SO2 emissions to the atmosphere from active volcanoes in Guatemala and El Salvador, 1999–2002

Rodríguez, Lizzette A.; Watson, I. Matthew; Rose, William I.; Branan, Y. K.; Bluth, G. J.; Chigna, Gustavo; Matías, O.; Escobar, Demetrio; Carn, S. A.; Fischer, Tobias P.

doi:10.1016/j.jvolgeores.2004.07.008

Cited by 51 publications

(41 citation statements)

References 36 publications

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“…First, we assume there is a constant SO 2 emission rate for these short term measurements (one set of traverses in a day), as we are attempting to measure a single portion of the plume as it travels downwind. However, previous studies have shown that the emission rate can vary in short time scales (e.g., Sutton et al, 2001;Edmonds et al, 2003;Rodríguez et al, 2004). The second assumption is that there is no formation of SO 2 in the plume.…”

Section: Resultsmentioning

confidence: 99%

“…Anthropogenic emissions contribute about 78 Tg S yr -1 to the atmosphere (Bates et al, 1987;, which is ~76% of the global S emissions (Bates et al, 1992;Spiro et al, 1992;Andres and Kasgnoc, 1998). The uncertainties in the measurements of passive emissions are caused by (1) the study of only a fraction of passive degassing volcanoes, (2) errors arising from measurement techniques (Rodríguez et al, 2004), and (3) factors unique to each volcano that can make measurements logistically difficult and less accurate (e.g., access, meteorology, volcanic activity). Even at volcanoes that are intensively monitored, there are often uncertainties in some of the parameters needed to calculate the emission rates accurately.…”

Section: Introductionmentioning

confidence: 99%

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SO2 loss rates in the plume emitted by Soufrière Hills volcano, Montserrat

Rodríguez

Watson

Edmonds

et al. 2008

Journal of Volcanology and Geothermal Research

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Abstract. To improve interpretation of volcanic SO 2 flux data, it is necessary to quantify and understand reactions involving SO 2 in volcanic plumes. SO 2 is lost in volcanic plumes through a number of mechanisms. Here we report SO 2 measurements made with miniature ultraviolet spectrometers at Soufrière Hills volcano, Montserrat; a low altitude volcano (~1000 m above sea level) whose plume entrains humid marine air in the planetary boundary layer. Traverses very near (<400 m) beneath the ash-free plume were made at various distances from the source (from ~2 km to ~16 km), thereby spanning plume ages of about 6 to 35 minutes with minimal attenuation. We find average SO 2 loss rates of ~10 -4 s -1 (e-folding time of ~2.78 hours), slightly lower than estimated previously for Soufrière Hills. These are in the fast end of the range of loss rates measured at other volcanoes (10 -3 -10 -7 s -1 , e-folding times of 0.28-2778 hr), indicating that Montserrat plumes have short SO 2 lifetimes. This work is more detailed and precise than previous work and is likely to represent the general case at Montserrat. SO 2 flux measurements made >2 km downwind from Soufrière Hills volcano significantly underestimate atsource SO 2 emission rates, on the order of 70-146%, when not accounting for the decay rate. Similar SO 2 loss is likely to occur in plumes from other tropical low altitude volcanoes under conditions of high relative humidity (~20% of active volcanoes worldwide). These results suggest that the global volcanic SO 2 emission rate may be underestimated as the estimates are based on measurements taken downwind of volcanoes, by which time significant loss of SO 2 may have taken place. The loss rates calculated here could be used, in conjunction with downwind SO 2 fluxes, to estimate atsource SO 2 emission rates from volcanoes with similar environmental conditions to those at Soufrière Hills volcano.3

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Section: Resultsmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

SO2 loss rates in the plume emitted by Soufrière Hills volcano, Montserrat

Rodríguez

Watson

Edmonds

et al. 2008

Journal of Volcanology and Geothermal Research

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“…Eggers [16] originally proposed that the petrographic and chemical uniformity of Pacaya's lavas through time implied a continuous supply of magma to an open conduit. This has been further proven by excessive degassing at the volcano [30][31][32][33][34], which implies that Pacaya has a substantial convecting and circulating magma body near the surface that is degassing but not erupting completely on the surface [21,33]. Additionally, gravity changes measured by Eggers [35] were accounted for by density changes caused by very shallow magma bodies (depths of 100 to 200 m below the surface).…”

Section: Post-sliding Flank Deformationmentioning

confidence: 97%

Post-Eruption Deformation Processes Measured Using ALOS-1 and UAVSAR InSAR at Pacaya Volcano, Guatemala

2016

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Pacaya volcano is a persistently active basaltic cone complex located in the Central American Volcanic Arc in Guatemala. In May of 2010, violent Volcanic Explosivity Index-3 (VEI-3) eruptions caused significant topographic changes to the edifice, including a linear collapse feature 600 m long originating from the summit, the dispersion of~20 cm of tephra and ash on the cone, the emplacement of a 5.4 km long lava flow, and~3 m of co-eruptive movement of the southwest flank. For this study, Interferometric Synthetic Aperture Radar (InSAR) images (interferograms) processed from both spaceborne Advanced Land Observing Satellite-1 (ALOS-1) and aerial Uninhabited Aerial Vehicle Synthetic Aperture Radar (UAVSAR) data acquired between 31 May 2010 and 10 April 2014 were used to measure post-eruptive deformation events. Interferograms suggest three distinct deformation processes after the May 2010 eruptions, including: (1) subsidence of the area involved in the co-eruptive slope movement; (2) localized deformation near the summit; and (3) emplacement and subsequent subsidence of about a 5.4 km lava flow. The detection of several different geophysical signals emphasizes the utility of measuring volcanic deformation using remote sensing techniques with broad spatial coverage. Additionally, the high spatial resolution of UAVSAR has proven to be an excellent compliment to satellite data, particularly for constraining motion components. Measuring the rapid initiation and cessation of flank instability, followed by stabilization and subsequent influence on eruptive features, provides a rare glimpse into volcanic slope stability processes. Observing these and other deformation events contributes both to hazard assessment at Pacaya and to the study of the stability of stratovolcanoes.

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“…Considering that at least two more similar rivers drain the thermal springs, we estimate a total SO 2 output for Tacaná of 60-90 t/d. Such SO 2 fluxes are typical for quiescent degassing volcanoes (Andres et al 1993;Taran et al 2002;Rodríguez et al 2004;Aiuppa et al 2005;Inguaggiato et al 2012). Besides dissolved magmatic volatiles, the thermal springs efficiently transport heat from the volcanohydrothermal system towards the surface (springs, rivers).…”

Section: 5mentioning

confidence: 96%

Fluid Geochemistry of Tacaná Volcano-Hydrothermal System

Rouwet

Taran

Inguaggiato

2015

Active Volcanoes of the World

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Tacaná hosts an active volcano-hydrothermal system, characterized by boiling temperature fumaroles, near the summit (3,600-3,800 m asl), and bubbling degassing thermal springs near its base (1,000-2,000 m asl). The magmatic signature of gases rising to the surface is attested by their high CO 2 contents (δ 13 C CO2 = −3.6 ± 1.3 ‰), and relatively high 3 He/ 4 He ratios (6.0 ± 0.9 R A ), with a CO 2 / 3 He ratio typical for the Central American Arc (2.3 × 10 10 -6.9 × 10 11 ). Such magmatic signature is practically identical for the near-summit fumaroles, and the bubbling gases at the base of Tacaná edifice. Besides the HCO 3 -enrichment in thermal spring waters, the springs (pH 5.8-6.7) show a SO 4 -and minor Cl-enrichment: a CO 2 and H 2 S + SO 2 -rich magmatic steam condenses into a deeper geothermal aquifer, and the resulting hydrothermal fluid mixes with meteoric waters near the surface. The recharge area for the thermal springs is located at higher elevations (>400 m higher than spring outlet elevation), as inferred from the δD-δ 18 O data for rivers, thermal and cold springs. These general insights of the Tacaná volcano-hydrothermal system serve as the baseline for future volcanic surveillance, and geothermal prospection. The main locus of hydrothermal activity is located inside the Tacaná horseshoe-shaped crater in the northwestern sector of the volcanic edifice. In terms of volcanic hazard, this sector can be considered the most probable site for future phreatic activity.

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SO2 emissions to the atmosphere from active volcanoes in Guatemala and El Salvador, 1999–2002

Cited by 51 publications

References 36 publications

SO2 loss rates in the plume emitted by Soufrière Hills volcano, Montserrat

SO2 loss rates in the plume emitted by Soufrière Hills volcano, Montserrat

Post-Eruption Deformation Processes Measured Using ALOS-1 and UAVSAR InSAR at Pacaya Volcano, Guatemala

Fluid Geochemistry of Tacaná Volcano-Hydrothermal System

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