what does the water content in a volcano do to the lava

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• Published: 29 September 2014

Water content in arc basaltic magma in the Northeast Japan and Izu arcs: an estimate from Ca/Na sectionalisation between plagioclase and melt

Earth, Planets and Space volume 66, Article number:127 (2014) Cite this article

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Abstract

The variation in water content of arc basaltic magmas in the Northeast Japan arc and the Izu arc was estimated using a simple plagioclase phenocryst hygrometer. In club to construct a plagioclase phenocryst hygrometer optimized for arc basalt magmas, we have conducted high-pressure melting experiments of relatively primitive basalt from the Miyakejima volcano, a frontal-arc volcano in the Izu arc. As a consequence of the experiments, nosotros found that the Ca/Na segmentation coefficient between plagioclase and hydrous basaltic melt increases linearly with an increase in H₂O content in the melts. We then selected from literature geochemical information sets of relatively archaic basaltic rocks with no bear witness of magma mixing and the almost frequent Ca-rich plagioclase phenocrysts from xv basaltic arc volcanoes including both frontal-arc and rear-arc volcanoes. In the xv volcanoes studied, plagioclase phenocrysts of high anorthite content (An > 90) were usually observed, whereas plagioclase phenocrysts in rear arc volcanoes usually had a lower anorthite content (xc > An > lxxx). In all volcanoes studied, the estimated H_twoO content of basaltic magma was at least 3 wt.% H₂O or higher. The magmas of volcanoes located on the volcanic front have about 5 wt.% H₂O in magma whereas those from the rear-arc side are slightly lower in H₂O content.

Findings

Introduction

Primary arc basalt magma is generated by partial melting of the sub-arc drapery with the addition of dehydrated aqueous fluid from the subducting slab. H₂O has profound effects on the melting temperature of the mantle, crystallization pathways of generated magmas, and the explosivity of magmas. Therefore, magmatism in an island arc along a subduction zone is controlled by H₂O released by the dehydration of a subducting slab. Precise estimation of H₂O content in arc basalt magma is important for evaluating the outcome of H₂O on generation, differentiation, and eruption of magmas in subduction zones. However, estimation of pre-eruptive H₂O content on arc magmas is hard attributable to degassing from erupting magmas.

Sakuyama (1979) discussed lateral variation of the H₂O content of basalt magmas across the Northeast Japan arc. Based on the systematic differences in phenocryst mineral assemblages in andesite and dacite and the assumption that these rocks are derived from basalt magmas past partial crystallization, Sakuyama (1979) concluded that primary magmas from a volcanic front have a lower H₂O concentration than those of a rear arc. This conclusion was further extended by Tatsumi et al. (1983) in constructing a magma genesis model for arc basalt magmas. However, this assumption is non always true because magma mixing and melting of crustal components may occur oft to derive silicic magma. More recently, Nakamura and Iwamori (2009) estimated lateral variation of the fluid component in the source mantle based on the systematics of trace elements and isotopic compositions of arc volcanic rocks. Co-ordinate to their estimates, rear-arc volcanoes in central Japan are enriched in the fluid component of their mantle source, whereas the basaltic volcanoes on the volcanic front in the Izu arc are depleted in the fluid component of their source.

In experimental research on arc basalt magmas, many studies (e.g. Sisson and Grove 1993a; Kawamoto 1996; Pichavant and Macdonald 2007; Hamada and Fujii 2008) proposed that partial crystallization of hydrous basalts yields calc-alkaline trends whereas relatively depression H₂O content in basaltic magma yields tholeiitic fractionation trends. On the contrary, recent melt inclusion studies (east.chiliad. Sisson and Layne 1993; Newman et al. 2000; Saito et al. 2005, 2010; Ikehata et al. 2010) indicated that the H_iiO content in tholeiitic basaltic cook is larger than iii wt.% at the volcanic front.

The anorthite content of plagioclase is shown to increase with an increase in H_iiO content of coexisting cook in all experimental studies (e.g., Johannes 1978; Sisson and Grove 1993a; Takagi et al. 2005; Hamada and Fujii 2007). Based on this relation, several plagioclase phenocryst hygrometers have been proposed (Housh and Luhr 1991; Putirka 2005; Hamada and Fujii 2007; Lange et al. 2009). Loftier anorthite content of plagioclase phenocrysts (An > 90) is often reported in basaltic rocks from frontal-arc volcanoes (e.thousand. Kimata et al. 1995; Amma-Miyasaka and Nakagawa 2002), suggesting that magmas erupting from frontal-arc volcanoes are H_iiO-rich such every bit >3 wt.% H_iiO in basaltic cook from the Izu-Oshima volcano (Hamada and Fujii 2007). A major disadvantage of the plagioclase phenocryst hygrometers proposed thus far, however, is that they can be used only when the pressure level, temperature, and compositions of coexisting plagioclase and melts are known.

In this study, we conducted high-pressure and loftier-temperature melting experiments on arc basalt from the Miyakejima volcano at an H₂O-undersaturated condition and at 100 to 200 MPa, which is the pressure corresponding to a shallower crustal magma bedroom. In club to hash out the variation of H_twoO content in arc basalts, a unproblematic plagioclase phenocryst hygrometer is proposed. Using this simple hygrometer, the H₂O content in basalt magma occurring in the Northeast Japan and Izu arcs is estimated.

Methods

High-pressure and loftier-temperature experiments

Starting material

In order to construct a plagioclase phenocryst hygrometer for arc basalt magma, high-force per unit area and loftier-temperature experiments were conducted on Ofunato scoria (OFS), which is a relatively primitive basalt from the Miyakejima volcano. Miyakejima is an active volcanic island located well-nigh 200 km southward of Tokyo on the volcanic forepart of the Izu-Mariana arc. The OFS is one of the well-nigh archaic basalts to have erupted in the last 10,000 years in the Ofunato Phase 7,000 to x,000 years ago (Tsukui et al. 2002; Niihori et al. 2003). The whole-rock composition of the OFS is every bit follows: 50.11 wt.% SiO₂, 0.92 wt.% TiO_two, xviii.09 wt.% Al₂O₃, 11.06 wt.% FeO (total), 0.21 wt.% MnO, five.78 wt.% MgO, 11.78 wt.% CaO, 1.85 wt.% Na_twoO, 0.22 wt.% Yard₂O, 0.01 wt.% P_iiO₅, and Mg# (=Mg/(Mg + Fe) × 100) = 48.ii, which was determined through assay of glass fused at 1 atm using an electron microprobe. OFS has 0.vii vol.% of olivine and x.9 vol.% of plagioclase phenocrysts in which core compositions are Mg# = 78 to 82 and An (=Ca/(Ca + Na) × 100) = 90 to 96 (Figure one). The most frequent core composition of plagioclase phenocrysts in OFS is An94. All phenocrysts have a large clear core and a narrow normal-zoned rim with a sharp purlieus. The amount of magma mixing with the evolved magma is negligible. Hydrous OFS spectacles with diverse H_iiO contents were synthesized and were used every bit starting materials for loftier-pressure and high-temperature melting experiments in this study (Additional file 1: Table S1).

Figure 1

Frequency distribution of plagioclase compositions in phenocrysts and groundmass, in Ofunato scoria (OFS) erupted from Miyakejima volcano. The virtually frequent limerick of plagioclase phenocrysts is An = 94.

Full size prototype

Experimental and analytical procedures

Nosotros conducted experiments at pressures of 100, 150, and 200 MPa using SMC-2000 and SMC-5000 internally heated pressure vessels (IHPVs; Miyagi et al. 1997; Tatsumi and Suzuki 2009; Tomiya et al. 2010; Hamada et al. 2013) installed at the Magma Manufacturing plant, Tokyo Institute of Technology, Tokyo, Japan. These IHPVs use argon gas as the pressurizing medium and tin can be pressurized up to 200 and 480 MPa, respectively. Pressure was measured past a strain-gauge pressure transducer. For SMC-2000, a unmarried W5Re-W26Re thermocouple about the capsule was used to monitor temperature. For SMC-5000, ii W5Re-W26Re thermocouples were used that were spaced ten mm apart vertically; the observed temperature gradient beyond the capsule was less than 10°C. Experiments were performed in the temperature and pressure ranges of 1,050°C to 1,150°C and 100 to 200 MPa, respectively. Run durations were 12 h for experiments at 1,150°C and 24 h for the other experiments. The double-capsule method was used to buffer oxygen fugacity with a solid powder Ni-NiO (10:i, wt.) assemblage. A metal tube with a limerick of either Au₇₅Pd₂₅ (ii.5/ii.2φ), Au₇₅Pd₂₅ (2.5/2.iiiφ) or Ag₅₀Pd₅₀ (2.3/2.0φ) was used as an inner sample tube that was welded on one cease and weighed. Hydrous glasses synthesized at high pressure equally a starting cloth was inserted into the inner capsule and weighed, so welded on the other end and weighed. The weight loss during welding was generally <0.00005 g. We likewise prepared a metal tube (Pt, 3.0/2.8φ) that was welded on 1 terminate. Ni-NiO powder and distilled water were then inserted into the tube, and the other terminate was only crimped rather than welded. Prepared sample capsules and a buffer capsule were placed into the outer capsule (Au_lxxxPd₂₀; half dozen.0/5.6φ, Au₇₅Pd₂₅; eight.0/vii.viiiφ or Au₈₀Pd₂₀; 8.0/vii.6φ), and the outer capsule was then welded. The entire capsule was kept at 110°C in an oven for xx to thirty min and was weighed to ensure that the seal on the sheathing was constructive. Afterward each run and quenching of the products, experimental charges were weighed to mensurate volatile loss and were punctured to verify the presence of liquid H₂O. In each buffered capsule, the presence of two phases of Ni and NiO was confirmed. The phase assemblage of the run products and compositions of minerals and glass were adamant by using a JEOL JXA-8530 F electron microprobe (JEOL Ltd., Tokyo, Nippon) for plagioclase; JXA-8800 was used for the others. To analyze small plagioclase 5- to 20-μm long, the acceleration voltages were x kV for plagioclase and 15 kV for the other phases. The beam current and time spent on each elemental pinnacle, except for Na and the groundwork, were 12 nA, 20 due south and 10 s, respectively. Na was analyzed for 10 s (groundwork: 5 south) without a peak search to avoid count loss. Minerals were analyzed using a focused electron beam, whereas a defocused electron axle x to xv μm in diameter was employed for the glass. A loss of Na count was non detected for minerals and hydrous glasses during analyses. The H₂O content of hydrous glass as a starting material was analyzed using a fifteen to 89 μm doubly polished wafer of glass and transmittance measurements of Fourier transform infrared spectroscopy (FTIR; Jasco FT/IR-6100 and IRT-5000, vacuum type, JASCO Corporation, Tokyo, Nippon) with an aperture size of 100 μm. A Ge/KBr beam splitter and HgCdTe (MCT) detector were too used. The thicknesses of the doubly polished thin sections, 15 to 89 μm, were analyzed past a digital micrometer (Mitutoyo Corporation, Kanagawa, Japan) with ±one μm precision. The dispersion of sample thickness was ±two μm. Homogeneity of hydrous glasses was confirmed in analyses of several different points. Following the procedures of Yamashita et al. (1997), the absorbance elevation heights at the iii,500 cm⁻¹ ring were used to quantify the H_iiO content. The density of the hydrous basaltic drinking glass was calculated by applying the equation of Ohlhorst et al. (2001). The H₂O content of the run products was analyzed by reflectance measurements using the aforementioned FTIR (Boosted files 2 and iii). The calibration curve of H₂O in the melt versus the Δreflectance at peak near 3,650 cm⁻¹, shown in Boosted file 2: Figure A1, was used to estimate the H₂O content in the hydrous glass in the run products.

Results and discussion

Experimental results and proposal for a plagioclase phenocryst hygrometer

Experimental conditions and results are listed in Tabular array 1 and Table 2. All experiments except for C1839 were conducted most the liquidus of plagioclase (±magnetite); therefore, the composition of the melt was essentially same equally the starting material. Oxygen fugacity was determined for C1839 using a plagioclase-olivine oxygen fugacity barometer (Sugawara 2001). That for C1839 was conducted at a low temperature in order to crystallize mafic minerals; the estimated fO_ii was ΔNNO + 0.8. Although fO_ii in the other run products was not estimated due to the lack of plausible mineral assemblages, the value would be close to that of NNO for three reasons. Ni and NiO coexisted in recovered buffer capsules in all runs, and similar fO₂ was estimated in previous works using the same double-capsule technique and like apparatus. Moreover, the FeO content of plagioclase depends on fO₂ (Sugawara 2001) and the range of the FeO (total) content of plagioclase in all run products was narrow (1.3 ± 0.ane wt.%). Hamada and Fujii (2007, 2008) conducted high-pressure, loftier-temperature experiments using the double-sheathing method with the NNO + H_twoO buffer and an internally heated pressure vessel (IHPV) appliance similar to SMC-5000 at the University of Tokyo. Hamada and Fujii (2007) estimated that the fO₂ condition was ΔNNO +0.8 to two.0 by using the Co-Pd alloy redox sensor technique (Taylor et al. 1992), and Hamada and Fujii (2008) estimated that fO₂ was ΔNNO +1 (±0.eight) past using the oxygen barometer of Sugawara (2001). Nosotros conducted experiments for a shorter duration (12 h) at ane,150°C compared to 24 h in the others in order to minimize the loss of diffusive H₂ from the capsule assemblage. Plagioclase was euhedral and rectangular and upward to fifteen μm. Magnetite was up to 10 μm in bore. Both minerals were compatible in composition throughout the recovered run products, indicating that equilibrium was accomplished. The H_twoO content of the melt was calculated by mass remainder calculation of all phases assuming that water was concentrated in simply the melt. The H_iiO content in the melt in run products relatively poor in crystals was measured by the reflectance infrared (IR) method (Boosted files ii and 3); the results agreed with mass residuum calculations (Table 1). Effigy 2a shows the relation between H₂O content in the melt and the anorthite content of plagioclase in our run products. In the range of experimental conditions, the anorthite content of plagioclase positively correlated with the H₂O content in melt. As shown in Figure 2a, $K_{\mathrm{D}\mathrm{pl}-\mathrm{melt}}^{\mathrm{Ca}-\mathrm{Na}}$ (= (Ca/Na)_pl/(Ca/Na)_melt) was proportional to the H₂O content in the melt (Figure 2b), and the furnishings of temperature and pressure were not significant. A simple plagioclase hygrometer is expressed as a linear part as

$$\begin{array}{l}{K}_{\mathrm{D}\mathrm{pl}-\mathrm{melt}}^{\mathrm{Ca}-\mathrm{Na}}=0.74{\mathrm{10}}_{{\mathrm{H}}_2\mathrm{O}}\left(\mathrm{wt}.\right)\times 100+0.36\\ R^2=0.917\mathrm{\text{Standard}}\mathrm{\text{error}}=0.23\text{.}\end{array}$$

(ane)

Table 1 Experimental conditions and results

Total size table

Table ii Volcanoes which were estimated past Equation ane

Full size table

Figure 2

Relation between H ₂ O concentration in melt and (a) anorthite content of coexisting about-liquidus plagioclase or (b) ${\mathit{M}}_{\mathbf{D}\mathbf{pl}\mathbf{-}\mathbf{melt}}^{\mathbf{Ca}\mathbf{-}\mathbf{Na}}$ . At one.0, 1.5, and 2.0 kbar. (b) Dashed lines represent the range in typical basalt from the Northeast Japan and Izu arcs (0.32 < Al_twoO_iii/SiO₂ < 0.39). When the H₂O content was estimated by Equation 1, the expected fault was within that indicated by the dashed lines. Source: Berndt et al. (2005) and Sisson TW et al. 1993b.

Full size prototype

Strictly speaking, this equation is applicative for just arc basalts with compositions and pressure and temperature atmospheric condition like to those in the nowadays experiments. According to Hamada and Fujii (2007), $K_{\mathrm{D}\mathrm{pl}-\mathrm{melt}}^{\mathrm{Ca}-\mathrm{Na}}$ depends strongly on the Al_iiO_three/SiO_ii ratio of the melt. In order to check the result of the melt limerick on ${\mathrm{1000}}_{\mathrm{D}\mathrm{pl}-\mathrm{cook}}^{\mathrm{Ca}-\mathrm{Na}}$, previous experimental data obtained at 100 to 300 MPa with various ratios of Al₂O₃/SiO₂ of basaltic cook were compiled, every bit shown in Figure 2b. Most previous experiments were conducted with melts in limited ranges of Al₂O_three/SiO_two ratio (Al_iiO_iii/SiO_two = 0.31 to 0.39). Lower Al₂O₃/SiO₂ (=0.27) experiments (MA44) by Hamada and Fujii (2007) show significantly lower $K_{\mathrm{D}\mathrm{pl}-\mathrm{cook}}^{\mathrm{Ca}-\mathrm{Na}}$ than that in other experiments. If Equation 1 was applied to estimate the H₂O content in relatively primitive arc basalts (Al₂O₃/SiO₂ = 0.31 to 0.39; Table 2), the error of the plagioclase phenocryst hygrometer would exist approximately ±1 wt.% H₂O (Figure 2b).

Contrary to the effect of dissolved H₂O in the cook, crystallized plagioclase becomes sodic with increasing pressure level at a given melt composition (e.thousand. Takagi et al. 2005). Takagi et al. (2005) adamant experimentally that anorthite-rich plagioclase (An > 90) phenocrysts can exist crystallized at only a shallow-level crustal magma chamber (200 to 300 MPa) with 5 to 6 wt.% dissolved H₂O in the melt. Because H_twoO solubility depends strongly on pressure, magma chambers that crystallize anorthite-rich plagioclase should not be too shallow. Therefore, nosotros assume that the typical pressure is 200 MPa for anorthite-rich plagioclase phenocrysts in arc basaltic rocks. This assumption is supported by geophysical imaging of magma chambers beneath the Northeast Japan and the Izu arc volcanoes (e.g. Mikada et al. 1997; Murakami et al. 2001). In our experimental study, high-An plagioclase (An = 94) was not crystallized considering the loftier H_iiO content in the melt depressed the liquidus temperature of the plagioclase. Thus, the origin of highly Ca-rich plagioclase phenocrysts needs further experimental report.

In Equation i, ${\mathrm{Grand}}_{\mathrm{D}\mathrm{pl}-\mathrm{cook}}^{\mathrm{Ca}-\mathrm{Na}}$ was expressed as a part of simply H₂O in the cook without regard to temperature and force per unit area. The present hygrometer can be applicable to arc basalt magmas nether pressure and temperature conditions at to the lowest degree similar to those in nowadays experiments (100 to 200 MPa, 1,075°C to 1,150°C). Our starting material was slightly higher in Al₂O_three than basaltic magmas from the Izu-Oshima volcano without plagioclase accumulation (Nakano and Yamamoto 1991). Nevertheless, our scale can be applicative to arc basalts in a broad sense. Hamada and Fujii (2007) suggested that the Ca/Na partition betwixt plagioclase and the cook depends on the Al₂O₃/SiO₂ ratio. Nosotros estimated the mistake of Equation 1 at ±1 wt.% by comparison with previous experimental data in terms of Al₂O_iii/SiO₂ ratios; the range of arc basalts listed in Table 2 is 0.31 to 0.39.

Comparison to other hygrometers

Plagioclase phenocryst hygrometers take been proposed by many authors (Housh and Luhr 1991; Putirka 2005; Hamada and Fujii 2007; Lange et al. 2009). The results calculated past our elementary hygrometer were compared with those by other hygrometers using experimental melting written report data of arc basalts (see Figure 3 and Additional file iv: Table S2).

Figure 3

Relation between measured H ₂ O content in lt and calculated H ₂ O content using hygrometers. Hygrometers used are of this and previous studies listed. Experimental information that was plotted in this figure is listed in Additional file v: Table S3.

Full size image

Calculation results using Equation i were mostly college than those reported past Lange et al. (2009). In particular, the discrepancy was large for depression H_twoO content. On the contrary, results using Putirka'due south calculations (2005) were similar to those with Equation 1. Furthermore, in order to examine various basaltic compositions, the calculated h2o contents based on Equation 1, Lange et al. (2009) and Putirka (2005) for previous experimental studies on alkali basalt, mid-ocean ridge basalt (MORB) and arc basalt are compared in Additional file 5: Tabular array S3. For this calculation, experimental pressure and temperature conditions and the compositions of melt and plagioclase of the reported values were used. It is important to notation that the calculated H₂O contents estimated by Equation 1 show good understanding (±1 wt.% H₂O) with experimental values. The agreement is peculiarly good for low to medium Thou tholeiitic basalt, (i.east., those of Izu-Oshima (Hamada and Fujii 2007) and Iwate volcanoes (Takagi et al. 2005)). Because the alkali dependency noted by Honma (2012), Equation 1 may be less reliable for alkali basalts. As demonstrated in Figure three, our uncomplicated hygrometer is useful for estimating the water content in natural magma, although its application is express in melt composition and pressure and temperature conditions for the crystallization of arc basalts.

Pre-eruptive H₂O content in arc basalt magmas

Procedure of estimation of h2o content in arc basalt magma

Nosotros used the bulk rock limerick as the melt limerick to be in equilibrium with the loftier-An plagioclase. Although majority rock compositions more often than not practice not represent melt compositions towing to selective phenocryst accumulation, trial calculations utilizing groundmass composition every bit the cook composition resulted in aberrant H_twoO interpretation of the melt and, therefore, selected the bulk rock composition to calculate the equilibrium H₂O contents of relatively archaic arc basalt magmas using Equation 1. The post-obit discrimination rules in choosing samples were adopted: 1) Samples should come from volcanoes that have erupted basalt (SiO₂ < 53 wt.%); 2) among the basalt products, the frequency of plagioclase phenocryst limerick is known and shows a unimodal compositional spectrum (Figure ane); 3) we selected the least fractionated rock that satisfies the first two constraints from each volcano tiptop composition of plagioclase phenocryst for the estimation of H₂O content of arc basaltic magma. If magma mixing occurred, estimation of melt composition that was equilibrated with plagioclase phenocrysts is hard. Therefore, basalt without bear witness of magma mixing had to be selected. Co-ordinate to Sakuyama (1981), the plagioclase limerick frequency diagram is the all-time indicator for judging the occurrence of magma mixing.

Pre-eruptive H₂O content of arc basalt magma

The estimated H_iiO content of the basalt magma beneath each volcano is listed in Table 2. In magmas erupting from frontal-arc volcanoes, anorthite-rich plagioclase phenocrysts (An > xc) are commonly constitute. On the contrary, plagioclase phenocryst tends to be slightly sodic (An < ninety) in magmas erupting from rear-arc volcanoes. We estimated the H₂O content of arc basalt magma using the most frequent composition of plagioclase phenocrysts using Equation 1 (Figure 4). The estimated H₂O content of arc basalt magmas is in the range of iii to five wt.% at both frontal-arc and rear-arc volcanoes. In the rear-arc region, the H₂O content was estimated in only iv volcanoes (Myoko, Ueno, Fuji, and Niijima); therefore, systematic differences between volcanoes in a volcanic front and those in a rear arc with regard to pre-eruptive H_iiO content were difficult to assess.

Figure four

Map of estimated H ₂ O content in relatively primitive basalt from the Northeast Japan and Izu arcs. Volcanoes represented by larger symbols are listed in Table 2. Numbers near a circular symbol shows the H_twoO content of pre-eruptive basalt estimated by Equation one and are listed in Tabular array 2. Superscript 'a' indicates that the estimated water content has doubtfulness because the reference used had no frequency distribution of plagioclase phenocryst compositions (Iwate volcano: Kuritani et al. 2014a; Funagata volcano: Fujinawa, 1982). Superscript 'b' indicates that the reference used suggested the occurrence of magma mixing. In this case, although the h2o content was not estimated, the compositions of virtually anorthite-rich plagioclase is shown by circular symbols (Chokai volcano: Hayashi and Aoki 1985).

Full size paradigm

In some volcanoes, H₂O content in basaltic magma was estimated by melt inclusion analysis. In the example of the Fuji volcano, Yasuda (2011) analyzed melt inclusions of olivine phenocrysts in the Fuji products and estimated the H₂O content was 3.8 wt.%. Products of Takatsukayama and Sukumoyama volcanoes located in the Higashi-Izu monogenetic volcano field contain up to 3.iv wt.% H₂O in olivine phenocrysts (Nichols et al. 2012). In the case of Izu-Oshima volcano, the maximum H₂O content of melt inclusions in the olivine phenocrysts was 3.4 wt.% past assay of products of the older Oshima group (Ikehata et al. 2010). In the case of Miyakejima volcano, Saito et al. (2005, 2010) analyzed cook inclusions of plagioclase and olivine phenocrysts from the AD 2000 eruption and estimated the H_twoO content to exist 3.3 wt.% in olivine-hosted melt inclusions. These analyses are consistent with the values of pre-eruptive H_twoO content in melt estimated in this study.

Kuritani et al. (2014a) estimated the H₂O content of relatively archaic basalt (8.87 wt.% MgO) located at the volcanic forepart in Iwate volcano to be 4 to 5 wt.% based on petrologic study. Rose-Koga et al. (2014) besides analyzed olivine-hosted melt inclusions from the AD 1686 products in Iwate volcano to determine a maximum H₂O content of iii.65 wt.%. These results are consistent with our new approximate. In the case of Sannomegata volcano, which is a rear-arc volcano in the Northeast Nippon arc, Kuritani et al. (2014b) estimated the H₂O content of primitive basalt and source curtain and estimated H₂O content to be vi to vii wt.% in the primary melt. Their estimation is based on a magma genesis model with several assumptions. In dissimilarity, our estimates of the pre-eruptive H₂O content are based on uncomplicated ascertainment on plagioclase phenocrysts. The discrepancy between these studies tin can exist a central issue for understanding magma differentiation processes from the upper mantle to the surface and is a topic for future investigation. Kimura and Yoshida (2006) and Kimura et al. (2010) analyzed trace chemical element and isotope compositions of basalts in the Northeast Nippon arc and the Izu-Mariana arc, respectively, and estimated the composition of primary melt, the amount of added aqueous fluid, and the H_twoO content in principal melt based on forwards modeling of magma genesis in a subduction zone. Their estimations of H_twoO content in primary melts based on frontward modeling are generally accordance with our estimates based on plagioclase phenocryst compositions. Sakuyama (1979) proposed across-arc lateral variation in H₂O content of basalt magma in the Northeast Japan arc based on systematic differences in phenocryst mineral aggregation in evolved rocks. This theory, such that magmas in the rear-arc are more enriched in H₂O than those along the volcanic front was supported past Uto (1986) and Kawamoto (1996) based on systematic changes in Al_iiO_three content during fractionation. Reverse to previous conventionalities, our observation showed that volcanoes on a volcanic forepart erupt the most H_iiO-rich basalt magma (3 to 5 wt.%; Figure 4) or there is no measurable across arc difference in the water content of basalt magmas. In a detail study at Miyakejima volcano (Ushioda 2014), we showed that the water content in differentiated magmas strongly depends on the presence or absence of shallow-level magma chambers in a volcano. Therefore, comparison of phenocryst mineral assemblages in differentiated rocks (Sakuyama 1979) or that of the Al_twoO_iii content amid fractionation trends (Uto 1986; Kawamoto 1996) does not necessarily correspond differences in water content in parental basalt magmas.

In other arc magmas, the H₂O content has been estimated past analysis of melt inclusions. For case, in the instance of the Kamchatka arc, Portnyagin et al. (2007) indicated that primitive melts in a volcanic front end contain an H₂O content equal to or slightly higher than those in a rear-arc. Similarly, arc basaltic melts along the Central American Volcanic Arc (Walker et al. 2003; Sadofsky et al. 2008) and the Michoacan-Guanajuato Volcanic Field of Cardinal Mexico (Johnson et al. 2009) accept slightly higher H₂O content in a volcanic forepart.

In subduction zones, volcanoes along the volcanic forepart produce the largest volume of magmas, and those from volcanoes along the rear-arc produce significantly less (Sugimura et al. 1963). Therefore, the fact that basaltic magma in a volcano on the volcanic front is H₂O-rich has primal importance in the consideration of mass flux of H₂O in subduction zones. Magma genesis models in subduction zones (e.g., Tatsumi et al. 1983) that assume well-nigh dry melting conditions beneath the volcanic front need to exist reconsidered. Lateral variation of the fluid component in the source pall based on the systematics of trace elements and isotopes reported by Nakamura and Iwamori (2009) may need reconsideration and revision since they show very small fluid addition in some volcanoes on the volcanic front end.

Conclusions

In order to approximate the variation of H₂O content in relatively primitive basalt in the Northeast Japan and the Izu arcs, we constructed a unproblematic plagioclase phenocryst hygrometer applicable for temperature and pressure of shallow crustal magma chamber beneath arc volcanoes. The H_twoO content in representative basaltic rocks from 15 volcanoes in eastern Japan was estimated using our newly constructed simple hygrometer. High anorthite (An > ninety) plagioclase phenocrysts were shown to exist common in volcanoes forth volcanic front end whereas those along the rear arc were slightly lower (An > 80). We conclude that volcanoes on the volcanic front generally erupt H₂O-rich basalt magma (3 to v wt.%). Every bit was suggested past Sakuyama (1979), across-arc variation in H₂O content of basaltic magmas is not valid for pre-eruptive H₂O content of basaltic magmas inferred from plagioclase-melt equilibria.

References

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Acknowledgements

We give thanks Dr. Kenji Niihori for his helpful advice in collecting primitive basalt (Ofunato scoria) at Miyakejima volcano. This work was supported past MEXT Grant-in-Aid, Nos. 21109004 and 25247088 to ET. MU thank you the Global COE programme 'From the Earth to Earths' for financial support as RA. Nosotros are indebted to Dr. Tatsuhiko Kawamoto, Professor Hiroaki Sato and bearding reviewers for effective discussions and comments for improving this manuscripts.

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Affiliations

1. Magma Factory, Department of World and Planetary Sciences, Tokyo Found of Technology, two-12-i Ookayama, Meguro-ku, Tokyo, 152-8551, Nippon

   Masashi Ushioda, Eiichi Takahashi, Morihisa Hamada & Toshihiro Suzuki

2. Department of Solid Globe Geochemistry, Nihon Agency for Marine-Earth Scientific discipline and Applied science, 2-xv Natsushima-cho, Yokosuka, 237-0061, Japan

   Morihisa Hamada & Toshihiro Suzuki

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Correspondence to Masashi Ushioda.

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The authors declare that they take no competing interests.

Authors' contributions

MU conducted the experimental petrological studies and drafted the manuscript. ET conceived of the study, participated in the design of the study, and contributed to drafting of the manuscript. MH participated in its design and coordination and contributed to drafting of the manuscript. TS contributed to performing the high-pressure experiments. All authors read and canonical the final manuscript.

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Ushioda, Grand., Takahashi, E., Hamada, Thousand. et al. Water content in arc basaltic magma in the Northeast Nihon and Izu arcs: an estimate from Ca/Na partitioning betwixt plagioclase and melt. World Planet Sp 66, 127 (2014). https://doi.org/ten.1186/1880-5981-66-127

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• Received: 13 December 2013

• Accepted: 15 September 2014

• Published: 29 September 2014

• DOI : https://doi.org/10.1186/1880-5981-66-127

Keywords

• Island arc basalt
• Water content
• Plagioclase
• Hydrous melting experiments
• Across-arc geochemical variation

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