE-He213 Trace Element Ratio (dpeaa)DE-He213 MORB Source (dpeaa)DE-He213
topic	misc Magmatic Rock misc Incompatible Trace Element misc Alkali Granite misc Trace Element Ratio misc MORB Source
topic_unstemmed	misc Magmatic Rock misc Incompatible Trace Element misc Alkali Granite misc Trace Element Ratio misc MORB Source
topic_browse	misc Magmatic Rock misc Incompatible Trace Element misc Alkali Granite misc Trace Element Ratio misc MORB Source
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title	Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia
ctrlnum	(DE-627)SPR020201060 (SPR)S0869591109020040-e
title_full	Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia
author_sort	Kovalenko, V. I.
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author_browse	Kovalenko, V. I. Kozlovsky, A. M. Yarmolyuk, V. V.
container_volume	17
format_se	Elektronische Aufsätze
author-letter	Kovalenko, V. I.
doi_str_mv	10.1134/S0869591109020040
title_sort	trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the haldzan-buregtey massif and the haldzan-buregtey rare-metal deposit, western mongolia
title_auth	Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia
abstract	Abstract The Haldzan-Buregtey group of alkali granitoid massifs with an age of 391–395 Ma is located among the Early Caledonides of the Ozernaya zone of western Mongolia and consists of seven intrusive phases, including two rare-metal phases with Zr, Mn, Y, and REE mineralization. In order to identify the magma sources of the massifs, the abundances and canonical ratios of incompatible trace elements in the rocks of various intrusive phases are analyzed and compared with those in the volcanic rocks of Pantelleria island. The latter rocks were taken as the reference association of rocks linked through crystallization differentiation. The rocks of the Haldzan-Buregtey Complex were formed by mixing an OIB source (with participation of MORB) and host ophiolites, while alkali granitoids of phase 2 originated via mixting these sources with the host non-alkaline granitoids. Practically all rocks have mixed sources, with all transitional varieties from OIB, MORB to ophiolites. OIB was the main source for the rocks, while the host ophiolites could serve as sources for anatectic magmas or contaminants of the magmas of other considered rocks. The rare-metal granitoids were produced from the same sources as the barren magmatic rocks of the Haldzan-Buregtey Complex. The rocks of the Haldzan-Buregtey Complex show a bimodal distribution, with the practically complete absence of intermediate varieties between basite dikes and syenite-granite rocks. This seems to be related to the formation of the least differentiated sialic rocks (nordmarkites, pantellerites, some alkali granites) by anatexis of their own parental basite rocks (dolerites and basites), their cumulates, or ophiolites. Most of the phase-2 alkali granites likely resulted from the differentiation of the phase-1 nordmarkites coupled with assimilation of the host ophiolites. Ekerites are geochemically similar to the nordmarkites and can be interpreted as their residual in situ melts or their anatectic melts. © Pleiades Publishing, Ltd. 2009
abstractGer	Abstract The Haldzan-Buregtey group of alkali granitoid massifs with an age of 391–395 Ma is located among the Early Caledonides of the Ozernaya zone of western Mongolia and consists of seven intrusive phases, including two rare-metal phases with Zr, Mn, Y, and REE mineralization. In order to identify the magma sources of the massifs, the abundances and canonical ratios of incompatible trace elements in the rocks of various intrusive phases are analyzed and compared with those in the volcanic rocks of Pantelleria island. The latter rocks were taken as the reference association of rocks linked through crystallization differentiation. The rocks of the Haldzan-Buregtey Complex were formed by mixing an OIB source (with participation of MORB) and host ophiolites, while alkali granitoids of phase 2 originated via mixting these sources with the host non-alkaline granitoids. Practically all rocks have mixed sources, with all transitional varieties from OIB, MORB to ophiolites. OIB was the main source for the rocks, while the host ophiolites could serve as sources for anatectic magmas or contaminants of the magmas of other considered rocks. The rare-metal granitoids were produced from the same sources as the barren magmatic rocks of the Haldzan-Buregtey Complex. The rocks of the Haldzan-Buregtey Complex show a bimodal distribution, with the practically complete absence of intermediate varieties between basite dikes and syenite-granite rocks. This seems to be related to the formation of the least differentiated sialic rocks (nordmarkites, pantellerites, some alkali granites) by anatexis of their own parental basite rocks (dolerites and basites), their cumulates, or ophiolites. Most of the phase-2 alkali granites likely resulted from the differentiation of the phase-1 nordmarkites coupled with assimilation of the host ophiolites. Ekerites are geochemically similar to the nordmarkites and can be interpreted as their residual in situ melts or their anatectic melts. © Pleiades Publishing, Ltd. 2009
abstract_unstemmed	Abstract The Haldzan-Buregtey group of alkali granitoid massifs with an age of 391–395 Ma is located among the Early Caledonides of the Ozernaya zone of western Mongolia and consists of seven intrusive phases, including two rare-metal phases with Zr, Mn, Y, and REE mineralization. In order to identify the magma sources of the massifs, the abundances and canonical ratios of incompatible trace elements in the rocks of various intrusive phases are analyzed and compared with those in the volcanic rocks of Pantelleria island. The latter rocks were taken as the reference association of rocks linked through crystallization differentiation. The rocks of the Haldzan-Buregtey Complex were formed by mixing an OIB source (with participation of MORB) and host ophiolites, while alkali granitoids of phase 2 originated via mixting these sources with the host non-alkaline granitoids. Practically all rocks have mixed sources, with all transitional varieties from OIB, MORB to ophiolites. OIB was the main source for the rocks, while the host ophiolites could serve as sources for anatectic magmas or contaminants of the magmas of other considered rocks. The rare-metal granitoids were produced from the same sources as the barren magmatic rocks of the Haldzan-Buregtey Complex. The rocks of the Haldzan-Buregtey Complex show a bimodal distribution, with the practically complete absence of intermediate varieties between basite dikes and syenite-granite rocks. This seems to be related to the formation of the least differentiated sialic rocks (nordmarkites, pantellerites, some alkali granites) by anatexis of their own parental basite rocks (dolerites and basites), their cumulates, or ophiolites. Most of the phase-2 alkali granites likely resulted from the differentiation of the phase-1 nordmarkites coupled with assimilation of the host ophiolites. Ekerites are geochemically similar to the nordmarkites and can be interpreted as their residual in situ melts or their anatectic melts. © Pleiades Publishing, Ltd. 2009
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title_short	Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia
url	https://dx.doi.org/10.1134/S0869591109020040
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author2	Kozlovsky, A. M. Yarmolyuk, V. V.
author2Str	Kozlovsky, A. M. Yarmolyuk, V. V.
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doi_str	10.1134/S0869591109020040
up_date	2024-07-03T14:32:03.581Z
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Trace element ratios as indicators of source mixing and magma differentiation of alkali granitoids and basites of the Haldzan-Buregtey massif and the Haldzan-Buregtey rare-metal deposit, western Mongolia

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