Relevant bibliographies by topics / Lava Dome

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Academic literature on the topic 'Lava Dome'

Author: Grafiati
Published: 4 June 2021
Last updated: 12 February 2022

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Journal articles on the topic "Lava Dome"

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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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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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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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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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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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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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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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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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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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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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Dissertations / Theses on the topic "Lava Dome"

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Holland, Alastair Simon Peter. "Degassing processes at Santiaguito lava dome, Guatemala." Thesis, University of Bristol, 2011. http://ethos.bl.uk/OrderDetails.do?uin=uk.bl.ethos.558078.

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This thesis focuses on using spectroscopic gas emissions data to understand degassing processes occurring during low-intensity explosive activity at Santiaguito lava dome, Guatemala. It results in a refinement of the ultra violet camera spectroscopic technique; the proposal of a trigger mechanism for low-intensity explosions during lava dome growth; and the first successful modelling of an unsteady explosion plume. The ultra violet camera provides high spatial and temporal resolution spectroscopic measurements of volcanic 802, However, data collection is difficult under the non-ideal conditions typically encountered at silicic volcanoes. A new processing protocol is developed that corrects for plume-instrument distance and in-plume ash/aerosols, permitting data collection at 8antiaguito. The resulting dataset is used to constrain the trigger mechanism of 8antiaguito explosions. The lava dome is found to be continuously permeable, whilst explosions contain as little as 150 kg 802 - characteristics incompatible with gas pressurisation beneath an impermeable plug. Rather, the data support a model in which transient explosive degassing pathways are generated at the conduit margins through shear-driven fracturing. Rheological modelling shows that this process is likely to occur during even extremely slow extrusion of high-crystallinity intermediate magma, on account of the very high viscosity of such magma. This model is further supported by the discovery of tuffisite veins in Santiaguito dacite. Santiaguito explosions form short-duration plumes that may be used as observable proxies for larger Vulcanian plumes. Ultra violet camera data have been used to define time-varying boundary conditions for a cutting-edge unsteady plume model. This represents a first attempt to compare field observations of a volcanic plume with model predictions using field-derived boundary conditions. The resulting simulation closely recreates the observed plume ascent, in contrast to approximations made using steady and instantaneous plume models. This explicitly shows that unsteady effects are critical to understanding Vulcanian plume dynamics.
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Ball, Jessica Lynne. "Field and numerical investigations of lava dome hydrothermal systems and their effects on dome stability." Thesis, State University of New York at Buffalo, 2014. http://pqdtopen.proquest.com/#viewpdf?dispub=3612916.

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This study investigates the potential for hydrothermal alteration and circulation in lava domes using combined analytical, remote sensing and numerical modeling approaches. This has been accomplished in three parts: 1) A comprehensive field, geochemical and remote sensing investigation was undertaken of the hydrothermal system in the Santiaguito lava dome complex in Guatemala. The Santiaguito domes were found to contain mainly hydrous silica alteration, which is unlikely to weaken dome rock, but the summit of Santa Maria was found to contain pervasive argillic alteration (clay minerals), which do pose more of a collapse-related hazard. These results were confirmed by hot spring geochemistry which indicated that water in the domes was responsible for some rock dissolution but had a residence time too short to allow for secondary mineralization. 2) A finite element numerical modeling approach was developed which was designed to simulate the percolation of meteoric water in two dome geometries (crater-confined and 'perched'), and the results were compared to the surface expression of hydrothermal systems on existing lava domes. In both cases, we concluded that simulated domes which lacked a high-temperature (magmatic) heat source could not develop a convecting hydrothermal system and were dominated by gravitational water flow. In these low-temperature simulations, warm springs (warmer high fluid fluxes) were produced at the base of the dome talus and cool springs were dispersed lower down the slope/substrate; fumaroles (high vapor fluxes) were confined to the dome summits. Comparison with existing dome cross sections indicates that the simulations were accurate in predicting fumarole locations and somewhat accurate at predicting spring locations, suggesting that springs may be subject to permeability contrasts created by more complicated structural features than were simulated in this study. 3) The results of the numerical modeling were used to calculate alteration potential in the simulated domes, indicating the most likely areas where alteration processes might either reduce the strength of a dome or reduce permeability that could contribute to internal pressurization. Rock alteration potential in low-temperature lava domes was found to be controlled by material permeability and the presence or absence of a sustained heat source driving hydrothermal circulation. High RAI values were preserved longer in low-permeability domes, but were more strongly developed in domes with higher permeabilities. Potential for mineral dissolution was highest at the base of the dome core, while the potential for mineral precipitation is highest at the dome core-talus interface. If precipitated minerals are impermeable, the dome core/talus interface would be a likely location for accumulation of gases and initiation of gas-pressurization-related collapse; if alteration is depositing weak (i.e. clay) minerals in this area, the dome core/talus interface might be a candidate for collapses occurring as the result of alteration processes.

The results of this study are all geared toward answering two broad questions: Where are hydrothermal alteration processes likely to occur or be focused within lava domes? and What effect could these processes have on dome stability? In the specific case of the Santiaguito dome complex, the combination of a quickly-recharged, low-temperature hydrothermal system in the inactive domes actually indicated a low possibility of collapse related to alteration minerals. This result was reinforced by the results of the numerical modeling, which indicated that domes are unlikely to develop sustained hydrothermal convection without the presence of a significant (magmatic) heat source and—in the case of Santiaguito—are likely to produce more hydrous silica alteration minerals when they also lack a source of acidic gases. Models of alteration potential do detail, however, that both shallow and deep dome collapses are still a possibility with a low-temperature hydrothermal system, given either a) a source of acidic gases to drive the formation of clay minerals (which are most likely to be deposited at the core/talus interface of a dome, or b) enough deposition of silica minerals in pore spaces to lower permeability in dome rock and promote internal gas pressurization. The results of this study are not limited to lava domes, as the volcanic edifices on which they rest are composed of the same materials that comprise lava domes and are therefore susceptible to the same hydrothermal processes. Further simulations of both lava domes and their associated edifices, including mineral species models, could help constrain under what conditions a lava dome or volcano is likely to develop areas of weak mineral precipitates (such as clay minerals) which could provide sites for collapse, or develop an impermeable cap of silicate minerals which could trap rising vapor and contribute to the pressurization of the edifice in question (which can in turn lead to collapse).

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Hale, Alina Jane. "Computationally Modelling the Lava Dome at Soufriere Hills Volcano, Montserrat." Thesis, University of Reading, 2005. http://ethos.bl.uk/OrderDetails.do?uin=uk.bl.ethos.485361.

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Finite element method (FEM) models using the commercially available software package FASTFLO and traditional low-level computational programming methods have been used to consider the Peleean lava dome extruded on Soufriere Hills Volcano, Montserrat. Phenomenological nonNewtonian models are used to describe the complex rheology of the lava and time-dependent processes. Four research areas are studied: endogenous dome growth, the transition from endogenous to exogenous dome growth, conduit flow dynamics and the stability of structures containing lava domes. An elasto-viscoplastic FEM model is used to analyse the rheological gradients and the growth and evolution of an endogenous lava dome. The transition from endogenous to exogenous dome growth is an important process in Peleean lava domes. It is found that the development of shear planes within the conduit and lava dome ultimately govern this process and that the lava must be non-Newtonian for shear planes to form. Temporal non-linearities observed in the extrusion rate for Soufriere Hills Volcano are analysed in conduit flow models. Accelerating extrusion rates can be explained by a change in magma chamber over-pressure and a 'rheological memory' associated with the magma. Non-Newtonian magma may form unstable shear planes due to gas over-pressure in the conduit and it is thought that this process is responsible for hybrid seismicity and oscillatory flow. Model results show a first order fit to the cyclicity behaviour observed. The graZritational instability of lava domes may be influenced by viscous relaxation. Instability models show a possible time-delayed collapse mechanism as well as enhanced front lobe toppling. Numerical models are only as useful as the data used to constrain them and due to a paucity of data these models should be regarded as qualitative rather than quantitative.
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Lamb, O. D. "Monitoring lava dome eruptions : a seismic, acoustic and experimental study." Thesis, University of Liverpool, 2017. http://livrepository.liverpool.ac.uk/3008537/.

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Lava dome eruptions are one of the most dangerous forms of volcanic activity. Geophysical, experimental, field or numerical investigations over the past few decades have improved our understanding of dynamic processes associated with these eruptions. In this thesis, I use multi-disciplinary approaches to analyse unrest at four different volcanoes: Volcán de Colima, Unzen, Santiaguito dome complex and Mt. Redoubt. At Volcán de Colima, waveform correlation and seismic interferometry techniques are used to analyse seismic data collected prior to the November 1998 eruption. A decrease in seismic velocity is observed during pre-eruptive activity, consistent with rock failure caused by increased stress associated with the migration of magma towards the surface. This mechanism is confirmed by measurements during experimental Brazil tests on lava samples from the volcano. Furthermore, repetitive micro-cracking during the experiments suggest some repeating earthquakes detected at Volcán de Colima were produced by repeated tensile failure. At Unzen, I analyse seismic data collected during the formation of a lava spine during the last phase of the 1991-95 eruption. Two large groups of repeating earthquakes are identified and further analysis demonstrates how their sources migrated during their period of activation. Citing experimental and field observations, repeated slip motion along the margins of the spine are inferred as the source mechanisms for these earthquakes. Santiaguito dome complex is one of the most active volcanoes in the world, and here I present the first long-term seismo-acoustic dataset to be recorded at the volcano. The dataset captures a major transition in explosive activity that took place in 2015. Variations in energies and waveform arrival times are used to gain insights into the explosion source dynamics. During its eruption in 2009, Mt. Redoubt volcano erupted 19 times, at least 16 of which produced ash plumes tall enough to disrupt air traffic in the region. Using infrasound data recorded during two of these explosions and a three-dimensional plume rise model, I demonstrate how it is possible to efficiently and accurately estimate the ash plume height soon after an eruption begins. These four case studies demonstrate how using a combination of geophysical, experimental, numerical, and field observations can provide more robust interpretations of dynamic processes prior to or during lava dome eruptions. Therefore, multi-disciplinary approaches to studying volcanic activity can have important implications for hazard assessments at active volcanoes worldwide.
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Hornby, A. J. "Fracture, friction and fragmentation : brittle processes at lava dome volcanoes." Thesis, University of Liverpool, 2016. http://livrepository.liverpool.ac.uk/3005862/.

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The extent to which transitions from dominantly viscous to dominantly brittle magma deformation regulate eruptive activity has not been widely explored in volcanology. Within this thesis, investigations combining experiments, petrology and geophysical signals are presented to help decipher and understand the role of brittle deformation during lava dome eruptions. Lava domes are commonly associated with explosions and dome collapse events, both of which generate volcanic ash. In order to recognise and discriminate fragmentation mechanisms from ash samples, the physical properties and mineralogy of natural ash produced during a typical Vulcanian explosion and a dome collapse event were compared. Measurements of the componentry of several thousand ash particles were conducted using QEMSCAN® Particle Mineralogical Analysis, a rapid automated SEM-EDS mapping technique. Analysis of images obtained by QEMSCAN® reveals that the relative distribution of plagioclase and glass present along the ash particle boundaries varied for both generation mechanisms. Deconvolution of particle size distributions and particle shape analyses shows that ash ejected in Vulcanian explosions has a more complex fragmentation and transport history, while ash produced in pyroclastic flows shows the dominance of a single process. These results suggest mechanism-dependent controls on the surface composition and componentry of volcanic ash – future work is required to discriminate fragmentation mechanisms from ash characteristics through the use of QEMSCAN® data. Explosive fragmentation at lava dome volcanoes is likely to be triggered by tensile failure of magma following stress accumulation. In order to investigate pressure-driven fracturing of conduit magma, Brazilian tensile tests were conducted on lava samples from Santiaguito volcano at ambient and magmatic temperatures. These tests reveal that deformation style becomes sensitive to small changes in temperature and strain rate at temperatures of 750-800 °C. Higher temperatures generated increasingly viscous deformation, while faster strain rates promoted more brittle behaviour. Experimental constraints on the strain rate and strain leading to failure can be compared to natural deformation timescales recorded in cycles of inflation preceding explosions at Santiaguito, which shows that a viscous component accompanies deformation and suggests that fractures propagate away from a pressure source prior to explosive eruption. Following fracture propagation, any remaining energy is likely to be accommodated by fault slip along the fracture plane. These faulting events are investigated using a high-velocity rotary shear apparatus, showing that the response to faulting generates temperatures sufficient to produce frictional melt within ~10 cm of slip under the slip rates and normal stresses constrained through monitoring of the volcanic behaviour at Santiaguito. The range of mechanical response to slip events in the volcanic conduit and their relation to concurrent seismic signals are investigated in greater detail during the extrusion of a lava spine at Mt Unzen (Japan). Examination of textures at the spine margins and similarity of the seismic signals that accompanied its extrusion has determined that spine emplacement proceeds by incremental fault slip events in the shallow edifice. Waveform analysis together with spine growth observations allow calculation of the average slip distance (8.9 cm) and slip velocity (0.75 m.s-1). These calculations are combined with results from laboratory measurements in a high-velocity rotary shear apparatus to define the range of depths where average faulting events would induce viscous remobilisation (at >275m) and frictional melting along the fault plane (at >500 m). The frictional properties of the dome rocks and the viscosity of the frictional melt in the fault zone suggest that at shallow depths frictional melts act as a viscous brake to fault slip, potentially augmenting stick-slip spine growth. Taken together, the failure, faulting and fragmentation of dome-forming magma demonstrates that our interpretation of eruptive activity at lava dome volcanoes requires a fundamental understanding of brittle processes.
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Scott, Jeannie A. J. "Origin and evolution of the Santiaguito lava dome complex, Guatemala." Thesis, University of Oxford, 2013. http://ora.ox.ac.uk/objects/uuid:d6e6be78-4464-4b6d-b236-46e22ff8826d.

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Subduction zone volcanoes are a major natural hazard, frequently endangering lives and livelihoods. The eruptive history of many subduction zone volcanoes includes the extrusion of blocky, silicic lava that forms domes or flows, but we do not yet understand what determines the duration of dome-forming behaviour, what path magma may take to the surface, or how these systems may change over time. This thesis presents an investigation of the Santiaguito complex of lava domes and flows in Guatemala, which has been erupting continuously since its inception in 1922. The Santiaguito lavas are predominantly dacitic to andesitic, with a gradual reduction in SiO2 content from ~66 wt% in the 1920s, to ~62 wt% in 2002. This is consistent with a ~15% decrease in the extent of fractional crystallization over that time. The compositions of plagioclase phenocryst cores indicate a diminished role for magma mixing after the 1940s. I model the Santiaguito system as progressively extracting magma from an extensive, chemically-stratified storage zone. Petrological data are consistent with a storage zone extending from ~25 to ~12 km depth, and magma storage temperatures of ~940 to ~980°C. Phenocryst-hosted apatites suggest melt in this storage zone contained 401 to 1199 ppm S, 600 to 1300 ppm F, and 4100 to 6200 ppm Cl. Ascending magma may pass slowly through a conduit bottleneck, or plug, at shallow depths; groundmass texture suggests that melt rigidifies at or near the base this plug. Pre-eruptive melt volatile concentrations suggest time-averaged fluxes of 40 to 263 Mg d-1 SO2, 32 to 145 Mg d-1 HF, and 247 to 708 Mg d-1 HCl, giving ratios of 0.6 to 0.8 HF/SO2, and 2.7 to 6.2 HCl/SO2. These results are consistent with the few direct measurements of SO2 at Santiaguito, and with measured halogen emissions from other silicic dome-forming systems.
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Kingsbury, Cole G. "Physical Volcanology of Obsidian Dome, California: A Complex Record of Emplacement of a Youthful Lava Dome." Thèse, Université d'Ottawa / University of Ottawa, 2012. http://hdl.handle.net/10393/22840.

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Obsidian Dome is a 550-650 year old, 1.5 by 1.8 km extrusion of high silica rhyolite situated along the Inyo Craters in eastern California. Field, and observations of drill core, reveals discrete metre-scale thick zones of rhyolitic glass exposed along the margin of Obsidian Dome as well as within its interior. Millimetre-scale flow-banded obsidian, pumice and rhyolite range from planar to chaotically folded, the latter a product of ductile, compressive deformation. Fractures, some of which display en-echelon splitting patterns are a result of brittle failure. Taken together, these features along with others, result from flow during lava dome growth and suggest complex emplacement patterns signified by vesiculation, crystallization and repeated brittle-ductile deformation, owing to episodic crossing of the glass transition. Evidence further shows that gas loss from the system occurred due to explosions, pumice formation and also brecciation of the melt as it episodically crossed the glass transition. Loss of gas by these mechanisms along with the inherent high viscosity of rhyolite melt explains the large amount of glass found on and within Obsidian Dome and other similar rhyolite extrusions in comparison to less silica-rich systems.
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Ashwell, Paul. "Controls on rhyolite lava dome eruptions in the Taupo Volcanic Zone." Thesis, University of Canterbury. Geological Sciences, 2014. http://hdl.handle.net/10092/8965.

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The evolution of rhyolitic lava from effusion to cessation of activity is poorly understood. Recent lava dome eruptions at Unzen, Colima, Chaiten and Soufrière Hills have vastly increased our knowledge on the changes in behaviour of active domes. However, in ancient domes, little knowledge of the evolution of individual extrusion events exists. Instead, internal structures and facies variations can be used to assess the mechanisms of eruption. Rhyolitic magma rising in a conduit vesiculates and undergoes shear, such that lava erupting at the surface will be a mix of glass and sheared vesicles that form a permeable network, and with or without phenocryst or microlites. This foam will undergo compression from overburden in the shallow conduit and lava dome, forcing the vesicles to close and affecting the permeable network. High temperature, uniaxial compression experiments on crystal-rich and crystal-poor lavas have quantified the evolution of porosity and permeability in such environments. The deformation mechanisms involved in uniaxial deformation are viscous deformation and cracking. Crack production is controlled by strain rate and crystallinity, as strain is localised in crystals in crystal rich lavas. In crystal poor lavas, high strain rates result in long cracks that drastically increase permeability at low strain. Numerous and small cracks in crystal rich lavas allow the permeable network to remain open (although at a lower permeability than undeformed samples) while the porosity decreases. Flow bands result from shear movement within the conduit. Upon extrusion, these bands will become modified from movement of lava, and can therefore be used to reconstruct styles of eruption. Both Ngongotaha and Ruawahia domes, from Rotorua caldera and Okataina caldera complex (OCC) respectively, show complex flow banding that can be traced to elongated or aligned vents. The northernmost lobe at Ngongotaha exhibits a fan-like distribution of flow bands that are interpreted as resulting from an initial lava flow from a N – S trending fissure. This flow then transitioned into intrusion of obsidian sheets directly above the conduit, bound by wide breccia zones which show vertical movement of the sheets. Progressive intrusions then forced the sheets laterally, forming a sequence of sheets and breccia zones. At Ruawahia, the flow bands show two types of eruption; long flow lobes with ramp structures, and smaller spiny lobes which show vertical movement and possible spine extrusion. The difference is likely due to palaeotopography, as a large pyroclastic cone would have confined the small domes, while the flow lobes were unconfined and able to flow down slope. The vents at Ruawahia are aligned in a NE – SW orientation. Both domes are suggested to have formed from the intrusion of a dyke. The orientations of the alignment or elongation of vents at Ngongotaha and Ruawahia can be attributed to the overall regional structure of the Taupo Volcanic Zone (TVZ). At Ngongotaha, the N – S trending elongated vent is suggested to be controlled by a N – S trending caldera collapse structure at Rotorua caldera. The rest of the lobes at Ngongotaha, as well as other domes at Rotorua caldera, are controlled by the NE – SW trending extensional regional structure or a NW – SE trending basement structure. The collapse of Rotorua caldera, and geometry of the deformation margin, are related to the interplay of these structures. At Ruawahia, the NE – SW trending vent zone is parallel to the regional extension across the OCC, as shown by the orientation of intrusion of the 1886AD dyke through the Tarawera dome complex. The NE – SW trending regional structures observed at both Rotorua caldera and Okataina caldera complex are very similar to each other, but differ from extension within the Taupo rift to the south. Lava domes, such as Ngongotaha, that are controlled by this structure show that the ‘kink’ in the extension across Okataina caldera complex was active across Rotorua caldera during the collapse at 240 ka, and possibly earlier. This study shows the evolution of dyke-fed lava domes during eruption, and the control of regional structures in the location and timing of eruption. These findings improve our knowledge of the evolution of porosity and permeability in a compacting lava dome, as well as of the structures of Rotorua caldera, the longevity of volcanic activity at dormant calderas and the hazard potential of dyke-fed lava domes.
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9

Friedlander, Elizabeth Anne. "The nature and evolution of conduit faults in the 2004-2008 Mount St. Helens lava dome eruption." Thesis, University of British Columbia, 2012. http://hdl.handle.net/2429/40473.

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Mount St. Helens reawakened 24 years after erupting in the 1980’s. This effusive eruption produced 95 million cubic meters of dacite in the form of 7 discrete, competent spines or domes of lava between September 2004- June 2008. The spines comprise low-porosity dacite that is inferred to have crystallized at a depth of about 1 km and are enveloped by a 1-3 meter carapace of fault gouge. The rate of linear extrusion of the spines peaked at 11 m/day in November 2004 and subsequently slowed to < 0.5 m/day. Dome growth was accompanied by a “drumbeat” seismicity that was sourced from 1-0.5 km below the vent. Here, field, petrographic, and microstructural observations on the nature of deformation attending the extrusion of Spines 4, 5 and 7 at Mount St. Helens (2004-2006) are presented. The enveloping fault zones provide a static view of the cumulative strain produced by shear along the conduit wall. The conduit faults narrow from Spine 4 to Spine 7 and exhibit fewer macroscopic brittle features. Strain accommodation is achieved through a scale-dependent ductility. The subsurface ascent velocities for each packet of magma are reconstructed using surface observed extrusion rates. Computed shear strain rates for the margins of the conduit range from 1x10⁻⁴ to 7.9x10⁻⁵ s⁻¹. As ascent rate decreases, fault zone width also decreases maintaining an average shear strain rate of 4.3x10⁻⁵ s⁻¹. Intense strain localization within each fault zone is expressed by 0.001 m thick slickensides implying very high (co-seismic) transient shear-strain rates of 1x10⁻¹s⁻¹ (Spines 4-5) to 2.2x10⁻²s⁻¹ (Spine 7). I conclude with a time and space model for the evolution of the fault zone as magma ascends the conduit, and how the fault zones evolve through time. The factors that contribute to the differences in conduit fault zone width and nature throughout the eruption are: 1) differences in ascent rates at the onset and origin of brittle failure, 2) variations in shear strain rates, 3) and the increasing residence time throughout the eruption that the damaged fault rocks experienced at high temperatures within the conduit.
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Zorn, Edgar Ulrich Verfasser], Thomas [Akademischer Betreuer] Walter, and Ulrich [Gutachter] [Küppers. "Monitoring lava dome growth and deformation with photogrammetric methods and modelling / Edgar Ulrich Zorn ; Gutachter: Ulrich Küppers ; Betreuer: Thomas Walter." Potsdam : Universität Potsdam, 2020. http://d-nb.info/1223022455/34.

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Books on the topic "Lava Dome"

1

Holcomb, Robin T. Maps showing growth of the Lava Dome at Mount St. Helens, Washington. Reston, VA: U.S. Geological Survey, 1995.

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Fink, Jonathan H., ed. Lava Flows and Domes. Berlin, Heidelberg: Springer Berlin Heidelberg, 1990. http://dx.doi.org/10.1007/978-3-642-74379-5.

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Brzezinski, Zbigniew K. Cztery lata w Białym Domu: Wspomnienia doradcy do spraw bezpieczeństwa państwa 1977-1981. London: Polonia, 1986.

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Meyer, Karl-Heinz Schumacher and Wilhelm. Rheinische Landschaften Heft 57: Geopark Vulkanland Eifel: Lava-Dome Und Lavakeller in Mendig. Rheinischer Verein Fur Denkmalpflege Und Landschaftsschutz, 2006.

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Fink, Jonathan H. Lava Flows and Domes. Springer-Verlag Berlin and Heidelberg GmbH & Co. K, 1989.

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Fink, Jonathan H. Emplacement of Silicic Domes and Lava Flows. Geological Society of Amer, 1987.

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H, Fink Jonathan, and Geological Society of America. Meeting, eds. The Emplacement of silicic domes and lava flows. Boulder, Colo: Geological Society of America, 1987.

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The Emplacement of Silicic Domes and Lava Flows. Geological Society of America, 1987. http://dx.doi.org/10.1130/spe212.

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Fink, Jonathan H., and Gustav Wagner. Lava Flows and Domes: Emplacement Mechanisms and Hazard Implications. Springer, 2011.

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H, Fink Jonathan, and International Union of Geodesy and Geophysics., eds. Lava flows and domes: Emplacement mechanisms and hazard implications. Berlin: Springer-Verlag, 1990.

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Book chapters on the topic "Lava Dome"

1

Melnik, Oleg, R. Stephen J. Sparks, Antonio Costa, and Alexei A. Barmin. "Volcanic Eruptions: Cyclicity During Lava Dome Growth." In Encyclopedia of Complexity and Systems Science, 9763–84. New York, NY: Springer New York, 2009. http://dx.doi.org/10.1007/978-0-387-30440-3_578.

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Melnik, Oleg, R. Stephen J. Sparks, Antonio Costa, and Alexei A. Barmin. "Volcanic Eruptions: Cyclicity During Lava Dome Growth." In Extreme Environmental Events, 1035–81. New York, NY: Springer New York, 2011. http://dx.doi.org/10.1007/978-1-4419-7695-6_56.

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Melnik, Oleg, R. Stephen J. Sparks, Antonio Costa, and Alexei A. Barmin. "Volcanic Eruptions: Cyclicity During Lava Dome Growth." In Encyclopedia of Complexity and Systems Science, 1–28. Berlin, Heidelberg: Springer Berlin Heidelberg, 2019. http://dx.doi.org/10.1007/978-3-642-27737-5_578-2.

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Melnik, Oleg, R. Stephen J. Sparks, Antonio Costa, and Alexei A. Barmin. "Volcanic Eruptions: Cyclicity During Lava Dome Growth." In Complexity in Tsunamis, Volcanoes, and their Hazards, 619–46. New York, NY: Springer US, 2021. http://dx.doi.org/10.1007/978-1-0716-1705-2_578.

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Fadeli, A. "Volcanic Earthquakes at Merapi (Central Java) During the Lava Dome Building Beginning in October 1986." In IAVCEI Proceedings in Volcanology, 62–73. Berlin, Heidelberg: Springer Berlin Heidelberg, 1992. http://dx.doi.org/10.1007/978-3-642-77008-1_5.

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Blake, S. "Viscoplastic Models of Lava Domes." In IAVCEI Proceedings in Volcanology, 88–126. Berlin, Heidelberg: Springer Berlin Heidelberg, 1990. http://dx.doi.org/10.1007/978-3-642-74379-5_5.

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Têtu, M., M. Chamberland, P. Tremblay, C. Beaulieu, S. Paquet, A. Fekecs, G. Lessard, M. L. Charès, and C. Laperle. "Photonics Applied to Phased Array Antennas: Work Done at Université Laval." In Applications of Photonic Technology, 157–62. Boston, MA: Springer US, 1995. http://dx.doi.org/10.1007/978-1-4757-9247-8_31.

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Kubanek, Julia, Malte Westerhaus, and Bernhard Heck. "On the Use of Bistatic TanDEM-X Images to Quantify Volumetric Changes of Active Lava Domes." In International Association of Geodesy Symposia, 427–33. Cham: Springer International Publishing, 2015. http://dx.doi.org/10.1007/1345_2015_172.

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Iverson, R. M. "Lava Domes Modeled as Brittle Shells that Enclose Pressurized Magma, with Application to Mount St. Helens." In IAVCEI Proceedings in Volcanology, 47–69. Berlin, Heidelberg: Springer Berlin Heidelberg, 1990. http://dx.doi.org/10.1007/978-3-642-74379-5_3.

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"lava dome." In Dictionary Geotechnical Engineering/Wörterbuch GeoTechnik, 786. Berlin, Heidelberg: Springer Berlin Heidelberg, 2014. http://dx.doi.org/10.1007/978-3-642-41714-6_120719.

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Conference papers on the topic "Lava Dome"

1

Keenan, Martin P., and Paul Ashwell. "MODELING LAVA DOME COLLAPSE USING CORRELATION BETWEEN POROSITY AND UNCONFINED COMPRESSIVE STRENGTH." In GSA Annual Meeting in Denver, Colorado, USA - 2016. Geological Society of America, 2016. http://dx.doi.org/10.1130/abs/2016am-284238.

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Campo, Chloe, and Kurt Knesel. "PRE-ERUPTIVE TEMPERATURES AND ERUPTION DYNAMICS OF RHYOLITE LAVA, NIMBIN RHYOLITE DOME COMPLEX, EASTERN AUSTRALIA." In 54th Annual GSA North-Central Section Meeting - 2020. Geological Society of America, 2020. http://dx.doi.org/10.1130/abs/2020nc-348134.

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Grabsky, Varlen, F. Velázquez-Carreón, S. Aguilar, J. Urrutia-Fucugauchi, and J. Zmeskal. "Prototype-module of a muon tracker to investigate the density distribution of the Popocatepetl volcano lava dome." In 36th International Cosmic Ray Conference. Trieste, Italy: Sissa Medialab, 2019. http://dx.doi.org/10.22323/1.358.0275.

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Saepuloh, Asep, Ketut Wikantika, and Minoru Urai. "Observing lava dome roughness on synthetic aperture radar (SAR) data: Case study at Mt. Sinabung and Merapi — Indonesia." In 2015 IEEE 5th Asia-Pacific Conference on Synthetic Aperture Radar (APSAR). IEEE, 2015. http://dx.doi.org/10.1109/apsar.2015.7306289.

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Dykstra, Brooke A., Zenja Seitzinger, and Kurt Knesel. "MICROLITE ORIENTATIONS AND STRAIN LOCALIZATION WITHIN THE BASAL SHEAR ZONE OF A LARGE RHYOLITE LAVA DOME, MINYON FALLS, AUSTRALIA." In 54th Annual GSA North-Central Section Meeting - 2020. Geological Society of America, 2020. http://dx.doi.org/10.1130/abs/2020nc-348339.

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Maher, Sean P., Jeffrey H. Tepper, Jeffrey H. Tepper, Paul Ashwell, and Paul Ashwell. "TRACKING THE GROWTH OF A TRACHYTE LAVA DOME ON AKAROA VOLCANO, NEW ZEALAND WITH STRUCTURAL OBSERVATIONS, GEOCHEMISTRY AND CRYSTAL SIZE DISTRIBUTIONS." In 112th Annual GSA Cordilleran Section Meeting. Geological Society of America, 2016. http://dx.doi.org/10.1130/abs/2016cd-274277.

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Casaus, Justin. "A PETROLOGIC EVALUATION OF THE LAYOU IGNIMBRITE AND MORNE TROIS PITON LAVA DOME: HOW DO CHANGES IN PRE-ERUPTIVE CONDITIONS AFFECT ERUPTIVE BEHAVIOR?" In Keck Proceedings. Keck Geology Consortium, 2018. http://dx.doi.org/10.18277/akrsg.2019.31.07.

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Canonica, G. W. W., J. C. Virchow, M. Kots, F. Zuccaro, E. Carzana, A. Vele, G. Georges, and S. Petruzzelli. "Efficacy and Safety of High ICS Dose Fixed-Combination ICS/LABA/LAMA pMDI Compared with ICS/LABA and ICS/LABA + LAMA in Patients with Uncontrolled Asthma: The TRIGGER Study." In American Thoracic Society 2019 International Conference, May 17-22, 2019 - Dallas, TX. American Thoracic Society, 2019. http://dx.doi.org/10.1164/ajrccm-conference.2019.199.1_meetingabstracts.a7362.

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Ludlam, Abadie P., Holli M. Frey, and Matthew R. F. Manon. "DECOMPRESSION INDUCED AMPHIBOLE BREAKDOWN IN LAVA DOMES ON DOMINICA, LESSER ANTILLES." In 53rd Annual GSA Northeastern Section Meeting - 2018. Geological Society of America, 2018. http://dx.doi.org/10.1130/abs/2018ne-311190.

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Buhl, Roland, Carl-Peter Criée, Peter Kardos, Claus Vogelmeier, Nadine Lossi, and Heinrich Worth. "Low rate of exacerbations following initiation of LABA/LAMA fixed-dose combinations: An analysis of the DACCORD real life study." In ERS International Congress 2017 abstracts. European Respiratory Society, 2017. http://dx.doi.org/10.1183/1393003.congress-2017.pa1070.

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Reports on the topic "Lava Dome"

1

Staack, G. C. Recovery of a tritaiated LANA sample for dose conversion factor determination. Office of Scientific and Technical Information (OSTI), November 2010. http://dx.doi.org/10.2172/1123138.

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Maps showing growth of the lava dome at Mount St. Helens, Washington, 1980-1986. US Geological Survey, 1995. http://dx.doi.org/10.3133/i2359.

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