Petrology of lavas from episodes 2?47 of the Puu Oo eruption of Kilauea Volcano, Hawaii: Evaluation of magmatic processes

Garcia, Michael O.; Rhodes, J. M.; Wolfe, Edward W.; Ulrich, G. E.; Ho, R A

doi:10.1007/bf00301115

Cited by 91 publications

(72 citation statements)

References 20 publications

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“…The range for individual layers is as large as that observed for olivine in the large suite of submarine basalts from the east rift zone of Kilauea Volcano (e.g., Sample 842B-2H-5, 90-92 cm; forsterite 90.8% to 79.4% vs. 90.3% to 77.8%; Clague et al, in press). However, the range for the layers is similar in magnitude to that observed for the long-lived, current eruption (1983 to present) of Kilauea (forsterite 88% to 73%; Garcia et al, 1992). Thus, olivine composition is apparently not a useful discriminant for evaluating the time period represented by individual sand layers, because Hawaiian shield lavas display a relatively restricted range in major element composition, and single eruptive events can produce as much compositional variation in olivine as observed on a regional scale.…”

Section: Olivinesupporting

confidence: 68%

Pliocene-Pleistocene Volcanic Sands from Site 842: Products of Giant Landslides

Garcia¹

1993

Proceedings of the Ocean Drilling Program

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Several distinct, thin (2-7 cm), volcanic sand layers ("ashes") were recovered in the upper portions of Holes 842A and 842B. These holes were drilled 320 km west of the island of Hawaii on the outer side of the arch that surrounds the southern end of the Hawaiian chain. These layers are Pliocene to Pleistocene in age, graded, and contain fresh glass and mineral fragments (mainly olivine, Plagioclase, and clinopyroxene) and tests of Pleistocene to Eocene radiolarians. The glass fragments are weakly vesicular and blocky to platy in shape. The glass and olivine fragments from individual layers have large ranges in composition (i.e, larger than expected for a single eruption). These features are inconsistent with an explosive eruption origin for the sands. The only other viable mechanism for transporting these sands hundreds of kilometers from their probable source, the Hawaiian Islands, is turbidity currents. These currents were probably related to several of the giant debris slides that were identified from Gloria sidescan images around the islands. These currents would have run over the ~500-m-high Hawaiian Arch on their way to Site 842. This indicates that the turbidity currents were at least 325 m thick.Paleomagnetic and biostratigraphic data allow the ages of the sands to be constrained and, thus, related to particular Hawaiian debris flows. These correlations were checked by comparing the compositions of the glasses from the sands with those of glasses and rocks from islands with debris flows directed toward Site 842. Good correlations were found for the 110-ka slide from Mauna Loa and the ~1.4-Ma slide from Lanai. The correlation with Kauai is poor, probably because the data base for that volcano is small. The low to moderate sulfur content of the sand glasses indicates that they were derived from moderately to strongly degassed lavas (shallow marine or subaerially erupted), which correlates well with the location of the landslide scars on the flanks of the Hawaiian volcanoes. The glass sands may have been formed by brecciation during the landslide events or spallation and granulation as lava erupted into shallow water.:

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Section: Olivinesupporting

confidence: 68%

Pliocene-Pleistocene Volcanic Sands from Site 842: Products of Giant Landslides

Garcia¹

1993

Proceedings of the Ocean Drilling Program

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“…Mineral compositions and modes are consistent with these cumulate gabbros representing the Hawaiian volcanic system (Keil et al 1972;Fodor et al 1975Fodor et al 1977Fodor et al 1993Garcia et al 1989Garcia et al 1992Fodor and Moore 1994;Clague et al 1995), and in particular Mauna Kea tholeiitic magmas that crystallized in shallow-level reservoirs (Fodor and Galar 1997). For example, clinopyroxene and plagioclase compositions overlap those for phenocrysts in Hawaiian tholeiitic basalt (Figs.…”

Section: Host Gabbrossupporting

confidence: 53%

“…In composite xenolith 69, the dike orthopyroxene is approximately one Mg * unit lower than the host orthopyroxene, 73.6 vs 74.7. Garcia et al (1989Garcia et al ( , 1992, Helz and Wright (1992), Fodor and Moore (1994), Ho and Garcia (1988), Moore et al (1980), and Nicholls and Stout (1988); plagioclase in Mauna Loa and Mauna Kea basalts from Frey et al (1990;1991) and Garcia et al (1995); plagioclase in MORB from Dixon et al (1986), Davis and Clague (1990), Frey et al (1974), Fodor (1989), Davis and Clague (1987), and LeRoex et al (1989 Plagioclase…”

Section: Orthopyroxenementioning

confidence: 96%

“…b Clinopyroxene Mg * s [100batomic Mg/(MgcFe)], Al 2 O 3 , and TiO 2 (wt.%) for host gabbros and dikes. Hawaiian reference field for tholeiitic lavas compiled from data for Kilauea, Mauna Loa, and Mauna Kea volcanoes (Helz and Wright 1992;Garcia et al 1989Garcia et al , 1992Moore et al 1980;Ho and Garcia 1988;Nichols and Stout 1988;Fodor and Moore 1994;Rhodes 1995;Garcia et al 1995;Frey et al 1991). Reference data field for alkalic basalts is from Fodor et al (1975), Beeson (1976), Chen et al (1990), andFrey et al (1990).…”

Section: Clinopyroxenementioning

confidence: 98%

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Magma-reservoir crystallization processes: small-scale dikes in cumulate gabbros, Mauna Kea Volcano, Hawaii

Hoover

Fodor

1997

Bulletin of Volcanology

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Gabbroic xenoliths that represent cumulate environments within Mauna Kea Volcano are, in rare examples, penetrated by small-scale (~7 cm) dikes. We examined four dike/host composite xenoliths to establish how this evidence for magma seemingly injected into cumulate gabbro fits into the evolution of igneous processes in shield volcano magma reservoirs. Olivine, clinopyroxene, and plagioclase compositions in both host gabbros and dikes are characteristically tholeiitic and evolved (Fo 71-66 , cpx-Mg * 79-77, An 72-51 ) with respect to Hawaiian magmatism. Dikes, however, when compared with their host gabbros, have slightly greater abundances of some incompatible elements and slightly more evolved olivine compositions (e.g., Fo 68 vs Fo 71) . Compared with Mauna Kea lava compositions, both host gabbros and dikes have lower incompatible-element abundances, positive Eu anomalies, and, notable for dikes, major-element compositions unlike those of lavas (e.g., SiO 2~4 6 wt.%). The small-scale dikes, therefore, also have cumulate characteristics. We interpret them as representing late-stage liquids (e.g., 5 wt.% MgO, based on ~Fo 70 ) "squeezed" from solidifying cumulus piles of evolved (e.g., FFo 70 ) gabbroic assemblages. The compositions of the dikes, however, do not match those of the most evolved liquids expected in reservoirs because they appear to have lost interstitial liquids (e.g., positive Eu anomalies, low abundances of some trace elements). Because minerals in the dikes were in equilibrium with highly evolved liquids, conditions for small-scale dike formation in cumulate environments apparently occur only at the last stages of reservoir magma differentiation and solidification.

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“…For H 2 O-poor melt inclusions, the presumed low-pressure degassing must have occurred prior to crystallization of olivine and entrapment of melt inclusions. For Whole-rock analysis is from Garcia et al (1992) and has been normalized to 100% Fig. 1 Dissolved H 2 O contents of melt inclusions (shaded circles), submarine basaltic glasses, and fountain spatter from Kilauea volcano.…”

mentioning

confidence: 99%