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  5.     <title>UTas ePrints - Re-equilibration of melt inclusions trapped by magnesian olivine phenocrysts from subduction-related magmas: petrological implications</title>
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  13.     <meta content="Danyushevsky, L.V." name="eprints.creators_name" />
  14. <meta content="Della-Pasqua, F.N." name="eprints.creators_name" />
  15. <meta content="Sokolov, S." name="eprints.creators_name" />
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  23. <meta content="Re-equilibration of melt inclusions trapped by magnesian olivine phenocrysts from subduction-related magmas: petrological implications" name="eprints.title" />
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  28. <meta content="melt inclusions, olivine, petrology, geochemistry, subduction, magmatism, re-equilibration" name="eprints.keywords" />
  29. <meta content="The original publication is available at www.springerlink.com" name="eprints.note" />
  30. <meta content="We describe and model a potential re-equili-
  31. bration process that can affect compositions of melt
  32. inclusions in magnesian olivine phenocrysts. This pro-
  33. cess, referred to as ``Fe-loss'', can operate during natural pre-eruptive cooling of host magma and results in lower
  34. FeOt and higher MgO contents within the initially
  35. trapped volume of inclusion. The extent of Fe-loss is
  36. enhanced by large temperature intervals of magma
  37. cooling before eruption. The compositions of homoge-
  38. nised melt inclusions in olivine phenocrysts from several
  39. subduction-related suites demonstrate that (1) Fe-loss is
  40. a common process, (2) the maximum observed degree of
  41. re-equilibration varies between suites, and (3) within a
  42. single sample, variable degrees of re-equilibration can be
  43. recorded by melt inclusions trapped in olivine pheno-
  44. crysts of identical composition. Our modelling also
  45. demonstrates that the re-equilibration process is fast
  46. going to completion, in the largest inclusions in the most
  47. magnesian phenocrysts it is completed within 2 years.
  48. The results we obtained indicate that the possibility of
  49. Fe-loss must be considered when estimating composi-
  50. tions of parental subduction-related magmas from nat-
  51. urally quenched glassy melt inclusions in magnesian
  52. olivine phenocrysts. Compositions calculated from
  53. glassy inclusions affected by Fe-loss will inherit not only
  54. erroneously low FeOt contents, but also low MgO due to
  55. the inherited higher Mg# of the residual melt in re-
  56. equilibrated inclusions. We also demonstrate that due to
  57. the higher MgO contents of homogenised melt inclu-
  58. sions affected by Fe-loss, homogenisation temperatures
  59. achieved in heating experiments will be higher than
  60. original trapping temperatures. The extent of overheat-
  61. ing will increase depending on the degree of re-equili-
  62. bration, and can reach up to 50 degrees C in cases where
  63. complete re-equilibration occurs over a cooling interval
  64. of 200 degrees C." name="eprints.abstract" />
  65. <meta content="2000-01" name="eprints.date" />
  66. <meta content="published" name="eprints.date_type" />
  67. <meta content="Contributions to Mineralogy and Petrology" name="eprints.publication" />
  68. <meta content="138" name="eprints.volume" />
  69. <meta content="1" name="eprints.number" />
  70. <meta content="68-83" name="eprints.pagerange" />
  71. <meta content="10.1007/PL00007664" name="eprints.id_number" />
  72. <meta content="UNSPECIFIED" name="eprints.thesis_type" />
  73. <meta content="TRUE" name="eprints.refereed" />
  74. <meta content="http://dx.doi.org/10.1007/PL00007664" name="eprints.official_url" />
  75. <meta content="Anderson AT (1974) Evidence for a picritic, volatile-rich magma
  76. beneath Mt. Shasta, California. J Petrol 15: 243±267
  77. BarsdellM(1988) Petrology and petrogenesis of clinopyroxene-rich
  78. tholeiitic lavas, Merelava volcano, Vanuatu. J Petrol 29: 927±
  79. 964
  80. Bowen NL (1928) The evolution of the igneous rocks. Dover, New
  81. York, p 334
  82. Chakraborty S (1997) Rates and mechanisms of Fe-Mg interdif-
  83. fusion in olivine at 980±1300 °C. J Geophy Res 102B: 12317±
  84. 12331
  85. Crawford AJ, Falloon TJ, Eggins S (1987) The origin of island arc
  86. high-alumina basalts. Contrib Mineral Petrol 97: 417±430
  87. Danyushevsky LV, Sobolev AV (1996) Ferric-ferrous ratio and
  88. oxygen fugacity calculations for primitive mantle-derived melts:
  89. calibration of an empirical technique. Mineral Petrol 57: 229±
  90. 241
  91. Danyushevsky LV, Sobolev AV, Falloon TJ (1995) North Tongan
  92. high-Ca boninite petrogenesis: the role of Samoan plume and
  93. subduction zone-transform fault transition. J Geodynamics 20:
  94. 219±241
  95. Danyushevsky LV, Sobolev AV, Kononkova NN (1992) Methods
  96. of studying melt inclusions in minerals during investigations on
  97. water-bearing primitive mantle melts (Tonga trench boninites).
  98. Geochem Int 29: 48±62
  99. Della-Pasqua FN (1997) Primitive ankaramitic magmas in volcanic
  100. arcs: evidence from melt inclusions. PhD Thesis, University of
  101. Tasmania
  102. Della-Pasqua FN, Varne R (1997) Primitive ankaramitic magmas
  103. in volcanic arcs: a melt inclusion approach. Can Mineral 35:
  104. 291±312
  105. Eggins S (1993) Origin and di€erentiation of picritic arc magmas,
  106. Ambae (Aoba), Vanuatu. Contrib Mineral Petrol 114: 79±100
  107. Falloon TJ, Green DH (1986) Glass inclusions in magnesian olivine
  108. phenocrysts from Tonga: evidence for highly refractory paren-
  109. tal magmas in the Tonga arc. Earth Planet Sci Lett 81: 95±103
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  111. volcano, east Sunda arc: a model for island arc petrogenesis.
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  114. equilibria: temperature, pressure and composition dependence
  115. of the crystal/liquid cation partition coecients for Mg, Fe2+,
  116. Ca and Mn. J Petrol 24: 256±265
  117. Gurenko AA, Sobolev AV, Kononkova NN (1992) New petrolog-
  118. ical data on Icelandic rift alkali basalts. Geochem Int 29: 41±53
  119. Gurenko AA, Sobolev AV, Polyakov AI, Kononkova NN (1988)
  120. Primary melt of rift tholeiites of Iceland: composition and
  121. conditions of crystallisation. Trans (Doklady) USSR Acad Sci
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  124. melts of Vulsini (Roman Province): evidence from mineralogy
  125. and melt inclusions. Contrib Mineral Petrol 120: 186±196
  126. Kamenetsky VS, Sobolev AV, Joron JL, Semet MP (1995b) Pe-
  127. trology and geochemistry of Cretaceous ultrama®c volcanics
  128. from eastern Kamchatka. J Petrol 36: 637±662
  129. Kamenetsky VS, Crawford AJ, Eggins S, MuheR(1997) Phenocryst
  130. and melt inclusion chemistry of near-axis seamounts, Valu Fa
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  132. of subduction components. Earth Planet Sci Lett 151: 205±223
  133. Lange RA, Carmichael ISE (1987) Densities of Na2O-K2O-CaO-
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  137. Lee J, Stern RJ (1998) Glass inclusions in Mariana Arc pheno-
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  139. intra-oceanic arc. J Geol 106: 19±33
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  141. residual mantle: Implications for buoyancy forces beneath mid-
  142. ocean ridges. J Geol 99: 767±775
  143. Portnyagin MV, Danyushevsky LV, Kamenetsky VS (1997) Co-
  144. existence of two distinct mantle sources during formation of
  145. ophiolites: a case study of primitive pillow-lavas from the
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  157. chromite within Kilauea Iki lava lake, Hawaii. Contrib Mineral
  158. Petrol 107: 8±20
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  169. Sobolev AV, Danyushevsky LV (1994) Petrology and geochemistry
  170. of boninites from the North termination of the Tonga trench:
  171. constraints on the generation conditions of primary high-Ca
  172. boninite magmas. J Petrol 35: 1183±1211
  173. Sobolev AV, Slutskiy AB (1984) Composition and crystallisation
  174. conditions of the initial melt of the Siberian meimechites in
  175. relation to the general problem of the ultrabasic magmas. Sov
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  178. AB (1980) The formation conditions of the high-magnesium
  179. olivines from the monomineralic fraction of Luna 24 regolith.
  180. Proceedings of the 11th Lunar Sci Conf, pp 105±116
  181. Sobolev AV, Danyushevsky LV, Dmitriev LV, Suschevskaya NM
  182. (1989) High-alumina magnesian tholeiite as the primary basalt
  183. magma at Midocean ridge. Geochem Int 26: 128±133
  184. Sobolev AV, Portnyagin MV, Dmitriev LV, Tsamerian OP,
  185. Danyushevsky LV, Kononkova NN, Shimizu N, Robinson PT
  186. (1993) Petrology of ultrama®c lavas and associated rocks of the
  187. Troodos Massif, Cyprus. Petrology 1: 331±361
  188. Tait S (1992) Selective preservation of melt inclusions in igneous
  189. phenocrysts. Am Mineral 77: 146±155
  190. Ulmer P (1989) The dependence of the Fe2+±Mg cation-parti-
  191. tioning between olivine and basaltic liquid on pressure,
  192. temperature and composition. An experimental study to
  193. 30 kbar. Contrib Mineral Petrol 101: 261±273
  194. Walker DA, Cameron WE (1983) Boninite primary magmas: evi-
  195. dence from the Cape Vogel peninsula, PNG. Contrib Mineral
  196. Petrol 83: 150±158" name="eprints.referencetext" />
  197. <meta content="Danyushevsky, L.V. and Della-Pasqua, F.N. and Sokolov, S. (2000) Re-equilibration of melt inclusions trapped by magnesian olivine phenocrysts from subduction-related magmas: petrological implications. Contributions to Mineralogy and Petrology, 138 (1). pp. 68-83." name="eprints.citation" />
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  201. <meta content="Danyushevsky, L.V." name="DC.creator" />
  202. <meta content="Della-Pasqua, F.N." name="DC.creator" />
  203. <meta content="Sokolov, S." name="DC.creator" />
  204. <meta content="260101 Mineralogy and Crystallography" name="DC.subject" />
  205. <meta content="260102 Igneous and Metamorphic Petrology" name="DC.subject" />
  206. <meta content="We describe and model a potential re-equili-
  207. bration process that can affect compositions of melt
  208. inclusions in magnesian olivine phenocrysts. This pro-
  209. cess, referred to as ``Fe-loss'', can operate during natural pre-eruptive cooling of host magma and results in lower
  210. FeOt and higher MgO contents within the initially
  211. trapped volume of inclusion. The extent of Fe-loss is
  212. enhanced by large temperature intervals of magma
  213. cooling before eruption. The compositions of homoge-
  214. nised melt inclusions in olivine phenocrysts from several
  215. subduction-related suites demonstrate that (1) Fe-loss is
  216. a common process, (2) the maximum observed degree of
  217. re-equilibration varies between suites, and (3) within a
  218. single sample, variable degrees of re-equilibration can be
  219. recorded by melt inclusions trapped in olivine pheno-
  220. crysts of identical composition. Our modelling also
  221. demonstrates that the re-equilibration process is fast
  222. going to completion, in the largest inclusions in the most
  223. magnesian phenocrysts it is completed within 2 years.
  224. The results we obtained indicate that the possibility of
  225. Fe-loss must be considered when estimating composi-
  226. tions of parental subduction-related magmas from nat-
  227. urally quenched glassy melt inclusions in magnesian
  228. olivine phenocrysts. Compositions calculated from
  229. glassy inclusions affected by Fe-loss will inherit not only
  230. erroneously low FeOt contents, but also low MgO due to
  231. the inherited higher Mg# of the residual melt in re-
  232. equilibrated inclusions. We also demonstrate that due to
  233. the higher MgO contents of homogenised melt inclu-
  234. sions affected by Fe-loss, homogenisation temperatures
  235. achieved in heating experiments will be higher than
  236. original trapping temperatures. The extent of overheat-
  237. ing will increase depending on the degree of re-equili-
  238. bration, and can reach up to 50 degrees C in cases where
  239. complete re-equilibration occurs over a cooling interval
  240. of 200 degrees C." name="DC.description" />
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  354.     <h1 class="ep_tm_pagetitle">Re-equilibration of melt inclusions trapped by magnesian olivine phenocrysts from subduction-related magmas: petrological implications</h1>
  355.     <p style="margin-bottom: 1em" class="not_ep_block"><span class="person_name">Danyushevsky, L.V.</span> and <span class="person_name">Della-Pasqua, F.N.</span> and <span class="person_name">Sokolov, S.</span> (2000) <xhtml:em>Re-equilibration of melt inclusions trapped by magnesian olivine phenocrysts from subduction-related magmas: petrological implications.</xhtml:em> Contributions to Mineralogy and Petrology, 138 (1). pp. 68-83.</p><p style="margin-bottom: 1em" class="not_ep_block"></p><table style="margin-bottom: 1em" class="not_ep_block"><tr><td valign="top" style="text-align:center"><a href="http://eprints.utas.edu.au/721/1/CMP2000.pdf"><img alt="[img]" src="http://eprints.utas.edu.au/style/images/fileicons/application_pdf.png" class="ep_doc_icon" border="0" /></a></td><td valign="top"><a href="http://eprints.utas.edu.au/721/1/CMP2000.pdf"><span class="ep_document_citation">PDF</span></a> - Full text restricted - Requires a PDF viewer<br />548Kb</td><td><form method="get" accept-charset="utf-8" action="http://eprints.utas.edu.au/cgi/request_doc"><input accept-charset="utf-8" value="731" name="docid" type="hidden" /><div class=""><input value="Request a copy" name="_action_null" class="ep_form_action_button" onclick="return EPJS_button_pushed( '_action_null' )" type="submit" /> </div></form></td></tr></table><p style="margin-bottom: 1em" class="not_ep_block">Official URL: <a href="http://dx.doi.org/10.1007/PL00007664">http://dx.doi.org/10.1007/PL00007664</a></p><div class="not_ep_block"><h2>Abstract</h2><p style="padding-bottom: 16px; text-align: left; margin: 1em auto 0em auto">We describe and model a potential re-equili-&#13;
  356. bration process that can affect compositions of melt&#13;
  357. inclusions in magnesian olivine phenocrysts. This pro-&#13;
  358. cess, referred to as ``Fe-loss'', can operate during natural pre-eruptive cooling of host magma and results in lower&#13;
  359. FeOt and higher MgO contents within the initially&#13;
  360. trapped volume of inclusion. The extent of Fe-loss is&#13;
  361. enhanced by large temperature intervals of magma&#13;
  362. cooling before eruption. The compositions of homoge-&#13;
  363. nised melt inclusions in olivine phenocrysts from several&#13;
  364. subduction-related suites demonstrate that (1) Fe-loss is&#13;
  365. a common process, (2) the maximum observed degree of&#13;
  366. re-equilibration varies between suites, and (3) within a&#13;
  367. single sample, variable degrees of re-equilibration can be&#13;
  368. recorded by melt inclusions trapped in olivine pheno-&#13;
  369. crysts of identical composition. Our modelling also&#13;
  370. demonstrates that the re-equilibration process is fast&#13;
  371. going to completion, in the largest inclusions in the most&#13;
  372. magnesian phenocrysts it is completed within 2 years.&#13;
  373. The results we obtained indicate that the possibility of&#13;
  374. Fe-loss must be considered when estimating composi-&#13;
  375. tions of parental subduction-related magmas from nat-&#13;
  376. urally quenched glassy melt inclusions in magnesian&#13;
  377. olivine phenocrysts. Compositions calculated from&#13;
  378. glassy inclusions affected by Fe-loss will inherit not only&#13;
  379. erroneously low FeOt contents, but also low MgO due to&#13;
  380. the inherited higher Mg# of the residual melt in re-&#13;
  381. equilibrated inclusions. We also demonstrate that due to&#13;
  382. the higher MgO contents of homogenised melt inclu-&#13;
  383. sions affected by Fe-loss, homogenisation temperatures&#13;
  384. achieved in heating experiments will be higher than&#13;
  385. original trapping temperatures. The extent of overheat-&#13;
  386. ing will increase depending on the degree of re-equili-&#13;
  387. bration, and can reach up to 50 degrees C in cases where&#13;
  388. complete re-equilibration occurs over a cooling interval&#13;
  389. of 200 degrees C.</p></div><table style="margin-bottom: 1em" cellpadding="3" class="not_ep_block" border="0"><tr><th valign="top" class="ep_row">Item Type:</th><td valign="top" class="ep_row">Article</td></tr><tr><th valign="top" class="ep_row">Additional Information:</th><td valign="top" class="ep_row">The original publication is available at www.springerlink.com</td></tr><tr><th valign="top" class="ep_row">Keywords:</th><td valign="top" class="ep_row">melt inclusions, olivine, petrology, geochemistry, subduction, magmatism, re-equilibration</td></tr><tr><th valign="top" class="ep_row">Subjects:</th><td valign="top" class="ep_row"><a href="http://eprints.utas.edu.au/view/subjects/260101.html">260000 Earth Sciences &gt; 260100 Geology &gt; 260101 Mineralogy and Crystallography</a><br /><a href="http://eprints.utas.edu.au/view/subjects/260102.html">260000 Earth Sciences &gt; 260100 Geology &gt; 260102 Igneous and Metamorphic Petrology</a></td></tr><tr><th valign="top" class="ep_row">ID Code:</th><td valign="top" class="ep_row">721</td></tr><tr><th valign="top" class="ep_row">Deposited By:</th><td valign="top" class="ep_row"><span class="ep_name_citation"><span class="person_name">Assoc. Prof Leonid Danyushevsky</span></span></td></tr><tr><th valign="top" class="ep_row">Deposited On:</th><td valign="top" class="ep_row">14 Feb 2007</td></tr><tr><th valign="top" class="ep_row">Last Modified:</th><td valign="top" class="ep_row">09 Jan 2008 02:30</td></tr><tr><th valign="top" class="ep_row">ePrint Statistics:</th><td valign="top" class="ep_row"><a target="ePrintStats" href="/es/index.php?action=show_detail_eprint;id=721;">View statistics for this ePrint</a></td></tr></table><p align="right">Repository Staff Only: <a href="http://eprints.utas.edu.au/cgi/users/home?screen=EPrint::View&amp;eprintid=721">item control page</a></p>
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