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Pyroclastic Density Current Hazards at the Baekdusan Volcano, Korea: Analyses of Several Scenarios from a Small-Case to the Worst-Case Colossal Eruption

Written By

Angelo Paone and Sung-Hyo Yun

Submitted: November 24th, 2015 Reviewed: February 2nd, 2016 Published: September 21st, 2016

DOI: 10.5772/62340

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The Baekdusan volcano was formed through three stages of activity: (a) a basalt shield (aging between 22.6 and 1.48 Ma), (b) a trachytic comendite stratocone (aging between 1.19 and 0.02 Ma), (c) a trachyte-comendite ignimbrite deposits (aging from 20 ka till date). Volcanic seismicity, ground deformation, and volcanic gas geochemistry yield new evidence for magmatic unrest of the volcano between 2002 and 2006. The monitoring data suggest that Mt. Baekdusan is a potentially active volcano and that its close monitoring is needed. One of the possible volcanic hazards from this volcano is the pyroclastic density currents. In order to evaluate the small-scale pyroclastic flow emplacement scenario of the 1903 AD eruption, Titan2d mass-flow model is used. The 1668–1702 AD and the Millennium eruption are characterized by 4–5 and ~7 VEI, respectively. The Millennium eruption can be considered as the last colossal super-eruption like Tambora, and so Baekdusan volcano could have even a global effect. The parameters used are as follows: volume (5–10 × 107, 1 × 109, 2 × 1010 m3), the vents of the 1903, 1668–1702, and Millennium eruptions; the pyroclastic flow runout calculated in the field are small (3,000 m :1903 eruption), intermediate (5,000 m :1668–1702 eruptions), and large (7–80,000 m, Millennium eruption). The initial velocities (m/s) range from 50 (1903 eruption) to as high as 300 (Millennium eruption). The input parameters have constructed three scenarios (1903, 1668–1702, and Millennium eruptions) following the recent volcanic history of Baekdusan volcano. These eruptions embrace all the possibly explosive eruptive scenarios that can occur at Baekdusan volcano in the future. The 1903 type scenario has been performed; according to the vent location, the flow moves in diverse directions (NE, SE) with a thickness of 3 m, and if the vent is the center of the caldera the flow fills the caldera with a thickness of 5 m. The emplacement of the 1668–1702 AD scenarios will involve at least two populated cities nearest to Baekdusan volcano. The scenario of the Millennium eruption will be much more severe and it will hit all the cities and towns within a range of 80 km. The impact will be from regional to global. This, however, is an underestimation of the runout for the diluted pyroclastic density currents.


  • Baekdusan volcano
  • pyroclastic density currents
  • hazard
  • eruptive scenario
  • super-eruption
  • Titan2d

1. Introduction

When active volcanoes are located in strategic and controversial territory with a history of political and military conflicts [1, 2], their studies and the better understanding of how those volcanoes work are much more difficult, especially when the earth scientists have to deal with mitigation measures to protect the population living around [36]. This is surely the case of an active volcano known by a few until 15 years ago, situated between the China and North Korea borders, called by different names by the countries that surround it. The name of the volcanic field surrounding Tianchi(=Cheonji) caldera lake is 长白頭山 in Chinese characters which means “White Head Mountain” These characters are Romanized as Baegdu-san, Baekdu-san, or Paektu-san in Korea, Hakuto-san in Japan, and Changbaishan(長白山) in China [7, and references therein]. From now on, we will use the Korean name, Baekdusan, to avoid confusion. Baekdusan volcano has recently become of greater interest to volcanologists after the sign of unrest during the period 2002–2009, with several volcanic precursors such as volcanic earthquake, surface inflation, specific volcanic gas emission, higher temperatures of hot springs [810], which have prompted the Eastern Asian Volcanological Community to pay major attention to this volcano by establishing a Volcanological Observatory (the Chinese Tianchi Volcanological Observatory has collected data since 1999 [11]) and by setting up an improved monitoring network around the volcano [12, 13]. Since 2012, the South Korean scientists have also taken steps in this direction, and the National Emergency Management Agency of Korea (Ministry of Public Safety and Security of Korea) has sponsored a vast research project on Baekdusan volcano (NEMA-BAEKDUSAN-2012-1-2), granted from the Volcanic Disaster Preparedness Centre (MPSS-NH-2015-81), and through the Natural Hazard Mitigation Research Group. Under the auspices of these groups, we analyzed the hazards from pyroclastic density currents and their impact on the population and infrastructures around Baekdusan volcano [14]. Further, we present arguments as to why this volcano has many characteristics as a potential site for the development of the conditions that can cause a super-eruption. Thus, we must also consider this extreme event if we do have to prepare for the next eruption, as it would have a global impact [15].


2. Regional tectonic of Baekdusan volcano and an outline of the plumbing system

Figure 1.

Regional setting of Baekdusan (Tianchi) volcano. Symbols mean the following. ○ Densely populated city or town: (a) Erdaobaihe; (b) Songjianghe; (c) Changbai; (d) Hyesan; (e) Baishan; (f) Fusong; (g) Lushuihe; (h) Yanji, and (i) Tumen. ° Populated village. ∆ Mountain tops with the elevation asl.Baekdusan (Tianchi) volcano. Capital letters indicate places referred to in text: T, Baekdusan (Tianchi) volcano; W, Wangtiane volcano; B, Bukpotaesan volcano; Z, Zhenfengshan volcano; SH, Songhua River; YL, Yalu(Aprok) River; and TM, Tumen (Duman) River.

Figure 2.

A.Regional tomography from the surface down to 1,300 km depth along a cross-section line shown on the inset map. The velocity perturbation scale is shown below the cross section. White dots denote earthquakes. The two dashed lines show the 410 and 670 km discontinuities. The red and black triangles show the active volcanoes. The surface topography along the profile is shown at the top of the tomographic image. The blue lines on the inset map denote the major plate boundaries (modified from [17]).B. A sketch showing the main features of the upper-mantle structure around Baekdusan volcano in East Asia, emphasizing the possible relationship between the intraplate volcanism and deep earthquakes in the Pacific slab [17], DXAL, Daxing-Anling (modified from [17]).

Figure 3.

Siping–Changbaishan–Japan seismic profile of the structure of Changbaishan area [24].

Baekdusan volcano is an intraplate stratovolcano included in the larger Changbaishain area, where we can list a series of intraplate volcanoes (Wangtiane volcano, Bukpotaesan volcano, Zhenfengshan volcano, [7], Figure 1). Cenozoic intraplate basalts are widely distributed around the Changbaishan volcanic area. Beneath the Baekdusan volcano, a prominent low-velocity anomaly with a plume-like shape has been imaged in the upper mantle by P-wave tomography [16, 17]. This suggests an upwelling of hot and wet material from the mantle transition zone (410–670 km [18]), where a stagnant subducted Pacific slab produces fluids and deep earthquakes through faults preserved in the stagnant slab. Hence, fluids and magmas may be supplied to the upper mantle under Baekdusan volcano, unlike beneath other volcanic and nonvolcanic areas in NE Asia, because large deep earthquakes occur frequently in the vicinity (a distance of about 200 km) of the Baekdusan volcano. At least some of these earthquakes are caused by the reactivation of faults which were produced within the plate, even after plate subduction. Further, the fluids could be released to the overlying mantle wedge from the preserved faults in the slab when large deep earthquakes occur. As a result, the Baekdusan volcano has to be considered much more active and prominent than other intraplate volcanoes in NE Asia [9, 10], because more magmas are produced from the fluids released from the slab by the deep earthquakes [19]. Further, Kuritani et al. [20] use the trace element and Pb isotope data to demonstrate the intense hydration of the big mantle wedge beneath the Baekdusan volcano, through two different dehydration events of an ancient stagnant slab (~1.5 Gyr) and the most recent subducted Pacific slab (Figure 2A and B show the most recent setting). The wet mantle wedge is likely to result in more frequent rise of diapiric wet melts, as shown from the tomography [17, references therein], and develop a deep hot zone intruded by mafic sills repeatedly at the MOHO depth or/and scattered in the lower crust [21, and references therein]. Enrichment in fluid-mobile elements (e.g. Cs, Ba, K, Sr, U, Pb), a lack of enrichment in nonfluid-mobile elements (e.g. Nb, Ta, Ti, etc), together with specific isotopic signatures (e.g. 87Sr/86Sr, 206Pb/204Pb) in island-arc basalt or subduction- related magmatism are interpreted as a result of metasomatism of the magma source by slab-derived fluids or melts. Their detailed investigation has helped to establish the current, rather empirical, model of slab dehydration and subduction-related melting processes. But, according to petrochemical characteristics and magma genesis of Holocene volcanic rocks at Mt. Baekdusan [22], trace elements from the Baekdusan volcano do not indicate significant contributions from a subduction slab of the Pacific plate. Volcanic activity in Mt. Baekdusan summit during Holocene resulted from intraplate magmatism [after 23, 24], caused by upwelling of asthenospheric mantle under extensional tectonic conditions (Figure 3 [24]). Hot zone melts are H2O-rich as in Baekdusan volcano (e.g., Millennium eruption [25]). Consequently, they have low viscosity and density, and can readily detach from their source and ascend rapidly. Crystallization begins only when the ascending magma intersects its H2O-saturated liquidus at shallow depths. Decompression and degassing are the driving forces behind crystallization, which take place at shallow depths on timescales of decades or less. Degassing and crystallization at shallow depths lead to large increases in viscosity and stalling of the magma to form volcano-feeding magma chambers [26, 27]. The above model is well confirmed from the study of Wei [24] at the Baekdusan volcano. The heating of the deep crust was inefficient in early times, because much of the basalts erupted out directly, and much of the heat from magma was not used to heat the wall rocks. Annan and Sparks [27] state that there is an initial incubation period in which the basalt intrusions solidify. Generation of silicic melts initiates when the solidus temperature of either the basalt magma or the surrounding crust is reached. At an intrusion rate of 50 m per 10,000 years, incubation periods in the range 105–106 years are estimated, consistent with geochronology and stratigraphy at Baekdusan volcano, with its evolution from mafic to silicic volcanism (the stratigraphy and geochronology will be treated in the next section). Once a zone of residual partial melt develops in the deep hot zone and starts to prevent the basalt from eruption, the temperature rises more efficiently, and the production of residual melt is accelerated. Large amounts of evolved residual silicic melt have been formed in the last 10,000 years and then intruded into the upper crust to form magma chambers large enough to result in the caldera-forming explosive eruptions. The repose time between eruptions of size similar to the Millennium eruption was about thousands of years, one order greater than less-explosive parasitic eruptions of hundreds of years [7].


3. Summary of stratigraphy and geochronology of Baekdusan volcano

The volcanic activity at the Baekdusan volcano goes back as far as nearly 25 Ma B.P [7, 28, 29]. Wei et al. [7] describe the volcanic activity in three stages: early shield-forming; middle cone-construction; and late ignimbrite-forming eruptions. The volcanic rocks were alkaline and tholeiitic basalts during the shield stage, trachyte and comendite lavas, and their pyroclastic equivalents during the cone-construction stage, and mostly comenditic pyroclastic rocks in the final stage (Table 1, Figure 4). However, Yang et al. [30] affirm on the basis of a large amount of age and stratigraphic data (40Ar/39Ar, U-series disequilibria) that Baekdusan volcano has been more active in the last 20 ka (~19, 16, 11 ka) than that was previously thought. From historical records, several authors [31, 32] affirm the high frequency of eruptive events, and since the Millennium eruption, more than 31 eruptive events have been documented, most of which are the Plinian eruptions with volcanic ash that dispersed into the regions in the vicinity of the volcano. Many authors concord that the last explosive eruptions are in chronological order, 1668 AD (Figure 5), 1702 AD (Figure 6), and 1903 AD (Figure 7) [3234]. In Figure 4 is shown the Baekdusan volcano’s geological map with all the terrains outcropping (see the legend of Figure 4 for more major details). The shield-forming stage lasted from the Miocene into the early Pleistocene. Alkali olivine and tholeiite basalt form the main part of a shield-like lava plateau that covers an area of 7,200 km2 centered at Cheonji. In addition to the eruptions from central vents, there also were fissure eruptions, as evidenced by feeder dikes along the headwaters of the Tumen (Duman) and Heishihe Rivers. The youngest shield basalts are located near Cheonji cone and are overlain by the alkaline trachytes of the cone, except in the northwestern part of the shield. The shield basalts are ∼150 m thick near the Baishan Forestry Center in the headwaters of the Yalu River (Aprok River). The cone-construction stage lasted from ∼1.0 Ma to perhaps as young as ∼20 ka. The latter is about the age of the youngest trachyte lava on the caldera rim near Tianwenfeng (K–Ar, 19 ± 5 ka) and one of the youngest comendite lavas, Qixiangzhan, which was dated recently at 17 ± 1 ka. This stage was characterized by eruption of trachyte and comendite lavas and pyroclastic rocks, and dominated by trachyte lava effusion from the center of Cheonji volcano. The cone-construction stage has been subdivided into four stratigraphic formations for the main cone and the Laofangzixiaoshan part of the shield (Table 1). In general, outcrops of lava decrease image with elevation on the cone. In plane view, the eastern sector of the cone consists of younger trachytes, whereas older lavas are distributed more widely. However, all the rocks share similar geochemical compositions and appear to be genetically related. The young Laohudong basalts are sparsely distributed as monogenetic vents around the caldera. Its largest and most explosive Plinian eruption occurred around 946–947 AD and is known as the “Millennium eruption.”

StagesFormation and ageLithologies
Liuhaojiie Tuff Ring (1903 AD)Comendite phreatomagmatic eruption
Late:Wuhaojie (1702 AD)White gray comentite fine glass
Igninbrite-Baguamiao (1668 AD)Dark gray trachyte ignimbrite and pumice
White gray comentite ignimbrite and
Millennium eruption (~936–1200 AD)Air fall pumice with minor trachyte
Ignimbrite and air fall pumice
Qixiangzhan (17 ka)Comentite lava and pyroclasts
Middle: ConeBaitoushan III (0.02–0.22 Ma)Trachyte and comendite lava
constructionBaitoushan II (0.25–0.44 Ma)Trachyte with Laohudong basalt
Baitoushan I (0.53–0.61 Ma)Trachyte
Laofangzixiaoshan (0.75–1.17 Ma)Basalt
Xiaobaishan (0.75–1.17 Ma)Trachyandesite and trachyte
Baishan (1.48–1.66 Ma)Basalt
Early: Shield-Toudao (2.35–5.02 Ma)Basalt
formingNaitoushan (15.6–22.6 Ma)Basanite, Basalt

Table 1.

Baekdusan volcano stratigraphy and petrography of the volcanic products simplified after Wei et al. [7, 28, 29].

Figure 4.

Geological map of the summit area of Baekdusan volcano. Northeast distribution of the basaltic shield, trachytic composite cone, and the comenditic ignimbrite sheet of the Baekdusan volcano. 1, Torrent deposit, the fourth debris flow (1994); 2, The third fan-shaped debris flow; 3, 1903 phreatomagmatic eruption; 4, The second fan-shaped debris flow; 5, Dark trachytic ignimbrite and surge (1668); 6, Dark trachytic fallout (1668); 7, The first fan-shaped debris flow; 8, Rock fall deposit; 9, Fallout (?1413–1668); 10, Outer flank dark lahar; 11, The Millennium ignimbrite and secondary deposits; 12, The Millennium valley and pond ignimbrite; 13, The Millennium eruption comenditic Plinian fallout; 14, Outer flank avalanche deposits; 15, Qixiangzhan distal comenditic lava; 16, Qixiangzhan middle comenditic lava; 17, Qixiangzhan proximal comenditic lava; 18, Qixiangzhan calstogenic lava, comendite, and obsidian; 19, Ice ground brown and gray trachytic ignimbrite, lahar; 20, Heifengkou Lag breccias (3950 ±120 a); 21, Upper trachyte and comendite cone (0.04–0.2 Ma); 22, Middle trachyte cone (0.25–0.44 Ma); 23, Lower trachyte cone (0.53–0.61 Ma); 24, Xiaobaishan trachyandesite and trachyte (1–1.49 Ma); 25, Laohudong parasitic basalt and scoria (0.32–0.34 Ma); 26, Laofangzixiaoshan basalt (0.31–0.58 Ma); 27, Baishan basalt (0.93–1.39 Ma); 28, Toudao basalt (1.91–2.77 Ma); 29, Comendite dyke; 30, Trachytic welded tuff dyke; 31, Trachyte dyke; 32, Ring and radioactive faults; 33, Caldera rim; 34,Avalanche scar; 35,Vent; 36, Hot spring; 37, Inferred geologic boundary; 38, Flow units boundary; 39, Facies boundary; 40, National boundary. β, Basalt; τ, Trachyte; λ, Comendite; π, Porphyry dyke (modified from [7]; Yun, unpublished data).

Figure 5.

The Buguamiao welded ignimbrite of the 1668 AD pyroclastic flow eruption is shown in all the pictures. The outcrops are in the vicinity of the Tianchi caldera.In the Baguamiao ignimbrite is also apparent its welded character.

Figure 6.

The 1702 AD pyroclastic flow eruption on the summit of the cliff.

Figure 7.

The 1903 AD pyroclastic flow deposits. The outcrop is separated by levels. The 1° level belongs to the 1702 AD eruption, and the others belong to the 1903 pyroclastic flow eruption. It is clear that the thickness of the 1903 deposit is near the caldera.

Figure 8.

Distribution of pyroclastic density currents of the Millennium eruption in China side. Numbers are thickness (m). Units C and F are the two pyroclastic flow levels.

This eruption has a volcanic explosivity index (VEI) of 7, comparable to the 1815 eruption of Tambora in Indonesia. Horn and Schmincke [25] have suggested that the Cheonji eruption column reached ca 25 km in height, injecting about 9 ×1010 kg of volatile halogens into the atmosphere, with an estimated volume of pyroclastic material on the order of ~100 km3. Volcanic ash from the eruption has been found 1,000 km away from the site of the eruption. A 5 cm thick deposit was observed in southern Hokkaido, Japan [38]. Accordingly, the Millennium eruption of the Baekdusan Cheonji volcano has been considered as one of the greatest volcanic eruptions of the past 2000 years.

Figure 9.

Stratigraphy of the Millennium eruption on the eastern slope of Baekdusan volcano (modified from [35]). pfa, pyroclastyc fall deposit; pfl, pyroclastic flow deposits; dfl, debris flow deposits.

3.1. An outline of the Millennium eruption

One of the most largest destructive eruptions from the Baekdusan volcano occurred on Earth in the last millennium, about 1,000 years ago, and it is named the Millennium eruption [25, 29, 34, 35]. It involved more than ~100 km3 of magma erupted [10], and the Plinian column was estimated to have had a height of 25 km. A widespread ash-fall deposit has been traced across the Sea of Japan to Hokkaido, and it is several centimeters thick, at more than 1,000 km from the source [35, 37]. Unwelded pyroclastic flows associated with collapse events of the Plinian eruption column extended to more than 70 km from the crater rim (Figure 8). The Millennium eruption formed a large caldera with a diameter of about 5 km and an area of 20 km2, forming the Cheonji (Tianchi = Sky) lake. Currently, the lake has a maximum depth of 374 m and an area of ~ 9.8 km2, with a water surface elevation of 2,189 m. It has a volume of 2 km3. A composite stratigraphic section of the Millennium eruption is given by Machida et al. ([35]; Figure 9). According to Machida et al. [35], the section is broadly composed of five levels (A, B, C, E, F; for major details, see Figure 9). Figure 10 shows some unwelded Millennium pyroclastic flow outcrops with relative thicknesses and sites. However, there is a controversy if the complete volcanological section of the Millennium eruption has to be interpreted as a single continuous eruption rather than one with two distinct pulses, with the initial phase anticipating the major phases of tens or hundreds of years [39]. The scientific literature reports a large range of ages for the Millennium eruption [40]. The results show a variety of periods ranging from approximately AD eighth to fourteenth centuries, which are the dates of the Balhae(= Bohai) and Goryeo dynasties [40, and references therein]. The last geochronological data (radiocarbon wiggle-match dating) on the Millennium eruption show a much more restricted range, respectively, of 938–939 AD [41], 946–947 AD [42], and 1024 AD [28].

Figure 10.

Millennium unwelded pyroclastic flow outcrops at the north and south flanks of the caldera with the respective thicknesses. (A) Millennium eruption pyroclastic flow deposits, northern slope: 20 m thickness. (B) Millennium eruption pyroclastic flow deposits, southern slope: 60 m thickness.


4. Scenarios of the 1903 AD, 1668–1702 AD, and the Millennium eruptions

The scenarios envisaged here are based on the large amount of data that have been collected by the Korean research project, CATER2011-5210 [36], and by the new literature produced [25, 3234, among others] in order to assign a selected VEI (Volcanic Explosivity Index [43]). The main parameters are summarized in Table 2 (VEI, maximum volume erupted, and column height) for each eruption. The volumes considered for just the pyroclastic density currents are obviously less than the total volume and are listed in Table 3. Figure 11 shows that between several volcanic-related disasters, the pyroclastic density currents have to be considered the most dangerous, given the number of fatalites in the last 2,000 years.

Eruption dateVEIVolume (m3)Column height (km)
1903 AD eruption2106–1081–5
1668–1702 AD eruption4108–101010–25
Millennium eruption71011–1012>25

Table 2.

Summary of the main parameters for the 1093 AD, 1702 AD, 1668 AD, and the Millennium eruptions. Volumes are taken from Newhall and Self [43] compared with the VEI for each eruption.

Eruption typeRunout length (m)Volume (m3)Initial velocity (m/s)Time duration (s)
1668–1702 type~4000–500010950>3600
Millennium eruption7–80,000101080–300>3600

Table 3.

Main parameters used to analyze the impact of the pyroclastic density currents and to show small-scale simulations [34, 61].

Figure 11.

Statistical percentage of fatalities for volcanic-related phenomena in last 2000 years. Pyroclastic density current is the most deadly phenomena in the last 2,000 years (Figure taken from the web and modified).

Branney and Kokelaar [44] illustrate in detail how different types of pyroclastic density currents originate (Figure 12). From Figure 12, the pyroclastic density currents most likely to occur at Beakdusan volcano are the following: A, B, C, depending on the size and the amount of interaction with external water. For laterally moving systems, the pyroclastic density currents can be identified as two end-member types: (A) Concentrated currents or pyroclastic flows, (B) Dilute currents or pyroclastic surges (Note that these are often a spectrum, with gradations in between). The end-member A has the following main characteristics:

  1. It has solids in concentrations of tens of volume percentage, and so they have higher densities than surges.

  2. They have a free surface, above which solids’ concentration decreases sharply.

  3. Transport of material is by fluidization, and most flows are considered to be laminar.

  4. Velocities vary, typically by 10s of meters per second up to several hundred meters per second, inferred from the heights of obstacles overcome by flows.

Figure 12.

Origins of pyroclastic density currents. (A) Short single-surge current derived by momentary collapse from a Plinian eruption column. (B) Sustained current derived from prolonged pyroclastic fountaining. The height of the jet (gas thrust) that feeds the current may vary and is transitional into (C). (C) A sustained current derived from a prolonged low pyroclastic fountaining explosive eruption. (D) Current with a single (or multiple) surge derived from lateral blasts initiated by catastrophic decompression of a magmatic and/or hydrothermal system. (E) Single-surge current derived from a collapsing lava dome or flow front. Hot rock avalanches generate turbulent density currents. (F) Deposit-derived pyroclastic density current caused by gravitational collapse and avalanching of unstable loose ignimbrite. The current may be a single-surge or more sustained where the collapse is retrogressive. Most large-volume ignimbrites derive from current types (B) and (C), which may involve periods of quasi-steady flow. Many may include significant components derived from currents of type (F) [44,45]. For Baekdusan, we chose the following three types: Soufriere, Pelee, and Merapi types (modified from [62]).

The end-member B has the following main characteristics:

  1. It contains less than 0.1–1.0% by volume of solids, even near ground surface, and so they are relatively of low density.

  2. They are density-stratified, with the highest particle concentration near the ground surface.

  3. Material is transported primarily by turbulent suspension.

  4. Transport system is modeled as one that loses particles by sedimentation, which depletes the system of mass. Eventually, the system may become buoyant, in which case it becomes a plume.

  5. Velocities vary, typically by 10s of meters per second, but they can also be much faster [4448].

Figure 13.

4D immersive visualization of the simulated partial column collapse scenario at Vesuvius. The collapse of the volcanic eruption column and the propagation of pyroclastic density currents (PDCs), for selected medium-scale (sub-Plinian) eruptive scenarios at Vesuvius, Italy (modified from [55]).

In fluid dynamics, the equations that govern the concentrated current are well known [49, 50], and the mathematics based on this volcanic phenomena is broadly used to model pyroclastic flows, along with other gravity currents: avalanches, seafloor turbidity currents, lahars, and lava flows. Two numerical codes apply these equations with small differences: Titan2D [51] and Volcflow [52, 53], but so far they have not produced any modeling for diluted currents. The only numerical code that models the diluted currents is called PDAC [54]. An application is shown for Somma-Vesuvius volcano, where pyroclastic density currents are modeled on the data of the 1631 AD sub-Plinian eruption ([55]; Figure 13). Kelfourn [53] tried to model two-fluid model block-ash flows and cloud-ash surge at Merapi volcano, developing new equations, but there is not yet an agreement (Kelfourn, personal communication). The importance of modeling diluted currents together with dense currents for the hazard of an explosive active volcano is commonly witnessed from the volcanological history, as seen in the work of Mastrolorenzo [56] who demonstrate the causes of mortality in PDCs at Pompeii and surroundings, on the basis of a multidisciplinary volcanological and bioanthropological study. Field and laboratory studies of the eruption products and victims, merged with numerical simulations and experiments, indicate that heat was the main cause of death. Their results show that exposure to at least 250°C hot surges at a distance of 10 km from the vent was sufficient to cause instant death, even if people were sheltered within buildings. Despite the fact that impact force and exposure time to dusty gas declined toward PDCs’ periphery up to the survival conditions, lethal temperatures were maintained up to the PDCs’ extreme depositional limits. This study suggests that diluted currents are very dangerous, and if the runout of the pyroclastic flow must be chosen, it is always underestimated when considering diluted currents, especially for large eruption.


5. Relationship between the Baekdusan eruptions: 1903 AD, 1668–1702 AD, and Millennium eruptions, and the most devastating eruptions in the recent history of the earth

As indicated in Table 1, the 1903 AD, 1668–1702 AD, and the Millennium eruptions are characterized by the following VEI, respectively: 2–3, 4–5, and ~7. From the classification of Newhall and Self [43], the magnitude of each eruption with all the volcanological parameters can be deduced. If we compare the total volume ejected from Baekdusan volcano in the last Millennium activity with the most devastating eruptions in the recent history of volcanology, it appears that the two most recent eruptions shown, from Mount St. Helens and Mount Pinatubo, each caused extensive damage and received intense media interest. Ejected volumes, however, were only about 1/10,000 (St. Helens) and 1/500 (Pinatubo) of the volumes associated with either the 74 ka Toba or the 2 Ma Yellowstone super-eruptions. Even the 1883 Krakatau eruption, which accounted for over 35,000 deaths, was smaller than the Toba and Yellowstone eruptions by two orders of magnitude. The 1815 Tambora eruption, which had an ejected volume of less than 5% of those of Toba or Yellowstone and was distinctly less than “super,” affected global climate and was responsible for over 50,000 deaths (Figure 14A and B [57]). The 1903 AD eruption can be compared to two recent eruptions: (A) Nevado del Ruiz, Colombia, 1985, (B) Soufrière Hills, West Indies, 1995 (Figure 14B). The two eruptions of 1668–1702 AD of similar size can be compared to the following eruptions: (A) Soufrière Hills, West Indies, 1995, (B) Mount St. Helens, USA, 1980 (Figure 14B). The Millennium eruption may have been slightly larger than the 1815 Tambora eruption, Indonesia. Millennium eruption can be considered a super-eruption alike other eruptions (e.g., Campanian Ignimbrite, Campi Flegrei, Napoli [58]; Figure 15). This assumption is confirmed from some South Korean scientists that during the 2nd International Workshop for Volcanic Disaster Preparedness at Chungbuk National University, Korea affirmed that the Millennium eruption could have been as high as 7VEI. Further, Xu et al. [42, 59] suggest that the Millennium eruption was a Toba-like "ash giant/sulfur dwarf" and had much smaller global climatic impacts. Sun et al. [60] confirm that the eruption most probably occurred around AD 940s, 7 years after the Eldgjá eruption on Iceland, and examining the eruption’s potential for climate-forcing using the sulfate records from the ice cores, they conclude that it was unlikely to have had a global impact. Zircons U–Th data of Millennium eruption indicate that magma resided only ~8 ka prior to eruption. Therefore, Baekdusan volcano can produce catastrophic, explosive eruptions in the foreseeable future [36]. Thus, Baekdusan is the most active volcano in China [14], and it is a high-risk volcano because more than 100,000 people live on or near the slopes, with the addition of many tourists.

Figure 14.

A. Relative volumes of pyroclastic material erupted from the large eruption in the 2 Ma [57].B. Classification of the VEI modified after [4] (modified from [57]).

Figure 15.

The Volcanic Explosivity Index (VEI) is calculated with a logarithmic-based scale of erupted mass, as well as past examples, estimated frequency, and probability. It includes large eruptions from 40 km3 in magma volume up to the largest super-eruptions known (modified from [15]).

5.1. An example of Titan2D simulation with the size of 1903 AD eruption

The size of the 1903 AD eruption has been evaluated, and consequently some Titan2D simulations are presented, taking into account where the vents of the 1903 AD, 1668 AD, and 1702 AD were located. Five vent locations are considered: three inside the caldera lake and two outside the caldera, as illustrated in Figure 16. The simulations start with an initial column (or pile) that collapses. The column is a vertical cylinder with a diameter 250 m and the height Hcol (Table 4). In Figure 17 we report the thickness of the deposit when the flow is stopped. We consider 1 h (3,600s) after the initial collapse of the eruption column which can be formed by the Plinian eruption. The scenario performed shows, according to the vent locations, that the flow moves in diverse directions (NE, SE) with a thickness of 3 m, and that if the vent is located inside the caldera the flow fills the caldera with a thickness of 5 m. If the vent is on the border of the caldera, the flow will deposit thickly, mostly in the northern valley, the upper stream region of Erdaobaihe (Figure 17 [34, 61]).

Figure 16.

Location of the considered vents for the Titan2D simulation of the small-scale 1903 AD eruption.

NumberVentInt. frict.Bed. FrictHcol (m)Diameter (m)Volume (m3)
1A302510002504.9 × 107
2A301610002504.9 × 107
3A251610002504.9 × 107
4A251620002509.8 × 107
5B251620002509.8 × 107
6C251620002509.8 × 107
7D251620002509.8 × 107
8E251620002509.8 × 107

Table 4.

Parameters used to simulate the pyroclastic flow of 1903 AD eruption needed by Titan2D code.

Figure 17.

Results of the Titan2D simulation for a small-scale scenario (VEI 3) similar to the 1903 AD eruption [34,61].


6. The impact of 1668–1702 AD and Millennium eruption around Baekdusan volcano

Figure 18.

Possible area covered by a pyroclastic density current of the size of the 1668–1702 AD eruption. The runout chosen could have been underestimated so that the impact would be more severe than expected.

From the pyroclastic density currents scenario of the 1668–1702 AD eruptions with a runout around 5,000 m (Figure 18), two densely populated cities which are nearest to Baekdusan volcano would suffer significant damage: Erdaobaihe and Songjianghe. Possibly, the pyroclastic density currents could also affect two other cities located slightly further away, such as Fusong and Lushuihe. In the case of the Millennium eruption, considering only the direct impact, without considering the indirect effect which in the case of such eruption could be severe, and considering an underestimation of the runout, the following cities will be hit: Erdaobaihe, Songjianghe, Changbai, Huishan, Baishan, Fusong, Lushuihe, and Tumer (Figure 19).

Figure 19.

Possible area covered by a pyroclastic density current of the size of the Millennium eruption. The runout chosen could have been underestimated so that the impact would be more severe than expected and surely of regional scale, if not global.


7. Concluding remarks on the worst-case scenario

The worst-case scenario is surely an eruption of a colossal size (Millennium eruption), but it has to be excluded from the scenario of the 1668–1702 AD eruption. In this case, the hazard and the risk must be evaluated carefully, and the population around Baekdusan volcano must be informed in detail. We think in this case, the population at risk is not aware of the possible hazard of the volcano. In all sorts of circumstances, the population has to be alerted. Every sign of unrest has to be monitored and communicated to everybody involved in the decision-making to the people. As far as we are concerned there is not a robust monitoring system around Baekdusan volcano, especially on North Korea side. An emergency plan must be created for Baekdusan volcano.


8. Future research prospectives

In the near future, there are several points in research direction that the Asian scientists could undertake, if they have not done yet: (A) Evolution of the Baekdusan volcano plumbing system in the least 20,000 years. (B) Developing an open source numerical code to model diluted density currents (surge) for the worst-case scenario, (C) Making an event tree study of Baekdusan volcano like that of Somma-Vesuvius volcano, Napoli, Italy.



This research was supported by a grant [MPSS-NH-2015-81] through the Natural Hazard Mitigation Research Group funded by Ministry of Public Safety and Security of Korean government. Thanks to Dr. Giovanni Macedonio for helping in making the simulation of Figure 17 at Osservatorio Vesuviano, INGV, Napoli, Italy. Thanks to Chris Hawkesworth for an early review of the manuscript. Thanks to Steve Sparks to critically looking at the manuscript and addressing the journal for the content of the manuscript.


  1. 1. Gomà Daniel, 2004. Border Disputes between China and North Korea. China Perspectives, 52 Online since 23 April 2007. URL:
  2. 2. Gomà Daniel, 2006. The Chinese-Korean border issue: an analysis of a contested frontier. Asian Survey, Vol. 46, No. 6, pp. 867–880. URL:
  3. 3. Cashman K. V., Sparks R. S. J., 2013.How volcanoes work: a 25 year perspective. Geological Society of America Bulletin, Vol. 125, No. 5–6, pp. 664–690.
  4. 4. Sparks R. S. J., Biggs J., Neuberg J. W., 2012. Monitoring volcanoes. Science, Vol. 335, pp. 1310–1311.
  5. 5. Sparks R.S.J., 2003. Forecasting volcanic eruptions. Earth and Planetary Science Letters, Vol. 210, pp. 1–15.
  6. 6. Newhall C., Andreastuti S., Lara L., Rosi M., Woo G., 2014. (3.I.F) Managing Worst-Case Scenarios (with Reference to Merapi 2010, St. Helens 1980, Pinatubo 1991, and The Next VEI 7 Eruption) Cities on Volcanoes 8, Living in Harmony with Volcano: Bridging the will of nature to society, Yogyakarta, 9–13 September 2014
  7. 7. Wei H., Liu G., Gill J., 2013. Review of eruptive activity at Tianchi volcano, Changbaishan, northeast China: implications for possible future eruptions. Bulletin of Volcanology, Vol. 75, pp. 1–14.
  8. 8. Yun S. H., Lee J. H., 2012. Analysis of unrest signs of activity at the Baegdusan volcano. Journal of Petrological Society of Korea, Vol. 21, pp. 1–12.
  9. 9. Yun S. H., Lee J. H., Chang C., 2013. A study on the change of magma activity from 2002 to 2009 at Mt. Baekdusan using surface displacement. Journal of Korean Earth Science Society, Vol. 34, No. 6, pp. 470478 (in Korean with English abstract).
  10. 10. Xu J., Liu G., Wu J., Ming Y., Wang Q., 2012. Recent unrest of Changbaishan volcano, northeast China: a precursor of a future eruption? Geophysical Research Letters, Vol. 39, p. L16305, doi: 10.1029/2012GL052600
  11. 11. Liu G., Liu G. R., Zhang H. R., Kong Q. J., Wu C. Z., Guo F., Zhang C. F., 2004. Elementary analysis of data from Tianchi volcano. Journal of Geoscience Research NE Asia, Vol. 7, No. 2, pp. 156–16.
  12. 12. Gun U. Y., Ok J. U., Song K. M., Song R. G., Nam R. K., Hammond J. O., Oppenheimer C., Whaler K., Park S., Dawes G., Iacovino K., 2013.The Mt. Paektu geoscientific experiment. IAVCEI 2013 Scientific Assembly, July 20–24, Kagoshima, Japan.
  13. 13. Liu G., 2013.Changbaishan seismic mornitoring network and recent unrest of the volcano. IAVCEI 2013 Scientific Assembly, July 20–24, Kagoshima, Japan.
  14. 14. Wei H., Sparks R. S. J., Liu R., Fan Q., Wang Y., Hong H., Zhang H., Chen H., Jiang C., Dong J., Zheng Y., Pan Y., 2003. Three active volcanoes in China and their hazards, Journal of Asian Earth Sciences, Vol. 21, pp. 515–526.
  15. 15. Sparks S., Self S., Grattan J., Oppenheimer C., Pyle D., Rymer H., 2005. Super-eruptions: Global Effects and Future Threats. Report of a Geological Society of London Working Group (2nd (print) Edn.). Original (Web) edition available at
  16. 16. Lei J., Zhao D., 2005. P-wave tomography and origin of the Changbai intraplate volcano in Northeast Asia. Tectonophysics, Vol. 397, pp. 281–295.
  17. 17. Zhao D., 2012.Tomography and dynamics of western-Pacific subduction zones. Monographs on Environment, Earth and Planets, Vol. 1, No. 1, 1–70.
  18. 18. Zhao D., Liu L., 2010. Deep structure and origin of active volcanoes in China. Geoscience Frontiers, Vol. 1, pp. 31–44.
  19. 19. Zhao D., Tian Y., 2013. Changbai intraplate volcanism and deep earthquakes in East Asia: a possible link? Geophysics Journal International, Vol. 195, pp. 706–724.
  20. 20. Kuritani T., Ohtani E., Kimura J.-I., 2011.Intensive hydration of the mantle transition zone beneath China caused by ancient slab stagnation. Nature Geoscience, Vol. 4, pp. 713–716.
  21. 21. Annen C., Blundy J.D., Sparks R. S. J., 2006. The genesis of intermediate and silicic magmas in deep crustal hot zones. Journal of Petrology, Vol. 47, pp. 505–539.
  22. 22. Yun S. H., Koh J. S., Chang C. W., 2015. Magma genesis of Holocene volcanism at Mt. Baekdusan. Abstract Book, 2015 Fall Joint Conference of Geological Science of Korea (2015. 10. 28-31), Jeju, Korea, pp. 518, 39.
  23. 23. Yun S. H., Won C. K., Lee M. W., 1993. Cenozoic volcanic activity and petrochemistry of volcanic rocks in the Mt. Paektu area. Journal of Geological Society of Korea, Vol. 29, pp. 291–307 (in Korean with English abstract).
  24. 24. Wei H., 2010. Magma up-moving process within the magma prism beneath the Changbaishan volcanoes. Earth Science Frontiers, Vol. 17, No. 1, pp. 11–23 (in Chinese with English abstract).
  25. 25. Horn S., Schmincke H.U., 2000. Volatile emission during the eruption of Baitoushan Volcano (China/North Korea) ca. 969 AD. Bulletin of Volcanology, Vol. 61, pp. 537–555.
  26. 26. Annen C., Blundy J. D., Sparks R. S. J., 2006. The sources of granitic melt in deep hot zones. Transactions of the Royal Society of Edinburgh: Earth Sciences, Vol. 97, pp. 297–309, doi: 10.1017/S0263593300001462
  27. 27. Annen C., Sparks R. S. J., 2002. Effects of repetitive emplacement of basaltic intrusions on thermal evolution and melt generation in the deep crust. Earth and Planetary Science Letters, Vol. 203, pp. 937–955.
  28. 28. Wei H., Wang Y., Jin J., Gao L., Yun S.H., Jin B., 2007.Timescale and evolution of the intracontinental Tianchi volcanic shield and ignimbrite-formation eruption, Changbaishan, Northeast China. Lithos, Vol. 96, pp. 315–324.
  29. 29. Wei H., Taniguchi H., Myamoto T., Jin B., 2007. Stratigraphic sequences and magmatic cycles of the Tianchi volcano, Changbaishan. Northeast Asian studies Vol. 11, pp. 173–193.
  30. 30. Yang L., Wang F., Feng H., Wu L., Shi W., 2014.40Ar/39Ar geochronology of Holocene volcanic activity at Changbaishan Tianchi volcano, Northeast China. Quaternary Geochronology, Vol. 21, pp. 106–114.
  31. 31. Yun S. H., 2013.Volcanological interpretation of historical eruptions of Mt. Baekdusan volcano. Journal Korean Earth Science Society, Vol. 34, No. 6, pp. 456469.
  32. 32. Yun S. H., Cui Z. X., 1996. Historical eruption records on the Cheonji caldera volcano in the Mt. Peaktu. Journal of Korean Earth Science Society, Vol. 17, No. 5, pp. 376–382 (in Korean with English abstract).
  33. 33. Yun S. H., Lee J. H., 2011. Volcanological interpretation of historic record of 1702 fallout-ash from the Mt. Baekdusan. Journal of Petrological Society of Korea, Vol. 20, No. 4, pp. 243–250 (in Korean with English abstract).
  34. 34. Yun S. H., Lee J. H., Kim S., Chang C., Cho E., Yang I., Kim Y., Kim S., Lee K., Kim S., Macedonio G., 2013. TITAN2D simulations of pyroclastic flows from small scale eruption at Mt. Baekdusan. Journal of Korean Earth Science Society, Vol. 34, No. 7, pp. 615625 (in Korean with English abstract).
  35. 35. Machida H., Hiroshi M., Zhao D. C., 1990, The recent major eruption of Changbai eruption and its environmental effects. Geophysical Reports of Tokyo Metropolitan University, Vol. 25, pp. 1–20.
  36. 36. Yun et al., 2012. A study on the cooperative diagnosis on eruption possibility of Baegdusan volcano. Pusan National University Project. CATER 2011–5210 pp. 1–131 (in Korean with the references in English).
  37. 37. Zou H., Fan Q., Zhang H., 2010. Rapid development of the great Millennium eruption of Changbaishan (Tianchi) volcano, China/North Korea: evidence from U–Th zircon dating. Lithos, Vol. 119, pp. 289–296.
  38. 38. Machida H., Arai F., 1992, Atlas of Tephra in and around Japan. University of Tokyo Press, Tokyo. 276 p (in Japanese).
  39. 39. Nakagawa M., Nishimoto J., Miyamoto T., Taniguchi H., 2013. Magma system and its eruption processes of the caldera-forming 10th century eruption of Changbaishan (Baitoushan) Volcano: inferred from petrological and geochemical characteristics. IAVCEI 2013 Scientific Assembly, July 20–24, Kagoshima, Japan.
  40. 40. Chu K. S., Tsuji Y., Baag C. E., Kang T. S., 2011.Volcanic eruptions of Mt. Baekdu Changbai occurring in historical times. Bulletin of Earthquake Research Institute, University of Tokyo, Vol. 20, pp. 11–27 (in Japanese with English abstract).
  41. 41. Yin J., Jull T., Burr G. S., Zheng Y., 2012. A wiggle-match age for the Millennium eruption of Tianchi volcano at Changbaishan, Northeastern China. Quaternary Science Reviews, Vol. 47, pp. 150–159.
  42. 42. Xu J., Pan B., Liu T., Hajdas I., Zhao B., Yu H., Liu R., Zhao P., 2013. Climatic impact of the Millennium eruption of Changbaishan volcano in China: new insights from high-precision radiocarbon wiggle-match dating. Geophysical Research Letters, Vol. 40, pp. 1–6, doi: 10.1029/2012GL054246
  43. 43. Newhall C., Self S., 1982.The volcanic explosivity index (VEI): an estimate of explosive magnitude for historical volcanism. Journal of Geophysical Research, Vol. 87, pp. 1231–1238.
  44. 44. Branney M. J., Kokelaar P., 2002.Pyroclastic Density Currents and the Sedimentation of Ignimbrites.Geological Society, London, Memoirs, 27, pp. 152.
  45. 45. Sparks R. S. J., Bursik M. I., Carey S. M., Gilbert J. S., Glaze L. S. Sigurdsson H., Woods A. W., 1997.Volcanic Plumes. Wiley, Chichester.
  46. 46. Gilbert J. S., Sparks R. S. J. (eds), 1998. The Physics of Explosive Volcanic Eruptions.Geological Society, London, Special Publications, Vol. 145, pp. 193.
  47. 47. Parfitt E. A., Wilson L., 2008. Fundamentals of Physical Volcanology. Blackwell Publishing Ltd., pp. 256.
  48. 48. Fagents S. A., Gregg T. K. P., Lopes R. M. C., 2012. Modeling Volcanic Processes. The Physics and Mathematics of Volcanism. Cambridge University Press, pp. 448.
  49. 49. Savage S. B., Hutter H., 1989. The motion of a finite mass of granular material down a rough incline. Journal of Fluid Mechanics, Vol. 199, pp. 177-215
  50. 50. Iverson Denlinger, 2001. Flow of variably fluidized granular masses across three-dimensional terrain 1. Coulomb mixture theory. Journal of Geophysical Research, Vol. 106, p. 537.
  51. 51. Patra A. K., Bauer A. C., Nichita C., Pitman E. B., Sheridan M. F., Bursik M. I., 2005.Parallel adaptive simulation of dry avalanches over natural terrain. Journal of Volcanology and Geothermal Research, Vol. 139, pp. 1–21.
  52. 52. Kelfoun K., 2011.Suitability of simple rheological laws for the numerical simulation of dense pyroclastic flows and long‐runout volcanic avalanches. Journal of Geophisical Research, Vol. 116, p. B08209, doi: 10.1029/2010JB007622
  53. 53. Kelfourn K., 2011. A two-fluid model for block-and-ash flows and ash-cloud surge confronted with the 1994 eruption of Merapi volcano (Indonesia). European Geosciences Union. General Assembly, Vienna, Austria, Poster.
  54. 54. Esposti O. T., Cavazzoni C., Erbacci G., Neri A., Salvetti M. V., 2007. A parallel multiphase flow code for the 3D simulation of explosive volcanic eruptions. Parallel Computer. doi: 10.1016/j.parco.2007.04.003
  55. 55. Neri A., Esposti Ongaro T., Menconi G., De’ Michieli Vitturi M., Cavazzoni C., Erbacci G., Baxter P.J., 2007. 4D simulation of explosive eruption dynamics at Vesuvius. Geophysical Research Letters, Vol. 34, p. L04309.
  56. 56. Mastrolorenzo G., Petrone P., Pappalardo L., Guarino F.M., 2010. Lethal thermal impact at periphery of pyroclastic surges: evidences at Pompeii. PLoS ONE, Vol. 5, No. 6, pp. 1–12.
  57. 57. Miller C. F., Wark D. A., 2008. Supervolcanoes and their explosive supereruptions. Elements, Vol. 4, pp. 11–16.
  58. 58. Costa A., Folch A., Macedonio G., Giaccio B., Isaia R., Smith V. C., 2012. Quantifying volcanic ash dispersal and impact of the Campanian Ignimbrite super-eruption. Geophysical Research Letters, Vol. 39, p. L10310, doi: 10.1029/2012GL051605
  59. 59. Xu J., Pan B., Liu T., Hajdas I., Zhao B., Yu H., Liu R., 2013.The millennium eruption of Changbaishan volcano in northeast China: high-precision wiggle-match radiocarbon chronology and implications. IAVCEI 2013 Scientific Assembly, July 20–24, Kagoshima, Japan.
  60. 60. Sun C., Plunkett G., Liu J., Zhao H., Sigl M., McConnell J. R., Pilcher J. R., Vinther B., Steffensen J. P., and ValerieHall, 2014. Ash from Changbaishan Millennium eruption recorded in Greenland ice: implications for determining the eruption’s timing and impact. Geophysical Research Letters, Vol. 41, pp. 694–701, doi: 10.1002/2013GL058642.
  61. 61. Yun S. H., Paone A., Macedonio G., Jeong Lee H., Kim S. K., Cho E., Kim Y. J., 2013. A preliminary evaluation of the impact of pyroclastic flows using Titan 2D at the Baegdusan volcano according to three different scenarios. 2nd International Workshop for Volcanic Disaster Preparedness. Chungbuk National University. Abstract and Oral communication.
  62. 62. Francis P., 1993, Volcanoes: A planetary perspective. Oxford University Press, Walton Street, New York, 249, 443 p.

Written By

Angelo Paone and Sung-Hyo Yun

Submitted: November 24th, 2015 Reviewed: February 2nd, 2016 Published: September 21st, 2016