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Reconstruction of a phreatic eruption on 27 September 2014 at Ontake volcano, central Japan, based on proximal pyroclastic density current and fallout deposits
© Maeno et al. 2016
- Received: 1 December 2015
- Accepted: 18 April 2016
- Published: 17 May 2016
The phreatic eruption at Ontake volcano on 27 September 2014, which caused the worst volcanic disaster in the past half-century in Japan, was reconstructed based on observations of the proximal pyroclastic density current (PDC) and fallout deposits. Witness observations were also used to clarify the eruption process. The deposits are divided into three major depositional units (Units A, B, and C) which are characterized by massive, extremely poorly sorted, and multimodal grain-size distribution with 30–50 wt% of fine ash (silt–clay component). The depositional condition was initially dry but eventually changed to wet. Unit A originated from gravity-driven turbulent PDCs in the relatively dry, vent-opening phase. Unit B was then produced mainly by fallout from a vigorous moist plume during vent development. Unit C was derived from wet ash fall in the declining stage. Ballistic ejecta continuously occurred during vent opening and development. As observed in the finest population of the grain-size distribution, aggregate particles were formed throughout the eruption, and the effect of water in the plume on the aggregation increased with time and distance. Based on the deposit thickness, duration, and grain-size data, and by applying a scaling analysis using a depth-averaged model of turbulent gravity currents, the particle concentration and initial flow speed of the PDC at the summit area were estimated as 2 × 10−4–2 × 10−3 and 24–28 m/s, respectively. The tephra thinning trend in the proximal area shows a steeper slope than in similar-sized magmatic eruptions, indicating a large tephra volume deposited over a short distance owing to the wet dispersal conditions. The Ontake eruption provided an opportunity to examine the deposits from a phreatic eruption with a complex eruption sequence that reflects the effect of external water on the eruption dynamics.
- Phreatic eruption
- Pyroclastic density current
- Ontake volcano
- Grain-size distribution
- Particle concentration
- Flow speed
Volcanic eruptions can violently expel only non-juvenile materials. Such eruptions are caused by catastrophic failure of country rock owing to pressurization of the gas–fluid sources or flashing of superheated water at shallow levels (e.g., Wohletz and Heiken 1992). The eruptions are often called ‘phreatic’ eruptions, implying that heated groundwater is a major driving force in the expulsion of the country rock, or a ‘hydrothermal’ eruption, if fluid from a hydrothermal system is involved (e.g., Hedenquist and Henley 1985; Mastin 1995). Heating by ascending fresh magma can also trigger eruptions of non-juvenile material as seen in precursor events of magmatic eruptions (e.g., Barberi et al. 1992; Young et al. 1998; Suzuki et al. 2013). Phreatic eruptions tend to be of smaller scale in terms of the volume of the products, and the temperature of the ejected material (a few 100 °C) is generally much lower than that of magmatic eruptions (Feuillard et al. 1983; Hedenquist and Henley 1985; Barberi et al. 1992; Browne and Lawless 2001). However, non-juvenile eruptions are not necessarily less disastrous; rather, they are more likely to cause damage than magmatic eruptions in some situations. They are occasionally very intense and often occur without clear precursor signals. They can also last a relatively long period (e.g., ~8 months for the La Soufrière event, Guadeloupe, in 1975–1976), resulting in a difficult scenario that requires managing a complex eruption sequence (Feuillard et al. 1983; Hincks et al. 2014). Moreover, non-magmatic eruptions sometimes lead to partial edifice collapse and laterally directed violent explosions (e.g., Bandai, Japan; Tongariro, NZ; La Soufrière, Guadeloupe).
The eruption at Ontake volcano on 27 September 2014 was the worst volcanic disaster (58 deaths and five missing persons) in Japan in the past half-century; many of the casualties were climbers who were close to the summit of the mountain at the time of the eruption. Reconstruction of phreatic events based on geological and witness records is important to understand the nature of these eruptions and to evaluate potential hazards related to phreatic eruptions. However, such studies are limited to relatively large-scale past phreatic events (e.g., Bandai volcano, Yamamoto et al. 1999; Adatara volcano, Fujinawa et al. 2008) and recent well-observed eruptions (e.g., Heiken et al. 1980; Ohba et al. 2007; Lube et al. 2014), and there are still uncertainties on quantitative estimation of the eruption processes based on geological records. The eruption at Ontake volcano provides an opportunity to study the process of a phreatic eruption. In this paper, we characterize the proximal pyroclastic density currents (PDCs) and fallout deposits of this eruption. We reconstruct the eruption process and estimate the physical parameters (volume, velocity, and particle concentration) of the associated PDCs based on geological and witness records and apply a scaling analysis using a depth-averaged model of gravity currents flowing down slopes.
First, we overview the eruption at Ontake volcano on 27 September 2014, based on direct observations by monitoring instruments and witnesses. Then, we present geological data obtained by our field surveys at proximal and distal sites. The distribution, thickness, and description of the tephra deposit are presented. The data were used to estimate the physical parameters of the eruption such as tephra volume. We also present laboratory analysis of the grain-size characteristics of the deposit using the mechanical sieving method and laser diffraction particle-size analyzer, and component analysis by microscope and X-ray powder diffractometer (XRD). Based on the geological and witness records and the laboratory data, we discuss the eruption process.
Outline of the eruption
The eruption began at 11:52 (local time, used hereafter) on 27 September with vigorous ash emission from the Jigokudani area at an altitude of around 2700–2750 m a.s.l., about 500 m from Kengamine Peak. Immediately before the eruption, volcanic tremor and tilt changes were recorded at 11:41 and 11:45, respectively, at the JMA stations at Tanohara, 2 km SE of the summit (Japan Meteorological Agency 2014). The migration of VT earthquakes in the up-dip direction during the last 10 min before the eruption, which coincided with tremor and tilt changes, suggests that the vertical conduit was filled with pressurized fluids that rapidly propagated to the surface (Kato et al. 2015). These geophysical records are thought to be precursor phenomena of the eruption, although it was not possible to issue alerts before the eruption based on these phenomena. The eruption was confirmed at 11:52 by seismic and tilt records at the Tanohara station (Japan Meteorological Agency 2014). At the same time, climbers around the summit area witnessed an ash cloud rapidly rising from the Jigokudani valley and then a growing ash cloud covering the summit with a shower of ballistic ejecta.
According to interviews with climbers who stayed in and around the huts at the summit area [e.g., from The Shinano Mainichi Shimbun (2015)], the eruption cloud began to rise with no discernible sounds. After the emergence of the eruption cloud, some people heard a loud noise repeatedly from the direction of Jigokudani, followed by the development of the eruption cloud. As the ash cloud covered the sky, it grew dark; in the darkness, which lasted 20–30 min, climbers and staff who found shelter in the huts heard noises caused by sandy material and blocks hitting the roofs, walls, and windows of the buildings violently and intermittently. After 30 min, it became light for a short time and then darkened again. The interview reports suggest that the eruption event was dominated by intermittent, vigorous fallout or PDCs and ballistic ejecta in the proximal area and that the deposition of most of the eruptive material lasted at least half an hour. Oikawa et al. (2016) suggested that the temperature of the PDCs partially exceeded 100 °C but was mostly in the range 30–100 °C, based on an analysis of the interview reports. Most of the injures and deaths that occurred in this eruption are thought to have been caused by ballistic blocks with high velocity, hence high landing energy (Tsunematsu et al. 2016), that continued to land throughout most of the eruption period, rather than by low-temperature, dilute PDCs that mainly occurred in the initial phase of the eruption.
Sato et al. (2015) reported that the plume height eventually increased and reached about 10,000 m a.s.l. at 12:10, based on analyses of Doppler radar data. Therefore, when the photographs of the PDCs were taken from Ninoike-Honkan, the main eruption plume had just developed. The plume height then decreased to 7000 m a.s.l. at 12:20 and reached 4000–5000 m a.s.l. by 18:00 (Sato et al. 2015). The direct observations and the plume height data suggest that multiple PDCs were generated at the summit area by partial collapse of the growing eruption plume. Ash fall was observed mainly at the eastern side of the volcano. The tephra dispersal area extended to at least ~80 km from the summit. The ash-fall deposit is thought to have developed from a direct plume and a co-PDC plume. In the source area of the Jigokudani valley, at least three pyroclastic cones formed within about 3 h after the onset of the eruption in the vent area, trending NW–SE. One of these cones is thought to have been the main source of the initial eruption phase (the largest circle in the vent area in Fig. 1), and the others were formed at least 2–3 h after the initial eruption, based on analyses of aerial photographs (Kaneko et al. 2016). Aerial photographs indicate that the diameter of each crater is several tens of meters and the average height of the vent area is a few to 10 m. Mudflows emerged from some of the cones and flowed down the Jigokudani valley. Wet products characterize the later phase of the eruption, as indicated by sun cracks that developed on the deposit surface and by the residual water at the bottom of impact craters observed during a helicopter survey on the day following the eruption (Kaneko et al. 2016). However, there is no evidence of wet deposition in the proximal area during the initial phase (Oikawa et al. 2016). Thus, the eruption started in a relatively dry state and eventually changed to wet conditions.
Distribution and thickness of the eruptive deposits
The deposits around the summit area include not only fallout tephra but also PDC deposits (Fig. 4a). The distribution of the PDC deposits on the southern and western slopes was determined based on aerial photographs taken by the Geospatial Information Authority of Japan (GSI) (2014) and Kaneko et al. (2016). The major PDC deposits extend 1.5 km and 2.4 km from the vent in the NW and SW directions, respectively. Although it is difficult to determine the distribution of the PDC deposits in the northern and eastern sides based only on aerial photographs, geological and witness observations suggest that the PDC deposits also extend ~1 km or more from the vent on the NE and E sides. The distribution of the PDC deposits in this direction is a little narrower than the distribution of the PDCs determined based only on witness observations (Oikawa et al. 2016). The discrepancy may be owing to difficulty in determining the distal limit of the PDC deposits. Additionally, the dispersal axis of the fallout tephra extending ENE makes it difficult to distinguish between the fallout and the flow deposits in this direction. The thickness estimation may be close to the minimum value, because our surveys at the summit area were carried out more than 1 month after the eruption. Therefore, erosion and disturbance caused by the reworking process and searching operations for missing persons affected the original deposit structures at many locations. During the field survey, we carefully selected sites where the primary tephra deposits were preserved.
Distal ash fall from the Ontake eruption was observed at many locations in the eastern side of the volcano in the afternoon of 27 September 2014. The Joint Research Team for Ash Fall from the Ontake 2014 Eruption (2015) surveyed the distribution of ash-fall deposit and produced the isomass contour map (Fig. 4c). The 1 g/m2 contour extends ~80 km to the east. The isomass contours suggest that the eruption plume was primarily affected by a strong seasonal westerly wind, though minor ash fall was observed at the western side of the volcano.
Eruption deposit facies
Unit A consists of the lowest part of the deposit and is 1–5 cm thick (Fig. 4a), overlying the pre-eruption ground surface without erosion signatures. Generally, the thickness decreases with distance from the vent but is thicker in topographic depressions at some locations. The deposited material is gray, massive, and poorly sorted, with a dominant component of silt- to clay-sized fine ash (see “Grain-size characteristics” section). The unit shows almost no grading structures, but a discontinuous thin ash layer (a few mm thick) composed of sand-sized grains is occasionally embedded [e.g., at location (b)]. The distribution of Unit A is limited to the NE–N sides of the vent and is overlaid with a deposit a few tens of cm thick (Unit B). The contact between two units is diffusive. At locations (d, e), the maximum thickness is ~5 cm. At some locations near the vent area, altered, angular to subangular lava blocks with diameter up to ~10 cm, probably emplaced as ballistic ejecta (fallout) in the initial phase, are also contained in this unit. Unit A corresponds to the thin fine-grained ash layer generated from a PDC body at the initial phase shown in Figs. 2 and 3. The thickness of the deposit from the PDCs shown in the photograph taken from Ninoike (Fig. 3a) was <1 cm as observed around locations (g2, h).
Unit C consists of the uppermost part of the deposit. It is light gray, massive, and poorly sorted. The major components of this unit are silt- to clay-sized fine ash (Fig. 8), and the grain size is finer than that of Units A and B. Ash accretion textures can occasionally be recognized as observed in Unit B. Unit C can be found in various locations throughout the summit area; the layer thickness varies from a few to 10 cm (Fig. 7). Lava blocks with diameter up to ~10 cm, emplaced as ballistic ejecta, are also contained in this unit.
Large lava blocks up to a few tens of cm in diameter were observed on the surface throughout the deposit; some of these large ejecta damaged buildings around the summit area. These blocks were emplaced as ballistic ejecta and are embedded in Unit B and/or C. Immediately after the eruption, numerous impact craters produced by the ballistic ejecta were observed (Kaneko et al. 2016).
Grain-size analyses were carried out for samples from proximal and distal (6 and 10 km below the dispersal axis) locations for the different eruption units. For the proximal locations, the analyses were performed layer by layer. At locations (d, f), the samples were collected from eight and three stratigraphic levels, respectively. The distal fallout tephra contained aggregate particles; however, it was difficult to analyze the size distribution of the aggregates because they were fragile and the original size could be observed only in the field. Therefore, we analyzed the rough samples of the aggregates that included the fine particles. Thus, our data represent the entire grain-size distribution. Each sample was first sieved in wet conditions using a 3 − φ sieve. Then, the grain-size distribution for grains coarser than 3φ was determined by mechanical sieving at 0.5 − φ intervals. The grains that were finer than 3φ were classified by a laser diffraction particle-size analyzer under wet dispersion conditions, using the Sympatec HELOS & RODOS systems (Clausthal-Zellerfeld, Germany). The data obtained from both methods were combined to estimate the entire grain-size distribution assuming the same particle density.
The grain-size histograms for all the samples show widespread size distribution with multiple populations. The Inman parameters (Inman 1952) [the sorting coefficient (σ φ ) and median diameter (M d)] were used to determine the grain-size characteristics. The σ φ of all the samples is within the range 3–5φ, indicating extremely poor sorting (Fig. 8). The samples from the distal fallout and the top and bottom positions corresponding to Units A and C in the proximal region are characterized by larger M d and smaller σ φ values, but are still poorly sorted. The grain characteristics are comparable to representative phreatic and phreatomagmatic eruptions. Most of the samples from Unit B have features similar to those of fallout deposits from the Bandai 1888 eruption (Yamamoto et al. 1999) and the Adatara 1900 eruption (Fujinawa et al. 2008), but show slightly poorer sorting than the deposits from the Te Maari 2012 eruption (Unit C surge and fallout, Lube et al. 2014). One sample is similar to a lahar deposit from the Bandai eruption. However, finer samples such as those from Units A and C and distal fallout deposits show similar characteristics to accretionary lapilli deposits associated with the blast eruption at Mount St. Helens in 1980 (Hoblitt et al. 1981), or to the hydrovolcanic fine ash deposits summarized by Sheridan and Wohletz (1983). The dataset does not show the typical grain-size characteristics observed in magmatic pyroclastic flow, fall, and surge deposits (Walker 1971).
The major components of the eruptive materials are characterized by dense andesitic to dacitic lava with various degrees of alteration. The ash includes shattered crystals derived from the same lava. Hydrothermal minerals such as pyrite are often crystalized on the lava surface. No fresh juvenile components such as pumice or scoria were found in any of the samples. XRD analysis of the very fine components at location (d) found hydrothermal minerals such as smectite, kaolinite, pyrite, illite, pyrophyllite, and gypsum with quartz and plagioclase. There were no systematic changes in the components with height. This indicates that these products were derived primarily from fragmentation of country rock and hydrothermally altered material in a hydrothermal reservoir and along the pathways to the surface.
The products from the Ontake eruption consist of fallout tephra and PDC deposit. In the proximal area, it is difficult to determine each isopach contour of the fallout and the PDC deposits (Fig. 4). However, the PDC deposit layer is much thinner (10–15 % of the entire deposit) than the fallout tephra layer; hence, the contribution of the PDCs to the entire volume is small. This is validated by the volume estimation for PDCs based on other methods in a later section. Here, we calculate the total volume and mass for two extreme cases: case 1 that uses the proximal isopach contours for all the deposits (assuming 100 % fallout deposit) and case 2 that does not use the proximal isopach contours (assuming unknown thickness for proximal fallout and PDC deposits). The deposit density was assumed as ~1000 kg/m3 in all the calculations. For the two cases, the volume and mass of the fallout deposits were calculated using three methods: (a) integrating multiple exponential segments on a log(mass per unit area) versus log(area) plot (e.g., Froggatt 1982), (b) power-law fitting on log(thickness) versus square root of area plot (Bonadonna and Houghton 2005), and (c) Weibull fitting (Bonadonna and Costa 2012). For methods (a) and (b), different assumptions of tephra thickness at the source yielded maximum and minimum estimates. For the maximum estimates, the tephra thickness or mass at the rim of the vent area (average height) was assumed as 10 m or 104 kg/m2. For the minimum estimates, the tephra thickness or mass was assumed as 3 m or 103.5 kg/m2. The cone height at the vent area was roughly estimated based on aerial photographs in Kaneko et al. (2016). The distal extreme in method (a) was assumed as 10−4 kg/m2 for 104 km2 (minimum) or 105 km2 (maximum). For method (b), the distal extreme was set at 100 km. Both assumptions are based on extrapolation of the measured fallout tephra data. For method (c), fitted curves were integrated between zero and infinity for distance, and the parameter settings followed Bonadonna and Costa (2012) and Maeno et al. (2014).
Estimated volume and mass of Ontake eruption on 27 September 2014
Volumec (×106 m3)
Mass (×109 kg)
Fallout deposit and proximal pyroclastic density current deposit
Volumec (×106 m3)
Mass (×109 kg)
Pyroclastic density current deposit in S and W slopes
We also estimated the volume of the PDC deposits separately, excluding the deposit in the proximal area (shaded area in Fig. 4b). The PDC deposits extend to the southern and western slopes, but a detailed survey of the deposits was not possible because of difficulty of access. Based on aerial photographs taken by GSI, approximate distributions of the PDCs were drawn. The surface of the slopes covered by PDC deposits is whitish or light gray, but the average thickness is seemingly very thin, because colors from underlying leaves and ground surface are partially identifiable. The deposit is unlikely to be more than a few cm thick on average. Assuming a deposit thickness of 1–2 cm, the volume of the PDC lobes on the southern and western slopes is estimated to be 0.036–0.072 × 106 m3. This is a very rough estimate, but not significantly different from the results of a scaling analysis using a depth-averaged model for particle-laden flows on slopes as discussed in a later section.
Finally, the total volume of eruptive deposits is estimated to be 0.7–1.3 × 106 m3 (0.3–0.5 × 106 m3 in DRE), indicating that the magnitude of the eruption (M) is ~2. Although it is difficult to constrain the volumes of the PDCs that were emplaced in sequence toward the N–NE, our analyses suggest that the contribution of the PDCs to the total volume is <10 %. The estimated fallout deposit volume is similar to that of the phreatic eruption at Ontake in 1979, where the volume was estimated to be 0.95–1.23 × 106 m3 (0.4–0.5 × 106 m3 in DRE) by the same methods used for the 2014 eruption and using the tephra data by Kobayashi (1980).
Eruption process and formation of PDCs
To trigger such a phreatic eruption, a sealed, pressurized hydrothermal reservoir may be required at a certain level above a magmatic heat source as generally inferred from seismic data and component analysis (e.g., Feuillard et al. 1983; Boudon et al. 1998). The study by Nakamichi et al. (2009) of a VLP event at the Ontake volcano indicated a presence of gas flow–solid interaction in the hydrothermal system beneath the volcano. Maeda et al. (2015) also analyzed a VLP event that accompanied the 2014 eruption and revealed that a hydrothermal crack opened when gas ascended from a depth of 0.3–1 km to the surface immediately before the eruption. Thus, a pressurized reservoir may exist at some depth below the vent. When country rock overlying a gas reservoir with local equilibrium between gas and fluid (or water) is suddenly disrupted, pressurized material is rapidly discharged, as in the proposed mechanism of explosion caused by the interaction between hot lava and external water (e.g., Taniguchi 1996). The downward propagation of the expansion wave superheats the water and triggers its explosive vaporization. The country rock is then broken by the impact of the rapid release of the pressurized mixture of vapor and fragmented country rock, resulting in an intense explosion of the non-juvenile material. Numerous ballistic ejecta accompanied with PDCs probably originate from this vent-opening phase when the pressurized mixture is released (Fig. 12). Multiple PDCs (lobes) observed by eyewitnesses emerged and were deposited around the summit area during the initial phase (Figs. 2, 4), indicating that the initial plume was not buoyant enough and repeatedly partially collapsed in different directions. Eventually, the plume height increased and reached 10 km a.s.l. at 12:10 (Sato et al. 2015). The observations suggest that the main plume and/or co-PDC liftoff plumes became buoyant and continued to develop after the initial fountain collapse.
On mixing with air during vent development, the partial pressure of the vapor decreases and some of the water vaporizes. As air continues to be entrained, the temperature and density of the mixture can decrease as proposed for phreatomagmatic eruptions by Koyaguchi and Woods (1996). This process may be effective after the initial PDC phase and cause a plume development reaching 10 km a.s.l. (6–25 min in Fig. 12). As more cold air is added to the mixture by turbulence in the rising plume, the decrease in temperature begins to dominate the decrease in the partial pressure of the vapor. This leads to condensation of the vapor and the formation of aggregates of ash particles in the moist plume. Along with vigorous fallout of wet aggregates and lapillus from the spreading plume, ballistics is continuously ejected as the vent develops. Near the summit area, down currents from the partially collapsing column may also generate minor dilute PDCs. The vertical collapsing flow has relatively high particle concentration and high sedimentation rate, resulting in the formation of a massive poorly sorted deposit, which can be transformed into a lateral dilute traction–suspension current, as observed in large-scale laboratory experiments using cold pyroclastic materials (e.g., Sulpizio et al. 2014). Both sedimentation processes (the direct fallout from a spreading plume in the atmosphere and the down current from a partial column collapse) are plausible near the vent area, although it is difficult to distinguish these processes based only on the deposit data from the limited outcrops. This stage results in the formation of extremely poorly sorted deposits in the proximal area (Unit B). It is likely that this phase caused severe injuries to people and major damage to buildings around the summit area. The condensation effect was probably significant in the later phase of the eruption and in the distal area and led to the formation of wet aggregates (25 min in Fig. 12). Unit C corresponds to the declining stage that is characterized by the production of wet ash fall.
The effect of particle aggregation on the deposit characteristics
The grain-size distribution of the deposits reflects the transport process. Both the proximal and distal samples show populations of very fine ash particles with an 8 − φ peak (FP in Fig. 9), suggesting that the fine ash was transported as aggregates. The proximal deposits are generally massive and structureless, but are also characterized by ash accretion textures at some locations. Aggregate particles were also observed in distal tephra fallout with similar bulk grain-size characteristics to those of the accretionary lapilli from the Mount St. Helens eruption and hydrovolcanic fine ash deposits (Fig. 8, Hoblitt et al. 1981; Sheridan and Wohletz 1983). FP with an 8 − φ peak was also observed in a deposit from a low-temperature, dilute PDC from a phreatic eruption at Miyakejima in 2000 (Nakada et al. 2005). It is difficult to set constraints on the size distribution of the aggregate of the Ontake eruption; however, the apparent size distribution of the falling particles must be better sorted in a spreading plume. For the proximal deposit, the existence of FP also indicates the effect of aggregation, because the settling velocity of such very fine ash particles is too slow (orders of mm/s or less) to explain the duration of the deposition observed at the study site (Fig. 3).
Witness reports suggest that the depositional condition was relatively dry at the initial phase. Relatively dry conditions can give rise to dry aggregates such as loosely bound particle clusters, characterized by low densities and irregular morphologies (e.g., Sorem 1982). Moisture, electrostatic attraction, or mechanical interlocking may play a role in the formation of such dry aggregates (Carey and Sigurdsson 1982). With time, water may arise from the condensation of the water vapor directly onto the ash particles in the eruption plume, or from liquid drops ejected with the rock fragments. The growth of wet aggregates depends critically on the ability of the dynamics of these liquid bridges that dissipate the kinetic energy of particle collisions and promote the capture of finer particles (Iveson and Litster 1998). In the later phases of the Ontake eruption, the products changed to show a feature of wet deposition as exemplified by the mud rain. When water is present, the mixture becomes oversaturated and the aggregates collapse into structureless slurry or mud rain (e.g., Van Eaton et al. 2012) rather than form individual solid spherical particles such as accretionary lapilli. It is unlikely that accumulation of slurry generates distinct textures; however, the grain-size characteristic of the grains composing the aggregates may be reflected in the entire deposit characteristics as FP.
Sedimentation from PDCs near the summit
The source of the PDCs that spread west and northeast of the summit during the initial eruption phase was located 200–300 m above the vent area. The steep slope of the Jigokudani valley may have blocked the dense flow containing large particles (Fig. 12) and favored flow separation of the finer particles (e.g., Fisher 1990; Komorowski et al. 2013). Thus, the PDC deposits near the summit are thought to have been derived from finer particles transported by gravity-driven turbulent suspension currents. These currents may have been defected upward by the steep slope and propagated upward until they overflowed the valley rim, or were directly generated from a collapsing plume. The particles may settle directly from the turbulent suspension state with little or no traction, probably owing to their slow speed, forming an unstratified bed in the proximal area, as evidenced by the thin massive fine-grained facies of Unit A. The depositional process of Unit A is comparable to the direct fallout from the dilute PDCs (Branny and Kokelaar 2002; Surpizio and Dellino 2008), where particles are generally supported by fluid turbulence but their velocity is generally too low to create traction along the deposit surface. It is difficult to determine the exact duration of each PDC, but video footage that captured a PDC in Jigokudani and sequential photographs taken from Ninoike suggest that the initial phase lasted 3–6 min. At the summit area, the bottom layer (Unit A) is interpreted as a product from the body of the dilute PDCs. The thickness of Unit A around the summit area is 3–5 cm. Considering the duration, the sedimentation rate of the PDC that spread NE–NW is estimated to be ~1 cm per min in the summit area.
The grain-size distribution of the deposits has a few peaks, with the main component around 4φ (~60 μm) (Fig. 9); however, the falling particles may be larger because of aggregation, with a higher settling velocity. Carey and Sigurdsson (1982) studied the 1980 eruption of Mount St. Helens and found that all tephra particles <4φ in diameter fell as dry aggregates several hundred microns in diameter with a settling velocity of 0.35 m/s. Lane et al. (1993) demonstrated that the falling aggregates can be modeled as single particles using a reduced aggregate density dependent on the porosity, and deducing a relationship between the particle size and the settling velocity. Considering these studies, we estimate the size of a single particle or aggregate that would settle in dry conditions in the initial phase of the Ontake eruption as 2–4φ. Assuming sedimentation from a turbulent suspension current for a period Δt (s), the thickness of the deposit T (m) would be ρ p wC 0Δt/ρ s where ρ p is the density of the particle (2500 kg/m3), w is the particle settling velocity (m/s), C 0 is the volume fraction of the particles, and ρ s is the density of the dry deposit (~1000 kg/m3). The particle settling velocity can be determined from Lane et al. (1993). Using these parameters, the relationship between the sedimentation rate (s = T/Δt) and C 0 for each particle size can be correlated. As a result, C 0 is calculated as 2 × 10−4 for 2φ and 2 × 10−3 for 4φ, in which the aggregate porosity was assumed to be 0.4–0.8 (Lane et al. 1993). This result suggests that the volume fraction of the particles of the initial PDCs around the summit area was approximately 10−4–10−3.
Estimation of PDC parameters
The volume of the PDCs can also be constrained using mass flux and duration. For the case with duration of 360 s and a particle size of 2φ, the volume of the deposits (DRE) is estimated to be 7000, 3000, and 900 m3 for lobes 1, 2, and 3, respectively. If we use a particle size of 4φ, or a 1-min duration, the volumes decrease by 1/5. The results imply that the volume of the PDCs in the initial stage is of the order of 103–104 m3 (Table 1). The above estimation is based on the assumption of constant particle size inside the PDC; however, if the aggregation is more significant, the volume estimation will change because an increase in particle size owing to aggregation causes an increase in the settling velocity. This also causes a decrease in the particle concentration in the flow in the shorter duration. Therefore, to achieve the same runout distance, a higher initial discharge rate or higher particle concentration is required, resulting in a larger volume of deposit.
Origin of proximal deposit
The sizes of the particles transported in turbulent suspension depend on the speed of the current. We obtained the relationship between the speed of the turbulent PDC and the size of the particles in suspension using the turbulent boundary layer theory (Valentine 1987; Dellino et al. 2008). For lobe 3 with an initial velocity of 24–28 m/s, the particle sizes that can be transported by turbulent suspension are estimated to be less than ~1 mm. This is consistent with the fact that Unit A at locations (d, f, i) that are characterized by populations finer than 0φ (~500 μm) was formed by the initial PDCs. Larger clasts that are a few mm to cm in size are also occasionally contained in Unit A close to the vent area; however, it is unlikely that they were transported by PDCs as they cannot be sustained by the turbulence and settle rapidly. Such relatively larger particles would be transported mainly by fallout from the spreading plume. This also applies to particles deposited in the later stage. The deposit characteristics (the M d–σ φ plot in Fig. 8) support this idea; they are similar to those of the poorly sorted fallout deposits from phreatic eruptions at Bandai, Adatara, and Mount St. Helens; moreover, there is no solid evidence that larger-scale PDCs were produced in the later phase of the eruption. Although smaller PDCs may have occurred in the later stage, it is difficult to constrain the detailed process based only on data from the deposit.
Most of the deposits from the phreatic eruption at Ontake volcano on 27 September 2014 are characterized by massive, extremely poorly sorted, and multimodal grain-size distribution with a large fraction of silt- to clay-sized fine ash component. Based on the deposit facies observed in this study, we can divide the deposit into three major units (Units A, B, and C). Combining geological data with witness observations suggesting that the depositional condition was initially dry but eventually changed to wet, we conclude that Unit A originated from gravity-driven dilute PDCs in the relatively dry, vent-opening phase. Unit B was produced mainly by fallout from a vigorous moist plume during vent development. Unit C was formed by wet ash fall in the declining stage. As evidenced in the finest population of the grain-size distribution, aggregate particles were formed throughout the eruption, and the effect of the water in the plume on aggregation increased with time and distance.
The lithofacies and grain-size characteristics of the poorly sorted deposits observed in the proximal area are similar to those of mudflows or fallout tephra from past phreatic events. However, Unit A is certainly derived from PDCs. It is important to understand the similarity of the deposits when we interpret this type of poorly sorted deposit solely based on geological records. Particularly, care must be taken when reconstructing past eruption events and evaluating potential hazards relating to future phreatic eruptions. The Ontake eruption provided an important opportunity to study proximal deposits from a phreatic eruption that provides a complex eruption sequence and reflects the effect of water on the eruption dynamics.
Using geological records, witness observations, and a theoretical approach, the physical parameters of the eruption can be constrained. Based on the deposit thickness, duration, and grain-size data, the particle concentration and initial flow velocity for three PDC lobes in the initial phase were estimated to be 2 × 10−4–2 × 10−3 and 24–56 m/s, respectively, applying a scaling analysis using a depth-averaged model of turbulent gravity currents flowing down slopes. Further studies may enable to quantitatively evaluate the major factors that caused the many casualties and severe damage to buildings near the eruption source during the Ontake eruption.
FM analyzed samples and the data in the laboratory and wrote the first draft of the manuscript. TO, MY, JK, YI, YT, TS, SN, and FM carried out the field survey and discussed data in the field. MN analyzed the X-ray powder diffractometer data. SN and TK helped interpret the data and shape the manuscript. All the authors read and approved the manuscript.
The geological surveys around the summit area were carried out by the Joint Survey Team of the Coordinating Committee for Prediction of Volcanic Eruption, Japan. We thank the Japan Meteorological Agency, Kiso town and Otaki village, Nagano Prefecture, for permitting our field survey around the summit area. We also acknowledge S. Mukai, Y. Kuramoto, K. Yanagisawa, T. Kotani, R. Ishiyama, and Y. Kodera for their cooperation with our field survey team and for providing valuable information on their experiences during the eruption. T. Takemura and T. Kanamaru assisted the XRD analysis. Comments from R Sulpizio and an anonymous reviewer were helpful to improve the manuscript. This study was supported by Grant-in-Aid for scientific research (Nos. 2690002, 15K01246) from the Ministry of Education, Culture, Sports, Science and Technology, Japan.
The authors declare that they have no competing interests.
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