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Quartz zoning and the pre-eruptive evolution of the ~340-ka Whakamaru magma systems, New Zealand

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Abstract

Cathodoluminescence (CL) zoning in quartz crystals from rhyolitic pumices in two ignimbrite members of the ~340-ka Whakamaru super-eruption deposits, Taupo Volcanic Zone, New Zealand, is investigated in conjunction with the analysis of Ti concentration in quartz to reconstruct the history of changing magma chamber conditions and to elucidate the eruption-triggering processes. CL intensity images are taken as a proxy for Ti concentration and thus temperature and/or pressure and/or compositional variations during crystal growth history. Estimates of the maximum temperature changes (i.e., assuming other factors influencing Ti uptake remain constant) are made using the TitaniQ geothermometer based on the Ti concentration in quartz. These results are reviewed in comparison with Fe–Ti oxide, feldspar-melt and amphibole geothermometry. Core-to-rim quartz Ti profiles record a marked change in conditions (temperature increase and/or pressure decrease and/or change in melt composition) causing and then following a significant resorption horizon in the outer parts of the crystals. Two alternative models that could explain the quartz Ti zonation invoke a temperature increase caused by mafic recharge and/or a pressure decrease due to magma ponding and re-equilibration at shallow crustal levels. Concomitant changes in melt composition and Ti activity may, however, also have strongly influenced Ti uptake into the quartz. Some crystals also show other marked increases in CL brightness internally, but any accompanying magmatic changes did not result in eruption. Diffusion modelling indicates that this significant change in conditions occurred over ~10–85 years prior to caldera-forming eruption. This rapid thermal pulse or pressure change is interpreted as evidence for open-system processes, and appears to record a magma chamber recharge event that rejuvenated the Whakamaru magma system (melt-dominant magma plus crystal mush), and potentially acted as a trigger for processes that led to eruption.

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Acknowledgments

We thank Norman Charnley (University of Oxford) for his assistance with the electron microprobe work and helping acquire Ti-in-quartz data. Stuart Kearns (University of Bristol) is also acknowledged for his help with the CL imaging. We also thank Stephen Reed (University of Cambridge) for his interest in the CL of quartz during the early stages of this investigation. NEM acknowledges postgraduate funding from the Woolf Fisher Trust (New Zealand), and CJNW acknowledges support from the Marsden Fund (VUW0813) administered by the Royal Society of New Zealand. We thank Fidel Costa, an anonymous reviewer, journal editor Jon Blundy and Aidan Allan for their valuable comments.

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Authors and Affiliations

  1. Department of Earth Sciences, University of Oxford, South Parks Road, Oxford, OX1 3AN, UK

    N. E. Matthews, D. M. Pyle & V. van Hinsberg

  2. Research Laboratory for Archaeology and the History of Art, University of Oxford, South Parks Road, Oxford, OX1 3QY, UK

    V. C. Smith

  3. School of Geography, Environment and Earth Sciences, Victoria University, PO Box 600, Wellington, 6040, New Zealand

    C. J. N. Wilson

  4. School of Earth and Atmospheric Sciences, Georgia Institute of Technology, 311 Ferst Drive, Atlanta, GA, 30332, USA

    C. Huber

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Correspondence to N. E. Matthews.

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Communicated by J. Blundy.

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Below is the link to the electronic supplementary material. Full glass chemistry, Fe–Ti oxide compositions, feldspar rim compositions and Ti-in-quartz data are provided in the supplementary electronic appendix.

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410_2011_660_MOESM9_ESM.eps

Petrographic and BSE-SEM images of pumice clasts: A—Pyroxene-rich layers in sample P1915 in crossed-polarized light (CPL) and plain-polarized light (PPL); B—Crystal clots of pyroxene (pyx), Fe–Ti oxides (ox) and feldspars (feld) in samples P1915, P1920 and P1905; C—Strong oscillatory zoning, fracturing and sieve textures in plagioclase phenocrysts, indicating open-system processes. (EPS 21211 kb)

410_2011_660_MOESM10_ESM.eps

CL images of quartz in the 5 selected pumice samples; note bright-CL rims and complex internal zoning in dark cores. Scale bar is 500 μm for all images. Codes refer to pumice samples where P1905, P1910 and P1915 are Rangitaiki pumice and P1920 and P1827 are Whakamaru. (EPS 40387 kb)

Appendix

Appendix

The derivation for the 1D analytical method is described in Fig. 11. This method provides a means of accounting for the angle between the diffusion transect and the line perpendicular to the core–rim boundary.

Fig. 11
figure 11

Detail of the core–rim interface (plan view), where the black dashed line indicates the calibrated CL transect and the black line represents the ideal diffusion modelling profile, oriented perpendicular to the core–rim interface. In order to correct for this angle to the diffusion boundary, we consider the ‘true’ and ‘apparent’ widths of the transition zone, where the ratio of true/apparent widths is given by x/y = yCosα/y = cosα (where α is the angle to perpendicular from the core–rim boundary)

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Matthews, N.E., Pyle, D.M., Smith, V.C. et al. Quartz zoning and the pre-eruptive evolution of the ~340-ka Whakamaru magma systems, New Zealand. Contrib Mineral Petrol 163, 87–107 (2012). https://doi.org/10.1007/s00410-011-0660-1

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