Language：English   Publishing type：Research paper (scientific journal)  

DOI： https://doi.org/10.1016/j.jvolgeores.2022.107643

Language：English   Publishing type：Research paper (scientific journal)  

DOI： https://doi.org/10.1016/j.jvolgeores.2022.107613

Other Link： https://www.sciencedirect.com/science/article/pii/S0377027322001445?casa_token=FYM_AfUo_JgAAAAA:Fw_5_x3QRaMwlGdBgB328yPLJ-qm61dOGk0uuBPtJtHJ7hlzP5vUjGuK1weYXLlExMTuwXLn

Language：English   Publishing type：Research paper (scientific journal)  

DOI： https://doi.org/10.1063/5.0082506

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DOI： https://doi.org/10.1038/S41598-022-05252-5

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DOI： 10.1007/s00445-021-01484-x

Language：Japanese   Publishing type：Research paper (scientific journal)  

DOI： https://doi.org/10.3811/jjmf.2020.T012

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DOI： /10.1029/2019JB017796

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DOI： doi.org/10.1016/j.jvolgeores.2018.09.005

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DOI： 10.1002/2017JB014782

Language：English   Publishing type：Research paper (scientific journal)  

To reveal the cooling process of a rhyolite–obsidian flow, we studied the morphology of plagioclase microlites in the Tokachi–Ishizawa lava of Shirataki, northern Hokkaido, Japan, where the structure of the lava can be observed from obsidian at the base of the flow to the innermost rhyolite. Needle-like micron-scale textures, known as “projections” occur on the short side surfaces of the plagioclase microlites. Using FE–SEM we discovered a positive correlation between the lengths and spacings of these projections. On the basis of the instability theory of an interface between melt and crystal, and to understand the length and spacing data, we developed a model that explains the positive correlation and allows us to simultaneously estimate growth rates and growth times. Applying the model to our morphological data and the estimated growth rates and growth times, we suggest that the characteristics of the projections reflect the degree of undercooling, which in turn correlates with lava structure (the obsidian at the margin of the flow experienced a higher degree of undercooling than the interior rhyolite). The newly developed method provides insights into the degree of undercooling during the final stages of crystallization of a rhyolitic lava flow.

DOI： 10.1016/j.jvolgeores.2017.05.012

Language：English  

DOI： 10.1016/j.epsl.2014.07.035

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Language：English   Publishing type：Research paper (scientific journal)  

In shallow magmatic intrusions, a characteristic layering structure (hereafter referred to as cyclic layering) can sometimes be observed.
This cyclic layering is different from what is observed as rhythmic layering caused by gravity.
Here, we present examples of cyclic layering in Japan and Scotland.
The cyclic layering is visualized as differential weathering in response to the differential stiffness caused by textural variations such as those in the volume fraction, number density, and size of vesicles or crystals.
The spacing of layers seems to increase according to a geometric progression, like as in Liesegang bands of a diffusion-precipitation system.
Their geological occurrences suggest an origin in which the interplay between double diffusion (mass and heat) and the kinetics of crystallization or vesiculation has an important role.
In order to understand the development condition for cyclic layering and the characteristics of textural variations, such as the spacing of layering in crystallized multi-component melts by conductive cooling, we carried out a numerical experiment on the 1D crystallization process of a binary eutectic melt.
This simulation took into account the cooling from contact with country rock as well as the compositional and thermal diffusion and the kinetics of diffusion-limited crystallization.
The governing equations include dimensionless control parameters describing the relative importance of thermal diffusion or compositional diffusion (Lewis number, $Le$) and the effective latent heat release (Stefan number, $St$).
From the results of the numerical experiments, it was found that the layering develops through eutectic oscillation (compositional and thermal oscillation below the eutectic point), suggesting that the bi-activating condition, whereby both phases cooperatively activate their crystallization rates, is essential for the development of layering.
No layering is observed at the margin, and the length of the region with no layering increases exponentially with decreasing $St$.
The amplitude of textural oscillation decreases with decreasing $St$.
Thus, practically no layering develops at small latent heat release.
Three types of layering structure or oscillatory profiles of spatial texture are observed (short, long and multiple types), depending mainly on $Le$.
Realistic values of $Le$ and $St$ suggest that natural cyclic layering is the multiple or long type of layering.
Assuming that the spacing of natural layering corresponds to the distance between adjoining local maxima of textural quantities, such as crystal number density or mean crystal radius, the spacing in numerical experiments is mathematically well described by a geometric progression with common ratios that are functions of the controlling parameters,namely $Le$, $St$, nucleation barrier, and crystal growth rate scale.
The common ratios converge with increasing $Le$ to constants in the range of approximately 1.02 - 1.05, which is similar to the range of the natural observations.
Experiments with no latent heat release by the second-phase simulated vesicles show similar oscillatory behaviors, suggesting that the latent heat release of the first crystallizing phase is an essential factor for the development of vesicle layering.
Applying the results to vesicle layering, we propose a revised formation scenario in which the thermal effect of first-phase crystallization below the eutectic point dominates the effect of volatile diffusion.

Language：English   Publishing type：Research paper (scientific journal)  

DOI： 10.1016/j.jvolgeores.2009.05.012

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DOI： 10.1007/s004450050147

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DOI： 10.1029/94JB02775

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DOI： 10.1007/BF00307330

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DOI： 10.1016/0377-0273(90)90045-H

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The hydrodynamic behaviour of a two‐phase system with different densities and viscosities is investigated, assuming that both phases are continuous phases and incompressible and that no phase change occurs. Mass and momentum conservation equations describe the relative motion of the two phases under the gravitational force when the inertia term is not negligible. Using the derived equations the stability of a spatially constant structure along gravity is examined in the one‐dimensional case for an infinite system without boundaries, where the basic state is taken as constant velocity and volume fractions. Two special cases are considered: the first is a gas‐liquid system where the density of one of the phases is neglected; the second is a deformable solid‐liquid system where the densities of the two phases are taken to be the same except for the calculation of the buoyancy force. The linear stability analysis shows that a small perturbation always generates a propagating wave which grows unstably with a characteristic wavelength. Since the spatially uniform structure of a two‐phase system is always unstable, the growth pattern should be observed in nature if the growth rate and spatial scale of the system are suitable. The dependence of the wavelength and growth rate on parameters is divided into two regimes. In one regime the wavelength, which equals the compaction length, and growth rate depend on the typical pore size. In the other regime, on the other hand, they do not depend on the typical pore size but only on the kinematic viscosity of the liquid phase and the volume fraction, given the frictional law. Which regime a real system chooses depends on a nondimensional parameter. The first case (gas—liquid system) is applied to magma effusion in an eruption‐style volcano. The system consisting of a silicate liquid phase and a gas phase can have a wavelength from metres to tens of metres and a growth rate from the order of less than a second to 1 week depending on viscosities, typical pore size and volume fraction. As a result, the rhythm and discreteness of magma effusion observed at volcanic eruptions may be explained by the mechanism presented here. The theory provides a relation between the observed period of the magma effusion rate, the mixture exit velocity of gas plus magma and the volume fraction of magma, given the frictional law. Using the relation, the mixture exit velocity is estimated from the observed period for the 1986 Izu‐Oshima eruption. The applicability to partially molten systems in the mantle and the core and basic assumptions are discussed. Copyright © 1988, Wiley Blackwell. All rights reserved

DOI： 10.1111/j.1365-246X.1988.tb06707.x

Language：Others  

Publishing type：Research paper (scientific journal)  

Three color variations of grey members (including grey and banded juvenile clasts) were observed in the 52 ka ignimbrite deposits of Maninjau caldera, Indonesia; namely dark grey (DGM), pale grey (PGM), and light grey (LGM). All grey members were phenocryst-rich (24, 20, and 31 % for DGM, PGM, and LGM, respectively) and comprise plagioclase, pyroxene, amphibole, biotite, and oxides as the main phenocryst phases; however, apatite is exclusively present in DGM. Plagioclase with unzoned and coarsely sieved texture was observed in all grey members, while finely sieved and oscillatory zoned textures were exclusive in LGM. Notably, DGM is characterized by the highest MgO value among all grey members, followed by PGM and LGM (∼0.72, 0.46, and 0.34 wt% MgO under ∼74.0 wt% SiO2, respectively). Based on the amphibole geothermobarometer and plagioclase hygrometer, we found that all grey magmas were stored at a relatively similar range of pressure and water content, but DGM yields a higher apparent temperature than those of PGM and LGM. Such distinctive petrography and chemical characteristics, coupled with different temperature conditions strongly suggest that each grey member originated from different magma bodies, which were stored below the most voluminous white magma (the source of white pumice). The sudden decompression of the white magma via overpressure causes destabilization to the smaller grey magmatic bodies, allowing them to rise and erupt as grey and banded pumices during the final eruption stage. Our results enrich the evidence of the formation of multiple magma reservoirs in large-silicic magmatic systems, which might be a common behavior before large eruptions. Moreover, our detailed glass compositions for each juvenile type may be useful for further regional tephrochronology studies.

DOI： 10.1016/j.jseaes.2024.106332

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Publisher：Journal of Geophysical Research: Solid Earth  

In basaltic eruptions, bubbles move freely and collide within a volcanic conduit, leading to frequent bubble coalescence. Understanding the dynamics of buoyancy-driven coalescence of bubbles is crucial for predicting the explosivity of basaltic eruptions. We examine the evolution of the bubble volume distribution while considering buoyancy-driven coalescence and expansion due to decompression. We find that, at lower decompression rates, the bubble volume distribution (Formula presented.) rapidly evolves into a power-law distribution with an exponent of approximately (Formula presented.) as (Formula presented.). This suggests that, in basaltic magma, the repeated coalescence of bubbles rapidly forms large bubbles within 45 min to 3 days. We then examine the occurrence of eruption styles, specifically Strombolian or Hawaiian, under the assumption that the bursts of slugs, produced from bubble coalescence within the conduit, trigger Strombolian eruptions. Consequently, we identify a critical condition for the transition between eruption styles in terms of the ascent velocity of magma. This critical ascent velocity is consistent with the observed transitions between Strombolian and Hawaiian eruptions at Izu-Oshima and Kilauea.

DOI： 10.1029/2024JB029130

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Publishing type：Research paper (scientific journal)  

Constraining the magma supply to a subvolcanic reservoir is crucial to characterizing unrest and evaluating the potential for a forthcoming eruption. With the advent of GPS, tiltmeters, and satellite interferometry, it has been possible to infer changes in the supply rate of magma to shallow reservoirs over time scales of as much as decades. While these methods have impacted our ability to characterize volcanic unrest, they only probe magmatic activity over short time scales. Here, we constrain changes in magma supply rate at Sakurajima volcano (Kyushu, Japan) over the past five centuries. The combination of thermo-mechanical modeling, documented eruption history, and textural analyses of pumices allows us to tightly constrain the long-term rate of magma supply to the subvolcanic chamber through time. Specifically, we find that magma supply rate has increased by roughly an order of magnitude over the past 500 years and that the bubble content in the magma chamber has increased over time, explaining the changes in eruption volume between the Bunmei (ca. A.D. 1470), An-ei (ca. A.D. 1780), and Taisho (A.D. 1914) eruptions.

DOI： 10.1130/G51763.1

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The processes that control the crystallization of magmas, namely nucleation and growth, remain poorly constrained. Classical nucleation theory (CNT) has so far not provided a unified framework to explain crystal number density in laboratory experiments and the field. We use numerical experiments to study the influence of different cooling rates and CNT parameters on the crystal number density measured under constrained conditions in laboratory experiments. With varying the magnitude of pre-exponential factor (J0) of nucleation rate, which represents the number of cluster as heterogeneous nucleation sites, we find that the cooling rate exponent (ξ) of the crystal number density varies from 3/2 to −1, depending on the magnitude of J0, cooling rate and surface tension. Using the regime maps of ξ as functions of J0 and surface tension, we can successfully interpret the diversity of cooling rate exponents reported by laboratory experiments in terms of J0 and surface tension. For extreme case of a negative cooling rate exponent ξ = −1, we propose a new crystallization model with constant rates of nucleation and crystallization, which reproduces a log-linear crystal size distribution. In this condition, it is interesting that the crystal growth rate is inversely proportional to time, even if the diffusion-limited growth is inversely proportional to the square root of time. For the case study of zoning profiles in microlites formed by decompression-induced crystallization during the Shinmoedake 2011 subplinian eruptions, the comparison between theoretical predictions and natural volcanic products supports that our model is well applicable to magma ascent processes.

DOI： 10.1029/2023JB026481

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Whether the magma storage system is responsible for the formation of the 74 ka Youngest Toba Tuff (YTT) is still debatable. It is currently believed that the YTT super-eruption was formed either by a single voluminous chamber or by multiple magma chambers. This paper presents a detailed component analysis of eruption products, comprehensive stratigraphy, mineralogy, and geochemistry of phenocrysts and matrix glass to shed light on the issue. Based on the componentry, mineral assemblages, mineral and glass compositions, and vesicle texture, we identified four distinct pumice types: YtA–YtD. Of these, YtA is an amphibole-bearing pumice containing an average of 77.1 wt% SiO2. This type of pumice is characterized by abundant matrix vesicles, with plagioclase showing a wide range of anorthite content (An20–An90) and disequilibrium texture. The YtB and YtC types are the most evolved pumices, with 77.5 and 77.6 wt% SiO2, respectively. The plagioclase of these pumices commonly has an unzoned texture with low anorthite content (~An30). The YtB pumice is biotite-bearing, distinctively characterized by abundant pheno-vesicles; while the YtC pumice includes rare pheno-vesicles, skeletal-polyhedral quartz, and no biotite. The YtD type is a quartz- and sanidine-free pumice, with a less-evolved glass composition (76.3 wt% SiO2), and is characterized by dominant matrix-vesicles and crystal clots of plagioclase, amphibole, pyroxene, and biotite. The plagioclase of the YtD pumice shows a hollow texture and high anorthite content (~An50). In situ trace element analysis for the matrix glass of YtA, YtB, YtC, and YtD showed very distinct geochemical signatures, which correlated with the four pumice types. Bivariate plots (Ba vs. Y, Sr vs. Y, and Ba vs. Sr) showed that YtA pumice is characterized by medium Ba (400–875 ppm) and Sr (41–67 ppm), and variable Y (20–53 ppm) content. YtB and YtC pumices are characterized by low Ba (8–136 ppm) and Sr (13–37 ppm), and highly variable Y (27–77 ppm) content. YtD pumice is characterized by high Ba (1173–1340 ppm) and Sr (95–124 ppm), but a narrow range of Y (21–31 ppm) content. The trace-element geochemical signatures, occurrence and absence of certain minerals (i.e., biotite and quartz), and vesicle type from the distinct pumice type, suggest the presence of four distinct magma bodies before the eruptions, namely YtA, YtB, YtC, and YtD. The number of distinct glass shards and pumices with the same geochemical signatures represents the volume fraction of each magma type. The approximate total volume of the magma (5300 DRE km3) and the geographical distributions of each pumice type demonstrated that the voluminous YtA (3406 km3), medium YtB (1354 km3), and smallest YtD (168.5 km3) chambers in the northern direction, and the small YtC chamber (371.5 km3) in the southern caldera, were evacuated during the 74 ka YTT eruption. Eruptions from multiple magma chambers were initiated by a high supersaturation of pheno-vesicle-rich magma (YtB magma), triggering the subsequent eruptions of the YtA, YtB, YtC, and YtD magmas.

DOI： 10.1016/j.jvolgeores.2023.107804

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The formation of glass from silicic magmas during eruption is an enigmatic process. To understand the formation of obsidian, we used time–temperature–transformation (TTT) and time–pressure–transformation (TPT) diagrams to estimate the critical cooling and decompression rates needed to form glassy obsidian. The TTT diagram is a contour map of the crystallized volume fraction as a function of the crystallization temperature and time. A contour line for a given crystal fraction in a time versus temperature diagram has a cone shape, with the “nose” of the curve corresponding to the minimum time and corresponding temperature required to generate a specific crystal fraction. We also present a TPT diagram, based on the TTT diagram, and liquidus curve for decompression-induced crystallization. We applied the TTT diagram to the Tokachi–Ishizawa obsidian from Shirataki, Hokkaido, Japan, and used it to estimate the critical cooling rate that would have been required to form its glassy texture by cooling-induced crystallization during eruption. For decompression-induced crystallization, we used the TPT diagram to estimate the critical decompression rate needed to form glassy obsidian. Based on our calculation results, the critical cooling and decompression rates are highly dependent on the interfacial energy between crystals and melt. We compared the estimated critical cooling and decompression rates with those estimated from microlite number density and a one-dimensional solution of the heat conduction equation. Our calculation results reveal that glassy obsidian can be formed during an eruption, particularly under conditions of high interfacial energy.

DOI： 10.1016/j.jvolgeores.2023.107770

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The VEI 7 (220–250 km3), a 52 ka eruption of the Maninjau caldera in Indonesia produced two distinct types of white pumices: transparent (TWP) and non-transparent (NTWP). These pumices were identified on outcrops, based on their qualitative traits, without the use of laboratory analyses (geochemical and textural). TWPs are typically fragile, irregular in shape, and have a transparent glass of vesicle walls around visible large vesicles, whereas NTWPs are relatively strong, blocky in shape, and have a non-transparent glass due to invisible small vesicles. Based on chemical and petrographical analyses, both pumice types were crystal-poor (avg. of 3.3%), with similar mineralogy, glass compositions (avg. 78.5 wt% SiO2), and plagioclase core compositions (avg. of An28). From component analysis, we found that the abundance of TWP decreased towards the upper stratigraphic ignimbrite deposits, along with an increase in NTWP, grey pumice, banded pumice, and lithic (non-juvenile) contents. We defined two vesicle populations with a threshold diameter of 0.1 mm based on bimodal vesicle size distributions by textural analysis for TWP and NTWP. Large vesicles correspond to preexisting bubbles that form in the magma chamber (pheno-vesicle, > 0.1 mm), whereas small vesicles in the groundmass (matrix-vesicle, < 0.1 mm) are attributed to second nucleation in the conduit during the eruption. We performed a comparison using vesicle data (pheno- and matrix-vesicles) for these two white pumice types. Pheno- and matrix-vesicularity showed a negative correlation. Thus, the boundary between TWP and NTWP was also quantitatively confirmed by the volume fraction ratio of the pheno- and matrix-vesicles. This evidence suggests that TWP originated from pheno-bubble-dominated magma (at least 0.1% volume fraction of pheno-bubbles in the magma chambers), whereas NTWP originated from pheno-bubble-poor magma. The variation in the abundance of TWP and NTWP in the stratigraphic positions implies the rough stratification of pre-existing bubbles (pheno-bubbles) in the pre-eruptive magma chamber, where the overpressure developed to trigger and drive the eruption. The two regimes control the formation of matrix-vesicles: (1) a pheno-bubble-controlled regime, and (2) a decompression-controlled regime. Based on a correlation between pheno-vesicle number density (PVND) and matrix-vesicle number density (MVND) together with numerical calculations based on a previous study, we suggest that the TWPs with the highest pheno-vesicularity formed under conditions corresponding to the first regimes, while the NTWPs formed in the second regime, where MVND is mostly determined by decompression rate. We also argue that NTWP is the only representative juvenile for estimating magma decompression rate, as the MVND value in TWP do not represent the actual second nucleation processes. Therefore, the occurrence of NTWP in the entire deposits with a relatively similar MVNDs value might suggest that the early and final eruption stages experienced a relatively similar magma decompression rate.

DOI： 10.1016/j.jvolgeores.2022.107643

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Publishing type：Research paper (scientific journal)   Publisher：American Geophysical Union (AGU)  

DOI： 10.1029/2022GC010618

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We conducted laboratory experiments using a setup consisting of a flask and a conduit, which reproduces cyclic eruptions and the time-predictability of natural geysers. We measured pressure and temperature in the flask and the eruptive mass of each eruption, varying three geometric parameters of the experimental system: (i) the flask volume, (ii) the inner diameter of the glass conduit and (iii) the initial water level in the conduit. During the heating stage of each eruption cycle, continuous pressure oscillations were observed in the flask. The pressure measurement and visual observation using normal-speed and high-speed cameras revealed that the pressure oscillations consisted of two components: (i) lower-frequency fluctuation related to the vertical displacements of the water column in the conduit and (ii) superimposing pulses caused by bubble nucleation in the flask. The dominant frequency of the pressure oscillations decreased systematically toward the next eruption. To explain the frequency of pressure oscillations, we present a mathematical model relating the pressure change in the flask to the vertical displacements of the water column in the conduit. The frequency calculated by our model well explained the observed frequency, which suggested that the oscillation frequency was controlled by the three geometric parameters and the effective bulk modulus of the fluid in the flask. The systematic decrease of dominant frequency toward the next eruption was explained by a decrease in the effective bulk modulus of the fluid in the flask due to an increase in gas volume fraction by heating. We also found that the erupted mass of an eruption controlled the initial frequency just after the eruption. The larger erupted mass causes a larger temperature drop in the flask, lowering the initial gas volume fraction to increase the initial oscillation frequency.

DOI： 10.1016/j.jvolgeores.2022.107613

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Publishing type：Research paper (scientific journal)   Publisher：{AIP} Publishing  

DOI： 10.1063/5.0082506

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Language：English   Publishing type：Research paper (scientific journal)   Publisher：Springer Science and Business Media LLC  

<title>Abstract</title>An understanding of the dynamics of growth-driven coalescence is important in diverse fields across natural science and engineering. Motivated by the bubble coalescence in magma during volcanic eruptions, we study both experimentally and theoretically the coalescence of two growing bubbles in a Hele–Shaw cell. In our system, bubbles grow by gas expansion due to decompression and the diffusional influx of dissolved gas in the liquid. Our experiments show that the evolution of film thickness and bubble shape depends on viscosity, decompression rate, and cell gap. Through a scaling analysis and a perturbation approximation, we find that the hydrodynamic interaction between two bubbles is characterized by a film capillary number <inline-formula><alternatives><tex-math>$$Ca_f=(\eta {\dot{R } }/\sigma )(R/D)^2$$</tex-math><mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML">
<mml:mrow>
<mml:mi>C</mml:mi>
<mml:msub>
<mml:mi>a</mml:mi>
<mml:mi>f</mml:mi>
</mml:msub>
<mml:mo>=</mml:mo>
<mml:mrow>
<mml:mo>(</mml:mo>
<mml:mi>η</mml:mi>
<mml:mover>
<mml:mi>R</mml:mi>
<mml:mo>˙</mml:mo>
</mml:mover>
<mml:mo>/</mml:mo>
<mml:mi>σ</mml:mi>
<mml:mo>)</mml:mo>
</mml:mrow>
<mml:msup>
<mml:mrow>
<mml:mo>(</mml:mo>
<mml:mi>R</mml:mi>
<mml:mo>/</mml:mo>
<mml:mi>D</mml:mi>
<mml:mo>)</mml:mo>
</mml:mrow>
<mml:mn>2</mml:mn>
</mml:msup>
</mml:mrow>
</mml:math></alternatives></inline-formula> depending on viscosity <inline-formula><alternatives><tex-math>$$\eta$$</tex-math><mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML">
<mml:mi>η</mml:mi>
</mml:math></alternatives></inline-formula>, bubble radius <italic>R</italic>, growth rate <inline-formula><alternatives><tex-math>$${\dot{R } }$$</tex-math><mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML">
<mml:mover>
<mml:mi>R</mml:mi>
<mml:mo>˙</mml:mo>
</mml:mover>
</mml:math></alternatives></inline-formula>, interfacial tension <inline-formula><alternatives><tex-math>$$\sigma$$</tex-math><mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML">
<mml:mi>σ</mml:mi>
</mml:math></alternatives></inline-formula>, and cell gap <italic>D</italic>. The experimental results demonstrate that the film capillary number solely determines the bubble distortion just before coalescence. Under our experimental conditions, bubble coalescence occurs below a critical value of a nominal film capillary number defined as a film capillary number evaluated when two undeformed circular bubbles come into contact.

DOI： 10.1038/s41598-022-05252-5

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Other Link： https://www.nature.com/articles/s41598-022-05252-5

Language：English   Publishing type：Research paper (bulletin of university, research institution)  

DOI： https://doi.org/10.5109/4371995

Language：Japanese   Publishing type：Research paper (scientific journal)  

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DOI： 10.5026/jgeography.98.6_703

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In previous chapters, thermodynamic equilibrium conditions for vesiculation of magma and kinetics of nucleation and growth of bubbles have been explained. Bubbles in magma experience both simple elemental processes of nucleation and growth in supersaturated liquid and various processes before reaching the surface of the Earth. Among various processes bubbles experience, this chapter explains secondary growth, deformation, coalescence, detachment, collapse, and oscillation, which are relatively well studied. In addition to the previous chapters, theoretical examination is first conducted, followed by application of the theoretical examination to the experimental results.

DOI： 10.1007/978-981-16-4209-8_6

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In the previous chapter, we learned that, for bubble generation, a supersaturated state is required. So, how do bubbles actually form in a supersaturated liquid? How do these bubbles grow to bubbles that we can see? To answer these questions and understand bubble formation, it is absolutely necessary for us to consider the meaning of the size and number of bubbles present in highly vesiculated volcanic rocks such as pumice and scoria, described in Chap. 1. These concepts are necessary for us to understand the dominant factors controlling eruption styles and intensity from the bubble texture in highly vesiculated volcanic rocks. In this chapter, we will understand the mechanisms of such bubble formation and behavior of bubbles in liquids based on both theories and experiments.

DOI： 10.1007/978-981-16-4209-8_3

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Volcanic eruptions have the diversities in the time scales within 4.6 GA of the Earth’s age, the magnitude of eruptive volume, the style (how magmas erupt). Together with these, the tectonic setting where a volcano locates and the chemical compositions of magmas characterize the eruption. The complexity resulting from these diversities make it difficult to share our recognitions and interests on volcanic eruptions. Before learning the fundamental processes such as vesiculation and crystallization of magmas in volcanic eruptions, we need to have our common recognitions and interests to share for scientific approaches. In this chapter, I will show specific examples of eruptions to share the scientific interests for latter chapters.

DOI： 10.1007/978-981-16-4209-8_1

Scopus

Bubbles nucleating in supersaturated liquids grow by H2O diffusion in melts into bubbles (the number of H2O molecules in the bubbles increases) and expand by decompression (the number of H2O molecules in the bubbles does not change but the molecular volume increases). In this manner, “growth” (“grow”) and “expansion” (“expand”) are used differently for different phenomena in this chapter. Although growth and expansion simultaneously progress, their behavior will be separately understood by ignoring the other at first. Then, the two phenomena will be combined to understand the experimental results. In this chapter, important factors including time constants of various elemental processes and their dimensionless number ratios, such as the Pélclet number, which is the ratio of the diffusion to the viscosity-limited expansion rate, are discussed.

DOI： 10.1007/978-981-16-4209-8_4

Scopus

The previous chapters explained the mechanism of each individual process (elementary process) involved in the vesiculation and crystallization of magma; the overall time evolution of the vesiculation process and the crystallization process comprising the elementary processes; the roles of physical properties in the processes; and shared the accuracy and limits of theoretical understanding compared with experiments. This chapter introduces the examples of interpreting the texture of volcanic products and readings of quantitative information from them by applying the understanding achieved to date. Keeping correspondence with eruption styles in mind, this chapter deals with actual data obtained from the texture analysis of eruptive products and applies the understanding achieved to date to the actual data to quantitatively understand eruptive phenomena in the order of explosive eruptions and nonexplosive eruptions. The last section describes the application to intrusions. Moreover, the bubble texture and crystalline texture are separately explained.

DOI： 10.1007/978-981-16-4209-8_10

Scopus

In this chapter, the basis for the tool to interpret crystal size distribution (CSD) will be explained. First, we will address the background of CSD introduction, the physical interpretation of the exponential CSD often observed in nature, and the examples of studies on CSD in nature. Then, we will introduce two theoretical methods of describing CSD’s temporal development; the Eulerian and Lagrangian descriptions, which were introduced in the chapters on vesiculation and crystallization. In this chapter on CSD, we will obtain general solutions of CSD under various conditions in closed and open systems. The closed system is a system in which CSD is only determined by the dynamics of nucleation and growth of crystals, and liquid and crystals do not move. An open system is that in which exchange with the external system of crystals essentially influences CSD. An advantage of the mathematical disscussion of CSD is that when CSD obtained by models is compared with that obtained by experiments, the relationship between observable CSD and model parameters can be clearly undrestood than when we use an empirical rule obatained using numerical calculations. Finally, we will derive the CSD corresponding to the Avrami plot, which is often conducted in phade change experiments.

DOI： 10.1007/978-981-16-4209-8_9

Scopus

In Sect. 2.8, we learned that magma vesiculation, associated with decompression, induces decrease in water content in the silicate melt, leading to rise in the melting point of silicates. Therefore, for natural volcanic eruptions, when magma (which is saturated with water at depths) at a constant temperature spouts to the surface along with vesiculation, it becomes a supercooled state in most cases. In this chapter, we will summarize a point of similarity and a point of difference between cooling crystallization and decompression-vesiculation-induced crystallization (hereafter referred to as decompression-induced crystallization) from a thermodynamic perspective. Next, in cases where vesiculation progresses in equilibrium with decompression, we will explain a crystallization process. In this case, water content in melt is equivalent to solubility with respect to pressure. Then, because of the influence of bubble nucleation and growth processes, we will examine the case in which water content can change in disequilibrium with pressure. In the latter case, the rate of change in water content is greatly different between the disequilibrium and quasi-equilibrium regimes. Because there is no difference between both cases in the facts that crystallization undergoes crystal nucleation and growth, we use knowledge on cooling crystallization.

DOI： 10.1007/978-981-16-4209-8_8

Scopus

In this chapter, we will discuss the kinetics of the cooling crystallization of magma, i.e., nucleation and growth, to use it as a foundation for making tools for observing unknown information from crystallization texture similar to the vesiculation processes (equilibrium conditions Chap. 2, nucleation process Chap. 3, growth process Chap. 4, temporal development of vesiculation Chap. 5, and complex processes related to vesiculation Chap. 6) dealt with in previous chapters. In this chapter, for crystallization-related problems, we will explain the similar contents in one go because both vesiculation and crystallization are the formation of a new phase from solution or a phase transition process and have similarity. First, using a binary eutectic system as an example of a multi-component system, we will explain crystallization-related conditions from a liquid and define a solid—liquid equilibrium as well as supersaturation in terms of thermodynamics. Next, we will conduct the formulation of crystal nucleation and crystal growth, evaluate experiments using these results, and examine the classical theory. As the crystal growth-related problems, the compositional zoning that is often observed in crystals is discussed for simplified cases, involving the movement of the interface, which has been extensively studied in metallurgy.

DOI： 10.1007/978-981-16-4209-8_7

Scopus

In the previous chapter, we learned by observing highly vesiculated volcanic rocks (pumice and scoria) that bubble formation in magma, i.e., the vesiculation of magma, has an extremely close relationship with appearances of eruptions. Moreover, we learned that the expansion of gas generated by magma vesiculation is a driving force for volcanic explosions and that magma vesiculation progresses by cooling and solidification of magma as well as plays a role in triggering eruptions. Thus, the conditions (to be precise, the necessary conditions) for magma vesiculation, which play an important role in volcanic eruptions, are dependent on the solubility of water (H2 O) (the major component of the gas phase that vesiculates in magma) in silicate melt. Then, how has the solubility of water in melt been understood? Moreover, what types of conditions (such as temperature and pressure, etc.) influence the solubility? In this chapter, we will increase our understanding of the solubility of water in magma.

DOI： 10.1007/978-981-16-4209-8_2

Scopus

In this chapter as appendix, some fundamental knowledge and concepts, derivation of equations, material properties related to magmas, and practical methods of textural observation are briefly summarized for reader’s convenience. For more comprehensive understanding, readers will find the helpful illustration in cited articles.

DOI： 10.1007/978-981-16-4209-8_11

Scopus

Language：Japanese   Book type：Scholarly book

Event date： 2016.6 - 2016.7

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Event date： 2015.9

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：東京大学   Country：Japan  

Event date： 2015.8

Language：English   Presentation type：Oral presentation (general)  

Country：Czech Republic  

Event date： 2015.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2013.9 - 2013.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：猪苗代町体験交流館「学びいな」 〒969-3123 福島県耶麻郡猪苗代町鶴田141番地1   Country：Japan  

Event date： 2013.7

Language：English   Presentation type：Oral presentation (general)  

Venue：Kagoshima   Country：Japan  

Event date： 2013.7

Language：English   Presentation type：Oral presentation (general)  

Venue：Kagoshima   Country：Japan  

Event date： 2013.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

噴出物の組織や化学組成のミクロな特徴は、目に見えない火道中でのマグマの運動の歴史を記録している。その記録を、化学組成・組織のデータから定量的に読み解く手法の開発が、この10年で格段に進んできた。その中には、マイクロライト組成、気泡やマイクロライトのサイズ分布に基づくマグマの飽和深度や上昇の際の減圧速度、マグマ滞在時間の推定などが含まれる。そして、その応用の成果として、リアルタイムで取得されている地表での地球物理的・化学的観測データと併せて、マグマが移動を開始してから噴出に至るまでのマグマの運動のイメージがより現実的に描けるようになってきた。こうした手法の発達は、噴出物の組織や化学組成を再現する実験的研究、観察・測定技術、実験結果や観察結果を物理化学的に解釈する理論的研究が、相補的に進歩してきた結果である。しかし、そうした進歩にもかかわらず、物質科学的手法を利用して、マグマの運動を的確に予想し、また、地質学的情報と併せて、過去の噴火の推移を定量的に復元できるまでには至っていない。ましてや、噴出量や噴火様式の推移の指標となる観測量の発見さらにはそれらの間の関係性など、火山噴火研究の一つの目標である噴火現象に関する物質科学的基本法則の発見には程遠い状況である。こうした困難を意識したうえで、物質科学研究の現状を省みると、天然で見られる噴出物の組織や化学組成の特徴が定性的にも定量的にもおおかた理解できた訳では決してなく、その背後にある根本的な問題が数多く残されていることに気づく。例えば、気泡やマイクロライトのサイズ分布関数のさまざまな形の成因や、非平衡下で結晶化する際の結晶組成決定性の問題である。本講演では、それらの問題の一つであるマイクロライトの結晶サイズ分布（CSD）に関して現状と展望を語る。
CSDは、指数分布すなわち、横軸を結晶サイズ、縦軸をpopulation density（決まった結晶サイズの範囲にある結晶数）として片対数でプロットすると、直線的になる場合がしばしばある。指数分布になるには、時間の指数関数として結晶核形成速度が増加する必要があるが、その増加速度を決める時間の係数は、均質核形成理論と減圧結晶化実験から予想される値よりはるかに小さくなる。また、多くのCSDは、大きいサイズでは指数分布よりpopulation densityが大きくなり、小さいサイズでは小さくなり、指数分布からずれてくる。すなわち、指数分布のCSDは近似でしかなく、それと数学的に一致することの物理的理由を探ることに定量的意味はない。とはいえ、CSDが、結晶の核形成と成長の歴史を表していることに間違いはない。物理的にはCSDは、実効的冷却速度が大きくなれば傾きの絶対値と切片の値が大きくなる（細かい結晶が沢山形成することに相当する）から、傾きや切片の値は、時間スケールすなわち実効的冷却速度（減圧速度）や滞在時間の指標である。それ故、よく用いられるCSD法では、指数分布を仮定して、状況証拠的時間スケールを与えて、その傾きから結晶成長速度を推定するが、これは本末転倒と言える。講演者らは、結晶化のモデルを順問題として解き、その結果から、実効的冷却速度と結晶数密度（CSDの0次のモーメント）の関係を導き、それを用いて、結晶数密度から、実効的冷却速度を推定する方法を提案した。この方法では、核形成速度最大時の瞬間的な線形の冷却速度や減圧速度が推定できるが、CSDの最大値付近の接線の傾きと切片の情報しか利用していないことになる。しかし、CSDの形自体に、マグマの温度・圧力の時間変化に関してもっと多くの情報があるはずである。その情報を定量的に推定するために、Lagrange的なCSDの記述方法から出発し、温度圧力の非線形な時間変化を特徴づけるパラメータを未知数とした、逆問題を定式化する。講演では、その定式化と応用を示し、CSDインバージョンンの方法を提案しその可能性について議論したい。

Event date： 2013.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

Event date： 2013.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

Event date： 2011.12

Venue：SanFransico, USA   Country：Japan  

Event date： 2011.10

Presentation type：Oral presentation (general)  

Venue：旭川市大雪クリスタルホール 　　　〒070-8003　北海道旭川市神楽3 条7 丁目   Country：Japan  

Event date： 2011.6 - 2011.7

Presentation type：Oral presentation (general)  

Country：Australia  

Event date： 2011.5

Presentation type：Oral presentation (general)  

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

Event date： 2010.7

Presentation type：Oral presentation (general)  

Country：France  

Event date： 2010.5

Presentation type：Oral presentation (general)  

Venue：つくば市   Country：Japan  

Event date： 2009.12

Presentation type：Oral presentation (general)  

Country：Japan  

Event date： 2009.10

Presentation type：Oral presentation (general)  

Venue：神奈川県小田原市   Country：Japan  

Event date： 2008.8

Venue：アイスランド　レイキャビク   Country：Iceland  

Event date： 2008.8

Presentation type：Oral presentation (general)  

Country：Iceland  

Microlite systematics: Origin and implications for the
conduit flow

Event date： 2008.5

Presentation type：Oral presentation (general)  

Venue：千葉、幕張   Country：Japan  

Event date： 2008.5

Presentation type：Oral presentation (general)  

Venue：千葉、幕張   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：長崎県島原市   Country：Japan  

Presentation type：Oral presentation (general)  

Country：United States  

Presentation type：Oral presentation (general)  

Country：United States  

Other Link： http://www.agu.org/

Presentation type：Oral presentation (general)  

Venue：千葉、幕張   Country：Japan  

Presentation type：Oral presentation (general)  

Country：Japan  

Country：Japan  

Event date： 2022.5 - 2022.6

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：Online   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2022/top

Event date： 2022.5 - 2022.6

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：Online   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2022/top

Event date： 2022.5 - 2022.6

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：Online   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2022/top

Event date： 2022.5 - 2022.6

Language：Japanese   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2022/top

Event date： 2022.5 - 2022.6

Language：Japanese   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2022/top

Event date： 2022.5 - 2022.6

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：Online   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2022/top

Event date： 2021.5 - 2021.6

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：Online   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2021/top

Event date： 2021.5 - 2021.6

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2021/top

Event date： 2021.5 - 2021.6

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2021/top

Event date： 2021.5 - 2021.6

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2021/top

Event date： 2021.5 - 2021.6

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：Online   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2021/top

Event date： 2021.5 - 2021.6

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：Online   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2021/top

Event date： 2020.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：オンライン   Country：Japan  

Event date： 2020.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：オンライン   Country：Japan  

Event date： 2020.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：オンライン   Country：Japan  

Event date： 2020.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：オンライン   Country：Japan  

Event date： 2020.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：オンライン   Country：Japan  

Event date： 2020.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：オンライン   Country：Japan  

Event date： 2020.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：オンライン   Country：Japan  

Event date： 2020.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：オンライン   Country：Japan  

Event date： 2020.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：オンライン   Country：Japan  

Event date： 2020.6

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2020/top

Event date： 2020.6

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2020/top

Event date： 2020.6

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2020/top

Event date： 2020.6

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2020/top

Event date： 2020.6

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：Online   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2020/top

Event date： 2020.6

Language：Japanese   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2020/top

Event date： 2020.6

Language：Japanese   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2020/top

Event date： 2020.6

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：Online   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2020/top

Event date： 2020.6

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2020/top

Event date： 2020.5

Language：English   Presentation type：Oral presentation (general)  

Country：Austria  

Other Link： https://doi.org/10.5194/egusphere-egu2020-6694

Event date： 2019.12

Language：English   Presentation type：Oral presentation (general)  

Country：United States  

Other Link： https://www.agu.org/fall-meeting-2019

Event date： 2019.11

Language：English   Presentation type：Oral presentation (general)  

Country：Indonesia  

Other Link： http://fos.ubd.edu.bn/foscon/

Event date： 2019.11

Language：English   Presentation type：Oral presentation (general)  

Country：Indonesia  

Other Link： http://fos.ubd.edu.bn/foscon/

Event date： 2019.11

Language：English   Presentation type：Oral presentation (general)  

Country：Indonesia  

Other Link： http://fos.ubd.edu.bn/foscon/

Event date： 2019.11

Language：English   Presentation type：Oral presentation (general)  

Country：Indonesia  

Other Link： http://fos.ubd.edu.bn/foscon/

Event date： 2019.11

Language：English   Presentation type：Oral presentation (general)  

Country：Indonesia  

Other Link： http://fos.ubd.edu.bn/foscon/

Event date： 2019.11

Language：English   Presentation type：Oral presentation (general)  

Country：Indonesia  

Other Link： http://fos.ubd.edu.bn/foscon/

Event date： 2019.11

Language：English   Presentation type：Oral presentation (general)  

Country：Indonesia  

Other Link： http://fos.ubd.edu.bn/foscon/

Event date： 2019.11

Language：English   Presentation type：Oral presentation (general)  

Country：Indonesia  

Other Link： http://fos.ubd.edu.bn/foscon/

Event date： 2019.9

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Event date： 2019.9

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：神戸大学六甲台第2 キャンパス   Country：Japan  

Event date： 2019.9

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：神戸大学六甲台第2 キャンパス   Country：Japan  

Event date： 2019.9

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：神戸大学六甲台第2 キャンパス   Country：Japan  

Event date： 2019.9

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Event date： 2019.6

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Event date： 2019.5

Language：English   Presentation type：Oral presentation (general)  

Venue：Makuhari messe、Chiba   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2019/top

Event date： 2019.5

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2019/top

Event date： 2019.5

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2019/top

Event date： 2019.5

Language：English   Presentation type：Oral presentation (general)  

Venue：Makuhari messe、Chiba   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2019/top

Event date： 2019.5

Language：English   Presentation type：Oral presentation (general)  

Venue：Makuhari messe、Chiba   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2019/top

Event date： 2019.5

Language：English   Presentation type：Oral presentation (general)  

Venue：Makuhari messe、Chiba   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2019/top

Event date： 2019.4

Language：English   Presentation type：Oral presentation (general)  

Venue：Viena   Country：Austria  

Other Link： https://www.egu2019.eu/

Event date： 2019.1

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：九大西新プラザ   Country：Japan  

Event date： 2018.9

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：秋田大学手形キャンパス   Country：Japan  

Event date： 2018.9

Language：Japanese  

Venue：秋田大学手形キャンパス   Country：Japan  

Event date： 2018.9

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：秋田大学手形キャンパス   Country：Japan  

Event date： 2018.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：Makuhari messe、Chiba   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2018/top

Event date： 2018.5

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2018/top

Event date： 2018.5

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2018/top

Event date： 2018.5

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2018/top

Event date： 2018.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：Makuhari messe、Chiba   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2018/top

Event date： 2018.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：Makuhari messe、Chiba   Country：Japan  

Other Link： https://confit.atlas.jp/guide/event/jpgu2018/top

Event date： 2018.4

Language：English   Presentation type：Oral presentation (general)  

Country：Austria  

Other Link： https://www.egu2018.eu/

Event date： 2017.9

Language：Japanese  

Venue：熊本大学黒髪南キャンパス   Country：Japan  

Event date： 2017.9

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：熊本大学黒髪南キャンパス   Country：Japan  

Event date： 2017.9

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：熊本大学黒髪南キャンパス   Country：Japan  

Event date： 2017.5

Language：Japanese  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2017.5

Language：Japanese  

Country：Japan  

Event date： 2017.5

Language：Japanese  

Country：Japan  

Event date： 2017.5

Language：Japanese  

Country：Japan  

Event date： 2017.5

Language：Japanese  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2017.5

Language：Japanese  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2017.5

Language：Japanese  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2016.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：富士吉田市民会館・ふじさんホール   Country：Japan  

Event date： 2016.6 - 2016.7

Language：English  

Country：Japan  

Event date： 2016.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2016.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2016.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2016.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2016.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2015.9

Language：Japanese  

Venue：富山大学   Country：Japan  

Event date： 2015.9

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：富山大学   Country：Japan  

Event date： 2015.9 - 2015.8

Language：English   Presentation type：Public lecture, seminar, tutorial, course, or other speech  

Country：United States  

Event date： 2015.7

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：北海道大学低温研究所   Country：Japan  

Event date： 2015.6

Language：English   Presentation type：Symposium, workshop panel (public)  

Country：Japan  

Event date： 2015.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2015.5

Language：English   Presentation type：Oral presentation (general)  

Country：Japan  

Event date： 2015.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2015.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2015.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2015.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：千葉幕張メッセ   Country：Japan  

Event date： 2015.5

Language：English   Presentation type：Oral presentation (general)  

Venue：Nihon University   Country：Japan  

Event date： 2014.12

Language：Japanese   Presentation type：Oral presentation (general)  

Country：Japan  

Event date： 2014.11

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：福岡大学   Country：Japan  

Event date： 2014.11

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：福岡大学   Country：Japan  

Event date： 2014.11

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：福岡大学   Country：Japan  

Event date： 2014.11

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：福岡大学   Country：Japan  

Event date： 2014.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：横浜パシフィコ   Country：Japan  

Event date： 2014.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：横浜パシフィコ   Country：Japan  

Event date： 2014.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：横浜パシフィコ   Country：Japan  

Event date： 2014.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：横浜パシフィコ   Country：Japan  

Event date： 2014.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：横浜パシフィコ   Country：Japan  

Event date： 2013.12

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：福岡大学理学部8号館   Country：Japan  

Event date： 2013.9 - 2013.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：猪苗代町体験交流館「学びいな」 〒969-3123 福島県耶麻郡猪苗代町鶴田141番地1   Country：Japan  

Event date： 2013.7

Language：English  

Venue：Kagoshima   Country：Japan  

Event date： 2013.7

Language：English   Presentation type：Oral presentation (general)  

Venue：Kagoshima   Country：Japan  

Event date： 2013.7

Language：English  

Venue：Kagoshima   Country：Japan  

Event date： 2013.7

Language：English  

Venue：Kagoshima   Country：Japan  

Event date： 2013.5

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

Event date： 2012.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：長野県御代田市 エコール御代田   Country：Japan  

Event date： 2012.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：長野県御代田市 エコール御代田   Country：Japan  

Event date： 2012.10

Language：Japanese   Presentation type：Oral presentation (general)  

Venue：長野県御代田市 エコール御代田   Country：Japan  

Event date： 2012.6

Language：English  

Country：Japan  

Event date： 2012.6

Language：English  

Country：Japan  

Event date： 2012.5

Language：Japanese  

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

Event date： 2012.5

Language：Japanese  

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

Event date： 2012.5

Language：Japanese  

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

Event date： 2012.5

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

Event date： 2012.5

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

Event date： 2012.4

Language：English   Presentation type：Oral presentation (general)  

Country：Austria  

Event date： 2012.4

Language：English   Presentation type：Oral presentation (general)  

Country：Austria  

Event date： 2011.10

Country：Japan  

Event date： 2011.10

Presentation type：Oral presentation (general)  

Venue：旭川市大雪クリスタルホール 　　　〒070-8003　北海道旭川市神楽3 条7 丁目   Country：Japan  

Event date： 2011.10

Venue：旭川市大雪クリスタルホール 　　　〒070-8003　北海道旭川市神楽3 条7 丁目   Country：Japan  

Event date： 2011.5

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

Event date： 2011.5

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

Event date： 2011.5

Venue：幕張メッセ国際会議場(〒261-0023 千葉市美浜区中瀬2-1)   Country：Japan  

Event date： 2011.3

Venue：東京都   Country：Japan  

Event date： 2011.1

Presentation type：Oral presentation (general)  

Venue：鹿児島市   Country：Japan  

Event date： 2010.10

Presentation type：Oral presentation (general)  

Venue：京都市   Country：Japan  

Event date： 2010.10

Venue：京都市   Country：Japan  

Event date： 2010.10

Presentation type：Oral presentation (general)  

Venue：京都市   Country：Japan  

Event date： 2010.5

Venue：千葉幕張   Country：Japan  

Event date： 2010.5

Venue：千葉幕張   Country：Japan  

Event date： 2010.5

Venue：千葉幕張   Country：Japan  

Event date： 2010.5

Venue：千葉幕張   Country：Japan  

Event date： 2010.5

Venue：千葉幕張   Country：Japan  

Event date： 2010.4

Presentation type：Oral presentation (general)  

Country：Japan  

Event date： 2009.12

Country：Japan  

Event date： 2009.12

Venue：SanFransico, USA   Country：Japan  

Event date： 2009.9

Country：Japan  

Event date： 2009.5

Venue：千葉幕張   Country：Japan  

Event date： 2009.5

Venue：千葉幕張   Country：Japan  

Event date： 2009.5

Presentation type：Oral presentation (general)  

Venue：千葉幕張   Country：Japan  

Event date： 2009.5

Country：Japan  

Interaction between andesite and liquid water: temporal variation of rock surfacial texture
and chemical composition of water

Event date： 2008.10 - 2008.11

Presentation type：Oral presentation (general)  

Venue：京都市   Country：Japan  

Event date： 2008.9

Presentation type：Oral presentation (general)  

Venue：京都府宇治市   Country：Japan  

Event date： 2008.8

Country：Iceland  

Event date： 2008.8

Country：Iceland  

Event date： 2008.8

Country：Iceland  

Event date： 2008.5

Venue：千葉幕張   Country：Japan  

Country：Japan  

Country：Japan  

Country：Japan  

Country：Japan  

Presentation type：Oral presentation (general)  

Venue：福岡   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：東京   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：福岡   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：静岡   Country：Japan  

Presentation type：Oral presentation (invited, special)  

Venue：千葉県幕張メッセ   Country：Japan  

Country：Japan  

Presentation type：Oral presentation (general)  

Presentation type：Oral presentation (general)  

Venue：東京  

Venue：千葉   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：千葉   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：千葉   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：千葉   Country：Japan  

Venue：千葉   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：福岡   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：東京   Country：Japan  

Venue：千葉   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：千葉   Country：Japan  

Venue：千葉   Country：Japan  

Venue：千葉   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：千葉   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：仙台市   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：熊本県阿蘇町   Country：Japan  

Venue：熊本県阿蘇町   Country：Japan  

Presentation type：Oral presentation (general)  

Country：United States  

Presentation type：Oral presentation (general)  

Venue：千葉、幕張   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：千葉、幕張   Country：Japan  

Presentation type：Oral presentation (general)  

Venue：茨城県つくば市   Country：Japan  

Country：Japan  

Type：Competition, symposium, etc. 

Audience： Infants,　Schoolchildren,　Junior students,　High school students

Type：Seminar, workshop