Dike emplacement near Parícutin volcano, Mexico in 2006

Gardine, M.; West, M. E.; Cox, T.

doi:10.1007/s00445-010-0437-9

Cited by 32 publications

(31 citation statements)

References 26 publications

Supporting

Mentioning

Contrasting

Unclassified

Order By: Relevance

“…Examples include Soufrière Guadeloupe, 1975-1976(Hirn and Michel 1979Dorel and Feuillard 1980;Feuillard et al 1983;Beauducel and Besson 2008), Akutan, Alaska, 1996(Lu et al 2000Power et al 2008), Mount Baker, Washington, 1975(Crider et al 2011), Iliamna, Alaska, 1996(Roman et al 2004Roman and Power 2011), Iwate, Japan, 1998(Nishimura and Ueki 2011), Parícutin, Mexico, 2006(Gardine et al 2011), Fourpeaked, Alaska, 2006(Gardine et al 2010), Mount Spurr, Alaska, 2004(Power 2004, and others. A few cases are well-studied, but many are poorly documented in the literature and so details of such events are often unavailable for comparison during an unrest episode.…”

Section: Introductionmentioning

confidence: 97%

Failed magmatic eruptions: late-stage cessation of magma ascent

2011

View full text Add to dashboard Cite

When a volcano becomes restless, a primary question is whether the unrest will lead to an eruption. Here we recognize four possible outcomes of a magmatic intrusion: "deep intrusion", "shallow intrusion", "sluggish/viscous magmatic eruption", and "rapid, often explosive magmatic eruption". We define "failed eruptions" as instances in which magma reaches but does not pass the "shallow intrusion" stage, i.e., when magma gets close to, but does not reach, the surface. Competing factors act to promote or hinder the eventual eruption of a magma intrusion. Fresh intrusion from depth, high magma gas content, rapid ascent rates that leave little time for enroute degassing, opening of pathways, and sudden decompression near the surface all act to promote eruption, whereas decreased magma supply from depth, slow ascent, significant enroute degassing and associated increases in viscosity, and impingement on structural barriers all act to hinder eruption. All of these factors interact in complex ways with variable results, but often cause magma to stall at some depth before reaching the surface. Although certain precursory phenomena, such as rapidly escalating seismic swarms or rates of degassing or deformation, are good indicators that an eruption is likely, such phenomena have also been observed in association with intrusions that have ultimately failed to erupt. A perpetual difficulty with quantifying the probability of eruption is a lack of data, particularly on instances of failed eruptions. This difficulty is being addressed in part through the WOVOdat database. Papers in this volume will be an additional resource for scientists grappling with the issue of whether or not an episode of unrest will lead to a magmatic eruption.

show abstract

Section: Introductionmentioning

confidence: 97%

Failed magmatic eruptions: late-stage cessation of magma ascent

2011

View full text Add to dashboard Cite

show abstract

“…Passarelli et al (2015b) showed that 3D dike geometry can explain oblique normal faulting sometimes observed in the region crowning a dike from the top to the side. The orientations of the pressure (P-) or tension (T-) axes derived from focal mechanism inversion support a model resulting often sub-perpendicular to the intrusion plane (Ukawa and Tsukahara, 1996;Roman and Cashman, 2006;Gardine et al, 2011). Dike-induced earthquakes generally show non-negligible non-DC components (Julian, 1983;Dahm and Brandsdóttir, 1997;Minson et al, 2007;Ruppert et al, 2011;Belachew et al, 2013).…”

Section: Magmatic Hypothesismentioning

confidence: 99%

“…The dike volume increases following asymptotic exponential growth (Rivalta, 2010). The earthquakes induced around the dike tip migrate with a similar asymptotic exponential growth of the distance to the magma chamber at speeds of the order of a few kilometers to tens of kilometers per day (Ukawa and Tsukahara, 1996;Keir et al, 2009;Gardine et al, 2011;Grandin et al, 2011;Ruppert et al, 2011;Maccaferri et al, 2016). On a distancetime graph the migrating seismicity often comprises two curves marking the migrating front and the line where the seismicity switches off, sometimes called the back-front (Brandsdóttir and Einarsson, 1979;Belachew et al, 2011;Grandin et al, 2011).…”

Section: Magmatic Hypothesismentioning

confidence: 99%

“…The source mechanisms and migration patterns of the hypocenters of volcanic and tectonic swarm earthquakes have helped to discern between different swarm-triggering processes, such as hydrofracturing, magmatic intrusion, pore-pressure diffusion, and slow-slip events (Brandsdóttir and Einarsson, 1979;Patanè et al, 2003;Wolfe et al, 2007;Roland and McGuire, 2009;Gardine et al, 2011;Hainzl et al, 2012;Jay et al, 2012;Mattia et al, 2015;Gudmundsson et al, 2016;Alpala et al, 2017;Cattania et al, 2017;Passarelli et al, 2018).…”

Section: Introductionmentioning

confidence: 99%

See 1 more Smart Citation

Magmatic or Not Magmatic? The 2015–2016 Seismic Swarm at the Long-Dormant Jailolo Volcano, West Halmahera, Indonesia

et al. 2018

View full text Add to dashboard Cite

Seismic swarms close to volcanoes often signal the onset of unrest. Establishing whether magma is the culprit and the unrest can be flagged as magmatic may be challenging. Here we analyze the spatio-temporal pattern of a seismic swarm that occurred in November 2015-February 2016 around Jailolo volcano, a long-dormant and poorly studied volcano located on Halmahera island, North Moluccas, Indonesia. The swarm included four M w > 5 earthquakes and hundreds of events were felt by the population. We relocate the earthquakes using both the Indonesian Seismic Network and singlestation location techniques. We find that the earthquakes cluster in a narrow strip, stretching 5 km E-W and 20 km N-S, migrating southward away from Jailolo volcano at ∼10 km/d. We investigate the source mechanisms of the largest earthquakes via full moment tensor inversion. The non-double-couple component is around 50%, such that the earthquakes, besides normal faulting, included a relatively large opening component. After a thorough examination of the possible causes of the Jailolo swarm we conclude that a laterally propagating dike of tens of millions of cubic meters is the triggering mechanism for the seismicity. The swarm marks the first documented magmatic unrest at Jailolo. We find that there is a probability >0.1 that the unrest will last for more than 2 years. This magmatic unrest calls for the classification of Jailolo volcano as active, and for an urgent assessment of the associated volcanic hazard.

show abstract

“…Dikes may reach lengths of tens of km, delivering magma and feeding eruptions for significant distances also outside volcanoes. However, dikes may often become arrested and not generate any eruption (e.g., Gardine et al, 2011). Several recent studies highlight the extremely rapid transfer of magma, up to m/s, from the mantle or shallower levels, even for rhyolitic compositions and in apparently unfavorable tectonic conditions (Castro and Dingwell, 2009;Ruprecht and Plank, 2013).…”

Section: Challenge 2: Propagation and Arrest Of Magmamentioning

confidence: 99%

Great challenges in volcanology: how does the volcano factory work?

Acocella

2014

Front. Earth Sci.

View full text Add to dashboard Cite

Dike emplacement near Parícutin volcano, Mexico in 2006

Cited by 32 publications

References 26 publications

Failed magmatic eruptions: late-stage cessation of magma ascent

Failed magmatic eruptions: late-stage cessation of magma ascent

Magmatic or Not Magmatic? The 2015–2016 Seismic Swarm at the Long-Dormant Jailolo Volcano, West Halmahera, Indonesia

Great challenges in volcanology: how does the volcano factory work?

Contact Info

Product

Resources

About