Journal articles: 'Lava flows'

1

Zschau, Jochen, and Malte Westerhaus. "Glowing Lava Flows." German Research 23, no. 1 (January 2001): 20–25. http://dx.doi.org/10.1002/germ.200100008.

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2

Bruno, B. C., G. J. Taylor, S. K. Rowland, P. G. Lucey, and S. Self. "Lava flows are fractals." Geophysical Research Letters 19, no. 3 (February 7, 1992): 305–8. http://dx.doi.org/10.1029/91gl03039.

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3

Kerr, Andrew Craig. "The geochemical stratigraphy, field relations and temporal variation of the Mull–Morvern Tertiary lava succession, NW Scotland." Transactions of the Royal Society of Edinburgh: Earth Sciences 86, no. 1 (1995): 35–47. http://dx.doi.org/10.1017/s0263593300002145.

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AbstractThe early Tertiary Mull-Morvern lava succession, NW Scotland, represents the thickest continuous section (1000 m from sea level to the top of Ben More) of Tertiary lavas exposed in the UK. This succession has been sampled and geochemically analysed, on a flow-by-flow basis, throughout the lava succession. Field observations during the course of this sampling suggest that the early lava flows (the Staffa Magma sub-Type) ponded in palaeovalleys along with interlava sediments. In the main part of the Mull lava succession (the Mull Plateau Group) the lava flows are on average ∼ 5 m thick. Most previous Hebridean workers have assumed that the red horizons commonly found between these later lava flows, represent weathered flow tops. However, this study has shown that in some places these red ‘boles’ appear to be a combination of both volcanic ash and weathered basalt.Chemically distinctive units of flows have been found throughout the succession. The two most abundant magma sub-types of the Mull Plateau Group, primitive (>9wt% MgO) basalts with Ba/Nb» 15 and more evolved (<9wt% MgO) basalts-hawaiites with Ba/Nb<15, form packets of flow units which can be up to 200 m thick. These chemically distinctive flow units have been correlated across the lava succession. However, the correlation of individual lava flows has proved difficult. The Mull Plateau Group lavas generally become more evolved and less contaminated with continental crust towards the top of the succession, culminating in the trachytes of the Pale Group on Ben More. Basaltic lavas above the Pale Group have markedly different trace element ratios, and seem to represent shallower, more extensive asthenospheric melting than the Mull Plateau Group.

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4

Sansone, Francis J., Joseph A. Resing, Gordon W. Tribble, Peter N. Sedwick, Kevin M. Kelly, and Ken Hon. "Lava-seawater interactions at shallow-water submarine lava flows." Geophysical Research Letters 18, no. 9 (September 1991): 1731–34. http://dx.doi.org/10.1029/91gl01279.

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5

Vilmundardóttir, Olga Kolbrún, Friðþór Sófus Sigurmundsson, Gro Birkefeldt Møller Pedersen, Joaquín Muñoz-Cobo Belart, Fadi Kizel, Nicola Falco, Jón Atli Benediktsson, and Guðrún Gísladóttir. "Of mosses and men: Plant succession, soil development and soil carbon accretion in the sub-Arctic volcanic landscape of Hekla, Iceland." Progress in Physical Geography: Earth and Environment 42, no. 6 (October 7, 2018): 765–91. http://dx.doi.org/10.1177/0309133318798754.

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Lava flows pose a hazard in volcanic environments and reset ecosystem development. A succession of dated lava flows provides the possibility to estimate the direction and rates of ecosystem development and can be used to predict future development. We examine plant succession, soil development and soil carbon (C) accretion on the historical (post 874 AD) lava flows formed by the Hekla volcano in south Iceland. Vegetation and soil measurements were conducted all around the volcano reflecting the diverse vegetation communities on the lavas, climatic conditions around Hekla mountain and various intensities in deposition of loose material. Multivariate analysis was used to identify groups with similar vegetation composition and patterns in the vegetation. The association of vegetation and soil parameters with lava age, mean annual temperature, mean annual precipitation and soil accumulation rate (SAR) was analysed. Soil carbon concentration increased with increasing lava age becoming comparable to concentrations found on the prehistoric lavas. The combination of a sub-Arctic climate, gradual soil thickening due to input of loose material and the specific properties of volcanic soils allow for continuing accumulation of soil carbon in the soil profile. Four successional stages were identified: initial colonization and cover coalescence (ICC) of Racomitrium lanuginosum and Stereocaulon spp. (lavas <70 years of age); secondary colonization (SC) – R. lanuginosum dominance (170−700 years); vascular plant dominance (VPD) (>600 years); and highland conditions/retrogression (H/R) by tephra deposition (70−860 years). The long time span of the SC stage indicates arrested development by the thick R. lanuginosum moss mat. The progression from SC into VPD was linked to age of the lava flows and soil depth, which was significantly deeper within the VPD stage. Birch was growing on lavas over 600 years old indicating the development towards birch woodland, the climax ecosystem in Iceland.

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6

Baloga, Stephen. "Lava flows as kinematic waves." Journal of Geophysical Research 92, B9 (1987): 9271. http://dx.doi.org/10.1029/jb092ib09p09271.

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7

Griffiths, R. W. "The Dynamics of Lava Flows." Annual Review of Fluid Mechanics 32, no. 1 (January 2000): 477–518. http://dx.doi.org/10.1146/annurev.fluid.32.1.477.

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8

Johnson, Catherine L., and David T. Sandwell. "Joints in Venusian lava flows." Journal of Geophysical Research 97, E8 (1992): 13601. http://dx.doi.org/10.1029/92je01212.

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9

Mossoux, Sophie, Mathijs Saey, Stefania Bartolini, Sam Poppe, Frank Canters, and Matthieu Kervyn. "Q-LAVHA: A flexible GIS plugin to simulate lava flows." Computers & Geosciences 97 (December 2016): 98–109. http://dx.doi.org/10.1016/j.cageo.2016.09.003.

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10

Braz Machado, F., E. Reis Viana Rocha-Júnior, L. Soares Marques, and A. J. Ranalli Nardy. "Volcanological aspects of the northwest region of Paraná continental flood basalts (Brazil)." Solid Earth 6, no. 1 (February 19, 2015): 227–41. http://dx.doi.org/10.5194/se-6-227-2015.

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Abstract. There has been little research on volcanological aspects of Paraná continental flood basalts (PCFBs), and all investigations have mainly been concentrated on the internal portions of the lava flows. Thus, this study describes for the first time morphological aspects of lava flows and structural characteristics caused by lava–sediment interaction in the northwestern PCFB province (NW-PCFB). Early Cretaceous (134 to 132 Ma) tholeiitic rocks of the PCFB were emplaced on a large intracratonic Paleozoic sedimentary basin (Paraná Basin), mainly covering dry eolian sandstones (Botucatu Formation). As this sedimentary unit is overlain by the basic lava flows of the PCFB, the interaction of lavas and unconsolidated sediments resulted in the generation of fluidal peperites. This aspect is significant because it shows that restricted wet environments should have existed in the Botucatu desert. The peperite zones of the NW-PCFB are associated with compound pahoehoe-type (P-type) flows and are always related to the first volcanic pulses. These flows have dispersed vesicles and sand-filled cracks in their base and top borders, as well as the presence of interlayered sandstones with irregular contacts and varied thicknesses. It is remarkable that, to the best of current knowledge, only in this area of the whole PCFB did the volcanic activity start with low-Ti basalt flows of Ribeira type (TiO2 < 2.3 wt%), which are scarce in the province.

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11

Diehl, J. F., and T. D. Haig. "A paleomagnetic study of the lava flows within the Copper Harbor Conglomerate, Michigan: new results and implications." Canadian Journal of Earth Sciences 31, no. 2 (February 1, 1994): 369–80. http://dx.doi.org/10.1139/e94-034.

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New paleomagnetic data have been obtained from the interbedded lava flows within the Copper Harbor Conglomerate on Michigan's Keweenaw Peninsula. Previous paleomagnetic studies of these lava flows, known collectively as the Lake Shore Traps, have produced contradictory results. To investigate the cause of these conflicting results, 30 sites encompassing the most complete section of lava flows possible were collected and analyzed.Well-defined characteristic directions of magnetization were isolated using either alternating-field or thermal demagnetization or a combination of both. These directions of magnetization are interpreted as primary magnetizations acquired during the original cooling of the lavas. Hysteresis, thermomagnetic, and petrographic analyses suggest the carrier of magnetization is a pseudo-single-domain, titanium-poor magnetite that has undergone some high-temperature oxidation.Site means determined from the 30 lava flows define three distinct directional clusters. Each cluster of directions corresponds to a different stratigraphic package of lava flows with the Copper Harbor Conglomerate. Between-site dispersion for each stratigraphic package or unit is much less than the expected value for Keweenawan-age rocks. Therefore, we suggest that most of the lava flows in each unit were extruded rapidly and that within an individual stratigraphic unit, paleosecular variation has not been adequately sampled. This explains why previous studies on the Lake Shore Traps have produced such different results; each study did not sample the entire range of directions possible in these lava flows.The paleomagnetic pole calculated from the 30 site-mean virtual geomagnetic poles is located at 22.2°N, 180.8°E (k = 35.0; A95 = 6.5°). The new Copper Harbor pole is now located in the appropriate chronological position with respect to the underlying Portage Lake Volcanics and the overlying Nonesuch Shale on the Keweenawan apparent polar wander path. The similarity of our Copper Harbor pole to that of the Portage Lake Volcanics reinforces the idea that the Copper Harbor Conglomerate is more closely related in time to the Portage Lake Volcanics than to the Nonesuch Shale.

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12

Baloga, Stephen, and David Pieri. "Time-dependent profiles of lava flows." Journal of Geophysical Research 91, B9 (1986): 9543. http://dx.doi.org/10.1029/jb091ib09p09543.

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13

Dietterich, Hannah R., Katharine V. Cashman, Alison C. Rust, and Einat Lev. "Diverting lava flows in the lab." Nature Geoscience 8, no. 7 (June 30, 2015): 494–96. http://dx.doi.org/10.1038/ngeo2470.

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14

Baum, B. A., W. B. Krantz, J. H. Fink, and R. E. Dickinson. "Taylor instability in rhyolite lava flows." Journal of Geophysical Research 94, B5 (1989): 5815. http://dx.doi.org/10.1029/jb094ib05p05815.

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15

Tiano, Pasquale, Alberto Incoronato, and Donald H. Tarling. "Palaeomagnetic study on Vesuvius lava flows." Geophysical Journal International 163, no. 2 (November 2005): 518–26. http://dx.doi.org/10.1111/j.1365-246x.2005.02768.x.

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16

Glaze, Lori S., and Stephen M. Baloga. "Simulation of inflated pahoehoe lava flows." Journal of Volcanology and Geothermal Research 255 (April 2013): 108–23. http://dx.doi.org/10.1016/j.jvolgeores.2013.01.018.

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17

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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18

Kerr, Ross C. "Thermal erosion by laminar lava flows." Journal of Geophysical Research: Solid Earth 106, B11 (November 10, 2001): 26453–65. http://dx.doi.org/10.1029/2001jb000227.

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19

Kristjánsson, Leó. "Paleomagnetic research on Icelandic lava flows." Jökull 58, no. 1 (December 15, 2008): 101–16. http://dx.doi.org/10.33799/jokull2008.58.101.

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20

Wilson, L., and J. W. Head. "Heat transfer in volcano–ice interactions on Earth." Annals of Glaciology 45 (2007): 83–86. http://dx.doi.org/10.3189/172756407782282507.

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AbstractThe very high temperature contrast between magma/ lava and water ice commonly leads to the assumption that significant melting will take place immediately upon magma/ lava ice contact, yet observations of active flows show little evidence of voluminous melting upon contact. We use analytical thermal models to reassess the efficiency with which heat can be transferred from magma to ice in three situations: lava flows erupted on top of glacial ice, sill intrusions beneath glacial ice evolving into subglacial lava flows and dyke intrusions into the interiors of glaciers. We find that the maximum ratios of thickness of ice that can be melted to the thickness of magmatic heat source are likely to be ∽2–5 for subaerial lava flows encroaching onto glaciers, ∽6–7 for subglacial lava flows and ∽10 for dykes intruded into glacial ice. Rates of ice melt production are not linear functions of time and flow thickness, however, and this may account for the observations of minimal immediate water release from beneath advancing lava flows. Field observations during future eruptions should be directed at measuring the temperature of released water.

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21

Kiernan, Kevin, Anne McConnell, and Tony Yates. "Tube-fed pahoehoe lava-flow features of Azorella Peninsula, Heard Island, southern Indian Ocean." Polar Record 34, no. 190 (July 1998): 225–36. http://dx.doi.org/10.1017/s0032247400025699.

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AbstractAzorella Peninsula on Heard Island in the sub-Antarctic comprises basaltic scoria that is overlain by basalt flows. Typical tube-fed pahoehoe flows characteristic of some Hawaiian-type volcanoes occur. The volcanic landforms of the peninsula include highly degraded volcano remnants and undissected scoria cones, pahoehoe flows, lava rises, tumuli, open vertical volcanic conduits, and lava tubes. Features produced by lava inflation are widespread but are generally of low topographic relief. Many detailed lava-flow features are preserved in dramatically fresh condition within the protected environment of lava tubes. They highlight the efficacy of the lava tubes in maintaining high temperatures and low viscosity of the flowing lava. The lava tubes on Heard Island are the only features of their kind hitherto recorded from Antarctic and sub-Antarctic latitudes.

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22

Boudal, Christian, and Claude Robin. "Relations entre dynamismes éruptifs et réalimentations magmatiques d'origine profonde au Popocatépetl." Canadian Journal of Earth Sciences 25, no. 7 (July 1, 1988): 955–71. http://dx.doi.org/10.1139/e88-096.

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The modern volcano Popocatépetl is 30 000 – 50 000 years old. Until 5000 years BP, its volcanic activity led to the construction of a 2000 m high cone, the El Fraile volcano. This edifice was later topped by the Popocatépetl summit. The volcanic activity was characterized by long-term construction by lava flows, alternating with periods of 1000–2000 years of mixed explosive and effusive activity. The El Fraile volcano experienced three periods of this type, marked by back-falling pyroclastic flows with heterogeneous magma products and thick air-fall deposits (ash and scoria). The first one occurred more than 10 000 years BP; the second, between 10 000 and 8000 years BP; the third, from 5000 to 3800 years BP. Each of these periods showed violent explosive episodes alternating with lava flows in cycles of 100 to several hundreds of years in duration. Whenever the explosive activity occurred, it destroyed the upper part of the volcano, opening large craters. After a ~ 2500 year period of lava-flow construction (from ~ 3800 to 1200 years BP), the Popocatépetl summit began a similar activity. The last event, producing pyroclastic flows, occurred just before me Hispanic Conquest, and since that time the activity has been effusive and Plinian.Heterogeneous to subhomogeneous pyroclastic flow products exhibit a complex mineralogy: Fe clinopyroxene, Mg clinopyroxene, Fe orthopyroxene, Mg orthopyroxene, plagioclase in equilibrium or disequilibrium, and scarce olivine. All lava flows show a similar paragenesis, suggesting magma-mixing processes. A model in which a basaltic magma is periodically injected in a differentiated chamber at the beginning of each explosive period (or each cycle?) is proposed to explain the heterogeneous products. However, calculations of mixing models do not agree with the high Mg and Ni values observed in some hybrid lavas. This excess is probably due to the remobilization of cumulative olivine by basic magma supplies in the lower part of the reservoir. On the other hand, lava flows emitted during the long phases of effusive activity correspond to evolution in a closed and zoned chamber, partly affected by convective movements. The convection explains the complex mineralogy of these lavas, which result from differentiation of a previously homogenized magma rather than directly from magma mixing.

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23

Casalbore, Daniele, Federico Di Traglia, Alessandro Bosman, Claudia Romagnoli, Nicola Casagli, and Francesco Latino Chiocci. "Submarine and Subaerial Morphological Changes Associated with the 2014 Eruption at Stromboli Island." Remote Sensing 13, no. 11 (May 22, 2021): 2043. http://dx.doi.org/10.3390/rs13112043.

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Stromboli is an active insular volcano located in the Southern Tyrrhenian Sea and its recent volcanic activity is mostly confined within the Sciara del Fuoco (SdF, hereafter), a 2-km wide subaerial–submarine collapse scar, which morphologically dominates the NW flank of the edifice. In August-November 2014, an effusive eruption occurred along the steep SdF slope, with multiple lava flows reaching the sea. The integration of multisensor remote sensing data, including lidar, photogrammetric, bathymetric surveys coupled with SAR amplitude images collected before and after the 2014 eruption enabled to reconstruct the dynamics of the lava flows through the main morphological changes of the whole SdF slope. Well-defined and steep-sided ridges were created by lava flows during the early stages of the eruption, when effusion rates were high, favoring the penetration into the sea of lava flows as coherent bodies. Differently, fan-shaped features were emplaced during the declining stage of the eruption or in relation to lava overflows and associated gravel flows, suggesting the prevalence of volcaniclastic breccias with respect to coherent lava flows. The estimated volume of eruptive products emplaced on the SdF slope during the 2014 eruption, accounts for about 3.7 × 106 m3, 18% of which is in the submarine setting. This figure is different with respect to the previous 2007 eruption at Stromboli, when a large lava submarine delta formed. This discrepancy can be mainly related to the different elevation of the main vents feeding lava flows during the 2007 eruption (around 400 m) and the 2014 eruption (around 650 m). Besides slope accretion, instability processes were detected both in the subaerial and submarine SdF slope. Submarine slope failure mobilized at least 6 × 105 m3 of volcaniclastic material, representing the largest instability event detected since the 2007 lava delta emplacement.

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24

Garcia, Michael O. "Lava Flows and Lava Tubes: What They Are, How They Form (DVD)." Eos, Transactions American Geophysical Union 84, no. 52 (December 30, 2003): 586. http://dx.doi.org/10.1029/2003eo520007.

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25

Rowland, Scott K., and George P. L. Walker. "Mafic-crystal distributions, viscosities, and lava structures of some Hawaiian lava flows." Journal of Volcanology and Geothermal Research 35, no. 1-2 (September 1988): 55–66. http://dx.doi.org/10.1016/0377-0273(88)90005-4.

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26

Groves, D. A., R. L. Morton, and J. M. Franklin. "Physical volcanology of the footwall rocks near the Mattabi massive sulphide deposit, Sturgeon Lake, Ontario." Canadian Journal of Earth Sciences 25, no. 2 (February 1, 1988): 280–91. http://dx.doi.org/10.1139/e88-030.

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Subaerial and shallow subaqueous mafic hyalotuffs, lava flows, and flow breccias, felsic lava flows, and pyroclastic flows and falls form a 2 km thick succession beneath the Mattabi massive sulphide deposit. The lowermost 800 m of section comprises massive to amygdaloidal mafic flows and flow breccias interlayered with repetitive sequences of thinly bedded felsic tuff: pillow lavas and hyaloclastites are absent. Amygdaloidal felsic lavas overlie the mafic flows and are locally capped by coarse explosion breccia. This breccia is believed to represent the start of mafic hydrovolcanism, which produced ash falls, surges, and flows. These pyroclastic deposits formed thin- to thick-bedded hyalotuffs that contain highly vesicular and quenched juvenile and accessory lithic fragments. Periods of water influx probably led to the construction of a tuff cone, which represents a submergent hydrovolcanic cycle.In the Mattabi area, pyroclastic flow deposits form the immediate mine footwall strata and include (i) massive basal beds and overlying bedded ash tuffs and (ii) massive pumiceous units. These deposits overlie and, to the west in the Darkwater Lake area, are intercalated with the mafic hyalotuff sequence. The morphology of the footwall volcanic rocks indicates that the Mattabi and the F-zone massive sulphide deposits formed in a shallow subaqueous environment.

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27

Emeleus, C. H. "The Tertiary lavas and sediments of northwest Rhum, Inner Hebrides." Geological Magazine 122, no. 5 (September 1985): 419–37. http://dx.doi.org/10.1017/s0016756800035342.

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AbstractSeveral small outliers of Tertiary lavas and sediments rest with strong unconformity on a buried landscape eroded from Torridonian sediments and Tertiary granophyre. Erosion continued during the period of sediment and lava accumulation. Four formations are recognized; these are, in order of increasing age, the Orval Formation (hawaiite and basaltic hawaiite lavas), the Guirdil Formation (icelandite lavas, interbedded conglomerates), the Upper Fionchra Formation (tholeiitic basaltic andesite lavas, hyaloclastite deposits, basal conglomerate) and the Lower Fionchra Formation (alkali and transitional basalt, basaltic hawaiite and hawaiite lava flows, basal conglomerate); each is separated by an erosional interval. Clasts in the conglomerates reveal a history of erosion of a terrain exposing gneisses, Torridonian sediments, igneous rocks derived from the Rhum Tertiary Central Complex (including allivalites), and Tertiary lavas of local origin but also including, in the oldest conglomerates, tholeiitic basalts not now preserved on or near Rhum. Prior to and during lava and sediment accumulation, erosion on Rhum had cut down to a level similar to that of the present day, although not to the extent that high-grade thermally altered rocks, which are a marked feature of the Central Complex, were being eroded in any quantity. A sequence of east–west trending valleys, possibly initiated on the line of the earlier Main Ring Fault, drained the area of the Central Complex which then, as now, must have been high ground. Small lakes occasionally formed in the valleys allowing the accumulation of fine-grained sediment with plant remains, and promoting the formation of hyaloclastite deposits when buried by later flows. No source for any of the lava formations is preserved on Rhum; they are thought to have come from feeders north of Rhum, possibly near Canna, and to have ponded against the hills and valleys near and in the Central Complex.The oldest tholeiitic lavas, not now found in situ, were followed by alkali and transitional flows compositionally similar to the Skye Main Lava Series but characteristically feldsparphyric; the most mafic also contain phenocrysts of magnesian olivine (with included Cr-Al-rich spinels) and aluminous spinel. Both the early alkalic/transitional basalts and the youngest hawaiites and basaltic hawaiites equilibrated at pressures < 9 kb; the tholeiitic basaltic andesites and icelandites equilibrated at relatively shallows depths.Apart from a few N–S to NW–SE-trending basalt dykes, the lava formations represent the youngest Tertiary igneous event on Rhum.

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Khan, Shuhab D., Essam Heggy, and Jaime Fernandez. "Mapping exposed and buried lava flows using synthetic aperture and ground-penetrating radar in Craters of the Moon lava field." GEOPHYSICS 72, no. 6 (November 2007): B161—B174. http://dx.doi.org/10.1190/1.2793298.

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The Craters of the Moon (COM) lava field has a multiple eruptive history. Burial of older flows has resulted in complex subsurface stratigraphy. For the older eruptive periods, the locations of source vents and the extension of lava flows are either speculative or unknown, because they are buried under more recent pyroclastics. In this study, we used surface and subsurface backscatter characteristics of the P- and L-band polarimetric airborne synthetic aperture radar (AIRSAR) data and ground-penetrating radar (GPR) soundings to resolve different exposed and buried lava flows. Our primary objective is to define the most effective polarization and frequency for mapping, resolving, and characterizing different lava types in the volcanic field. Polarimetric analysis of AIRSAR images from COM allows a clear recognition of the aa and pahoehoe lava types as a result of the variability in their roughness. Our results suggest that the HV cross-polarized, AIRSAR L-band is capable of producing a detailed map delineating surface lava with different surface backscattering properties. An accuracy assessment utilizing the geological map of the Inferno Cone area was performed to quantify the reliability of differentiating lava types and mapping the lava flows extension below loose pyroclastics using AIRSAR data. Results shows an ability of P-band SAR to map buried structures up to 3 meters deep under loose cinder and ash deposits, resolving buried fissures, outcrops, and lava flows that were validated with ground-truth GPR surveys. The techniques used in this study provide a tool to assess volcanic hazards in remote and inaccessible places. Also it could be an aid in the study of other planets and planetary bodies in the solar system.

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29

Vosgerau, Henrik, Pierpaolo Guarnieri, Rikke Weibel, Michael Larsen, Brian Bell, Erik V. Sørensen, and Henrik Nøhr-Hansen. "Sedimentology and reservoir architecture of a widespread siliciclastic intra-lava unit, Kangerlussuaq, East Greenland." Journal of Sedimentary Research 91, no. 6 (June 30, 2021): 662–82. http://dx.doi.org/10.2110/jsr.2021.02.

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ABSTRACT The Rosebank hydrocarbon discovery in 2004 proved that intra-lava sandstones form attractive reservoirs in the Faroe–Shetland Basin and the new volcanic play triggered the need for suitable analogues to describe and assess sedimentology, reservoir architecture, compartmentalization, and connectivity of intra-lava siliciclastic units. The onshore Kangerlussuaq Basin in East Greenland offers the opportunity to study Paleogene intra-lava siliciclastic sandstones and their interaction with lavas, on the scale of the Rosebank Field. The focus of this study is a siliciclastic-dominated intra-lava unit, 4–10 m thick, exposed in almost vertical cliff sections over distances of several kilometers. The unit reflects a short return to siliciclastic deposition following initiation of volcanic activity and extrusion of the first lava flows in the area. Deposition took place as shoreface and delta progradation in a marine-influenced, shallow embayment. Lateral variations in sedimentary facies distribution and geometry are prominent and were largely governed by an interplay of base-level variations and autocyclic processes, the surface roughness and type of substratum on which deposition took place, and differential block movements before and during deposition. Presence of local topographic barriers are of key importance and influenced the lava–sediment interaction and the resulting 3D-geometry of lava flows and sediment bodies. In addition, compartmentalization of the intra-lava sandstone unit is observed and is controlled by the offset across normal faults, intersecting dikes, and to a lesser extent by invasive and eroding lavas. A depositional model is suggested that incorporates the detailed sedimentological and 3D photogrammetric observations and presents a possible explanation for the contrasting architecture of the intra-lava unit observed in three areas located a few kilometers apart. The model embraces the complex interplay between siliciclastic and volcanic settings and reveals important aspects to consider when recoverable volumes of hydrocarbons are estimated in intra-volcanic subsurface reservoirs in volcanic rifted margins with poor seismic imaging of the relatively thin intra-lava reservoirs.

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30

Beresford, S. W., and R. A. F. Cas. "KOMATIITIC INVASIVE LAVA FLOWS, KAMBALDA, WESTERN AUSTRALIA." Canadian Mineralogist 39, no. 2 (April 1, 2001): 525–35. http://dx.doi.org/10.2113/gscanmin.39.2.525.

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31

Robertson, J. C., and R. C. Kerr. "Solidification dynamics in channeled viscoplastic lava flows." Journal of Geophysical Research: Solid Earth 117, B7 (July 2012): n/a. http://dx.doi.org/10.1029/2012jb009163.

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32

Oda, Yasuyuki, Tadahiro Fujimoto, Kazunobu Muraoka, and Norishige Chiba. "Particle-based Visual Simulation of Lava Flows." Journal of the Society for Art and Science 2, no. 1 (2003): 51–60. http://dx.doi.org/10.3756/artsci.2.51.

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33

Stephenson, P. J., A. T. Burch-Johnston, D. Stanton, and P. W. Whitehead. "Three long lava flows in north Queensland." Journal of Geophysical Research: Solid Earth 103, B11 (November 10, 1998): 27359–70. http://dx.doi.org/10.1029/98jb01670.

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34

Cashman, Katharine, Harry Pinkerton, and Jon Stephenson. "Introduction to Special Section: Long Lava Flows." Journal of Geophysical Research: Solid Earth 103, B11 (November 10, 1998): 27281–89. http://dx.doi.org/10.1029/98jb01820.

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35

Valet, Jean-Pierre, Tesfaye Kidane, Vicente Soler, Jacques Brassart, Vincent Courtillot, and Laure Meynadier. "Remagnetization in lava flows recording pretransitional directions." Journal of Geophysical Research: Solid Earth 103, B5 (May 10, 1998): 9755–75. http://dx.doi.org/10.1029/97jb03544.

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Blake, S., and B. C. Bruno. "Modelling the emplacement of compound lava flows." Earth and Planetary Science Letters 184, no. 1 (December 2000): 181–97. http://dx.doi.org/10.1016/s0012-821x(00)00278-8.

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Holcomb, Robin T., James G. Moore, Peter W. Lipman, and Robert H. Belderson. "Voluminous submarine lava flows from Hawaiian volcanoes." Geology 16, no. 5 (1988): 400. http://dx.doi.org/10.1130/0091-7613(1988)016<0400:vslffh>2.3.co;2.

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Fujita, Eisuke, Masataka Hidaka, Akio Goto, and Susumu Umino. "Simulations of measures to control lava flows." Bulletin of Volcanology 71, no. 4 (May 2009): 401–8. http://dx.doi.org/10.1007/s00445-008-0229-7.

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Pinkerton, H. "Factors affecting the morphology of lava flows." Endeavour 11, no. 2 (January 1987): 73–79. http://dx.doi.org/10.1016/0160-9327(87)90241-9.

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Dundas, Colin M., and Laszlo P. Keszthelyi. "Modeling steam pressure under martian lava flows." Icarus 226, no. 1 (September 2013): 1058–67. http://dx.doi.org/10.1016/j.icarus.2013.06.036.

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Howell, Robert R. "Thermal Emission from Lava Flows on Io." Icarus 127, no. 2 (June 1997): 394–407. http://dx.doi.org/10.1006/icar.1997.5686.

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CARRASCO-NÚÑEZ, GERARDO. "Lava flow growth inferred from morphometric parameters: a case study of Citlaltépetl volcano, Mexico." Geological Magazine 134, no. 2 (March 1997): 151–62. http://dx.doi.org/10.1017/s0016756897006614.

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Recent (Quaternary) lava fields, such as those of Citlaltépetl (Pico de Orizaba) volcano in Mexico, are excellent places to obtain precise measurements of flow-field dimensions that can be used to estimate volume, eruption duration and effusion rates. The relationship between these parameters and the influence of some other interrelated features such as lava composition, superficial structures and lava type are important tools that can help to infer conditions when the lavas were active and thus improve understanding of how flow fields grow. The Holocene lavas of Citlaltépetl volcano are homogeneous in composition (dacites) and are generally blocky with well-developed levees. The eruption duration obtained for the Citlaltépetl lavas by a method proposed by C. Kilburn and R. Lopes presents a good correlation with the different lava types morphologically classified here. Results from that method compare favourably with the inferred effusion rates estimated by an empirical cooling method (Graetz). The lavas show different behaviour, mainly controlled by fluctuations in the effusion rate that promote changes from single- to multiple-flow style. The maximum distance achieved by a flow is directly proportional to the effusion rate in Citlaltépetl lavas, but it is always lower for multiple flows, independent of the volume of erupted lava. Observations of Citlaltépetl lavas can be used to understand how lava flow growth occurs on other volcanoes.

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Sun, Qiliang, Christopher A. L. Jackson, Craig Magee, Samuel J. Mitchell, and Xinong Xie. "Extrusion dynamics of deepwater volcanoes revealed by 3-D seismic data." Solid Earth 10, no. 4 (August 2, 2019): 1269–82. http://dx.doi.org/10.5194/se-10-1269-2019.

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Abstract. Submarine volcanism accounts for ca. 75 % of the Earth's volcanic activity. Yet difficulties with imaging their exteriors and interiors mean that the extrusion dynamics and erupted volumes of deepwater volcanoes remain poorly understood. Here, we use high-resolution 3-D seismic reflection data to examine the external and internal geometry and extrusion dynamics of two late Miocene–Quaternary deepwater (> 2 km emplacement depth) volcanoes buried beneath 55–330 m of sedimentary strata in the South China Sea. The volcanoes have crater-like bases, which truncate underlying strata and suggest extrusion was initially explosive, and erupted lava flows that feed lobate lava fans. The lava flows are > 9 km long and contain lava tubes that have rugged basal contacts defined by ∼90±23 m high erosional ramps. We suggest the lava flows eroded down into and were emplaced within wet, unconsolidated, near-seafloor sediments. Extrusion dynamics were likely controlled by low magma viscosities as a result of increased dissolved H2O due to high hydrostatic pressure and soft, near-seabed sediments, which are collectively characteristic of deepwater environments. We calculate that long-runout lava flows account for 50 %–97 % of the total erupted volume, with a surprisingly minor component (∼3 %–50 %) being preserved in the main volcanic edifice. Accurate estimates of erupted volumes therefore require knowledge of volcano and lava basal surface morphology. We conclude that 3-D seismic reflection data are a powerful tool for constraining the geometry, volumes, and extrusion dynamics of ancient or active deepwater volcanoes and lava flows.

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MICHAUT, CHLOÉ, and DAVID BERCOVICI. "A model for the spreading and compaction of two-phase viscous gravity currents." Journal of Fluid Mechanics 630 (July 10, 2009): 299–329. http://dx.doi.org/10.1017/s0022112009006612.

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Two-phase viscous gravity current theory has numerous applications in the natural sciences, from small-scale lava, sedimentary and glacial flows, to large-scale flows of partially molten mantle. We develop the general equations for two-phase viscous gravity currents composed of a high viscosity matrix and low viscosity fluid for both constant volume and constant flux conditions. A loss of fluid phase is taken into account at the current's upper boundary and corresponds to the degassing of a lava flow or loss of water in sedimentary flows. As the current spreads, its surface increases and fluid loss is facilitated, which modifies the mixture density and viscosity and thus the current's shape; hence spreading of the flow affects fluid loss and vice-versa. Our results show that two-phase gravity currents retain and transport the fluid out to large distances, but the fluid is almost entirely lost within a region of finite radius. This ‘loss radius’ depends on the flow's volume or flux, fluid and matrix properties as well as on the size of fluid parcels or matrix permeability. Application to lava flows shows that degassing occurs over a large area, which affects gas release and transport in the atmosphere.

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Mitchell, Neil C., Christoph Beier, Paul L. Rosin, Rui Quartau, and Fernando Tempera. "Lava penetrating water: Submarine lava flows around the coasts of Pico Island, Azores." Geochemistry, Geophysics, Geosystems 9, no. 3 (March 2008): n/a. http://dx.doi.org/10.1029/2007gc001725.

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Chadwick Jr., William W., Tracy K. P. Gregg, and Robert W. Embley. "Submarine lineated sheet flows: a unique lava morphology formed on subsiding lava ponds." Bulletin of Volcanology 61, no. 3 (August 24, 1999): 194–206. http://dx.doi.org/10.1007/s004450050271.

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Hickson, Catherine J., James G. Moore, Lewis Calk, and Paul Metcalfe. "Intraglacial volcanism in the Wells Gray–Clearwater volcanic field, east-central British Columbia, Canada." Canadian Journal of Earth Sciences 32, no. 7 (July 1, 1995): 838–51. http://dx.doi.org/10.1139/e95-070.

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Small-volume, subaerial, subaqueous and subglacial basaltic eruptions occurred in the Wells Gray–Clearwater area during Quaternary time. Part of this time, significant thicknesses of glacial ice were present. Dating of intraglacial volcanic features corroborates other evidence of an Early Pleistocene, Cordilleran-wide ice sheet. Of the intraglacial volcanoes investigated, three were studied in detail and of these, two probably erupted during the Fraser glaciation (11–20 ka), when maximum ice level exceeded 2100 m elevation. Major-element and sulphur concentrations were measured in glass from the volcanoes to provide insight into vent conditions at the time of eruption. Hyalo Ridge (2102 m elevation, whole-rock K–Ar age of 0.02 ± 0.01 Ma) is a small volcanic edifice capped by lava flows with coherent pillowed lavas and interbedded hyaloclastite exposed over nearly 400 m altitude on its east flank. Low sulphur content (<0.03 wt.%) in pillow rim glasses indicates that the lavas are degassed. It is interpreted that the vent built above the water (or ice) surface then fed lava flows that crossed a shoreline and produced pillowed flows. Pyramid Mountain is a volcanic cone 240 m high, comprised of glassy, vesicular, lapilli-tuff breccia. The highly alkalic glass contains 0.1 wt.% S (considered high), and indicates a high original volatile content and drastic quenching, probably during phreatomagmatic eruption from a meltwater-flooded vent. East of the Clearwater River a sequence of massive pillowed flows and pillow joint-block breccias is exposed from 880 to 1320 m elevation (0.27 ± 0.05 Ma). The vent location is unknown. Moderate S content (0.040–0.055 wt.%) indicates that the lavas were erupted in shallow water and are largely degassed. The S content of glass in dykes cutting the pillow breccias is low. The dykes are interpreted as lava that has flowed laterally or down into cracks.

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Pedersen, Gro Birkefeldt Möller, Jorge Montalvo, Páll Einarsson, Olga Kolbrún Vilmundardóttir, Friðþór Sófus Sigurmundsson, Joaquín Munoz-Cobo Belart, Ásta Rut Hjartardóttir, et al. "Historical lava flow fields at Hekla volcano, South Iceland." Jökull 68, no. 1 (December 15, 2018): 1–26. http://dx.doi.org/10.33799/jokull2018.68.001.

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Hekla volcano is known to have erupted at least 23 times in historical time (last 1100 years); often producing mixed eruptions of tephra and lava. The lava flow volumes from the 20th century have amounted 80\% to almost 100\% of the entire erupted volume. Therefore, evaluating the extent and volume of individual lava flows is very important when assessing the historical productivity of Hekla volcano. Here we present new maps of the historical lava flow fields at Hekla in a digital format. The maps were produced at a scale of 1:2000–10000 using a catalogue of orthophotos since 1945, acquired before and after each of the last five eruptions, combined with field observation of stratigraphy, soil profiles, tephra layers and vegetation cover. The new lava flow maps significantly improve the historical eruptive history of Hekla, prior to the 1947 eruption. The historical lava flow fields from Hekla cover ∼233 km² and the lavas reach up to 16 km from Hekla volcano. Flow lengths up to 20 km are known, though lava flows only travelled up to 8–9 km from Hekla in the last 250 years. Identified historical vents are distributed between 0 and 16 km from Hekla volcano and vents are known to have migrated up to 5 km away from Hekla during eruptions. We have remapped the lava flow fields around Hekla and assigned the identified flow fields to 16 eruptions. In addition, ca. 60 unidentified lava units, which may be of historical age, have been mapped. It is expected that some of these units are from known historical Hekla eruptions such as the 1222, 1341, 1510, 1597, 1636 and potentially even from the previously excluded eruptions such as 1436/1439.

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Nádudvari, Ádám, Anna Abramowicz, Rosanna Maniscalco, and Marco Viccaro. "The Estimation of Lava Flow Temperatures Using Landsat Night-Time Images: Case Studies from Eruptions of Mt. Etna and Stromboli (Sicily, Italy), Kīlauea (Hawaii Island), and Eyjafjallajökull and Holuhraun (Iceland)." Remote Sensing 12, no. 16 (August 7, 2020): 2537. http://dx.doi.org/10.3390/rs12162537.

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Using satellite-based remote sensing to investigate volcanic eruptions is a common approach for preliminary research, chiefly because a great amount of freely available data can be effectively accessed. Here, Landsat 4-5TM, 7ETM+, and 8OLI night-time satellite images are used to estimate lava flow temperatures and radiation heat fluxes from selected volcanic eruptions worldwide. After retrieving the spectral radiance, the pixel values were transformed into temperatures using the calculated calibration constants. Results showed that the TIR and SWIR bands were saturated and unable to detect temperatures over the active lava flows. However, temperatures were effectively detected over the active lava flows in the range ~500–1060 °C applying the NIR-, red-, green- or blue-band. Application of the panchromatic band with 15 m resolution also revealed details of lava flow morphology. The calculated radiant heat flux for the lava flows accords with increasing cooling either with slope or with distance from the vent.

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Jorge-Villar, Susana E., and Howell G. M. Edwards. "Raman spectroscopy of volcanic lavas and inclusions of relevance to astrobiological exploration." Philosophical Transactions of the Royal Society A: Mathematical, Physical and Engineering Sciences 368, no. 1922 (July 13, 2010): 3127–35. http://dx.doi.org/10.1098/rsta.2010.0102.

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Volcanic eruptions and lava flows comprise one of the most highly stressed terrestrial environments for the survival of biological organisms; the destruction of botanical and biological colonies by molten lava, pyroclastic flows, lahars, poisonous gas emissions and the deposition of highly toxic materials from fumaroles is the normal expectation from such events. However, the role of lichens and cyanobacteria in the earlier colonization of volcanic lava outcrops has now been recognized. In this paper, we build upon earlier Raman spectroscopic studies on extremophilic colonies in old lava flows to assess the potential of finding evidence of biological colonization in more recent lava deposits that would inform, first, the new colonization of these rocks and also provide evidence for the relict presence of biological colonies that existed before the volcanism occurred and were engulfed by the lava. In this research, samples were collected from a recent expedition to the active volcano at Kilauea, Hawaii, which comprises very recent lava flows, active fumaroles and volcanic rocks that had broken through to the ocean and had engulfed a coral reef. The Raman spectra indicated that biological and geobiological signatures could be identified in the presence of geological matrices, which is encouraging for the planned exploration of Mars, where it is believed that there is evidence of an active volcanism that perhaps could have preserved traces of biological activity that once existed on the planet’s surface, especially in sites near the old Martian oceans.

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Journal articles on the topic 'Lava flows'

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