HR: 0800h
AN: V41F-1538    [Abstracts]
TI: Ti-in-Zircon Thermometer: Preliminary Results
AU: * Fu, B
EM: binfu@geology.wisc.edu
AF: Dept. of Geology and Geophysics, Univ. of Wisconsin, Madison, WI 53706
AU: Cavosie, A J
V41F-1538 AF: Dept. of Geology and Geophysics, Univ. of Wisconsin, Madison, WI 53706
AU: Cavosie, A J
V41F-1538 AF: Dept. of Geology, Univ. of Puerto Rico, Mayaguez, PR 00681-9017
AU: Clechenko, C C
V41F-1538 AF: Dept. of Geology and Geophysics, Univ. of Wisconsin, Madison, WI 53706
AU: Fournelle, J
V41F-1538 AF: Dept. of Geology and Geophysics, Univ. of Wisconsin, Madison, WI 53706
AU: Kita, N T
V41F-1538 AF: Dept. of Geology and Geophysics, Univ. of Wisconsin, Madison, WI 53706
AU: Lackey, J
V41F-1538 AF: Dept. of Geology and Geophysics, Univ. of Wisconsin, Madison, WI 53706
AU: Lackey, J
V41F-1538 AF: Dept. of Geology, The College of Wooster, Wooster, OH 44691
AU: Page, F
V41F-1538 AF: Dept. of Geology and Geophysics, Univ. of Wisconsin, Madison, WI 53706
AU: Wilde, S A
V41F-1538 AF: School of Applied Geology, Curtin Univ., Perth, WA 6845 Australia
AU: Valley, J W
EM: valley@geology.wisc.edu
AF: Dept. of Geology and Geophysics, Univ. of Wisconsin, Madison, WI 53706
AB: The titanium in zircon thermometer has been applied to 167 zircons from diverse rock types. These rocks include metamorphosed anorthosite and gabbro (1.15 Ga, intrusion age), and unmetamorphosed granitic pegmatite (0.9 Ga) from the Adirondack Highlands; metaluminous and peraluminous granites (114-90 Ma) of the Sierra Nevada Batholith; megacrysts from kimberlite pipes in southern Africa, Brazil, and Siberia; and detrital zircons (4.4-3.9 Ga) of metaconglomerate from Jack Hills, Western Australia. Titanium concentration in zircon was analysed using a CAMECA IMS-1280 ion microprobe (see Page et al., this volume). Spot analyses were correlated to U-Pb SHRIMP pits especially for Adirondack and Jack Hills zircons. The majority of zircons have Ti-content less than 10 ppm. Variability, in excess of analytical precision, within individual zircons is observed in about one-third of crystals. In general, there is no systematic change in Ti from core to rim (identified by cathodoluminescence) of zircons, or with regard to age, U content, Th/U ratio, or U-Pb age concordance for these non-metamict grains. The average temperatures for zircon crystallization in different rock suites using the experimental/empirical calibration of Watson and Harrison (W&H, 2005, Science 308:841), assuming the presence of rutile and quartz, are estimated to be: anorthosite 735±41°C (1SD, n=24; Ti = 10±5 ppm); metagabbro 714±31°C (n=19; Ti = 8±4 ppm); Adirondack pegmatite 500±16°C (n=5; Ti = 0.3±0.1 ppm); metaluminous and peraluminous granites from Sierra Nevada 681±67°C (n=53; Ti = 6±5 ppm) and 613±75°C (n=68; Ti = 3±3 ppm); kimberlite megacrysts 740±64°C (n=169; Ti = 14±13 ppm) (Page et al., this volume); and detrital zircons from Jack Hills metaconglomerate 718±63°C (n=64; Ti = 10±9 ppm). Most of the host rocks contain ilmenite or titanite suggesting that α(TiO₂)>0.5, but rutile activity is unknown for megacrysts and detrital zircons. Pegmatite contains no Ti-rich minerals, permissive of low rutile activity. Peraluminous granites have lower whole-rock TiO₂ content (0.02-0.21 wt.%) than metaluminous granites (0.54-0.91 wt.%), and both have similar zircon saturation temperatures (710-780°C). The low Ti content and apparent temperature in zircons from anorthosite and metagabbro (magmatic T = ca. 1000-1100°C) and the homogeneity of igneous zircon cores vs. metamorphic rims in metagabbro suggest that Ti content was reset during granulite-facies metamorphism (750°C, 1.0 Ga), in contrast to the current estimate of extremely low diffusivity of Ti in zircon. The Ti contents of >3.9 Ga Jack Hills detrital zircons are consistent with previously published data that were used to constrain magmatic temperature and thus the composition of unknown host rocks (W&H, 2005, Science 308:841). However, these values overlap those from both felsic and mafic rocks, and the Ti data are not sufficient to independently identify parent melt chemistry unless post-crystallization changes can be ruled out. The best evidence of pre-4 Ga evolved crust is provided by previously reported oxygen isotope ratios and felsic mineral inclusions in zircon (see Cavosie et al., 2005, EPSL 235:663).
DE: 1011 Thermodynamics (0766, 3611, 8411)
DE: 1036 Magma chamber processes (3618)
DE: 1042 Mineral and crystal chemistry (3620)
DE: 1065 Major and trace element geochemistry
DE: 3651 Thermobarometry
SC: Volcanology, Geochemistry, Petrology [V]
MN: Fall Meeting 2005