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Crystal and Magma Residence at Kilauea Volcano, Hawaii: 230Th^226Ra Dating of the 1955 East Rift Eruption

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Crystal and Magma Residence at Kilauea Volcano, Hawaii: 230Th^226Ra Dating of the 1955 East Rift Eruption Earth and Planetary Science Letters 184 (2001) 703^718 www.elsevier.com/locate/epsl Crystal and magma residence at Kilauea Volcano, Hawaii: 230Th^226Ra dating of the 1955 east rift eruption Kari M. Cooper a;b;*, Mary R. Reid a, Michael T. Murrell b, David A. Clague c a Department of Earth and Space Sciences, UCLA, 595 Charles Young Drive East, Los Angeles, CA 90095-1567, USA b Los Alamos National Laboratory, P.O. Box 1663, MS J514, Los Alamos, NM 87545, USA c Monterey Bay Aquarium Research Institute, P.O. Box 628, 7700 Sandholdt Road, Moss Landing, CA 95039, USA Received 29 March 2000; received in revised form 26 October 2000; accepted 2 November 2000 Abstract Previous estimates of crustal storage time of magmas at Kilauea Volcano, Hawaii, range from a few years to a few thousand years, leading to considerable uncertainty in the time scales of processes of magmatic storage and differentiation. We present a new approach for determining minimum magma residence times which involves dating phenocrysts in a magma using 226Ra^230Th disequilibria, and apply this approach to the early phase of the 1955 east rift eruption at Kilauea. When fractionation of Ra from Ba (a proxy for initial Ra in the crystals) during crystal growth is considered along with the effects of inclusions in the minerals, the data are consistent with co-precipitation of 300 plagioclase and clinopyroxene from a melt represented by the groundmass at a mean age of 10003400 a. Unless a significant fraction ( s 30%) of the crystals are remnants from an earlier batch of evolved magma in the system, these data constrain the minimum magmatic residence time to be V550 yr, considerably longer than most previous estimates of storage time at Kilauea as well as those for some other basaltic systems. For the temperature interval of augite+plagioclase growth in the early 1955 magma, a maximum constant cooling rate of 0.1³C/yr (1U1035³C/h) is derived from the minimum magmatic residence time of 550 yr. The total magma storage time would be s 2500 yr if this cooling rate applied to the entire thermal history of the magma, although a more complex cooling history where cooling rates were more rapid early in the storage history is permissive of a total residence time which is not much longer than 550 yr. The disparate estimates of magma residence at Kilauea may reflect the uncertainties in the methods of estimation in addition to true variations in storage time for different batches of magma. More work is necessary in order to determine whether a long residence time is characteristic of rift zone lavas and/or of Kilauean lavas in general. ß 2001 Elsevier Science B.V. All rights reserved. Keywords: Kilauea; Th-230/Ra-226; residence time 1. Introduction The residence time of magma in crustal reser- voirs has implications for our understanding of * Corresponding author. Tel.: +1-310-206-1938; rates of crystal growth and magmatic di¡erentia- Fax: +1-310-825-2779; E-mail: [email protected] tion, and for the thermal regime of magma reser- 0012-821X / 01 / $ ^ see front matter ß 2001 Elsevier Science B.V. All rights reserved. PII: S0012-821X(00)00341-1 EPSL 5692 4-1-01 704 K.M. Cooper et al. / Earth and Planetary Science Letters 184 (2001) 703^718 voir systems. The time scales of such processes are Our approach to constraining residence times di¤cult to quantify and, for Hawaiian volcanoes of Hawaiian magmas is the ¢rst direct measure- in particular, estimates are quite disparate. Some ment of magma residence in Kilauea's east rift of the range in ages may re£ect the fact that the reservoir and is based on 230Th^226Ra dating of di¡erent methods average residence times over mineral and groundmass separates from lavas. di¡erent time and length scales, such that esti- The magnitude of disequilibrium between 230Th 226 mates range from V10 yr for the last part of and its immediate daughter Ra (t1=2 = 1600 yr) the storage history of a single batch of magma is a function of the initial fractionation of Ra [1] based on crystal size distributions, to an aver- from Th and of the time elapsed since crystal age residence time of 90^180 and 30^40 yr based growth. One underlying uncertainty in this ap- on geochemical variations in magmas erupted at proach results from the fact that no longer-lived the summit during the early and late 20th century, isotope of Ra exists. In this study, we evaluate respectively [2], to an average residence time of potential complications involved in the standard 100^3000 yr [3,4] for the entire interconnected assumption that the magnitude of crystal^liquid volume of the magma reservoir system beneath fractionation of Ba can be used to delimit the Kilauea based on geophysical estimates of reser- amount of 226Ra incorporated initially by the voir size and magma supply rate. Furthermore, crystal. By accounting for these uncertainties, we few estimates of residence time for magmas obtain a minimum age of crystallization. From erupted from Kilauea's rift zones exist, although this, we determine a minimum magmatic residence an estimate of 7^14 yr [5] is an average for Puu time for the early stage of the 1955 east rift erup- Oo lavas based on temporal changes in geochem- tion of Kilauea, which will apply unless the mag- istry. ma contains a large ( s 30%) proportion of old xenocrysts. 2. Geological background The location, size and shape of Kilauea's reser- voir system is inferred from the locus of erup- tions, the distribution of aseismic zones within the volcanic edi¢ce [6], geodesy (e.g., [4]), and chemical variations in erupted lavas [2,7,8]. Shal- low storage of magma at Kilauea takes place in a relatively equant summit reservoir, the top of which is 2^4 km below the surface, and also in dike-like bodies beneath the rift zones which ex- tend radially from the summit reservoir, and from near-surface to V9 km depth (e.g., [6,9]). In de- tail, the size, shape, and degree of interconnectiv- ity of the summit and rift reservoirs are poorly Fig. 1. Map showing extent of the £ows of the 1955 east rift constrained (e.g., [2^4,10]), resulting in uncer- eruption and sample locality (after [11]). Early £ows shown tainty about the extent to which the magma res- in black, late £ows in stippled pattern. Inset shows index ervoirs can be considered physically and chemi- map of the island of Hawaii, showing the boundaries be- cally well-mixed. tween volcanoes, abbreviated as follows: KH, Kohala; MK, The data presented in this study are for a sam- Mauna Kea; HU, Hualalai; and ML, Mauna Loa. Kilauea ple of the early phase of Kilauea's 1955 east rift is shown in the ruled pattern, along with its summit (small circle) and rift zones (curved lines radiating from summit re- eruption collected near vents E and J (Fig. 1; vent gion), after [33]. Box indicates area shown in main ¢gure. nomenclature of [11]). This phase of the eruption EPSL 5692 4-1-01 K.M. Cooper et al. / Earth and Planetary Science Letters 184 (2001) 703^718 705 produced some of the most evolved lavas erupted and makes it a good candidate for having experi- at Kilauea, with compositions ranging from 5.0 to enced a measurable (longer than a few tens of 5.7 wt% MgO [7,11]. After approximately half of years) residence time. The 1955 eruption was the the V0.1 km3 total volume of the 1955 lava had ¢rst eruption on the lower east rift zone of Ki- erupted, the composition changed abruptly to the lauea in over 100 years, and followed by 31 years more magnesian (6.2^6.8% MgO) lavas character- the last intrusion recorded in the rift zone (in 1924 istic of the late 1955 eruption [11,12], and eruptive [7]). Thus, if the early 1955 lava was stored in the activity localized at a restricted number of up-rift rift zone prior to eruption, its storage time was at vents (Fig. 1). The early and late 1955 lavas have least 31 years. been interpreted to be related by crystal fraction- ation on the basis of modeling of major and trace element characteristics of erupted lavas [13]. How- 3. Results ever, more recent work [14] re-evaluated this con- clusion based on extensive petrographic work 3.1. U-series analyses of mineral separates combined with additional major and trace ele- ment analyses, and concluded that the late 1955 We measured Th and U isotopic compositions lavas were best modeled as a mixture of early and abundances of Ra, Th, Ba, and U in mineral 1955 compositions with a more primitive compo- separates, groundmass, and whole rock samples nent similar to the 1952 summit lava. The early of the early 1955 lava by TIMS; results are pre- 1955 magma appears una¡ected by mixing with sented in Table 1, and analytical methods are de- this primitive magma. However, reverse zoning scribed in Appendix A. 234U/238U activity ratios and rounding of oxide phenocrysts suggest that of all phases are within error of unity (2c errors the early 1955 magma could have formed by mix- generally 9 0.5%), as expected for unaltered vol- ing of two highly di¡erentiated magmas [15]. If canic rocks. The abundances of Ra, Th, U, and magma mixing occurred, the two components Ba in the plagioclase and pyroxene separates are were probably thermally and chemically similar lower (by factors of 3^50) than those measured in because compositions and textural relations of the same phases from olivine basalt and andesite the majority of silicate phenocrysts are consistent from Mount St.
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