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Phase relations and liquid lines of descent of an iron-rich peralkaline phonolitic melt: an experimental study

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Abstract

We experimentally investigated the phase relations of a peralkaline phonolitic dyke rock associated with the Ilímaussaq plutonic complex (South Greenland). The extremely evolved and iron-rich composition (magnesium number = 2, alkalinity index = 1.44, FeO* = 12 wt%) may represent the parental magma of the Ilímaussaq complex. This dyke rock is therefore perfectly suited for performing phase-equilibrium experiments, since in contrast to the plutonic rocks of the complex, no major cumulate formation processes complicate defining a reasonable starting composition. Experiments were carried out in hydrothermal rapid-quench cold-seal pressure vessels at P = 100 MPa and T = 950–750 °C. H2O contents ranging from anhydrous to H2O saturated (~5 wt% H2O) and varying fO2 (~ΔlogFMQ −3 to +1; where FMQ represents the fayalite–magnetite–quartz oxygen buffer) were applied. Reduced and dry conditions lead to substantial crystallization of alkali feldspar, nepheline, hedenbergite-rich clinopyroxene, fayalite-rich olivine and minor amounts of ulvøspinel-rich magnetite, which represent the phenocryst assemblage of the natural dyke rock. Oxidized and H2O-rich conditions, however, suppress the crystallization of olivine in favor of magnetite and clinopyroxene with less or no alkali feldspar and nepheline formation. Accordingly, combined low fO2 and aH2O force the evolution of the residual melt toward decreasing SiO2, increasing FeO* and alkalinity index (up to 3.55). On the contrary, high fO2 and aH2O produce residual melts with relatively low FeO*, high SiO2 and a relatively constant alkalinity index. We show that variations of aH2O and fO2 lead to contrasting trends regarding the liquid lines of descent of iron-rich silica-undersaturated peralkaline compositions. Moreover, the increase in FeO* and alkalinity index (reduced and dry conditions) in the residual melt is an important prerequisite to stabilize late-magmatic minerals of the dyke rock, for example, aenigmatite (Na2Fe5TiSi6O20), coexisting with the most evolved melts at 750 °C. Contrary to what might be expected, experiments with high aH2O and interlinked high fO2 exhibit higher liquidus T’s compared with experiments performed at low aH2O and fO2 for experiments where magnetite is liquidus phase. This is because ulvøspinel-poor magnetite crystallizes at higher fO2 and has a higher melting point than ulvøspinel-rich magnetite, which is favored at lower fO2.

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Acknowledgments

We thank Indra Gill-Kopp for the careful sample preparation. Norbert Walker and Barbara Maier kindly assembled gold and graphite capsules. Philipp Bellucci, Huy-Tung Nguyen, Stephan Reiche and Rainer Babiel are thanked for support with the experimental work. XRF analyses of the starting glasses were done by Heiner Taubald, Urs Dippon performed Mössbauer spectroscopy on the starting glasses, and Harald Behrens analyzed our samples with KFT. Special thanks go to Thomas Wenzel for invaluable support with challenging EMP analyses. We thank Renat Almeev, Bruno Scaillet and an anonymous reviewer for constructive and helpful comments. Financial support of the Deutsche Forschungsgemeinschaft (grants MA 2563/4-1 and NO 378/7-1) is gratefully acknowledged.

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  1. Eberhard Karls Universität Tübingen, Wilhelmstr. 56, 72074, Tübingen, Germany

    Christopher Giehl, Michael Marks & Marcus Nowak

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  1. Christopher Giehl
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  2. Michael Marks
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Correspondence to Christopher Giehl.

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Communicated by J. Hoefs.

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Supplementary material eFig. 1 Speciation of a C-O-H fluid in equilibrium with graphite (aC = 1) for the investigated T interval (calculated after O’Neill 1987a; Huizenga 2001) (EPS 272 kb)

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Supplementary material eFig. 2 Fe2O3 and TiO2 in Afs and Nph analyses show a roughly linear relationship indicating significant contamination from the surrounding residual glass for some analyses (EPS 299 kb)

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Supplementary material eFig. 3 Phase proportions of crystal phases and residual glasses: comparison of image analysis and mass balance (EPS 349 kb)

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Supplementary material eFig. 4 Comparison of H2O contents in glasses based on KFT and the EMP by-difference method. EMP error bars are ± 1σ. The oxidation state of iron is unknown, data points are calculated as XFe3+ = 0.5, the Fe2+/3+ error accounts for XFe3+ = 0-1 and is well within statistical uncertainty. The horizontal error indicate the uncertainty if the amount of Mag is under- or overestimated by a factor of two (EPS 273 kb)

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Supplementary material eFig. 5 (a) Abundance of Mag (wt. %) correlated with XUsp, typical errors are given for mass balance and image analysis, the error for XUsp is represented by the symbol size and (b) prevailing fO2 correlated with XUsp. Inherited Mag from hydrated starting glasses did not fully equilibrate in reduced H2O-bearing experiments (EPS 587 kb)

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Supplementary material eFig. 6 Correlation of T in dry experiments with XFe3+ in (a) Mag and (b) Cpx expressed as decreasing XUsp for Mag and increasing XAeg for Cpx. Corresponding (c) Na2O content (wt. %) and (d) A. I. of the coexisting residual melt are shown. For symbols, see Figs. 5 & 6 (EPS 336 kb)

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Giehl, C., Marks, M. & Nowak, M. Phase relations and liquid lines of descent of an iron-rich peralkaline phonolitic melt: an experimental study. Contrib Mineral Petrol 165, 283–304 (2013). https://doi.org/10.1007/s00410-012-0809-6

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  • DOI: https://doi.org/10.1007/s00410-012-0809-6

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