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Thermal evolution of silicic magma chambers after basalt replenishments

Published online by Cambridge University Press:  03 November 2011

Takehiro Koyaguchi  and
Katsuya Kaneko
Takehiro Koyaguchi
Affiliation:
Department of Complexity Science and Engineering, University of Tokyo, 7-3-1 Hongo, Bunkyo-ku, Tokyo 113-0033,Japan; e-mail: tak@eri.u-tokyo.ac.jp
Katsuya Kaneko
Affiliation:
Geological Survey of Japan, Tsukuba 305-8567,Japan; e-mail: katusya@gsj.go.jp
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Abstract

In order to understand the governing factors of petrological features of erupted magmas of island-arc or continental volcanoes, thermal fluctuations of subvolcanic silicic magma chambers caused by intermittent basalt replenishments are investigated from the theoretical viewpoint. When basaltic magmas are repeatedly emplaced into continental crust, a long-lived silicic magma chamber may form. A silicic magma chamber within surrounding crust is composed of crystal-melt mixtures with variable melt fractions. We define the region which behaves as a liquid in a mechanical sense (‘liquid part’) and the region which is in the critical state between liquid and solid states (‘mush’) collectively as a magma chamber in this study. Such a magma chamber is surrounded by partially molten solid with lower melt fractions. Erupted magmas are considered to be derived from the liquid part. The size of a silicic magma chamber is determined by the long-term balance between heat supply from basalt and heat loss by conduction, while the temperature and the volume of the liquid part fluctuate in response to individual basalt inputs. Thermal evolution of a silicic magma chamber after each basalt input is divided into two stages. In the first stage, the liquid part rapidly propagates within the magma chamber by melting the silicic mush, and its temperature rises above and decays back to the effective fusion temperature of the crystal-melt mixture on a short timescale. In some cases the liquid part no longer exists. In the second stage, the liquid part ceases to propagate and cools slowly by heat conduction on a much longer timescale. The petrological features of the liquid part, such as the amount of unmelted preexisting crystals, depend on the intensity of individual pulses of the basalt heat source and the degree of fractionation during the first stage, as well as the bulk composition of the silicic magma.

Keywords

conductionconvectiongranitemass and heat transfermush
Type
Research Article
Information
Earth and Environmental Science Transactions of The Royal Society of Edinburgh , Volume 91 , Issue 1-2: Fourth Hutton Symposium: The Origin of Granites and Related Rocks , 2000 , pp. 47 - 60
Copyright
Copyright © Royal Society of Edinburgh 2000

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References

Barboza, S. A.& Bergantz, G. W. 1998. Rheological transitions and progress of melting of crustal rocks. Earth and Planetary Science Letters 158, 19–29.Google Scholar
Bergantz, G. W. 1989. Underplating and partial melting: Implication for melt generation and extraction. Science 245, 1093–5.Google Scholar
Bergantz, G. W.& Dawes, R. 1994. Aspects of magma generation and ascent in continental lithosphere. In Ryan, M.P. (ed.) Magmatic Systems, 291–317. London: Academic Press.Google Scholar
Campbell, I. H.& Turner, J. S. 1986. Fountain in magma chambers. Journal of Petrology 30, 885–923.Google Scholar
Chen, C. H., Nakada, S., Shieh, Y. N.& DePaolo, D. J. 1999. The Sr, Nd and O isotopic studies of the 1991–1995 eruption at Unzen, Japan. Journal of Volcanology and Geothermal Research 89, 243–53.Google Scholar
Dawson, P. B., Evans, J. R.& Iyer, H. M. 1990 Teleseismic tomography of the compressional wave velocity structure beneath the Long Valley Region, California. Journal of Geophysical Research 95, 11021–50.Google Scholar
Fedotov, S. A. 1982. Temperatures of entering magma, formation and dimensions of magma chambers of volcanoes. Bulletin of Volcanology 45, 333–47.Google Scholar
Fernandez, A. N.& Barbarin, B. 1991. Relative rheology of coeval mafic and felsic magmas: Nature of resulting interaction processes and shape and mineral fabrics of mafic microgranular enclaves. In Didier, J.& Barbarin, B. (eds) Enclaves and Granitic Petrology, 263–75. Amsterdam: Elsevier.Google Scholar
Huppert, H. E.& Sparks, R. S. J. 1988a. The generation of granitic magmas by intrusion of basalt into continental crust. Journal of Petrology 29, 599–624.Google Scholar
Huppert, H. E.& Sparks, R. S. J. 1988b. Melting the roof of a chamber containing a hot, turbulently convecting fluid. Journal of Fluid Mechanics 188, 107–31.Google Scholar
Kerr, R. C. 1994. Melting driven by vigorous compositional convection. Journal of Fluid Mechanics 280, 255–85.Google Scholar
Koyaguchi, T.& Kaneko, K. 1999. A two-stage thermal evolution model of magmas in continental crust. Journal of Petrology 40, 241–54.Google Scholar
Marsh, B. D. 1981. On the crystallinity, probability of occurrences and rheology of lava and magma. Contributions to Mineralogy and Petrology 78, 85–98.Google Scholar
Marsh, B. D. 1989. On convection style and vigor in sheet-like magma chambers. Journal of Petrology 30, 479–530.Google Scholar
Mori, J., Eberhart-Phillips, D.& Harlow, D. H. 1996. Three-dimensional velocity structure at Mount Pinatubo: Resolving magma bodies and earthquake hypocenters. In Newhall, C.G.& Punongbayan, R.S. (eds) Fire and Mud: Eruptions and Lahars of Mount Pinatubo, Philippines, 371–82. Seattle: Philippine Institute of Volcanology and Seismology, Quezon City and University of Washington Press.Google Scholar
Nakamura, M. 1995. Continuous mixing of crystal mush and replenished magma in the ongoing Unzen eruption. Geology 23, 807–10.Google Scholar
Pallister, J. S., Hoblitt, R. P., Meeker, G. P., Knight, R J.& Siems, D. F. 1996. Magma mixing at Mount Pinatubo: petrographic and chemical evidence from the 1991 deposits. In Newhall, C. G.& Punongbayan, R. S. (eds) Fire and Mud: Eruptions and Lahars of Mount Pinatubo, Philippines. 687–731. Seattle: Philippine Institute of Volcanology and Seismology, Quezon City and University of Washington Press.Google Scholar
Petford, N. 1995. Segregation of tonalitic-trondhjemitic melts in the continental crust: The mantle connection. Journal of Geophysical Research 100, 15735–43.Google Scholar
Pitcher, W. S. 1991. Synplutonic dykes and mafic enclaves. In Didier, J.& Barbarin, B. (eds) Enclaves and Granitic Petrology, 383–91. Amsterdam: Elsevier.Google Scholar
Piwinskii, A. J.& Wyllie, P. J. 1968. Experimental studies of igneous rock series: A zoned pluton in the Wallowa batholith, Oregon. Journal of Geology 76, 205–34.Google Scholar
Piwinskii, A. J.& Wyllie, P. J. 1970. Experimental studies of igneous rock series: Felsic body suites from the Needle Point Pluton, Wallowa batholith, Oregon. Journal of Geology 78, 52–76.Google Scholar
Rutter, E. H.& Neumann, D. H. K. 1995. Experimental deformation of partially molten Westerly granite under fluid absent conditions, with implications for the extraction of granitic magmas. Journal of Geophysical Research 100, 15697–751.Google Scholar
Sakuyama, M.& Koyaguchi, T. 1984. Magma mixing in mantle xenolith-bearing calc-alkalic ejecta, Inchinomegata Volcano, Northeastern Japan. Journal of Volcanology and Geothermal Research 22, 199–224.Google Scholar
Shaw, H. R. 1980. The fracture mechanisms of magma transport from the mantle to the surface. In Hargreaves, R.B. (ed.) Physics of Magmatic Processes, 201–64. Princeton: Princeton University Press.Google Scholar
Spera, F. J. 1979. Thermal evolution of plutons: a parameterized approach. Science 207, 299–301.Google Scholar
Tsukui, M., Sakuyama, M., Koyaguchi, T.& Ozawa, K. 1986. Longterm eruption rates and dimensions of magma reservoirs beneath quaternary polygenetic volcanoes in Japan. Journal of Volcanology and Geothermal Research 29, 189–202.Google Scholar
Turcotte, D. L.& Schubert, G. 1982. Geodynamics: Applications of continuum physics to geological problems. New York: John Wiley & Sons.Google Scholar
Turner, J. S. 1973. Buoyancy effects in fluids. Cambridge: Cambridge University Press.Google Scholar
Vigneresse, J. L., Barbey, P.& Cuney, M. 1996. Rheological transitions during partial melting and crystallization with application to felsic magma segregation and transfer. Journal of Petrology 27, 1579–600.Google Scholar
Wiebe, R. A. 1991. Commingling of contrasted magmas and generation of mafic enclaves in granitic rocks. In Didier, J.& Barbarin, B. (eds) Enclaves and Granitic Petrology, 393–402. Amsterdam: Elsevier.Google Scholar
Wiebe, R. A. 1996. Mafic-silicic layered intrusions: the role of basaltic injections on magmatic processes and the evolution of silicic magma chambers. Transactions of the Royal Society of Edinburgh: Earth Sciences 87, 233–42.Google Scholar
Woods, A. W. 1991. Fluid mixing during melting. Physics of Fluids A 3, 1393–404.Google Scholar
Wyllie, P. J. 1977. Crustal anatexis: an experimental review. Tectono-physics 43, 41–71.Google Scholar