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Journal articles on the topic 'Lava Dome'

Author: Grafiati

Published: 4 June 2021

Last updated: 12 February 2022

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1

Starodubtseva, Yu V., I. S. Starodubtsev, A. T. Ismail-Zadeh, I. A. Tsepelev, O. E. Melnik, and A. I. Korotkii. "A Method for Magma Viscosity Assessment by Lava Dome Morphology." Journal of Volcanology and Seismology 15, no. 3 (May 2021): 159–68. http://dx.doi.org/10.1134/s0742046321030064.

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Abstract Lava domes form when a highly viscous magma erupts on the surface. Several types of lava dome morphology can be distinguished depending on the flow rate and the rheology of magma: obelisks, lava lobes, and endogenic structures. The viscosity of magma nonlinearly depends on the volume fraction of crystals and temperature. Here we present an approach to magma viscosity estimation based on a comparison of observed and simulated morphological forms of lava domes. We consider a two-dimensional axisymmetric model of magma extrusion on the surface and lava dome evolution, and assume that the lava viscosity depends only on the volume fraction of crystals. The crystallization is associated with a growth of the liquidus temperature due to the volatile loss from the magma, and it is determined by the characteristic time of crystal content growth (CCGT) and the discharge rate. Lava domes are modeled using a finite-volume method implemented in Ansys Fluent software for various CCGTs and volcanic vent sizes. For a selected eruption duration a set of morphological shapes of domes (shapes of the interface between lava dome and air) is obtained. Lava dome shapes modeled this way are compared with the observed shape of the lava dome (synthesized in the study by a random modification of one of the calculated shapes). To estimate magma viscosity, the deviation between the observed dome shape and the simulated dome shapes is assessed by three functionals: the symmetric difference, the peak signal-to-noise ratio, and the structural similarity index measure. These functionals are often used in the computer vision and in image processing. Although each functional allows to determine the best fit between the modeled and observed shapes of lava dome, the functional based on the structural similarity index measure performs it better. The viscosity of the observed dome can be then approximated by the viscosity of the modeled dome, which shape fits best the shape of the observed dome. This approach can be extended to three-dimensional case studies to restore the conditions of natural lava dome growth.

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2

Tsepelev, Igor, Alik Ismail-Zadeh, and Oleg Melnik. "Lava dome morphology inferred from numerical modelling." Geophysical Journal International 223, no. 3 (August 21, 2020): 1597–609. http://dx.doi.org/10.1093/gji/ggaa395.

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SUMMARY Lava domes form when highly viscous magmas erupt on the surface. Several types of lava dome morphology can be distinguished depending on the flow rate and the rheology of magma. Here, we develop a 2-D axisymmetric model of magma extrusion on the surface and lava dome evolution and analyse the dome morphology using a finite-volume method implemented in Ansys Fluent software. The magma/lava viscosity depends on the volume fraction of crystals and temperature. We show that the morphology of domes is influenced by two parameters: the characteristic time of crystal content growth (CCGT) and the discharge rate (DR). At smaller values of the CCGTs, that is, at rapid lava crystallization, obelisk-shaped structures develop at low DRs and pancake-shaped structures at high DRs; at longer CCGTs, lava domes feature lobe- to pancake-shaped structures. A thick carapace of about 70 per cent crystal content evolves at smaller CCGTs. We demonstrate that cooling does not play the essential role during a lava dome emplacement, because the thermal thickness of the evolving carapace remains small in comparison with the dome's height. A transition from the endogenic to exogenic regime of the lava dome growth occurs after a rapid increase in the DR. A strain-rate-dependent lava viscosity leads to a more confined dome, but the influence of this viscosity on the dome morphology is not well pronounced. The model results can be used in assessments of the rates of magma extrusion, the lava viscosity and the morphology of active lava domes..

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3

Holland, A. S. Peter, I. Matthew Watson, Jeremy C. Phillips, Luca Caricchi, and Marika P. Dalton. "Degassing processes during lava dome growth: Insights from Santiaguito lava dome, Guatemala." Journal of Volcanology and Geothermal Research 202, no. 1-2 (April 2011): 153–66. http://dx.doi.org/10.1016/j.jvolgeores.2011.02.004.

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4

Darmawan, Herlan, Thomas R. Walter, Valentin R. Troll, and Agus Budi-Santoso. "Structural weakening of the Merapi dome identified by drone photogrammetry after the 2010 eruption." Natural Hazards and Earth System Sciences 18, no. 12 (December 12, 2018): 3267–81. http://dx.doi.org/10.5194/nhess-18-3267-2018.

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Abstract. Lava domes are subjected to structural weakening that can lead to gravitational collapse and produce pyroclastic flows that may travel up to several kilometers from a volcano's summit. At Merapi volcano, Indonesia, pyroclastic flows are a major hazard, frequently causing high numbers of casualties. After the Volcanic Explosivity Index 4 eruption in 2010, a new lava dome developed on Merapi volcano and was structurally destabilized by six steam-driven explosions between 2012 and 2014. Previous studies revealed that the explosions produced elongated open fissures and a delineated block in the southern dome sector. Here, we investigated the geomorphology, structures, thermal fingerprint, alteration mapping and hazard potential of the Merapi lava dome by using drone-based geomorphologic data and forward-looking thermal infrared images. The block on the southern dome of Merapi is delineated by a horseshoe-shaped structure with a maximum depth of 8 m and it is located on the unbuttressed southern steep flank. We identify intense thermal, fumarole and hydrothermal alteration activities along this horseshoe-shaped structure. We conjecture that hydrothermal alteration may weaken the horseshoe-shaped structure, which then may develop into a failure plane that can lead to gravitational collapse. To test this instability hypothesis, we calculated the factor of safety and ran a numerical model of block-and-ash flow using Titan2D. Results of the factor of safety analysis confirm that intense rainfall events may reduce the internal friction and thus gradually destabilize the dome. The titan2D model suggests that a hypothetical gravitational collapse of the delineated unstable dome sector may travel southward for up to 4 km. This study highlights the relevance of gradual structural weakening of lava domes, which can influence the development fumaroles and hydrothermal alteration activities of cooling lava domes for years after initial emplacement.

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5

Chen, Yuchao, Qian Huang, Jiannan Zhao, and Xiangyun Hu. "Unsupervised Machine Learning on Domes in the Lunar Gardner Region: Implications for Dome Classification and Local Magmatic Activities on the Moon." Remote Sensing 13, no. 5 (February 24, 2021): 845. http://dx.doi.org/10.3390/rs13050845.

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Lunar volcanic domes are essential windows into the local magmatic activities on the Moon. Classification of domes is a useful way to figure out the relationship between dome appearances and formation processes. Previous studies of dome classification were manually or semi-automatically carried out either qualitatively or quantitively. We applied an unsupervised machine-learning method to domes that are annularly or radially distributed around Gardner, a unique central-vent volcano located in the northern part of the Mare Tranquillitatis. High-resolution lunar imaging and spectral data were used to extract morphometric and spectral properties of domes in both the Gardner volcano and its surrounding region in the Mare Tranquillitatis. An integrated robust Fuzzy C-Means clustering algorithm was performed on 120 combinations of five morphometric (diameter, area, height, surface volume, and slope) and two elemental features (FeO and TiO2 contents) to find the optimum combination. Rheological features of domes and their dike formation parameters were calculated for dome-forming lava explanations. Results show that diameter, area, surface volume, and slope are the selected optimum features for dome clustering. 54 studied domes can be grouped into four dome clusters (DC1 to DC4). DC1 domes are relatively small, steep, and close to the Gardner volcano, with forming lavas of high viscosities and low effusion rates, representing the latest Eratosthenian dome formation stage of the Gardner volcano. Domes of DC2 to DC4 are relatively large, smooth, and widely distributed, with forming lavas of low viscosities and high effusion rates, representing magmatic activities varying from Imbrian to Eratosthenian in the northern Mare Tranquillitatis. The integrated algorithm provides a new and independent way to figure out the representative properties of lunar domes and helps us further clarify the relationship between dome clusters and local magma activities of the Moon.

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6

Sakimoto, S. E. H., and M. T. Zuber. "The spreading of variable-viscosity axisymmetric radial gravity currents: applications to the emplacement of Venusian ‘pancake’ domes." Journal of Fluid Mechanics 301 (October 25, 1995): 65–77. http://dx.doi.org/10.1017/s0022112095003806.

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The Magellan images of Venus have revealed a number of intriguing volcanic features, including the steep-sided or ‘pancake’ domes. These volcanic domes or flows have morphologies that suggest formation by a single continuous emplacement of lava with a higher viscosity than that of the surrounding basaltic plains. Numerous investigators have suggested that such high viscosity is due to high silica content, leading to the conclusion that the domes are evidence of evolved magmatic products on Venus. However, viscosity depends on crystallinity as well as on silica content: high viscosity could therefore also be due to a cooler (and therefore higher crystal content) lava. Models of dome emplacement which include both cooling and composition factors are thus necessary in order to determine the ranges of crystallinity and silica content which might lead to the observed gross dome morphologies. Accordingly, in this study domes are modelled as radial viscous gravity currents with an assumed cooling-induced viscosity increase to include both effects. Analytical and numerical results indicate that pancake dome formation is feasible with compositions ranging from basaltic to rhyolitic. Therefore, observations of gross dome morphology alone are insufficient for determining composition and the domes do not necessarily represent strong evidence for evolved magmatism on Venus.

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7

Wadge, G., G. Ryan, and E. S. Calder. "Clastic and core lava components of a silicic lava dome." Geology 37, no. 6 (June 2009): 551–54. http://dx.doi.org/10.1130/g25747a.1.

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8

Barmin, A., O. Melnik, and R. S. J. Sparks. "Periodic behavior in lava dome eruptions." Earth and Planetary Science Letters 199, no. 1-2 (May 2002): 173–84. http://dx.doi.org/10.1016/s0012-821x(02)00557-5.

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9

Manley, Curtis R. "Lava dome collapse causes pyroclastic flows." Eos, Transactions American Geophysical Union 74, no. 27 (1993): 306. http://dx.doi.org/10.1029/93eo00453.

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10

Melnik, O., and R. S. J. Sparks. "Nonlinear dynamics of lava dome extrusion." Nature 402, no. 6757 (November 1999): 37–41. http://dx.doi.org/10.1038/46950.

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11

Wolpert, Robert L., Sarah E. Ogburn, and Eliza S. Calder. "The longevity of lava dome eruptions." Journal of Geophysical Research: Solid Earth 121, no. 2 (February 2016): 676–86. http://dx.doi.org/10.1002/2015jb012435.

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12

BALMFORTH, N. J., A. S. BURBIDGE, R. V. CRASTER, J. SALZIG, and A. SHEN. "Visco-plastic models of isothermal lava domes." Journal of Fluid Mechanics 403 (January 25, 2000): 37–65. http://dx.doi.org/10.1017/s0022112099006916.

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The dynamics of expanding domes of isothermal lava are studied by treating the lava as a viscoplastic material with the Herschel–Bulkley constitutive law. Thin-layer theory is developed for radially symmetric extrusions onto horizontal plates. This provides an evolution equation for the thickness of the fluid that can be used to model expanding isothermal lava domes. Numerical and analytical solutions are derived that explore the effects of yield stress, shear thinning and basal sliding on the dome evolution. The results are briefly compared with an experimental study. It is found that it is difficult to unravel the combined effects of shear thinning and yield stress; this may prove important to studies that attempt to infer yield stress from morphology of flowing lava.

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13

Hyman, David M., M. I. Bursik, and E. B. Pitman. "Pressure-driven gas flow in viscously deformable porous media: application to lava domes." Journal of Fluid Mechanics 869 (April 18, 2019): 85–109. http://dx.doi.org/10.1017/jfm.2019.211.

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The behaviour of low-viscosity, pressure-driven compressible pore fluid flows in viscously deformable porous media is studied here with specific application to gas flow in lava domes. The combined flow of gas and lava is shown to be governed by a two-equation set of nonlinear mixed hyperbolic–parabolic type partial differential equations describing the evolution of gas pore pressure and lava porosity. Steady state solution of this system is achieved when the gas pore pressure is magmastatic and the porosity profile accommodates the magmastatic pressure condition by increased compaction of the medium with depth. A one-dimensional (vertical) numerical linear stability analysis (LSA) is presented here. As a consequence of the pore-fluid compressibility and the presence of gravitation compaction, the gradients present in the steady-state solution cause variable coefficients in the linearized equations which generate instability in the LSA despite the diffusion-like and dissipative terms in the original system. The onset of this instability is shown to be strongly controlled by the thickness of the flow and the maximum porosity, itself a function of the mass flow rate of gas. Numerical solutions of the fully nonlinear system are also presented and exhibit nonlinear wave propagation features such as shock formation. As applied to gas flow within lava domes, the details of this dynamics help explain observations of cyclic lava dome extrusion and explosion episodes. Because the instability is stronger in thicker flows, the continued extrusion and thickening of a lava dome constitutes an increasing likelihood of instability onset, pressure wave growth and ultimately explosion.

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14

Mania, René, Thomas R. Walter, Marina Belousova, Alexander Belousov, and Sergey L. Senyukov. "Deformations and Morphology Changes Associated with the 2016–2017 Eruption Sequence at Bezymianny Volcano, Kamchatka." Remote Sensing 11, no. 11 (May 29, 2019): 1278. http://dx.doi.org/10.3390/rs11111278.

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Lava domes grow by extrusions and intrusions of viscous magma often initiating from a central volcanic vent, and they are frequently defining the source region of hazardous explosive eruptions and pyroclastic density currents. Thus, close monitoring of dome building processes is crucial, but often limited to low data resolution, hazardous access, and poor visibility. Here, we investigated the 2016–2017 eruptive sequence of the dome building Bezymianny volcano, Kamchatka, with spot-mode TerraSAR-X acquisitions, and complement the analysis with webcam imagery and seismic data. Our results reveal clear morphometric changes preceding eruptions that are associated with intrusions and extrusions. Pixel offset measurements show >7 months of precursory plug extrusion, being locally defined and exceeding 30 m of deformation, chiefly without detected seismicity. After a short explosion, three months of lava dome evolution were characterised by extrusions and intrusion. Our data suggest that the growth mechanisms were significantly governed by magma supply rate and shallow upper conduit solidification that deflected magmatic intrusions into the uppermost parts of the dome. The integrated approach contributes significantly to a better understanding of precursory activity and complex growth interactions at dome building volcanoes, and shows that intrusive and extrusive growth is acting in chorus at Bezymianny volcano.

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15

Bani, Philipson, Syegi Kunrat, and Devy Kamil Syahbana. "Insights into the recurrent energetic eruptions that drive Awu, among the deadliest volcanoes on Earth." Natural Hazards and Earth System Sciences 20, no. 8 (August 7, 2020): 2119–32. http://dx.doi.org/10.5194/nhess-20-2119-2020.

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Abstract. The little-known Awu volcano (Sangihe Islands, Indonesia) is among the deadliest, with a cumulative death toll of 11 048. In less than 4 centuries, 18 eruptions were recorded, including two VEI 4 and three VEI 3 eruptions with worldwide impacts. The regional geodynamic setting is controlled by a divergent-double-subduction collision and an arc–arc collision. In that context, the slab stalls in the mantle, undergoes an increase in temperature, and becomes prone to melting, a process that sustained the magmatic supply. Awu also has the particularity of hosting alternatively and simultaneously a lava dome and a crater lake throughout its activity. The lava dome passively erupted through the crater lake and induced strong water evaporation from the crater. A conduit plug associated with this dome emplacement subsequently channeled the gas emission to the crater wall. However, with the lava dome cooling, the high annual rainfall eventually reconstituted the crater lake and created a hazardous situation on Awu. Indeed with a new magma injection, rapid pressure buildup may pulverize the conduit plug and the lava dome, allowing lake water injection and subsequent explosive water–magma interaction. The past vigorous eruptions are likely induced by these phenomena, possible scenarios for future events.

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16

Clemmensen, Lars B. "Aeolian morpho_logy preserved by lava cover, the Precambrian Mussartut Member, Eriksfjord Formation, South Greenland." Bulletin of the Geological Society of Denmark 37 (October 14, 1988): 105–16. http://dx.doi.org/10.37570/bgsd-1988-37-09.

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Investigations of sedimentary deposits in elastic interval 5 of the Mussartilt Member have revealed the occurrence of aeolian sandstones. The aeolian deposits rest on pebbly sandstones and conglomerates of fluvial origin, and the are sharply overlain by a c. 70 m thick lava flow. The aeolian sandstones comprise up to 10 m thick and 200 m wide dome-shaped bodies that are initiated by thin and patchily preserved aeolian sand sheet deposits. The bulk of the aeolian sandstone bodies constitute low-medium-angle, dipping lee-side deposits of dome-shaped dunes. The dome-shaped dunes migrated towards a zone of distal alluvial fans perhaps during the influence of prevailing NE trade winds. Superimposed smaller-scale dunes formed during periodic strong winds from the E. Erosion of the dunes at the base of the lava flow was insignificant and most of the original dome-shape form of the dunes seems to have been preserved. The dome-shaped dunes may represent part of a migrating erg system, but continued dune migration was stopped by extrusion of the lava flow.

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17

NAKADA, SETSUYA. "Diversity of the eruption of a lava dome." Journal of Geography (Chigaku Zasshi) 105, no. 2 (1996): 244–45. http://dx.doi.org/10.5026/jgeography.105.2_244.

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18

Baptie, B. J. "Lava dome collapse detected using passive seismic interferometry." Geophysical Research Letters 37, no. 19 (March 27, 2010): n/a. http://dx.doi.org/10.1029/2010gl042489.

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19

Price, Stephen F., and Joseph S. Walder. "Modeling the dynamic response of a crater glacier to lava-dome emplacement: Mount St Helens, Washington, USA." Annals of Glaciology 45 (2007): 21–28. http://dx.doi.org/10.3189/172756407782282525.

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AbstractThe debris-rich glacier that grew in the crater of Mount St Helens after the volcano’s cataclysmic 1980 eruption was split in two by a new lava dome in 2004. For nearly six months, the eastern part of the glacier was squeezed against the crater wall as the lava dome expanded. Glacier thickness nearly doubled locally and surface speed increased substantially. As squeezing slowed and then stopped, surface speed fell and ice was redistributed downglacier. This sequence of events, which amounts to a field-scale experiment on the deformation of debris-rich ice at high strain rates, was interpreted using a two-dimensional flowband model. The best match between modeled and observed glacier surface motion, both vertical and horizontal, requires ice that is about 5 times stiffer and 1.2 times denser than normal, temperate ice. Results also indicate that lateral squeezing, and by inference lava-dome growth adjacent to the glacier, likely slowed over a period of about 30 days rather than stopping abruptly. This finding is supported by geodetic data documenting dome growth.

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20

Andaru, R., and J. Y. Rau. "LAVA DOME CHANGES DETECTION AT AGUNG MOUNTAIN DURING HIGH LEVEL OF VOLCANIC ACTIVITY USING UAV PHOTOGRAMMETRY." ISPRS - International Archives of the Photogrammetry, Remote Sensing and Spatial Information Sciences XLII-2/W13 (June 4, 2019): 173–79. http://dx.doi.org/10.5194/isprs-archives-xlii-2-w13-173-2019.

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<p><strong>Abstract.</strong> Lava dome changes detection during increasingly high volcanic activity are essential for hazard assessment purposes. However, it is challenging to conduct direct field measurement due to safety reason. Here, we investigate the lava dome changes of Mount Agung in Indonesia during the highest level of volcanic activity. On 22 September 2017, the rumbling and seismic activity in this volcano started increasing to the highest level for a period of time. We afterwards collected image data at lava dome area by using UAV over this time period. To accomplish the goal of change detection, we assembled and developed a fixed-wing UAV platform, i.e. Buffalo FX-79 to acquire images of Mount Agung whose elevation is roughly 3,142&thinsp;m above sea level. We acquired the UAV images on two dates, i.e. Oct 19 and Oct 21 of 2017. Due to an exclusion zone surround the volcano, we could only operate the UAV at 20&thinsp;km distance from the crater. With these data set, we produced three-dimensional point clouds, high-resolution Digital Elevation Model and orthophoto by using Structure from Motion (SfM) and Multi View Stereo (SfM-MVS) technique with Photoscan Pro software. From orthophoto data, we found two fluid areas at the crater's surface in NE direction (4,375.9&thinsp;sq-m) and SE direction (3,749.8&thinsp;sq-m). We also detected a fumarole which emitted steam and gases in the eastern part that continued for several days. In order to reveal the changes in lava dome surface, we used DEM to create cross-section profile. After that, we applied cloud to cloud comparison (C2C) algorithm to calculate the difference of lava dome based on two data set of point clouds and compared it with interferometric result from Sentinel-1A data. The data from the Sentinel-1A satellite (15 Oct &ndash; 27 Oct 2017) were processed to obtain the interferogram image of Mount Agung. This research therefore demonstrates a potential method to detect lava dome changes during high level of volcanic activity with photogrammetric methods by using UAV images. Within only two days the data were successfully acquired. From the DEM data and cross-section profile between two data set, we noticed that no significant surface change was found around the lava dome surface. Moreover, we also found that there was no significant lava dome changes and vertical displacement during these two time periods as the point cloud comparison and distance result. The average of difference distance is 2.27&thinsp;cm with a maximal and minimal displacement of 255&thinsp;cm and 0.37&thinsp;cm respectively. This result was then validated by using InSAR Sentinel that showed small displacement, i.e 6.88&thinsp;cm. It indicated that UAV photogrammetry showed a good performance to detect surface changes in centimeter fraction.</p>

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Andryushchenko, V. A., V. A. Goloveshkin, I. V. Murashkin, and N. N. Kholin. "Destruction of the Lava Dome of an Underwater Volcano." Mechanics of Solids 54, no. 5 (September 2019): 780–85. http://dx.doi.org/10.3103/s0025654419050030.

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Wadge, Geoffrey, David G. Macfarlane, Michael R. James, Henry M. Odbert, L. Jane Applegarth, H. Pinkerton, Duncan A. Robertson, et al. "Imaging a growing lava dome with a portable radar." Eos, Transactions American Geophysical Union 87, no. 23 (2006): 226. http://dx.doi.org/10.1029/2006eo230003.

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23

Sparks, R. S. J. "Causes and consequences of pressurisation in lava dome eruptions." Earth and Planetary Science Letters 150, no. 3-4 (August 1997): 177–89. http://dx.doi.org/10.1016/s0012-821x(97)00109-x.

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24

Buisson, C., and O. Merle. "Experiments on internal strain in lava dome cross sections." Bulletin of Volcanology 64, no. 6 (June 18, 2002): 363–71. http://dx.doi.org/10.1007/s00445-002-0213-6.

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25

von Aulock, F. W., A. R. L. Nichols, B. M. Kennedy, and C. Oze. "Timescales of texture development in a cooling lava dome." Geochimica et Cosmochimica Acta 114 (August 2013): 72–80. http://dx.doi.org/10.1016/j.gca.2013.03.012.

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Mueller, S. B., N. R. Varley, U. Kueppers, P. Lesage, G. Á. Reyes Davila, and D. B. Dingwell. "Quantification of magma ascent rate through rockfall monitoring at the growing/collapsing lava dome of Volcán de Colima, Mexico." Solid Earth 4, no. 2 (July 11, 2013): 201–13. http://dx.doi.org/10.5194/se-4-201-2013.

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Abstract. The most recent eruptive phase of Volcán de Colima, Mexico, started in 1998 and was characterized by dome growth with a variable effusion rate, interrupted intermittently by explosive eruptions. Between November 2009 and June 2011, activity at the dome was mostly limited to a lobe on the western side where it had previously started overflowing the crater rim, leading to the generation of rockfall events. As a consequence of this, no significant increase in dome volume was perceivable and the rate of magma ascent, a crucial parameter for volcano monitoring and hazard assessment could no longer be quantified via measurements of the dome's dimensions. Here, we present alternative approaches to quantify the magma ascent rate. We estimate the volume of individual rockfalls through the detailed analysis of sets of photographs (before and after individual rockfall events). The relationship between volume and infrared images of the freshly exposed dome surface and the seismic signals related to the rockfall events were then investigated. Larger rockfall events exhibited a correlation between its previously estimated volume and the surface temperature of the freshly exposed dome surface, as well as the mean temperature of rockfall mass distributed over the slope. We showed that for larger events, the volume of the rockfall correlates with the maximum temperature of the newly exposed lava dome as well as a proxy for seismic energy. It was therefore possible to calibrate the seismic signals using the volumes estimated from photographs and the count of rockfalls over a certain period was used to estimate the magma extrusion flux for the period investigated. Over the course of the measurement period, significant changes were observed in number of rockfalls, rockfall volume and hence averaged extrusion rate. The extrusion rate was not constant: it increased from 0.008 ± 0.003 to 0.02 ± 0.007 m3 s−1 during 2010 and dropped down to 0.008 ± 0.003 m3 s−1 again in March 2011. In June 2011, magma extrusion had come to a halt. The methodology presented represents a reliable tool to constrain the growth rate of domes that are repeatedly affected by partial collapses. There is a good correlation between thermal and seismic energies and rockfall volume. Thus it is possible to calibrate the seismic records associated with the rockfalls (a continuous monitoring tool) to improve volcano monitoring at volcanoes with active dome growth.

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Mueller, S. B., N. R. Varley, U. Kueppers, P. Lesage, G. Á. Reyes Davila, and D. B. Dingwell. "Quantification of magma ascent rate through rockfall monitoring at the growing/collapsing lava dome of Volcán de Colima, Mexico." Solid Earth Discussions 5, no. 1 (January 15, 2013): 1–39. http://dx.doi.org/10.5194/sed-5-1-2013.

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Abstract. The most recent eruptive phase of Volcán de Colima, Mexico, started in 1998 and was characterized by episodic dome growth with a variable effusion rate, interrupted intermittently by explosive eruptions. Between November 2009 and June 2011, growth at the dome was limited to a lobe on the western side where it had previously started overflowing the crater rim, leading to the generation of rockfall events. This meant that no significant increase in dome volume was perceivable and the rate of magma ascent, a crucial parameter for volcano monitoring and hazard assessment, could no longer be quantified via measurements of the dome's dimensions. Here, we present alternative approaches to quantify the magma ascent rate. We estimate the volume of individual rockfalls through the detailed analysis of sets of photographs (before and after individual rockfall events). The relationship between volume and infrared images of the freshly exposed dome surface and the seismic signals related to the rockfall events was then investigated. Larger events exhibited a correlation between the previously estimated volume of a rockfall and the surface temperature of the freshly exposed dome surface as well as the mean temperature of rockfall masses distributed over the slope. We showed that for larger events, the volume of the rockfall correlates with the maximum temperature at the newly formed cliff as well as the seismic energy. By calibrating the seismic signals using the volumes estimated from photographs, the count of rockfalls over a certain period was used to estimate the magma extrusion flux for the period investigated. Over the course of the measurement period, significant changes were observed in number of rockfalls, rockfall volume and hence averaged extrusion rate. The extrusion rate was not constant: it increased from 0.008 m3 s−1 to 0.02 m3 s−1 during 2010 and dropped down to 0.008 m3 s−1 again in March 2011. In June 2011, magma extrusion had come to a halt. The methodology presented represents a reliable tool to constrain the growth rate of domes that are repeatedly affected by partial collapses. There is a good correlation between thermal and seismic energies and rockfall volume. Thus it is possible to calibrate the seismic records associated with the rockfalls (a continuous monitoring tool) to improve both volcano monitoring at volcanoes with active dome growth and hazard management associated with rockfalls specifically.

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Pistone, Mattia, Alan G. Whittington, Benjamin J. Andrews, and Elizabeth Cottrell. "Crystal-rich lava dome extrusion during vesiculation: An experimental study." Journal of Volcanology and Geothermal Research 347 (November 2017): 1–14. http://dx.doi.org/10.1016/j.jvolgeores.2017.06.018.

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Johnson, Jeffrey B., and Jonathan M. Lees. "Sound produced by the rapidly inflating Santiaguito lava dome, Guatemala." Geophysical Research Letters 37, no. 22 (November 2010): n/a. http://dx.doi.org/10.1029/2010gl045217.

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Hale, A. J. "Lava dome growth and evolution with an independently deformable talus." Geophysical Journal International 174, no. 1 (July 2008): 391–417. http://dx.doi.org/10.1111/j.1365-246x.2008.03806.x.

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Miyamachi, Hiroki, Hidefumi Watanabe, Takeo Moriya, and Hiromu Okada. "Seismic experiments on Showa-Shinzan lava dome using firework shots." Pure and Applied Geophysics PAGEOPH 125, no. 6 (1987): 1025–37. http://dx.doi.org/10.1007/bf00879366.

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Harris, Andrew J., William I. Rose, and Luke P. Flynn. "Temporal trends in lava dome extrusion at Santiaguito 1922–2000." Bulletin of Volcanology 65, no. 2 (March 2003): 77–89. http://dx.doi.org/10.1007/s00445-002-0243-0.

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Horwell, Claire J., Jennifer S. Le Blond, Sabina A. K. Michnowicz, and Gordon Cressey. "Cristobalite in a rhyolitic lava dome: evolution of ash hazard." Bulletin of Volcanology 72, no. 2 (December 2, 2009): 249–53. http://dx.doi.org/10.1007/s00445-009-0327-1.

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34

Harnett, Claire E., and Michael J. Heap. "Mechanical and topographic factors influencing lava dome growth and collapse." Journal of Volcanology and Geothermal Research 420 (December 2021): 107398. http://dx.doi.org/10.1016/j.jvolgeores.2021.107398.

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35

Soetoyo, Soetoyo. "GUNUNGAPI KARUA DI DAERAH PANAS BUMI BITTUANG, TANA TORAJA, SULAWESI SELATAN:SALAH SATU GUNUNGAPI AKTIF TIPE B(?) DI INDONESIA." Buletin Sumber Daya Geologi 5, no. 1 (May 31, 2010): 27–34. http://dx.doi.org/10.47599/bsdg.v5i1.253.

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Gunungapi Karua merupakan Gunungapi strato yang pembentukannya dimulai pada Kuarter Bawah. Gunungapi soliter di Kabupaten Tana Toraja, Sulawesi Selatan ini geomorfologinya terdiri dari: Satuan morfologi Puncak Gunungapi Karua, Tubuh Gunungapi Karua, dan Kaki Gunungapi Karua. Batuan penyusunnya diawali dengan lava berkomposisi andesit dan produk selanjutnya mengarah ke dasitik.Pada akhir periode pembentukan terjadi letusan besar dan terbentuk Kaldera Karua berbentuk Tapal kuda, yang membuka kearah utara. Kegiatan Gunungapi Karua diakhiri oleh pembentukan lava dome pada bagian puncaknya. Akhir kegiatan Gunungapi Karua, meninggalkan sebuah kaldera dan lava dome yang berada di tengah-tengah Kaldera Karua.Sisa kegiatan lain berupa hembusan gas solfatara, air panas dan lapangan solfatara yang berada pada graben sempit di tubuh bagian selatan Gunungapi Karua.Gunungapi Karua tidak pernah bererupsi lagi pada masa sejarah, tetapi menurut informasi penduduk setempat, pernah terlihat asap tebal dipuncak Gunungapi Karua, yang ditafsirkan sebagai asap yang keluar dari puncak Gunungapi Karua.Gunungapi Karua dapat diklasifikasikan sebagai gunungapi Tipe B (?) dan merupakan tambahan kelompok gunungapi aktif di Indonesia.

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GRIFFITHS, ROSS W., and JONATHAN H. FINK. "Solidifying Bingham extrusions: a model for the growth of silicic lava domes." Journal of Fluid Mechanics 347 (September 25, 1997): 13–36. http://dx.doi.org/10.1017/s0022112097006344.

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In a previous study of the effects of cooling and solidification on flows issuing onto a horizontal plane and spreading under gravity we considered the case of a viscous fluid that solidifies to form a thin surface crust with a finite yield strength. In that case, the coupling of solidification and viscous stresses in the flow led to a sequence of flow regimes or styles of flow and crustal deformation. Here, we study the spreading, from a small source, of a plastic material having a yield strength before cooling. In this case the fluid again begins to freeze as it spreads radially under gravity, and forms a dome having a surface crust which is stronger than the extruded fluid. If cooling is sufficiently rapid compared to gravity-driven spreading, the flow is found to be controlled by solidification. The flow again takes on one of a number of flow regimes depending on the pace of solidification relative to the rate of lateral flow, or extrusion rate. However, these flow regimes are quite different from those for the viscous extrusions, implying that the internal yield stress has a strong influence on the behaviour. Styles of flow ranged from inflation of an axisymmetric dome to irregular extrusion of lateral lobes and vertical spines. These qualitatively different regimes have much in common with the eruption styles of volcanic lava domes produced by effusion of extremely viscous silicic magmas which may possess a yield strength, and the model provides information about the factors influencing the morphology and hazards of such volcanic flows.

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Loughlin, S. C., R. Luckett, G. Ryan, T. Christopher, V. Hards, S. De Angelis, L. Jones, and M. Strutt. "An overview of lava dome evolution, dome collapse and cyclicity at Soufrière Hills Volcano, Montserrat, 2005-2007." Geophysical Research Letters 37, no. 19 (May 1, 2010): n/a. http://dx.doi.org/10.1029/2010gl042547.

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Leroy, Jacques L., Rodolfo Rodriguez-Rios, and Sarah Dewonck. "The topaz-bearing rhyolites from the San Luis Potosi area (Mexico): characteristics of the lava and growth conditions of topaz." Bulletin de la Société Géologique de France 173, no. 6 (November 1, 2002): 579–88. http://dx.doi.org/10.2113/173.6.579.

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Abstract In Mexico, the topaz-bearing rhyolites occur mainly in the San Luis Potosi area (San Luis Potosi and Guanajuato States). These rhyolites appear as domes related to the Tertiary extensional tectonism. Three domes of the San Luis Potosi volcanic field were selected for study, according to the color, the habits and the size of the topaz they contain, in order to determine the characteristics of the lava and the growth conditions of the topaz. These rhyolites are high-silica, metaluminous to slightly peraluminous and alkali-rich lavas. They are enriched in fluorine and in incompatible lithophile elements such as Rb, Cs, Ta, U and Th and depleted in Ba, Sr, Ca, Mg, Ti and Ni. Therefore, they are very similar to the topaz-bearing rhyolites from western United States. In Cerro El Gato dome, both amber-colored and colorless topazes crystallized in voids and fractures. Comparing these different crystals with respect to their growth environment, habits, chemical compositions and EPR characteristics provides an explanation for the crystallization conditions and color of topaz. Colorless topaz from Cerro El Gato crystallized at a temperature above 500oC (lack of color centers) from fluids enriched in elements leached from the lava, whereas the amber-colored topaz crystallized below 500oC (based on the presence of color centers) and from fluids richer in volatile elements (As). In Cerro El Lobo, the topaz have intermediate characteristics between the colorless and the amber-colored topazes of Cerro El Gato.

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Dawid, Sepry, Ferdy Ferdy, and Guntur Pasau. "PENENTUAN LOKASI PERGERAKAN MAGMA GUNUNG API SOPUTAN BERDASARKAN STUDI SEBARAN HIPOSENTER GEMPA VULKANIK PERIODE MEI 2013 – MEI 2014." JURNAL ILMIAH SAINS 17, no. 1 (August 14, 2015): 88. http://dx.doi.org/10.35799/jis.15.2.2015.9222.

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PENENTUAN LOKASI PERGERAKAN MAGMA GUNUNG API SOPUTAN BERDASARKAN STUDI SEBARAN HIPOSENTER GEMPA VULKANIK PERIODE MEI 2013 – MEI 2014 ABSTRAK Gunung api Soputan merupakan gunungapi type strato yang aktif hingga saat ini. Aktifitasnya diduga dimulai pada masa plistosen bawah (kurang lebih 1,8 juta tahun yang lalu). Gempa vulkanik merupakan gempa yang terjadi akibat aktivitas gunungapi. Hal ini disebabkan oleh pergerakan magma ke atas di dalam gunungapi. Penelitian ini bertujuan untuk mengetahui letak hiposenter gempa vulkanik serta mengetahui letak pergerakan magma Gunung Soputan. Prinsip dari penelitian ini dilakukan dengan menganalisis data gempa vulkanik periode Mei 2013 – Mei 2014 yang berupa data sekunder dari hasil rekaman (seismogram) Gunung Soputan pada 3 stasiun seismometer yaitu stasiun Aesoput, Winorangian, dan Silian. Data gempa diolah dengan menggunakan software seismologi yang ada. Hasil penelitian menunjukkan bahwa distribusi hiposenter gempa vulkanik Gunungapi Soputan menyebar pada daerah kubah lava dan cenderung kearah barat laut, dengan kedalaman 100 m –– 8000 m di bawah kubah lava. Dari hasil analisa hiposenter diketahui terjadi pergerakan magma oleh gempa vulkanik dalam (VA), hal ini disebabkan posisi hiposenter yang naik menuju kubah lava. Kata Kunci: Gunung Soputan, Hiposenter, dan Pergerakan Magma ABSTRACT Soputan volcano is strato volcano that active till today. Its activity supposed began at down Pleistocene (1,8 million years ago). Volcanic earthquake is one of matter that caused by volcano. This happened because magmatic movement inside volcano. This research aimed to know location of hypocenter also to know location of magmatic movement Soputan volcano. Principles from this researchis conducted by analyzing volcanic earthquake data at May 2013 to May 2014 that consist secondary data from recording data (seismogram) volcano Soputan on 3 stations seismometer are Aesoput station, Winorangian, and Silian. The earthquake data processed using seismologic software. Result researchis shows that distribution of hypocenter volcanic earthquake soputan volcano scattered at lava dome area and inclined to northwest, that located on depth 100 m to 8000 m from lava dome. Result from hipocenter analyse to find a magmatic movement by deep volcanic earthquake (VA), this happened because position of hypocenter up movement to lava dome. Keywords: Mount Soputan, Hipocenter, and Magmatic Movement

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40

Wooster, M. J., T. Kaneko, S. Nakada, and H. Shimizu. "Discrimination of lava dome activity styles using satellite-derived thermal structures." Journal of Volcanology and Geothermal Research 102, no. 1-2 (October 2000): 97–118. http://dx.doi.org/10.1016/s0377-0273(00)00183-9.

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41

Jutzeler, Martin, Jocelyn McPhie, and Sharon R. Allen. "Explosive destruction of a Pliocene hot lava dome underwater: Dogashima (Japan)." Journal of Volcanology and Geothermal Research 304 (October 2015): 75–81. http://dx.doi.org/10.1016/j.jvolgeores.2015.08.009.

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42

Fink, Jonathan H., Michael C. Malin, and Steven W. Anderson. "Intrusive and extrusive growth of the Mount St Helens lava dome." Nature 348, no. 6300 (November 1990): 435–37. http://dx.doi.org/10.1038/348435a0.

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43

Costa, A., O. Melnik, and R. S. J. Sparks. "Controls of conduit geometry and wallrock elasticity on lava dome eruptions." Earth and Planetary Science Letters 260, no. 1-2 (August 2007): 137–51. http://dx.doi.org/10.1016/j.epsl.2007.05.024.

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44

Fink, J. H., and N. T. Bridges. "Effects of eruption history and cooling rate on lava dome growth." Bulletin of Volcanology 57, no. 4 (August 1995): 229–39. http://dx.doi.org/10.1007/bf00265423.

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45

Zorn, Edgar U., Thomas R. Walter, Michael J. Heap, and Ulrich Kueppers. "Insights into lava dome and spine extrusion using analogue sandbox experiments." Earth and Planetary Science Letters 551 (December 2020): 116571. http://dx.doi.org/10.1016/j.epsl.2020.116571.

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46

KARACIK, ZEKIYE, and SENGUL C. GENÇ. "Volcano-stratigraphy of the extension-related silicic volcanism of the Çubukludağ Graben, western Turkey: an example of generation of pyroclastic density currents." Geological Magazine 151, no. 3 (July 19, 2013): 492–516. http://dx.doi.org/10.1017/s0016756813000435.

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AbstractWestern Turkey's extension-related Cumaovası volcanic rocks (Lower Miocene, 17 Ma) are excellent examples of silicic eruptions. The sub-aerial silicic volcanism at Çubukludağ Graben between İzmir and Kuşadası in west–central Anatolia is mainly in the form of rhyolite domes, lava flows and pyroclastic deposits. The initial features of volcanism derived from phreatomagmatic explosive eruptions from silicic magma that came into contact with lake waters during Neogene times. Most of the volcanic succession represents pyroclastic density currents (PDCs), known as the Kuner ignimbrite. The deposits are fine grained and laminated at the base and pass laterally and vertically into deposits displaying well-developed traction structures, soft sediment deformation and/or erosion channels in the NE part of the region. Alternate deposits of massive, diffusely stratified lapilli and ash are the main products of the later explosive stage. Massive lithic breccias forming the top of the sequences are the proximal facies of the PDCs. The lava phase mainly consists of rhyolite extruded as dome and fissure eruptions of lavas, aligned along NE–SW-trending faults as well as from extensional cracks that are nearly perpendicular to the main graben faults. Considering the tectono-stratigraphical aspects and geochemical nature of the study area, we propose that the Cumaovası silicic volcanism was produced by extension-related crustal melting during the Late–Early Miocene period (17 Ma).

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Walder, Joseph S., Richard G. LaHusen, James W. Vallance, and Steve P. Schilling. "Emplacement of a silicic lava dome through a crater glacier: Mount St Helens, 2004–06." Annals of Glaciology 45 (2007): 14–20. http://dx.doi.org/10.3189/172756407782282426.

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AbstractThe process of lava-dome emplacement through a glacier was observed for the first time after Mount St Helens reawakened in September 2004. The glacier that had grown in the crater since the cataclysmic 1980 eruption was split in two by the new lava dome. The two parts of the glacier were successively squeezed against the crater wall. Photography, photogrammetry and geodetic measurements document glacier deformation of an extreme variety, with strain rates of extraordinary magnitude as compared to normal alpine glaciers. Unlike normal temperate glaciers, the crater glacier shows no evidence of either speed-up at the beginning of the ablation season or diurnal speed fluctuations during the ablation season. Thus there is evidently no slip of the glacier over its bed. The most reasonable explanation for this anomaly is that meltwater penetrating the glacier is captured by a thick layer of coarse rubble at the bed and then enters the volcano’s groundwater system rather than flowing through a drainage network along the bed.

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Watt, Sebastian F. L., David M. Pyle, and Tamsin A. Mather. "Geology, petrology and geochemistry of the dome complex of Huequi volcano, southern Chile." Andean Geology 38, no. 2 (August 9, 2011): 335. http://dx.doi.org/10.5027/andgeov38n2-a05.

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Huequi, a little-known volcano in the southern part of the Andean southern volcanic zone (SSVZ), shows a regionally unusual eruption style, mineralogy and geochemistry. The volcano comprises multiple highly-eroded lava domes. Past eruptions were accompanied by relatively minor explosive activity, most recently from 1890-1920. The rocks erupted by Huequi range from basaltic andesite to dacite, and are highly distinctive when compared to other volcanoes of the SSVZ, being K-poor and Al-rich, and containing euhedral hornblende phenocrysts. Overall compositions suggest a notably water-rich magma source, evolving through high levels of fractionation and subsequent degassing to produce highly porphyritic dome-forming andesites. The ultimate causes of water-rich magmas at this point in the arc remain unclear.

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Kasama, Tomohiro, Hiroyuki Yamashita, Kazutaka Mannen, Mitsuru Okuno, and Toshio Nakamura. "Futagoyama lava dome of Hakone volcano: an edifice formed by multiple eruptions." Journal of the Geological Society of Japan 116, no. 4 (2010): 229–32. http://dx.doi.org/10.5575/geosoc.116.229.

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KITAKAZE, Arashi. "Sulfide blebs in andesite from the lava dome, Tarumai volcano, Hokkaido, Japan." Japanese Magazine of Mineralogical and Petrological Sciences 39, no. 3 (2010): 104–9. http://dx.doi.org/10.2465/gkk.090318.

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