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  • Article
  • Open Access

The outline of the 2011 eruption at Shinmoe-dake (Kirishima), Japan

  • 1Email author,
  • 2,
  • 1,
  • 1 and
  • 1
Earth, Planets and Space201365:1

  • Received: 30 October 2012
  • Accepted: 31 March 2013
  • Published:


The climactic phase of the 2011 eruption at Shinmoe-dake was a mixture of subplinian and vulcanian eruptive events, successive lava accumulation (lava dome) within the crater, and repetition of vulcanian events after the dome growth. It was preceded by inflation and elevated seismicity for about one year and by phreatomagmatic explosions of one week before. Small pyroclastic flows and ash-cloud surges formed during the subplinian events, when the eruption column reached the highest level and the vent was widened. A lava dome, which was extruded close to the vent of subplinian events, grew by swelling upward and filling the crater. After the vent was covered by the lava, an intense vulcanian event occurred from the base of the dome and the swelled dome became deflated. After that, vulcanian events were repeated for three months. Simultaneous eruption styles in the crater (vulcanian events, continuous ash emission and dome growth) and some phreatomagmatic events in the vulcanian stage probably are due to a complex upper-conduit system developed in water-saturated country rock.

Key words

  • Subplinian event
  • vulcanian event
  • lava dome
  • phreatomagmatic event
  • phreatic event

1. Introduction

Plinian or subplinian eruptions sometimes happen after a dormant period as long as hundreds or thousands years. Forecasting them correctly from monitoring data is very critical to save lives of people living on and around the volcanoes. In order to minimize the risks from these eruptions, it is important to understand the precursory phenomena of these explosive eruptions and to illustrate the scenario of the eruption. However, the examples of detailed real-time observations of such eruptions are very few. Some happen suddenly, before monitoring is possible, or where the access to the volcano becomes dangerous. The eruption at Shinmoe-dake volcano, Kirishima, in Kyushu, Japan (Fig. 1), which began in January 2011, is a well-monitored example. This eruption took place about 300 years after the last magmatic eruption. The main phase is represented by subplinian/vulcanian events and successive lava accumulation, which was followed by repeated vulcanian events (Figs. 2 and 3). Subplinian eruptions may be transitional between vulcanian explosions and plinian eruptions in terms of magnitude and intensity (e.g., Cashman, 2004). The transition between two phenomena is common (Cioni et al., 2000; Morrissey and Mastin, 2000; Cashman and Mc-Connell, 2005). Therefore, it is expected that the eruption process of the 2011 eruption at Shinmoe-dake may give the valuable information to illustrate the transition between vul-canian and subplinian eruptions.
Fig. 1.
Fig. 1.

Location and shaded-relief map of the Kirishima volcano group. The shaded-relief map was produced by the Asia Air Survey Co. Ltd. (JMA, 2005).

Fig. 2.
Fig. 2.

Photographs showing explosive events at Shinmoe-dake Volcano (Kirishima) on 26 and 27 January 2011. A: Northwesterly view of rising eruption column of subplinian event. Snowcapped volcanic cone in the left, whose northern wall is collapsed, is Karakuni-dake, and the crater filled by water in front is Ohnami-ike. Taken by Kazuo Shimousuki at 17h14m, 26 January. B: Westerly view of the summit crater. Grooves on the western outer slope (front) are the vents of the 1959 eruption, aligned east-west and providing a good marker of the direction among the photographs. Explosion occurred southwestern part in the summit crater. Taken by K. Shimousuki at 17h17m, 26 January. C: Eruption column of the first vulcanian event, taken from about 3 km south of Shinmoe-dake by S. Nakada at 15h42m, 27 January. D: Northwesterly view of eruption column of the third subplinian event. Ash overflowed from the summit crater to the northeast. Taken from Karakuni-dake by T. Nagatomo at 17h07m, 27 January.

Fig. 3.
Fig. 3.

Photographs showing changes of the summit crater of Shinmoe-dake in 2011. A: Northeasterly view of steaming within the craters after the phreatomagmatic event on 19 January 2011. Dry gray ash of the event covers the southern rim. Irregular small holes on the right side of steaming on the crater wall are vents formed by phreatic events in 2008. Taken by JMA at 14h23m, 21 January. B: Northerly view after subplinian events. Continuous emission of fine ash occurred near the open explosion crater of subplinian events, and a small lava dome was found just behind the continuous ash emission. Taken from a light aircraft by S. Nakada at 10h19m, 28 January. C: About 50 m across lava dome was growing, pushing pyroclastic formations aside. Taken from the north by S. Nakada at 10h20m, 28 January. D: Southwesterly view of lava dome which almost filled the summit crater. Taken by T. Kobayashi around 13h44m, 31 January. E: Northwesterly view of lava accumulated in the summit crater. Lava ridges were almost covered by vulcanian event products. Taken by S. Nakada on 4 February. F: Northwesterly view of lava in the crater, partly altered by fumarolic activity. Grooves on the surface are the pits formed by repeating vulcanian events. A small vent in the southern margin of the crater (the deepest part in the photo), which is surrounded by reddish yellow ash deposits, appeared in continuous ash emission (phreatomagmatic event) in the end of February or early March. Taken by K. Shimousuki on 13 August 2011.

This paper outlines the chronology of the Shimmoe-dake eruption, especially the surface manifestations. Individual eruption phenomena are called “events” in this paper to avoid confusion with the eruption in 2011 as a whole. “Phreatomagmatic events” are used for long-lasting eruptive events which produced very fine ash having the grain size distribution clearly different from those of subplinian and vulcanian events, but similar to those of phreatic events (figure 13 of Suzuki et al., 2013a), and containing minor amounts of juvenile particles.

2. Background of Shinmoe-dake

Shinmoe-dake and Ohachi are the most active eruptive centers in the Kirishima volcano group, Southern Kyushu, Japan (Fig. 1). The volcanic activity of Kirishima started about 600 ka with caldera-forming eruptions, and changed to form stratovolcanoes with plinian, vulcanian, strombo-lian and phreatomagmatic eruptions about 330 ka (Imura, 1992; Nagaoka and Okuno, 2011). Migration of eruption centers during these 330 thousand years produced more than 25 stratocones and pyroclastic cones. Recent activity at Shinmoe-dake was characterized by phreatic explosions in 1822, 1959 and 1991 (Imura and Kobayashi, 1991; Tsutsui et al., 2005).

According to Imura and Kobayashi (1991), the main phase of the 1716–17 eruption had continued for about three months, including multiple subplinian and vulcanian events. It was preceded by a phreatic event 8 months before, and followed by the large subplinian event about 7 months after. During the subplinian events small-scale pyroclastic flows reached about 2 km from the crater. The total volume of the tephra is estimated about 0.07 km3 DRE (Imura and Kobayashi, 1991). Before the 2011 eruption, the bottom of the summit crater was covered by a lava flow convex downward with concentric steps on the surface (Figs. 3(A) and 4(A)). Endo and Kobayashi (2012, pp. 165–166) considered that the lava which once had pooled in the crater was drained back into the conduit. Since Tsutsui et al. (2005) concluded that the latest magmatic eruption at Shinmoe-dake occurred in 1716–1717, the lava at the crater bottom probably is the product of the 1716–17 eruption.
Fig. 4.
Fig. 4.

Maps showing the temporal change of the summit crater of Shinmoe-dake and the surrounding area. A: Before the 2011 eruption. The southern vents in the summit crater were used in the January 19 event. Distribution of vents including fissure vents of phreatic eruption in 1959 are after Geshi et al. (2010). B: On the morning of 28 January 2011. Within the crater, the open explosion vent (west side), the growing lava dome and the vent (east side) from which volcanic ash was continuously emitting. C: In the summer of 2012. The center of concentric pressure-ridges is emission point of lava, which locates near the center of the crater before the 2011 eruption. The surface of the lava dome, which grew during 28–31 January 2011, was broken by successive vulcanian events after 1 February 2011 and thickly covered by blocks and ash derived from the dome.

3. Monitoring and Observation at Shinmoe-dake

The volcanic activity of Shinmoe-dake has been monitored by Japan Meteorological Agency (JMA), Geospatial Information Authority of Japan (GIAJ), National Institute for Earth Science and Natural Disasters (NIED), national universities and the Kagoshima Prefecture. After the sub-plinian events at the end of January 2011, the monitoring network was strengthened by each organization. The summit of Shinmoe-dake was monitored with real-time cameras at Onami-ike, about 3 km west-northwest of Shimoe-dake by the Kagoshima Prefecture and at Inokoishi, about 8 km south-southwest of Shinmoe-dake by JMA. Those camera records were very helpful to understand the temporal changes in eruption condition, including the height of ash column, the location of eruption site and topography of the summit crater. The Doppler radars in Fukuoka and Tane-gashima JMA stations were also used to measure the eruption column height (Shimbori and Fukui, 2012). Satellite SAR images, especially JAXA EROC and terra SAR-X images, were very useful to understand what happened within the crater even in cloudy days and estimate the volume of lava accumulated within the crater (NIED, 2012).

Geological field survey was carried out several times since the afternoon of 27 January 2011. As of the summer 2012, the summit area was restricted to approach even for researchers and observation of deposits near or within the crater area was insufficient. This situation results in large uncertainty of estimation of tephra volume of this eruption. In order to watch the volcanic activity, air inspections were carried our many times with helicopters by JMA, being supported by Self Defense Force, Ministry of Land, Infrastructure and Transport, and Kagoshima Prefecture, and with airplanes hired by researchers.

4. Chronology of the 2011 Eruption

4.1 Phreatic stage and precursory phenomena

The chronology of the 2011 eruption is summarized in Table 1. The eruption was preceded by phreatic events which occurred on 22 August 2008 (Geshi et al., 2010) and were repeated during March to July 2010. The 2008 event occurred along a fissure in the western outer slope of the crater, the western rim and bottom of the crater (Fig. 4(A)). Vents on the western rim produced successive phreatic events during March–July 2010 (JMA, 2011).
Table 1.

Chronology of the 2011 eruption at Shinmoe-dake.

Phreatic Stage


22 Aug. 2008

Phreatic event

31 Mar., 17 Apr., 6 & 27 May, 27 & 28 Jun., 5 & 10 Jul. 2010

Phreatic events

Subplinian Stage


19 Jan. 2011

Phreatomagmatic event

26–27 Jan. 2011

Continuous activity including three subplinian events

27 Jan. 2011

Vulcanian even just prior to the third subplinian event

Lava-accumulation Stage


28–29 Jan. 2011

Continuous emission of fine ash (phreatomagmatic)

28–31 Jan. 2011

Continuous lava accumulation event in the crater

28 & 30 Jan. 2011

Vulcanian events during lava accumulation

Vulcanian Stage


1,2,3,4,6,7,9,10,11,14,18,24 &28Feb.,l Mar. 2011

Vulcanian events

7 to 9 Feb., 28 Feb. to 1 Mar., 3 to 4 Mar. 2011

Continuous ash emission events (phreatomagmatic)

8,13,23, & 29 Mar., 3 & 18 Apr. 2011

Vulcanian events

Phreatomagmatic Stage


16,23 & 29 Jun. to 1 Jul., 6 Aug., Aug. 31 to 6&7 Sep. 2011

Continuous ash emission events (phreatomagmatic)

Rapid inflation of the Kirishima volcano group before the main phase of the 2011 eruption was clearly detected in the GPS network by Geospatial Information Authority of Japan (Fig. 5, GIAJ, 2011, 2012). The three baselines of the triangle GPS network anchored at the Ebino (about 15 km N of Shimoe-dake), Makizono (about 13 km WSW) and Miyakonojo (about 10 km ENE) stations, surrounding Shinmoe-dake, had elongated by 2 to 4 cm with nearly constant rate since December 2010. The main source of inflation was determined at about 7 km northwest of Shimoe-dake with the depth of 6 to 10 km (GIAJ, 2012; NIED, 2012; Nakao et al., 2013).
Fig. 5.
Fig. 5.

Temporal variations in the GPS baseline length (Ebino-Makizono) and the monthly number of earthquakes around Shinmoe-dake. The Ebino GPS site is about 16 km N of Shinmoe-dake, and the Makizono site is about 14 km SW of Shinmoe-dake. The upper diagram is from the data of Geospatial Information Authority of Japan (GIAJ, 2012). In the lower diagram, the months when eruptive event(s) occurred are shown by triangles; gray and white triangles are for phreatic and magmatic events, respectively. Numbers of earthquakes are from JMA.

According to the JMA reports (JMA, 2011, 2012), seismic activity at Shinmoe-dake increased first at the time of the phreatic eruption event in August 2008 and second in the phreatic eruptive events during March–July 2010 (Fig. 5). After the phreatic events, the seismic activity declined but remained a higher level up to a few hundred events monthly.

4.2 Subplinian stage

Volcanic tremor was first recorded at 01h27m (JST), 19 January and continued from the 19 January afternoon to the morning of 23 January (JMA, 2012). During the volcanic tremor event, the phreatomagmatic eruption occurred and tephra of this event fell on the southeastern area of Shinmoe-dake on the morning of 19 January. The ash contained up to 10 vol% in volume fresh pumice fragments (Miyabuchi et al., 2013; Suzuki et al., 2013a). The majority of the ash is intensively to partly altered materials as same as the ash of the 2008 and 2010 phreatic events (Suzuki et al., 2013a). Juvenile material in the products of the 19 January 2011 event was very suggestive of approaching of the climactic event. Steaming from these vents had continued until the morning of 26 January. Vigorous steaming was observed at small vents on the crater bottom on 21 January (Figs. 3(A) and 4(A)).

Dark ash clouds began gushing after a small eruptive event at 07h31m, 26 January, and the activity increased around 14h49m, leading to the first subplinian event (JMA, 2012). A clear increase in seismicity started that morning. Subplinian events occurred three times from the afternoon of 26 January to the evening of 27 January (Fig. 5). The height of the eruption cloud was monitored by the real-time camera of JMA and the Doppler radar (Fig. 6). The maximum column heights were about 7 km above the crater and almost identical among three events. The column height increased with time and peaked in the latest stages of the first and second events. The third subplinian event occurred about 40 minutes after the first vulcanian event (Fig. 2(C)). The duration of the third subplinian event was shorter than the first two subplinian events and the column was high from the beginning. The photographs of the first event taken from an aircraft by K. Shimousuki (Figs. 2(A) and (B)) show that fountains of gas, ash and blocks collapsed from curling ash-cloud masses on the outer-slope and generated ash-cloud surges. The vent of this eruption was in the southwestern part of the crater (right front in Fig. 2(B)). The site is close to one of the small vents of the phreatic events before the 2011 eruption in the western crater wall (Figs. 4(A) and (B)).
Fig. 6.
Fig. 6.

Time sequence of subplinian events and height of the eruption column. The height changes estimated with Doppler radars and camera (Shimbori and Fukui, 2012) are shown in gray color and dashed line, respectively. The latter provides the minimum height. Layers of deposits corresponding to individual eruptive events are shown in the top.

During the subplinian events a small pyroclastic flow descended on the western slope. The deposit was first found from the aircraft in the morning of 28 January 2011 (Fig. 7); trees attacked by this flow were toppled down and burnt. It traveled up to about 1 km and its toe is about 70 m wide. The distribution confirmed by the photographs and the Google Earth image (taken on 11 March 2011), traces back to the western part of the crater rim. This suggests that pyroclasts and gas which became the pyroclastic density currents descended not from the lowest part (NW) of the crater rim but over the higher western rim. This pyro-clastic flow event occurred at 18h25m, 26 January, based on the camera record of JMA; the incandescence was observed in the lowermost western slope of Shinmoe-dake. Simultaneously, the camera record at Ohnami-ike showed the northward migration (or expansion) of the base of eruption column. Ichihara et al. (2013) showed the temporal changes in the amplitude ratio of seismic signals between two seismometers installed south and north of the crater, and proposed northward migration of vents as the ratio decreased in the latest periods of the first and second sub-plinian events. Rather, these facts seem to indicate the vent was widened in the latest stages of these subplinian events when the eruption columns were highest. In the first event, only a small pyroclastic flow was generated. Widening of vent allowed repeated collapse of the eruption column (Wilson et al., 1980). It is considered that the vent was filled by their own materials after individual subplinian events. During the third subplinian event, pyroclastic surges flowed onto the northeastern slope (Fig. 2(D)). As during the first subplinian event, pyroclastic density currents formed when the eruption column was highest and the base of eruption column expanded to the north (Fig. 6).
Fig. 7.
Fig. 7.

Pyroclastic flow deposits on the southwestern slope of Shin-moe-dake. A: Northerly view of the pyroclastic flow deposits. Trees in the deposits were smoking on the morning of 28 January 2011. B: Close-up view of the toe of the pyroclastic flow deposits (A), taken from the unmanned autonomous helicopter on 27 May 2011 (Kaneko et al., 2011).

4.3 Lava accumulation stage

Following the subplinian events, a lava dome appeared within the crater. This finally filled the lower half of the crater (Fig. 4(C)). The lava dome was first found from an aircraft on 28 January 2012 (Figs. 3(B), 3(C) and 4(B)), about 50 m across and located near the pyroclastic cone formed around the vent of the subplinian events. The incandescence of the dome was observed in the sun-shaded angle. The surface of the dome was black and irregular in morphology like a gigantic cauliflower (Fig. 3(C)). Beds of pyroclastic materials, a few meters thick around the base of the dome, had been torn and lifted by intruding lava.

The lava grew, forming concentric pressure-ridges and keeping the dome shape (Fig. 3(D)), and covered the most area of the crater floor by 31 January (Fig. 4(C)). Vigorous steaming from the top of the dome was visible in daytime and incandescence after dark. The top of the lava dome could be seen over the crater rim by the real-time camera at Ohnami-ike. The camera was set at the 1366 m in altitude, almost same altitude as the western crater rim of Shinmoe-dake. The dome height was roughly estimated as 1380 m in altitude on the noon of 31 January. However, the dome top became invisible from the camera after the vulca-nian event on the morning of 1 February. The height on 1 February was about 1350 m according to the SAR analysis (GIAJ, 2012). This means that the dome-shaped lava became deflated after the 1 February vulcanian event, losing about 30 m in height. The vent for final lava accumulation in the crater is represented by the center of concentric ridges (Fig. 4(C)). Widths of ridges are not homogenous. In the western marginal part of the lava, the ridges are widest, implying faster motion of the lava there in the early stage of dome growth. Since the western part was the vent of the subplinian events (Fig. 4(B)), it is likely that lava flowed into and filled the vent.

Continuous and vigorous emission of fine ash, which was drifted to the east, was observed on the morning of 28 January (Figs. 3(B), and (C); phreatomagmatic event in Table 1). The ash contained juvenile scoria and pumice up to 20% (Suzuki et al., 2013a). The ash emission vent was located in the center of the crater adjacent to the growing lava dome, where a pond occupied before the eruption (Figs. 4(A) and (B)). This emission continued until the night of 29 January, probably when the vent was covered by growing lava.

Volcanic tremor event started on the morning of 26 January and ended on the afternoon of 7 February (JMA, 2012). The extensometer observation clearly recorded the strain change resulting from magma discharging in this eruption (Ishihara and Teraishi, 2011) and slow strain even after 31 January until 10 February 2011. These facts suggest that the magma leaking continued at a low rate into early February. The inflation of the volcano stopped abruptly with the sub-plinian event on 26 January. About 2/3 of the inflation was canceled by the deflation during 26–31 January. The deflation source was similar to that of the inflation source (GIAJ, 2012; NIED, 2012; Nakao et al., 2013). Soon after the effusion of lava (February 2011), the elongation of the three baselines resumed, suggestive of re-inflation of the magma chamber. The rate of the latter inflation was similar to that from December 2010 to just before the subplinian events, it then slowed and stopped in early 2012.

4.4 Vulcanian stage

Vulcanian events occurred first at 15h41m of 27 January, at 12h47m of 28 January and 13h57m of 30 January (JMA, 2012). By the first vulcanian event, hot pumice fragments, up to 15 cm across, and smaller lithic fragments fell about 2.9 km southeast of the crater (Fig. 3(C)). The latter two events occurred in the vent of the subplinian events during the lava dome growth in the crater. As they produced much smaller intensity shock waves than the event of 1 February (JMA, 2012), we infer that the vent had not yet been covered completely by the lava by the noon of 30 January. The event at 07h54m of 1 February 2011 was so violent that ballistic blocks with the weight of 1–2 t reached about 3.4 km west of the crater (Maeno et al., 2013). The camera record showed that the eruption cloud of this event projected westward and eastward. The aerial inspection on 4 February confirmed that the western and eastern walls of the crater were covered thickly by black colored deposits of fresh lava blocks and fragments (Fig. 4(D)). These facts suggest that the explosion occurred from the base of the lava, like a sudden escape of gas from margins of cooking pan cover. Sealing the subplinian vent by lava prohibited degassing from magma and resulted in the vulcanian event that day.

The black pressure-ridged surface of the lava was completely covered with eruption products of repeated vulca-nian events, like a sand pool (Figs. 3(E-F)). The vulcanian events created many small pits aligned concentrically, likely along the pressure-ridges (Fig. 3(F)). As mentioned above, the magma discharge had declined since 1 February and almost stopped after 10 February. Therefore, the pressur-ization needed for the vulcanian outbursts may have been mainly due to crystallization of the lava accumulated within the crater. However, the ash of the vulcanian events during February to April 2011 contains particles of pumice and scoria as much as 15%, which were depleted in microlites (Suzuki et al., 2013a). This may suggest that continuous degassing in the upper part of the conduit also contributed to the pressurization.

Vulcanian events occurred in March–April 2011, decreasing in frequency with time. The event with the highest eruption column (6 km above the crater; JMA, 2012) was observed on 13 March 2011. Some events in this stage were prolonged and emitted fine ash for more than several hours (Table 1). The SAR images showed that the open vent in the southern part of the crater, which was steaming vigorously during the aerial inspections in February 2011 (Fig. 4(B)), enlarged between the end of February and the beginning of March 2011 (NIED, 2012). Repeated eruptive events may have widened this southern vent. The vulcanian stage was followed two months later by phreatomagmatic events in June 2011 and from August to September 2011.

Tephra of phreatomagmatic events in June to September consists of particles finer than those of vulcanian events (Suzuki et al., 2013a). Fine particles of fresh lava occur together with recycled vulcanian products, which are lus-terless, partly altered and oxidized. The dispersion and fragmentation index falls near the Surtseyan-field in the Walker diagram (Miyabuchi et al., 2013). After 10 September 2011, no further eruptive activity occurred.

5. Crisis Management

JMA raised the volcanic alert level (Kato and Yamasato, 2013) from 2 to 3 at 18h of 26 January 2011 and access was restricted within 2 km from the crater center. After due consultation with local municipalities, the limit area was expanded under the same alert level from 2 to 3 km on 31 January when the lava dome filled the crater, and from 3 to 4 km on 1 February when ballistic blocks fell 3.2 km from the crater center. The SAR images taken at 22h36m, 29 January, and 10h39m, 30 January (GIAJ, 2012), showed continuous growth of the lava dome in the crater. This information was forwarded to the Takaharu Town, Miyazaki Prefecture, through JMA. The Takaharu Town is just 2 km east of Shiinmoe-dake (Fig. 1) and within the pyroclastic-flow hazard area of the hazard map, which was published by the local governments in 2009 and distributed to local people.

Based on the information of dome growth, the town officials decided by themselves to recommend evacuation of about 1100 people living in the area close to the volcano at the night of 30 January, because of the danger of pyro-clastic flow. However, the dome growth rate was very high and there was a high risk of intense vulcanian event due to insufficient degassing. The evacuation recommendation was canceled on 5 February, except for the area closest to Shinmoe-dake. The limit area was reduced to 2 km from the crater center by June 2012.

6. Eruption Products

6.1 Tephra

Tephra of this eruption was widely distributed to the southeast of Shinmoe-dake (Fig. 8; Maeno et al., in review). Although the exact thickness near the crater is unknown when this paper is written, rough estimation was possible by abundant photographs taken from the air and by a quick survey on the southern rim in the 2012 summer as illustrated in Fig. 9. Maeno et al. (in review) estimated the eruption column heights for these events as 7.6–9.8 km in altitude (6.2–8.4 km above the crater), based on the distribution of tephra and maximum pumice fragments. The numbers are close to the Doppler radar measurement (Fig. 6).
Fig. 8.
Fig. 8.

Isomass maps of tephra from the eruptive events around Shinmoe-dake in 2011 (modified from Maeno et al., in review). Small crosses are the inspection sites.

Fig. 9.
Fig. 9.

Representative outcrops of tephra of the 2011 eruption. A: about 3 km SE of the Shinmoe-dake. B: about 2 km S of Shinmoe-dake, on the southern slope of Nakadake. C: about 500 m from the crater rim, on the southern slope of Shinmoe-dake.

Fig. 10.
Fig. 10.

The whole-rock chemical composition of pumice and lava fragments of the 2011 eruption at Shinmoe-dake. Pumice lumps with different SiO2 contents were erupted in the subplinian events. The data are after Suzuki et al. (2013b).

Deposits of three subplinian events, continuous ash emission, and in the vulcanian stage can be easily distinguished in outcrops (Fig. 9). Layer 1 is a light yellow, thin layer covering the soil, and formed mainly from phreatomagmatic events of January 19 and the morning of January 26. Layer 2 consists mainly of pumice lapilli and lithic ash which become coarser upward, and is from the early part of sub-plinian event from 14h, 26 January. Layer 3 consists mainly of coarsest pumice fragments. Many leaves and stems of trees are observed near the boundary between the layers of 2 and 3, implying that leaves and shrubs fell due to falling of coarse pumice fragments. Layer 4 is of pumice lapilli smaller than in Layer 3, showing upward coarsening. Near the crater, a layer of lithic-rich dark gray ash is the boundary between layers 3 and 4 (layer 3/4 in Fig. 9(C)), and was deposited during a calm period between two subplinian events. Near the crater (Fig. 9(C)), an agglutinate layer thicker than a few tens of cm correlates with the uppermost part of layer 3, and the uppermost part of layer 4 is also found as agglutinate as thick as 30 cm.

Correlation of layers 2, 3 and 4 with the eruptive events is still uncertain (Fig. 6). Layer 4 is overlain by layer 4/5, a thin black layer of lithic-rich ash that was confirmed in the afternoon of 27 January, 2.9 km S of Shinmoe-dake. Layer 5 is the deposit, lighter in color, from the vulcanian event at 15h41m, 27 January and the end of the third subplinian event. This also shows upward coarsening. The topmost part of the layer 5 contains large pumice fragments with tree stems and leaves. Layer 6 is a thin layer of purple to dark gray fine ash during 28–29 January. Layer 7 consists of medium to coarse lapilli of glassy lava, gray to light brownish gray, which is the product of vulcanian events repeated from 1 February. The majority of the layer 7 is the product of the 13 May event.

Layer 6 inhibited infiltration of rainwater, so that the area covered by this layer had the risk of lahar when heavy rain fell. Fortunately no large lahar formed during the eruption (Shimizu et al., 2011).

6.2 Chemistry

The erupted magma ranges from andesite to silicic an-desite in chemical composition (Fig. 9). White-colored, and gray-colored pumices were issued simultaneously during the subplinian events. Mingling of both magmas in a single pumice lump is also found. The lava that accumulated in the crater is andesite with the composition of gray pumice. Therefore, mixing of magma with different compositions is suggested by Suzuki et al. (2013b) and Miyabuchi et al. (2013). The pumice and lava are plagioclase-phyric with lesser olivine, orthopyroxene, clinopyroxene and Fe-Ti oxides. Suzuki et al. (2013b) estimated that the endmembers of mixing were phyric silicic andesite magma at 870°C and aphyric basaltic andesite magma at 1030°C. They also proposed storage depths of these magmas before mixing at 5 and 10 km, respectively.

7. Volume of Erupted Magma

The lava dome started growing on the morning of 28 January and almost stopped by 31 January though it continued to grow slowly for another week as written above. The volume of lava accumulated at the crater was estimated as 14–18×106 m3 by using the oblique photographs and the SAR images taken on 31 January and 1 February, respectively (Sasaki et al., 2011; GIAJ, 2012; Kozono et al., 2013). The magma discharge rate was about 41−52 m3/s (1.0−1.3×105 kg/s), assuming the density of 2,500 kg/m3.

The mass of tephra erupted during the afternoon of 26 January and the early morning of 27 January is about 1.4− 2.5 × 107t (Maeno et al., 2013); that of tephra in the afternoon of 27 January, including the products of the first vul-canian and third subplinian events, is about 2.4−4.8×106 t. Fine ash continuously emitted in 28 and 29 January is about 1.2×106 t. The total mass of the tephra erupted during 26–29 January is 1.8−3.1 × 107 t (0.7−1.2 × 107 m3 in DRE). This estimated volume is a little smaller than the volume of magma calculated with the tilt changes by Kozono et al. (2013); 1.6 × 107 m3 DRE. They estimated the magma volume for tephra by partitioning tilt changes between sub-plinian events and lava accumulation into the volumes of tephra and the lava (1.5 × 107 m3). The volume of lava by SAR analysis (Kozono et al., 2013) includes new tephra beneath the lava. The thickness of tephra under the lava is considered to be a few tens of m. The additional difference may come from assumption of identical compressibility of magma at the source between the subplinian events and lava accumulation.

The total amount of magma erupted in the 2011 eruption is 2.1−2.7×107 m3 DRE (tephra of 0.7−1.2×107 m3 +lava of 1.5 × 107 m3). This is a low-end VEI 3 eruption.

8. Discussion

8.1 Comparison with the 1716–17 eruption

The tephra volume of the 1716–17 eruption is calculated as about 7 × 107 m3 DRE based on Imura and Kobayashi (1991) and is about 7 times larger than that of the 2011 eruption (0.7−1.2 × 107 m3). The 1716−17 eruption was more explosive than the 2011 eruption, and at least 5 subplinian events occurred being associated with pyroclastic flows of the scale larger than in 2011. The sequence of the 2011 eruption was simpler than that of the 1716–17 eruption.

Before 2011, the crater floor was covered by lava which seems to be the remnant of the lava drained back into the conduit (Endo and Kobayashi, 2012, pp. 165–166). This lava is considered to be the final product of the 1716–17 eruption. Similar lava drain-back may have occurred even in the 2011 eruption. However, the lava remained at least when the paper was written (March 2013). The lava viscosity may have become too high due to cooling to drain back into the conduit.

8.2 Transition from subplinian, vulcanian and dome growth

The first vulcanian event occurred after the second sub-plinian event. Repetition of subplinian and vulcanian are reported in several volcanoes; for example, the 1980 summer eruption at Mount St. Helens (Cashman and McConnell, 2005), and the transition is common in the waning stage (Morrissey and Mastin, 2000). Probably accumulation magma pressure for about 8 hours after the second sub-plinian event caused fragmentation of solidified magma in the upper part of the conduit, which had behaved as a cap rock for the underlying molten magma. The products of the first vulcanian event contain particles of pumice and fresh lava fragment (Suzuki et al., 2013a). Some of large pumice fragments of this event are polygonal and variable in vesicularity, probably implying that the magma was partly quenched under the ground and fragmented by the vulcanian event.

The magma discharge rates were 0.6−1.4×106 kg/s (240− 560 m3/s) for the first and second subplinian events and 0.2–1.1 × 106 kg/s (80–440 m3/s) for the first vulcanian and the third subplinian event (Maeno et al., in review). The rate for lava accumulation was one order of magnitude lower (1.0−1.3 × 105 kg/s or 41–52 m3/s), but as high as the rate that elsewhere has led to subplinian and vulcanian eruptions (Cashman, 2004). The reason that rapid dome growth continued without transition to more explosive eruption is probably that degassing from the underlying magma was effective through the vents of the subplinian events and fine-ash emission events. However, the second and third vulcanian events which occurred during the dome growth may have reflected insufficient degassing.

8.3 Interaction with water

Emission of fine ash on 28–29 January was a phreatomagmatic event. Fresh glassy particles dominate the ash, and the dispersion-fragmentation index of this tephra falls in the Surtseyan field of the Walker’s (1973) diagram (Miyabuchi et al., 2013). In addition, vigorous steaming in the southern part of the crater had continued since 28 January (Figs. 3 and 4). These facts suggest involvement of groundwater during the 2011 eruption. The mag-netotelluric experiment showed a low resistivity layer is extensively distributed at the depth of a few hundred meters under Shinmoe-dake, which can be interpreted as a water-saturated porous layer (Kagiyama et al., 1996). Under such the circumstance, the ascending magma likely interacts with groundwater. Coexistence of multiple vents within the crater for subplinian and vulcanian events during 26–30 January, the lava dome, continuous ash emission and vigorous steaming (Fig. 4(B)) imply a complex system in the upper part of the conduit. The reason that the magma which formed the lava dome did not ascend into the sub-plinian vent may be that it could ascend only where ground-water was not present.

9. Conclusions

Precursory phenomena of the 2011 eruption at Shinmoe-dake were inflation and seismicity since the end of 2009 and repeated phreatic eruption since 2008. Juvenile material in the ash of 19 January foreshadowed the fully magmatic stage which began on 26 January.

The first two subplinian events were relatively long but included periods with a low eruption column, and each event ended with the highest eruption column. Duration of the third subplinian event was short and preceded by the first vulcanian event. When the eruption column was highest, the crater was widened to the north and ash clouds flowed outside the crater. A lava dome appeared close to the vent of subplinian events within the crater, growing at a high effusion rate. During the dome growth, vulcanian events occurred at the subplinian vent. Degassing occurred effectively without destruction of the growing dome. The lava dome grew, swelling and extending for four days, and covered the subplinian vent. When an intense vulcanian event occurred on 1 February, the lava dome was deflated, and the vulcanian stage started. The eruption ended with phreatomagmatic events during June–September.

The total amount of magma erupted in the 2011 eruption is 2.1–2.7 × 107 m3 DRE. The magma discharge to the surface had almost finished on 1 February and continued at the low rate in early February 2011. Although re-inflation suggested magma re-supply after February, it had stopped in the end of 2011. The 2011 eruption was much smaller in scale than the 1716–17 eruption. The sequences are also different; the latter includes repetition of larger subplinian events and draining-back of the lava accumulated in the crater.




We would like to Kazuo Shimousuki, Take-haru Nagatomo, Tetsuo Kobayashi, and Japan Meteorological Agency for providing us photographs used in this paper. Field survey was supported by Yasuo Miyabuchi, Tetsuo Kobayashi, Nat-sumi Hokanishi, and the General Observation Team organized under the National Coordination Committee for Volcanic Eruption Prediction. The software to view continuous seismic waves and video-images simultaneously, WAVE VS IMAGE, developed by Mie Ichihara was very effective in this study. This research was supported by MEXT KAKENHI Grant No. 22900001 (SN). We thank Chris Newhall and Hiroshi Shinohara for careful reading of our manuscript and for giving useful comments.

Authors’ Affiliations

Earthquake Research Institute, The University of Tokyo, 1-1-1 Yayoi, Bunkyo-ku, Tokyo 113-0032, Japan
National Research Institute for Earth Science and Disaster Prevention, Ten’nodai 3-1, Tsukuba, Ibaraki 305-0006, Japan


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