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Dome Growth, Collapse, and Valley Fill at Soufrière Hills Volcano, Montserrat, from 1995 to 2013: Contributions from Satellite Radar

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Dome Growth, Collapse, and Valley Fill at Soufrière Hills Volcano, Montserrat, from 1995 to 2013: Contributions from Satellite Radar Research Paper GEOSPHERE Dome growth, collapse, and valley fill at Soufrière Hills Volcano, Montserrat, from 1995 to 2013: Contributions from satellite radar GEOSPHERE; v. 12, no. 4 measurements of topographic change doi:10.1130/GES01291.1 D.W.D. Arnold1, J. Biggs1, G. Wadge2, S.K. Ebmeier1, H.M. Odbert3,*, and M.P. Poland4 1COMET (Centre for Observation and Modeling of Earthquakes, Volcanoes and Tectonics), School of Earth Sciences, University of Bristol, Queen’s Road, Bristol BS8 1RJ, UK 4 figures; 5 tables; 1 supplemental file 2COMET (Centre for Observation and Modeling of Earthquakes, Volcanoes and Tectonics), Department of Meteorology, University of Reading, Earley Gate, P.O. Box 243, Reading RG6 6BB, UK 3School of Earth Sciences, University of Bristol, Queen’s Road, Bristol BS8 1RJ, UK 4U.S. Geological Survey, Cascade Volcano Observatory, 1300 S.E. Cardinal Court, Building 10, Suite 100, Vancouver, Washington 98683-9589, USA CORRESPONDENCE: david .arnold@ bristol .ac.uk CITATION: Arnold, D.W.D., Biggs, J., Wadge, G., ABSTRACT Fink, 1996; Fink and Griffiths, 1998; Watts et al., 2002; Hutchison et al., 2013). In Ebmeier, S.K., Odbert, H.M., and Poland, M.P., 2016, Dome growth, collapse, and valley fill at Soufrière steady state, lava effusion rate can constrain the volume and pressure change Hills Volcano, Montserrat, from 1995 to 2013: Contri- Frequent high-resolution measurements of topography at active vol- of shallow magma reservoirs (e.g., Dvorak and Dzurisin, 1993; Harris et al., butions from satellite radar measurements of topo- canoes can provide important information for assessing the distribution and 2003, 2007; Anderson and Segall, 2011), while long-lived volcanic eruptions graphic change: Geosphere, v. 12, no. 4, p. 1300– 1315, doi:10.1130/GES01291.1. rate of emplacement of volcanic deposits and their influence on hazard. At are often characterized by temporal variations in effusion rate or pauses in lava dome-building volcanoes, monitoring techniques such as LiDAR and photo- extrusion, which may be related to changes in the volcanic plumbing system Received 9 November 2015 grammetry often provide a limited view of the area affected by the eruption. or deeper magma supply (e.g., Sparks et al., 1998; Watts et al., 2002; Harris Revision received 8 March 2016 Here, we show the ability of satellite radar observations to image the lava et al., 2003; Ebmeier et al., 2012; Wadge et al., 2014a; Poland, 2014; Naranjo Accepted 11 April 2016 dome and pyroclastic density current deposits that resulted from 15 years of et al., 2016). Published online 27 May 2016 eruptive activity at Soufrière Hills Volcano, Montserrat, from 1995 to 2010. We Lava effusion rate is one of the more difficult eruption parameters to mea- present the first geodetic measurements of the complete subaerial deposition sure, even at well-monitored volcanoes (e.g., Wright et al., 2001; Poland, 2014). field on Montserrat, including the lava dome. Synthetic aperture radar obser- Field measurements require specific conditions, such as molten lava flowing vations from the Advanced Land Observation Satellite (ALOS) and TanDEM-X in a confined channel or lava, and provide instantaneous local lava flux mea- mission are used to map the distribution and magnitude of elevation changes. surements that may not reflect the longer-term effusion rate (e.g., Lipman and We estimate a net dense-rock equivalent volume increase of 108 ± 15M m3 of Banks, 1987; Kauahikaua et al., 1998; Wright et al., 2001), while satellite mea- the lava dome and 300 ± 220M m3 of talus and subaerial pyroclastic density surements of heat flux can be used to estimate a time-averaged effusion rate current deposits. We also show variations in deposit distribution during dif- (see Harris et al., 2007, for a review). However, this technique needs cloud-free ferent phases of the eruption, with greatest on-land deposition to the south satellite imagery, which may not be available and requires lava extent to be and west, from 1995 to 2005, and the thickest deposits to the west and north limited by cooling rather than topography (e.g., Harris et al., 2007; Ebmeier after 2005. We conclude by assessing the potential of using radar-derived et al., 2012). topographic measurements as a tool for monitoring and hazard assessment Topography is a major influence on hazard from eruptive products at active during eruptions at dome-building volcanoes. volcanoes (e.g., Guest and Murray, 1979; Blong, 1984; Cashman and Sparks, 2013), because local slope is a primary control for gravitationally driven flows, such as lava flows, pyroclastic density currents (PDCs), and lahars, influenc- 1. INTRODUCTION ing flow direction and velocity (e.g., Walker, 1973; Druitt, 1998; Carrivick et al., 2008). At active lava domes, rockfalls and PDCs are generated primarily in At active volcanoes, the rate of lava effusion acts as both an indicator of the the direction of dome growth (Watts et al., 2002), and more generally, where state of the subsurface magma system and influence on the style and distribu- the addition of new volcanic material causes a topographic slope to become tion of erupted material. over-steepened, this can lead to an increased risk of landslide, rockfall, and At basaltic systems, effusion rate is one of the main controls of lava flow sector collapse (e.g., Montgomery, 2001). The infilling of valleys with volcanic extent (e.g., Walker, 1973; Harris et al., 2007), while at andesitic domes, it deposits increases the probability of secondary lahar generation during heavy controls the extrusion style and the effusive-explosive transition (Gregg and rainfall (e.g., van Westen and Daag, 2005; Guzzetti et al., 2007). For permission to copy, contact Copyright The availability of up-to-date, high-resolution maps of the topography is Permissions, GSA, or [email protected]. *Current address: School of Earth and Environment, University of Leeds, Leeds LS2 9JT, UK therefore important both for hazard mitigation as well as improving volcano © 2016 Geological Society of America GEOSPHERE | Volume 12 | Number 4 Arnold et al. | Topographic change on Montserrat Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/12/4/1300/4178219/1300.pdf 1300 by guest on 26 September 2021 Research Paper mass budgets and scientific understanding of volcanic processes. Knowledge Hills Volcano has been particularly well studied using a wide variety of tech- of the direction volcanic flows are likely to travel and the ability to model niques, which enables us to assess the relative advantages and disadvan- their likely extent are greatly improved at volcanoes where a high-resolution tages of using satellite geodesy specifically for topographic measurements digital elevation model (DEM) is available (e.g., Stevens et al., 2003; Hubbard at active volcanoes. et al., 2007; Huggel et al., 2008), and comparing changes in topography over time can provide an estimate of the volume of erupted products, which may be used to estimate a time-averaged effusion rate (e.g., Lu et al., 2003; Harris 2. BACKGROUND et al., 2007; Ebmeier et al., 2012; Poland, 2014; Xu and Jónsson, 2014; Albino et al., 2015; Kubanek et al., 2015a, 2015b; Naranjo et al., 2016). Soufrière Hills Volcano, Montserrat, is a Peléean lava dome complex that We chose Soufrière Hills Volcano, Montserrat, to investigate changes in has been erupting intermittently since 18 July 1995. At the time of writing, topog raphy due to a long-lived, dome-building eruption. We use satellite despite the lack of lava extrusion since 11 February 2010, it is not clear that radar observations to constrain topographic changes due to the eruption, the eruption sequence has ended due to high SO2 flux (Wadge et al., 2014a). which allows us to track the location and thickness of deposits across the The eruption so far has been characterized by five extrusive phases lasting up whole island during the 1995–2010 eruption. Recent work has shown the bene- to three years separated by months to years of quiescence (Fig. 1C) (Wadge fit of satellite-based radar observations at volcanoes, both for monitor ing et al., 2014a). Activity is characterized by lava dome growth and collapse, with purposes and for improving the understanding of surface and subsurface Vulcanian explosions and PDCs (Sparks and Young, 2002). Wadge et al. (2014a processes (e.g., Dietterich et al., 2012; Sparks et al., 2012; Biggs et al., 2014; and references therein) provide a more detailed description of recent activity Salzer et al., 2014; Pinel et al., 2014). The 1995–2010 eruption of Soufrière at Soufrière Hills Volcano. N 18° N ′ A 2 km B 49 Barbuda 16° St. Kitts Figure 1. (A) Hill-shaded digital elevation ALOS model of the pre-eruptive topography of Montserrat. Major drainage pathways are shown in yellow: Belham River Valley N Antigua N Nevis (BRV), Tyers Ghaut (TyG), Mosquito Ghaut ′ 17° (MG), Paradise Ghaut (PG), Tuitt’s Ghaut 47 Montserrat (TuG), White’s Ghaut (WG), Tar River Valley 16° (TRV), Fort Ghaut (FG), Spring Ghaut (SG), TanDEM-X Gingoes Ghaut (GG), White River (WR). Key topographic features are labeled: Garibaldi Hill (GH), St. George’s Hill (SGH), N ′ Centre Hills N Guadeloupe Chances Peak (CP), Gage’s Mountain (GM). 45 Yellow dot shows location of reference 16° pixel used in InSAR processing. (B) Re- 16° 63°W 62°W 61°W PG gional map of the northern Lesser Antilles. 1200 Blue rectangle shows the area covered BR G GH V TyG C by ALOS ascending track 118, frame 320. Tu 1100 Red rectangle shows the area covered by N ′ MG TanDEM-X ascending track 104. Yellow SGH WG 43 GM TRV 1000 star shows the location of Soufrière Hills FG Dome Volcano. (C) Timeline of summit elevation 16 Plymouth CP 900 changes during the eruption (modified SG from Wadge et al., 2014a).
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