Overview of the 2006 eruption of Mt. Merapi

Ratdomopurbo, Antonius; Beauducel, François; Subandriyo, J.; Nandaka, I Gusti Made Agung; Newhall, Christopher G.; Suharna,; Sayudi, Dewi Sri; Suparwaka, Heru; Sunarta,

doi:10.1016/j.jvolgeores.2013.03.019

Cited by 82 publications

(42 citation statements)

References 12 publications

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“…Andreastuti et al 2000;Newhall et al 2000;Voight et al 2000;Gertisser et al 2012a;Surono et al 2012). The previous eruption in 2006 is a well-characterised extrusive, dome-forming eruption at Merapi (Charbonnier and Gertisser 2008;Gertisser et al 2012b;Preece et al 2013;Ratdomopurbo et al 2013). Although the 2006 eruption displayed typical Merapi dome-forming activity, peak dome extrusion rates reached 3.3 m 3 s −1 , which is high compared to other recent Merapi eruptions.…”

Section: The 2010 and 2006 Eruptions Of Merapimentioning

confidence: 81%

“…Surono et al 2012). In contrast to recent prolonged and effusive dome-forming eruptions at Merapi, such as the previous eruption in 2006 (Charbonnier and Gertisser 2008;Preece et al 2013;Ratdomopurbo et al 2013), the 2010 eruption began explosively and a new lava dome grew in the newly formed crater prior to explosive destruction of this dome during the peak of the eruption on 5 November 2010, followed by further explosive activity and extrusion of a new dome after 5 November (Surono et al 2012;Komorowski et al 2013;Pallister et al 2013) (Fig. 1).…”

Section: The 2010 and 2006 Eruptions Of Merapimentioning

confidence: 89%

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Pre- and syn-eruptive degassing and crystallisation processes of the 2010 and 2006 eruptions of Merapi volcano, Indonesia

Preece

Gertisser

Barclay

et al. 2014

Contrib Mineral Petrol

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clasts resulting from sub-plinian convective column collapse. This paper presents geochemical data for melt inclusions and their clinopyroxene hosts extracted from dense dome lava, grey scoria and white pumice generated during the peak of the 2010 eruption. These are compared with clinopyroxenehosted melt inclusions from scoriaceous dome fragments from the prolonged dome-forming 2006 eruption, to elucidate any relationship between pre-eruptive degassing and crystallisation processes and eruptive style. Secondary ion mass spectrometry analysis of volatiles (H 2 O, CO 2 ) and light lithophile elements (Li, B, Be) is augmented by electron microprobe analysis of major elements and volatiles (Cl, S, F) in melt inclusions and groundmass glass. Geobarometric analysis shows that the clinopyroxene phenocrysts crystallised at depths of up to 20 km, with the greatest calculated depths associated with phenocrysts from the white pumice. Based on their volatile contents, melt inclusions have reequilibrated during shallower storage and/or ascent, at depths of ~0.6-9.7 km, where the Merapi magma system is interpreted to be highly interconnected and not formed of discrete magma reservoirs. Melt inclusions enriched in Li show uniform "buffered" Cl concentrations, indicating the presence of an exsolved brine phase. Boron-enriched inclusions also support the presence of a brine phase, which helped to stabilise B in the melt. Calculations based on S concentrations in melt inclusions and groundmass glass require a degassing melt volume of 0.36 km 3 in order to produce the mass of SO 2 emitted during the 2010 eruption. This volume is approximately an order of magnitude higher than the erupted magma (DRE) volume. The transition between the contrasting eruptive styles in 2010 and 2006 is linked to changes in magmatic flux and changes in degassing style, with the explosive activity in 2010 driven by an influx of deep magma, which overwhelmed the shallower magma system and ascended rapidly, accompanied by closed-system degassing. AbstractThe 2010 eruption of Merapi (VEI 4) was the volcano's largest since 1872. In contrast to the prolonged and effusive dome-forming eruptions typical of Merapi's recent activity, the 2010 eruption began explosively, before a new dome was rapidly emplaced. This new dome was subsequently destroyed by explosions, generating pyroclastic density currents (PDCs), predominantly consisting of dark coloured, dense blocks of basaltic andesite dome lava. A shift towards open-vent conditions in the later stages of the eruption culminated in multiple explosions and the generation of PDCs with conspicuous grey scoria and white pumice Communicated by O. Müntener. Electronic supplementary materialThe online version of this article

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Section: The 2010 and 2006 Eruptions Of Merapimentioning

confidence: 81%

Section: The 2010 and 2006 Eruptions Of Merapimentioning

confidence: 89%

Pre- and syn-eruptive degassing and crystallisation processes of the 2010 and 2006 eruptions of Merapi volcano, Indonesia

Preece

Gertisser

Barclay

et al. 2014

Contrib Mineral Petrol

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“…) when dome growth took place subsequently (Surono et al 2012;Pallister et al 2013;Ratdomopurbo et al 2013). Activity in 2010 included several explosive stages generating a series of laterally directed dome explosions ('blasts'), a subplinian eruption column and maximum PDC runout distances of ∼16 km, more than twice those generated in the effusive dome-forming eruption in 2006 (Charbonnier and Gertisser 2008;Charbonnier et al 2013;Komorowski et al 2013).…”

Section: Eruption Chronology Deposits and Sampling Eruption Chronologymentioning

confidence: 99%

Transitions between explosive and effusive phases during the cataclysmic 2010 eruption of Merapi volcano, Java, Indonesia

et al. 2016

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Transitions between explosive and effusive activity are commonly observed during dome-forming eruptions and may be linked to factors such as magma influx, ascent rate and degassing. However, the interplay between these factors is complex and the resulting eruptive behaviour often unpredictable. This paper focuses on the driving forces behind the explosive and effusive activity during the well-documented 2010 eruption of Merapi, the volcano's largest eruption since 1872. Time-controlled samples were collected from the 2010 deposits, linked to eruption stage and style of activity. These include scoria and pumice from the initial explosions, dense and scoriaceous dome samples formed via effusive activity, as well as scoria and pumice samples deposited during subplinian column collapse. Quantitative textural analysis of groundmass feldspar microlites, including measurements of areal number density, mean microlite size, crystal aspect ratio, groundmass crystallinity and crystal size distribution analysis, reveal that shallow pre-and syn-eruptive magmatic processes acted to govern the changing behaviour during the eruption. High-An (up to ∼80 mol% An) microlites from early erupted samples reveal that the eruption was likely preceded by an influx of hotter or more mafic magma. Transitions between explosive and effusive activity in 2010 were driven primarily by the dynamics of magma ascent in the conduit, with degassing and crystallisation acting via feedback mechanisms, resulting in cycles of effusive and explosive activity. Explosivity during the 2010 eruption was enhanced by the presence of a 'plug' of cooled magma within the shallow magma plumbing system, which acted to hinder degassing, leading to overpressure prior to initial explosive activity.

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“…At some volcanoes, the timing and dimension of extrusive activity may be forecasted based on precursory signals such as earthquakes, tremors and long periodic seismicity (Kilburn and Voight, 1998;Neuberg, 2000;Bean et al, 2014), as well as ground displacements on different scales (Surono et al, 2012;Di Traglia et al, 2013) that can be readily identified and have been successfully used for timely evacuation. A large variety of conduit processes may generate precursory signals, including gas accumulation beneath a volcanic dome (Johnson et al, 2008), episodic slip on the conduit margins (Anderson et al, 2010), changes in a dynamic plumbing system (Kahl et al, 2011) or the accumulation of magmatic material at shallow levels (Ratdomopurbo et al, 2013).…”

Section: Introductionmentioning

confidence: 99%

“…In some cases, we can observe summit deformation caused by the pre-eruptive intrusion of magma to very shallow levels of the volcano (Dzurisin et al, 2008;Saepuloh et al, 2013). Since the newly injected material remains there, this deformation is static and lacks co-explosive subsidence (Ratdomopurbo et al, 2013). However, short term pre-eruptive deformation originating from conduit processes of smaller magnitude are rarely detected with geodetic instrumentation, yet may be related to a considerable proportion of pre-eruptive seismic signals.…”

Section: Introductionmentioning

confidence: 99%

Satellite radar data reveal short-term pre-explosive displacements and a complex conduit system at VolcÃ¡n de Colima, Mexico

et al. 2014

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The geometry of the volcanic conduit is a main parameter controlling the dynamics and the style of volcanic eruptions and their precursors, but also one of the main unknowns. Pre-eruptive signals that originate in the upper conduit region include seismicity and deformation of different types and scales. However, the locality of the source of these signals and thus the conduit geometry often remain unconstrained at steep sloped and explosive volcanoes due to the sparse instrumental coverage in the summit region and difficult access. Here we infer the shallow conduit system geometry of Volcán de Colima, Mexico, based on ground displacements detected in high resolution satellite radar data up to 7 h prior to an explosion in January 2013. We use Boundary Element Method modeling to reproduce the data synthetically and constrain the parameters of the deformation source, in combination with an analysis of photographs of the summit. We favor a two-source model, indicative of distinct regions of pressurization at very shallow levels. The horizontal location of the upper pressurization source coincides with that of post-explosive extrusion. The pattern and degree of deformation reverses again during the eruption; we therefore attribute the displacements to transient (elastic) pre-explosive pressurization of the conduit system. Our results highlight the geometrical complexity of shallow conduit systems at explosive volcanoes and its effect on the distribution of pre-eruptive deformation signals. An apparent absence of such signals at many explosive volcanoes may relate to its small temporal and spatial extent, partly controlled by upper conduit structures. Modern satellite radar instruments allow observations at high spatial and temporal resolution that may be the key for detecting and improving our understanding of the generation of precursors at explosive volcanoes.

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Overview of the 2006 eruption of Mt. Merapi

Cited by 82 publications

References 12 publications

Pre- and syn-eruptive degassing and crystallisation processes of the 2010 and 2006 eruptions of Merapi volcano, Indonesia

Pre- and syn-eruptive degassing and crystallisation processes of the 2010 and 2006 eruptions of Merapi volcano, Indonesia

Transitions between explosive and effusive phases during the cataclysmic 2010 eruption of Merapi volcano, Java, Indonesia

Satellite radar data reveal short-term pre-explosive displacements and a complex conduit system at VolcÃ¡n de Colima, Mexico

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