Melting process in the Hawaiian plume: An experimental study

Takáhashi, Eiichi; Nakajima, Katsuji

doi:10.1029/gm128p0403

Cited by 54 publications

(60 citation statements)

References 32 publications

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“…melting of a "plum-pudding" mantle As described in section 8.3, melting of mantle sources with multiple rock types, each with its own melting behavior and chemical and isotopic properties, is believed to be an important factor in producing the range of magma types characteristic of individual igneous provinces. An important example of such a compound source would be a dominantly peridotitic mantle with minor eclogitic or pyroxenitic veins, on which there is a large and growing literature (for example, Wood, 1979;Allègre and others, 1984;Langmuir and Bender, 1984;Zindler and others, 1984;Allègre and Turcotte, 1986;Prinzhofer and others, 1989;Ben Othman and Allègre, 1990;Langmuir and others, 1992;Chabaux and Allègre, 1994;Lundstrom and others, 1995;Hauri, 1996;Hirschmann and Stolper, 1996;Hofmann and Jochum, 1996;Lassiter and Hauri, 1998;Jackson and others, 1999;Lassiter and others, 2000;Sobolev and others, 2000;Kogiso and Hirschmann, 2001;Norman and others, 2002;Reiners, 2002;Takahashi and Nakajima, 2002;Hirschmann and others, 2003;Pertermann and Hirschmann, 2003;Sobolev and others, 2005). In section 8.3, we considered briefly the limiting case of a heterogeneous mantle with an infinitesimal amount of a low-melting source rock.…”

Section: Fractional Fusion Pathsmentioning

confidence: 99%

Insights into mantle melting from graphical analysis of one-component systems

Stolper

Asimow²

2007

American Journal of Science

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ABSTRACT.Decompression melting can be approximated as an isentropic (that is, reversible adiabatic) process. In such a process, specific entropy (S) and pressure (P) are the independent variables and equilibrium is achieved when the specific enthalpy (H) of the system reaches a minimum. We present a largely graphical analysis of decompression melting in one-component systems based on phase equilibria in H-P-S space. Although mantle sources contain more than one component, use of one-component model systems provides insights into several aspects of mantle melting that can be generalized to more complete and complex systems (for example, batch vs. fractional fusion; the influence of pressure-dependent solid-solid reactions on melting; melting of multilithologic mixtures such as peridotite plus eclogite; advection of heat and melting by rising magmas) and places these insights into the visualizable framework of simple phase diagrams. introductionIgneous activity is one of the most important of all planetary phenomena: It is the principal mechanism by which planetary interiors differentiate chemically; the generally upward motion of magmas relative to solids can advect significant energy toward planetary surfaces; intrusion of magma at shallow levels and extrusion on the surface are the principal mechanisms by which planetary crusts form; these processes ultimately provide the raw material that is weathered, reworked, and remobilized by near-surface geologic processes; and the eruption of magma at the surface has geomorphic expression and in many cases can have substantial influence on climate.As with most geological phenomena, igneous processes are complex and, as a result, geologists (students and professionals alike) have long relied on phase diagrams in compositionally simple model systems as frameworks for visualizing, understanding, and analyzing igneous phenomena in more complex natural systems. Thus, for example, given a particular magma composition at a constant pressure (P), generations of geologists have learned to follow crystallization paths on cooling using temperature (T) versus composition (X) diagrams in binary systems (with their familiar eutectics, peritectics, phase loops, azeotropes, solvi, et cetera) and polythermal liquidus diagrams in ternary systems (with their familiar configurations of isotherms traversing primary liquidus fields, cotectics leading to ternary eutectics, minima, critical end points, et cetera). These same simple diagrams can be used to analyze aspects of isobaric melting and more complex processes such as metasomatism, magma mixing, and assimilation. Although these simple phase diagrams are incomplete models of actual magmatic systems, many of the processes that occur in natural systems can be understood by analogy with them and, most importantly, these phase diagrams often make it possible to visualize complex processes in relatively simple terms. Their staying power in earth science reflects the easy to understand yet powerful

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Section: Fractional Fusion Pathsmentioning

confidence: 99%

Insights into mantle melting from graphical analysis of one-component systems

Stolper

Asimow²

2007

American Journal of Science

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“…4) and to Sc in some Kilauea lavas (e.g., 29-34 ppm; Chen et al 1996); its relatively low SiO 2 (49.4 wt%) and high FeO (11.6 wt%) are consistent with Kilauea, but they could also reflect weathering. According to Jackson et al (1999) and Takahashi and Nakajima (2002), different relative amounts of recycled ocean crust in the mantle source, expressed as garnet pyroxenite, can account for some compositional variations of magmas during Koolau construction (e.g., lower crustal component equates to higher Sc and lower SiO 2 in lavas).…”

Section: Discussionmentioning

confidence: 99%

Koolau shield basalt as xenoliths entrained during rejuvenated-stage eruptions: perspectives on magma mixing

Weinstein

Fodor

Bauer³

2004

Bulletin of Volcanology

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Rejuvenated-stage tuff cones (Honolulu Volcanics) on Koolau volcano, Oahu, Hawaii, contain xenoliths of Koolau shield basalt. Because Koolau subaerial shield lavas represent a Hawaiian geochemical 'end member', and submarine shield lavas have compositions with some affinities to Mauna Loa and Kilauea, we analyzed 28 xenolithic basalts from Salt Lake and Koko Head cones to determine how these seemingly random samplings of the Koolau profile compare to established Koolau geochemistry. Analyses reveal that 24 are shield tholeiitic basalt-the focus of this study-and 4 are rejuvenated-stage basaltic rocks. The tholeiitic xenoliths represent largely upper Koolau shield lavas, as these samples (8.3 to 5.8 wt% MgO) have, with one exception, overall major-and trace-element compositions that overlap those of Koolau subaerial shield lavas. Secondary processes, however, created some distinctions-namely, enrichments/depletions in K, Ba, Sr, SiO 2 , and FeO, and, due to zeolitization (chabazite with attending okenite and apophyllite), elevated CaO. One xenolithic basalt with 8.2 wt% MgO has higher Ti, Zr, Nb, and Sc, and lower Zr/Nb than subaerial lavas, and appears to represent relatively early, deeper shield-thereby reinforcing that the Koolau shield source varied temporally. Olivine, orthopyroxene, and plagioclase are the phenocrysts (clinopyroxene is rare), and their core compositions range widely across the suite-Fo 87.872 , orthopyroxene Mg#s 85-72, and An 74-60 . Several xenolithic basalts have both normally and reversely zoned orthopyroxene and plagioclase with a variety of core compositions (e.g., orthopyroxene-core Mg#s 82, 77, and 72, all in one sample). These compositions and zonations record evidence for wide compositional ranges of replenishment (MgO~13-8 wt%) and reservoir (MgO~7 to <5 wt%) magmas mixing in varying proportions; however, extreme MgO lavas (~13 and <5 wt%) are not observed as either subaerial or xenolithic basalt, but are indicated by phenocryst cores of Fo 87.8 and orthopyroxene-Mg# 72. The Koolau magma-mixing history resembles that of Kilauea, and is unlike the 'steady-state' mixing known for Mauna Loa. Finally, these basalt samples show that any xenolithic occurrence of Koolau lava is subject to the zeolitization prevalent in the tuff-cone hosts.

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“…Takahashi and Nakajima [7] proposed that magma produced near the axis of the plume head may be a mixture of two types of melts: 1) basaltic andesite melt formed by eclogite melting, and 2) picritic melts formed by the reactive melting of eclogite and peridotite. According to their study of the Koolau volcano, an eclogite block larger than 1000 km 3 supplied silica-rich magma at the last stage the volcano's formation, and remained in disequilibrium with peridotite during its lifetime.…”

Section: Implications For Hawaiian Magma Genesismentioning

confidence: 99%

“…A schematic model for melting processes in a heterogeneous Hawaiian plume is shown in Figure 7 (after Takahashi and Nakajima [7]). We have demonstrated that the entire compositional spectrum of Hawaiian tholeiites (basalt to picrite) can be formed by basalt-peridotite hybrid melting near to the dry peridotite solidus.…”

Section: Implications For Hawaiian Magma Genesismentioning

confidence: 99%

“…Dynamic modelling of eclogite-peridotite hybrid plumes has accounted for the distribution of Kea-type and Loa-type volcanoes, as well as the sequential change of igneous rock types in shield volcanoes [12] [13]. Further, several melting experiments and numerical modelling simulations of heterogeneous mantle plumes have been performed recently in order to clarify the petrogenesis of tholeiite magma in Hawaiian plume [7] [14] [15] [16].…”

Section: Introductionmentioning

confidence: 99%

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High-Pressure Melting Experiments on Basalt-Peridotite Layered Source (KLB-1/N-MORB): Implications for Magma Genesis in Hawaii

Gao¹,

Takáhashi²,

Suzuki³

2017

IJG

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In order to understand the melting processes that occur within recycled oceanic crust and mantle in a heterogeneous plume (e.g., that beneath the Hawaiian Islands), a series of high-pressure-high-temperature layered experiments were performed at 2.9 GPa, 5 GPa, and 8 GPa, from 1300˚C to 1650˚C, using a fertile peridotite KLB-1 and N-MORB. Our experiments at conditions below the dry peridotite solidus produced melt compositions that ranged from basaltic andesite to tholeiite. An Opx reaction band formed between eclogite and peridotite layers, likely via chemical reaction between a silica-rich eclogite-derived partial melt and olivine in the peridotite matrix. At temperatures at or above the dry peridotite solidus, substantial melting occurred in both basalt and peridotite layers, and fully molten basalt melt and melt pockets from the peridotite layer combined. In our layered experiments, major and minor element contents in reacted melts closely matched those of Hawaiian tholeiite and picrite, except for Fe. Partial melts of anhydrous run products had ~55 -57 wt% SiO 2 at low temperature (i.e., were andesitic) and had ~50 -53 wt% SiO 2 at high temperatures, slightly below the dry peridotite solidus (i.e., were tholeiitic, and similar to those that occur during the Hawaii shield-building stage). Based on the Fe-and LREE-enriched signature in Hawaiian tholeiites, we propose that recycled components in the Hawaiian plume are not modern N-MORB, but are Fe-rich tholeiite; a lithology that was common in the Archaean and early Proterozoic. We have demonstrated that the entire compositional spectrum of Hawaiian tholeiites (basalt to picrite) can be formed by basalt-peridotite reactive melting near the dry solidus of peridotite. Based on these results, we propose that the potential temperature of the sub-Hawaiian plume may be much lower than previously estimated.

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Melting process in the Hawaiian plume: An experimental study

Cited by 54 publications

References 32 publications

Insights into mantle melting from graphical analysis of one-component systems

Insights into mantle melting from graphical analysis of one-component systems

Koolau shield basalt as xenoliths entrained during rejuvenated-stage eruptions: perspectives on magma mixing

High-Pressure Melting Experiments on Basalt-Peridotite Layered Source (KLB-1/N-MORB): Implications for Magma Genesis in Hawaii

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