Catastrophic caldera-forming eruptions: Thermomechanics and implications for eruption triggering and maximum caldera dimensions on Earth

Gregg, P. M.; Silva, De; Grosfils, E. B.; Parmigiani, John P.

doi:10.1016/j.jvolgeores.2012.06.009

Cited by 176 publications

(217 citation statements)

References 62 publications

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“…Such overpressures can be sufficient to trigger an eruption, as the roof of the shallow magma chamber can undergo to intensive heating that can significantly weaken the strength of the overlying rocks (Gregg et al, 2012(Gregg et al, , 2015. Another end-member for triggering the eruption could be when a fracture opens from surface or all through the host rock above the magma chamber if there is a pre-existing fault.…”

Section: Control Of Local Stress Field On Eruption Dynamics and Intenmentioning

confidence: 99%

Stress Field Control during Large Caldera-Forming Eruptions

Costa

Martı́

2016

Front. Earth Sci.

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Crustal stress field can have a significant influence on the way magma is channeled through the crust and erupted explosively at the surface. Large Caldera Forming Eruptions (LCFEs) can erupt hundreds to thousands of cubic kilometers of magma in a relatively short time along fissures under the control of a far-field extensional stress. The associated eruption intensities are estimated in the range 10 9 -10 11 kg/s. We analyse syn-eruptive dynamics of LCFEs, by simulating numerically explosive flow of magma through a shallow dyke conduit connected to a shallow magma (3-5 km deep) chamber that in turn is fed by a deeper magma reservoir (>∼10 km deep), both under the action of an extensional far-field stress. Results indicate that huge amounts of high viscosity silicic magma ( 10 7 > Pa s) can be erupted over timescales of a few to several hours. Our study provides answers to outstanding questions relating to the intensity and duration of catastrophic volcanic eruptions in the past. In addition, it presents far-reaching implications for the understanding of dynamics and intensity of large-magnitude volcanic eruptions on Earth and to highlight the necessity of a future research to advance our knowledge of these rare catastrophic events.

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Section: Control Of Local Stress Field On Eruption Dynamics and Intenmentioning

confidence: 99%

Stress Field Control during Large Caldera-Forming Eruptions

Costa

Martı́

2016

Front. Earth Sci.

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“…Taking advantage of previous advances in thermomechanical modeling of calderas (Gregg et al, 2012(Gregg et al, , 2013, we utilize COMSOL Multiphysics 4.4 in combination with MATLAB 2014b to develop and implement a temperature-dependent, viscoelastic FEM for a resurgent caldera (Figures 7, 8). COMSOL is utilized for mesh development (including adaptive meshing), and solving for stress, strain, and displacement in response to applied loads in a linear viscoelastic solid using a Maxwell-Weichert formulation.…”

Section: Modeling Resurgence At Tobamentioning

confidence: 99%

“…Uplift due to magma chamber growth is also highly dependent on crustal rheology (Del Negro et al, 2009;Gregg et al, 2012Gregg et al, , 2013. We investigate two end-member cases for the crustal rheology: constant viscosity and temperature-dependent viscosity.…”

Section: Modeling Resurgence At Tobamentioning

confidence: 99%

“…The resulting calderas are thought to form when the roof of the magma chamber collapses into the magma chamber. The collapse may happen late in the eruption sequence either due to loss of support or underpressure caused by evacuation of the magma (e.g., Roche and Druitt, 2001) or early in the eruption due to failure of a weak and extended roof into a perched and primed magma reservoir (Gregg et al, 2012). After the "climactic" eruption and formation of the caldera, a period of recovery or "resurgence, " the afterparty to the big dance so to speak, is manifested as volcanic activity in the form of effusive lava eruptions and/or structural uplift of the caldera floor and intracaldera ignimbrite in the form of block uplift or a dome (Smith and Bailey, 1968;Acocella, 2007).…”

Section: Introductionmentioning

confidence: 99%

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Resurgent Tobaâ€”field, chronologic, and model constraints on time scales and mechanisms of resurgence at large calderas

et al. 2015

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Highlights• New data reveal for the first time a history of the last ∼33.7 ky of uplift of Samosir.• Minimum uplift rates were high (4.9 cm/year) for the first 11.2 ky but diminished after that to <1 cm/year for the last 22.5 ky.• Numerical modeling suggests that rebound of remnant magma augmented by deep recharge appears to be the most likely driver for uplift.• Detumescence makes a negligible contribution to resurgent uplift.• The volume of the resurgent dome is isostatically compensated by magma • Average rates of uplift at Toba are much lower than currently restless calderas indicating a distinction between resurgence and "restlessness".New data reveal details of the post-caldera history at the Earth's youngest resurgent supervolcano, Toba caldera in Sumatra. Resurgence after the caldera-forming ∼74 ka Youngest Toba Tuff eruption uplifted the caldera floor as a resurgent dome, Samosir Island, capped with 100 m of lake sediments. 14 C age data from the uppermost datable sediments reveal that Samosir Island was submerged beneath lake level (∼900 m a.s.l) at 33 ka. Since then, Samosir experienced 700 m of uplift as a tilted block dipping to the west. 14 C ages and elevations of sediment along a transect of Samosir reveal that minimum uplift rates were ∼4.9 cm/year from ∼33.7 to 22.5 ka, but diminished to ∼0.7 cm/year after 22.5 ka. Thermo-mechanical models informed by these rates reveal that detumescence does not produce the uplift nor the uplift rates estimated for Samosir. However, models calculating the effect of volume change of the magma reservoir within a temperature-dependent viscoelastic host rock reveal that a single pulse of ∼475 km 3 of magma produces a better fit to the uplift data than a constant flux. The cause of resurgent uplift of the caldera floor is rebound of remnant magma as the system re-established magmastatic and isostatic equilibrium after the caldera collapse. Previous assertions that the caldera floor was apparently at 400 m a.s.l or lower requires that uplift must have initiated between sometime between 33.7 and 74 ka at a minimum average uplift rate of ∼1.1 cm/year. The change in uplift rate from pre-33.7 ka to immediately post-33.7 ka suggests a role for deep recharge augmenting rebound. Average minimum rates of de Silva et al.Resurgence at Toba caldera, Sumatra resurgent uplift at Toba are at least an order of magnitude slower than net rates of "restlessness" at currently active calderas. This connotes a distinction between resurgence and "restlessness" controlled by different processes, scales of process, and controlling variables.

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“…The frequency of eruptions of M < 4 is potentially influenced by additional processes such as second boiling (Tait et al, 1989), and hence smaller eruptions may not satisfy the exchangeability assumption. Similarly, we restrict the upper bound of the data set to M7, as the processes triggering larger eruptions could differ from those responsible for eruptions of lower magnitude (Deligne et al, 2010;Gregg et al, 2012;Caricchi et al, 2014). To further satisfy the assumption of exchangeability and common geo-tectonic processes, we restrict the analysis to arc volcanoes.…”

Section: Datamentioning

confidence: 99%

Regional variability in the frequency and magnitude of large explosive volcanic eruptions

Sheldrake

Caricchi

2017

Geology

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Quantifying the frequency at which volcanic eruptions of different size occurs is important for hazard assessment. Volcanic records can be used to estimate the recurrence rate of large-magnitude eruptions (magnitude ≥4), but recording biases that impact data completeness complicate analysis. To overcome these biases, we conceptualize the volcanic record as a series of individual and unique time series associated by a common behavior. Thus, we approach issues of completeness on a volcano-by-volcano basis and use a hierarchical Bayesian approach to characterize the common frequency-magnitude (f-M) behavior for different groups of volcanoes. We identify variations in the f-M relationship between different volcano types and between different volcanic arcs. By accounting for systematic under-recording in the volcanic record, we also calculate the global recurrence rates for large-magnitude eruptions during the Holocene, which are similar to previous estimates. However, higher recurrence rates for smaller-magnitude events are observed, which is a result of our adjustments for data completeness. Quantifying how the f-M relationship varies between different groups of volcanoes provides an opportunity to understand how the tectonic setting influences f-M behavior, which is important to quantify long-term regional volcanic hazard.

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Catastrophic caldera-forming eruptions: Thermomechanics and implications for eruption triggering and maximum caldera dimensions on Earth

Cited by 176 publications

References 62 publications

Stress Field Control during Large Caldera-Forming Eruptions

Stress Field Control during Large Caldera-Forming Eruptions

Resurgent Tobaâ€”field, chronologic, and model constraints on time scales and mechanisms of resurgence at large calderas

Regional variability in the frequency and magnitude of large explosive volcanic eruptions

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