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Geochemistry and Geochronology of the Society Islands: New Evidence for Deep Mantle Recycling William M. White Dept. of Geological Sciences, Cornell University, Ithaca, New York Robert A. Duncan College of Oceanic and Atmospheric Sciences, Oregon State Universty, Corvalis, Oregon We report new K-Ar ages, Sr, Nd, and Pb isotope ratios and concentrations of 34 trace elements in volcanic rocks from the Society Islands. Maximum ages of volcanism at Mehetia, Tahiti, and Maupiti indicate that volcanism in the Society Islands progresses southeastward at a rate of 11 cm/yr, which is consistent with current estimates of Pacific Plate motion. Tahaa has the largest range in ages, 2.3 million years. This large range reflects the eruption of highly undersaturated lavas during a post- erosional phase that followed a volcanic hiatus of 1.2 million years. The entire range of isotope ratios observed in the Society Islands is nearly encompassed by the range observed on Tahaa: the two post- erosional lavas have among the most depleted isotopic signatures while the shield series lavas have the most enriched isotopic signatures. The isotopic and chemical evolution of Tahaa thus follows the Hawaiian pattern. There is a strong correlation between Sr and Nd isotope ratios and weaker correla- tions involving Pb isotope ratios. Compared to other oceanic islands, Sr and Nd ratios range to extremely high and low values respectively, but Pb isotope ratios are intermediate. The isotope correla- tions indicate the Society plume can be approximately modeled as consisting of two slightly hetero- geneous end members. All magmas are moderately to strongly enriched in light rare earth elements as well as other incompatible elements. After exclusion of weathered (as indicated by anomalous Ba/Rb ratios) and differentiated lavas, there are strong correlations between Hf/Sm, Pb/Ce, Zr/Nb, Nb/U, 87 86 ε 207 204 and Rb/Sr and Sr/ Sr (and Nd and Pb/ Pb) and weaker correlations between Nb/La and La/ 87 86 207 204 Sm and Sr/ Sr (and εNd and Pb/ Pb). This indicates the variation in Hf/Sm, Pb/Ce, Zr/Nb, Nb/ U, and Rb/Sr is largely due to variations in the composition of the source. This inference is confirmed by factor analysis. On the other hand, variance in the La/Sm ratio appears dominated by varying degrees of partial melting, perhaps because differences between the two end members in La/Sm are small. The high 87Sr/86Sr component in the plume has high 207Pb/204Pb and Pb/Ce and low Nb/U. These characteristics are consistent with this component consisting partly of sediment that has been subducted into the deep mantle. The low 87Sr/86Sr component in the Society plume appears to be also richer in incompatible elements than depleted mantle and is isotopically similar to the common com- ponent of plumes postulated by others. This component is most prevalent in late and very early stage Society magmas and thus probably constitutes the sheath of the Society plume. This sheath was most likely viscously entrained in the deep mantle during ascent of the plume. INTRODUCTION • Mantle plumes are not characterized by a single com- position, each plume is somewhat unique [e.g., Sun, 1980; It now seems well established that oceanic island basalts Zindler et al., 1982]. are derived from mantle plumes. In the nearly 25 years • Despite this, plumes can be divided on the basis of their since the papers of Morgan [1971] and Schilling [1973] isotope compositions into just a few classes [White, 1985]. that introduced and popularized the concept, a limited un- Schilling [1973], and later Wasserburg and DePaolo [1977], derstanding of the physics and chemistry of mantle plumes proposed that plumes consisted of “primordial”, or primi- has been achieved. This understanding may be summa- tive mantle. Although many plumes contain some primor- rized as follows: dial He, we now recognize primitive mantle cannot be the • Mantle plumes differ fundamentally in composition primary constituent of any of these plume classes. from the depleted upper mantle, the presumed source of • Fluid dynamic studies have demonstrated that plume- mid-ocean ridge basalts [Schilling, 1973; Hart et al., 1973]. like features arise from thermal boundary layers in con- vecting systems that are heated from below. Thus mantle plumes must arise from a thermal boundary layer in the Copyright 1995 by the American Geophysical Union. deep mantle. The most likely candidates are the core– Reprinted from: Isotope Studies of Crust-Mantle Evolution, mantle boundary or, if the γ-olivine–perovskite transition an AGU Monograph honoring M. Tatsumoto and G. Tilton. ed- is a barrier to whole mantle convection, the 660 km seis- ited by A. Basu and S. R. Hart. In press. mic discontinuity. WHITE AND DUNCAN: NEW EVIDENCE FOR DEEP MANTLE RECYCLING 2 • The plume heat flux is small compared to the heat loss and sediment. through plate creation, implying plumes are a second order We report on an isotopic and trace element study of eight feature of mantle convection [Davies, 1988]. Neverthe- of the Society Islands (Figure 1). Two of the islands, Ta- less, assuming the plume mass flux (presently about 2.5 × hiti and Tahaa, were selected for more detailed study. Ta- 1014 kg/yr) has been constant through geologic time, about hiti is the largest and one of the youngest of the Society 25% of the mass of the mantle has been cycled through Islands, and the results of our study are reported in Duncan plumes, hence plumes may have played a significant role et al. [1994]. We found that volcanic evolution there fol- in the chemical evolution of the Earth. If material resides lows the Hawaiian pattern in which late state magmas are in the thermal boundary layer for 109 yrs before being in- more alkalic and have less enriched isotopic signatures than corporated in plumes, then this boundary layer must con- magmas of the earlier shield building phase. In this report, stitute 6% of the mass of the mantle. This volume is an we show that post-erosional magmas from Tahaa, which order of magnitude larger than the continental crust. If in- were erupted after a hiatus of 1.3 Ma, have dramatically compatible element abundances in plumes are an order of lower Sr and Pb isotope ratios and higher Nd isotope ratios magnitude lower than in the continental crust, then the in- than magmas erupted during the main shield building stage. compatible element inventory in the plume source layer is We also show that Pb isotope and trace element ratio varia- comparable to that of the continents. tions, particularly Pb/Ce and Nb/U ratios, in the Society • The geochemistry of plumes, however, bears no im- Island magmas as a whole are consistent with the hypoth- print of their deep mantle origin. There is, for example, no esis that the high 87Sr/86Sr component in the Society plume evidence that plumes lost or gained siderophile elements consists in part of recycled marine sediment or continental through reaction with the core [Newsom et al., 1986]. There crust. The low 87Sr/86Sr component in the Society plume is no obvious imprint of trace element fractionation between may be the common component in plumes, which has been silicate liquid and deep mantle phases such as majorite or variously called FOZO [Hart et al.,1992], PHEM [Farley perovskite [Kato et al. 1987; Kato et al. 1988]. However, et al., 1992], and “C” [Hanan and Graham, 1994]. Since no studies have been specifically designed to test the latter. this latter component is most prevalent in early and late Because of the absence of this deep mantle imprint, stage lavas, we speculate that it constitutes the entrained geochemical studies have not contributed to resolving the sheath, whereas the recycled component, which dominates question of the depth from which plumes originate. the shield-building stage, constitutes the core of the plume. • Two principal theories have been proposed to describe how plumes may have acquired their peculiar geochemical ANALYTICAL METHODS features. First, Chase [1981] and Hofmann and White [1980, 1982] proposed that subduction carried oceanic crust Isotopic Analyses into the deep mantle, perhaps the core mantle boundary, where it is reheated and eventually risies buoyantly as To avoid sample contamination during grinding, rock mantle plumes. McKenzie and O’Nions [1983] proposed chips rather than powders were used for isotopic analysis. subcontinental lithosphere might sometimes delaminate, Two to three hundred mg of chips were weighed into teflon sink into the deep mantle, and eventually rising buoyantly beakers or capsules, and leached for approximately 30 min- as a mantle plume. Most current hypotheses for the geo- utes in 1 to 2 ml of hot 6N HCl prior to dissolution. The chemical evolution of plumes are variations on these two leaching process serves not only to remove Pb contamina- main ideas. Alternatively, delamination might remove and tion introduced during handling, but also to remove Sr con- “recycle” lower continental crust as well as mantle lithos- phere [Kay and Kay, 1991]. 153° 152° 151° 150° 149 148° 147° W The present study was undertaken with the specific ob- 15° 2000 m jective of testing the hypothesis that plumes, or at least some 3000 m of them, consist of deeply recycled oceanic crust and sedi- 16° 3000 m 4 ment. Earlier studies had shown that basalts from the So- Tupai 000 m Bora Bora ciety Islands have particularly radiogenic Sr [Duncan and Maupiti 4000 m Tahaa Hauhine Compston, 1976; Hedge, 1978]. White and Hofmann [1982] 17° Raiatea Tetiaroa 3000 m proposed on the basis of Sr and Nd isotope ratios that the Moorea 2000 m Teahetia Maiao Rocard Society mantle plume acquired its unique geochemical char- TahitiNui ° TahitiIti acteristics from subduction and recycling of ancient oce- 18 CyanaMehetia 4000 anic sediment.

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