Next Article in Journal
Impact of the Rainfall Duration and Temporal Rainfall Distribution Defined Using the Huff Curves on the Hydraulic Flood Modelling Results
Next Article in Special Issue
Erratum: Gliß, J.; et al. Pyplis–A Python Software Toolbox for the Analysis of SO2 Camera Images for Emission Rate Retrievals from Point Sources. Geosciences 2017, 7, 134
Previous Article in Journal
Landslides and Subsidence Assessment in the Crati Valley (Southern Italy) Using InSAR Data
Previous Article in Special Issue
Ground-Based Remote Sensing and Imaging of Volcanic Gases and Quantitative Determination of Multi-Species Emission Fluxes
 
 
Search for Articles:
Title / Keyword
Author / Affiliation / Email
Journal
Article Type
 
 
Advanced Search
 
Section
Special Issue
Volume
Issue
Number
Page
 
Journals
Geosciences
Volume 8
Issue 2
10.3390/geosciences8020068
geosciences-logo
Submit to this Journal Review for this Journal Propose a Special Issue
► Article Menu

Article Menu

share Share announcement Help format_quote Cite question_answer Discuss in SciProfiles thumb_up
...
Endorse textsms
...
Comment
first_page
settings
Order Article Reprints
Font Type:
Arial Georgia Verdana
Font Size:
Aa Aa Aa
Line Spacing:
Column Width:
Background:
Article

Ozone Depletion in Tropospheric Volcanic Plumes: From Halogen-Poor to Halogen-Rich Emissions

by
Tjarda J. Roberts
LPC2E Laboratoire de Physique et Chimie de l’Environnement et de l’Espace, UMR 7328 CNRS and Université d’Orléans, 3 Avenue de la Recherche Scientifique, 45071 Orléans, France
Geosciences 2018, 8(2), 68; https://doi.org/10.3390/geosciences8020068
Submission received: 15 November 2017 / Revised: 24 January 2018 / Accepted: 24 January 2018 / Published: 10 February 2018
(This article belongs to the Special Issue Volcanic Plumes: Impacts on the Atmosphere and Insights into Volcanic Processes)
Browse Figures
Versions Notes

Abstract

:
Volcanic halogen emissions to the troposphere undergo a rapid plume chemistry that destroys ozone. Quantifying the impact of volcanic halogens on tropospheric ozone is challenging, only a few observations exist. This study presents measurements of ozone in volcanic plumes from Kīlauea (HI, USA), a low halogen emitter. The results are combined with published data from high halogen emitters (Mt Etna, Italy; Mt Redoubt, AK, USA) to identify controls on plume processes. Ozone was measured during periods of relatively sustained Kīlauea plume exposure, using an Aeroqual instrument deployed alongside Multi-Gas SO2 and H2S sensors. Interferences were accounted for in data post-processing. The volcanic H2S/SO2 molar ratio was quantified as 0.03. At Halema‘uma‘u crater-rim, ozone was close to ambient in the emission plume (at 10 ppmv SO2). Measurements in grounding plume (at 5 ppmv SO2) about 10 km downwind of Pu‘u ‘Ō‘ō showed just slight ozone depletion. These Kīlauea observations contrast with substantial ozone depletion reported at Mt Etna and Mt Redoubt. Analysis of the combined data from these three volcanoes identifies the emitted Br/S as a strong but non-linear control on the rate of ozone depletion. Model simulations of the volcanic plume chemistry highlight that the proportion of HBr converted into reactive bromine is a key control on the efficiency of ozone depletion. This underlines the importance of chemistry in the very near-source plume on the fate and atmospheric impacts of volcanic emissions to the troposphere.

1. Introduction

Volcanoes release large quantities of gases and aerosols to the atmosphere. Very large explosive eruptions inject gases directly to the stratosphere, but a significant number of smaller eruptions and continuously passive degassing volcanoes release their emissions to the troposphere; the total global SO2 flux from passive degassing over 2004–2016 was recently estimated as 23 Tg/yr on average, exceeding volcanic eruptive emissions by about one order of magnitude [1]. To date, studies of the atmospheric chemistry and climate impacts of volcanic emissions have mostly focused on SO2 and its oxidation to sulfate particles in both the stratosphere (e.g., [2]) and troposphere (e.g., [3]). Volcanic sulfates also catalyse gas-aerosol reactions leading to reductions in stratospheric ozone levels, e.g., [4,5]. However, the volcanic release contains a number of other gases and particles, including notably the emission of volcanic halogens such as HBr and HCl (e.g., [6]). These were initially assumed to be simply washed out of the plume in the troposphere and deposited. Volcanic halogens can occasionally be injected into the stratosphere as evidenced by recent observations of HCl, OClO, BrO, and IO by satellite [7,8,9,10] and of HCl and HF by an instrumented aircraft that transected a high-altitude volcanic cloud [11]. Volcanic halogens that reach high altitudes may cause reductions in stratospheric ozone levels. This has been both observed [11] and simulated by numerical models (e.g., [12,13]) using atmospheric chemistry schemes that were originally developed to study impacts from anthropogenic sources of halogens (chlorofluorocarbons, CFCs) on stratospheric ozone.
The discovery of BrO in a volcanic plume in the troposphere through ground-based remote sensing by Borowski et al. [14] showed that volcanic HBr emissions can become transformed into reactive bromine over very short time-scales (minutes). Volcanic BrO has subsequently been observed in many tropospheric volcano plumes globally, e.g., [15,16] and references therein. A global analysis of satellite observations of volcanic BrO is provided by Hӧrmann et al. [17]. Volcanic OClO has also been reported in some tropospheric plumes [18,19,20,21]. The mechanism for reactive halogen formation in the troposphere at such very fast rates was not well understood. It was proposed that the formation of BrO in volcanic plumes could occur via a volcanic version of the autocatalytic “bromine explosion” (similar to that first identified in the polar boundary layer) [14,22]. This mechanism would lead to depletion of tropospheric ozone immediately downwind from the volcano, as has been confirmed by observations [23,24]. To better understand the fate of volcanic halogen emissions in the troposphere and their atmospheric chemistry impacts, two 1D or box models of the volcanic plume halogen chemistry were developed, [18,25,26], and the plume halogen chemistry was recently incorporated into a regional model [27]. The tropospheric chemistry model mechanisms are briefly outlined below.
Bromine is the main halogen species responsible for ozone depletion in volcanic plumes in the troposphere. Volcanic HBr emissions are converted into reactive bromine via an autocatalytic “bromine explosion” mechanism, involving gas-phase, photolytic, and heterogeneous (gas-aerosol) reactions; for a review, see Von Glasow et al. [28]. Cycles involving the formation and reactive uptake of HOBr and BrONO2 act to convert volcanic HBr into the reactive form Br2 that photolyses and can then deplete ozone via the reaction of Br with O3. A rapid interconversion cycle between BrO (self-reaction) and Br (that reacts with ozone to reform BrO) is suggested to be a major cause of ozone loss at high halogen concentrations (e.g., in the near-source plume). Upon depletion of plume HBr the reactive uptake of HOBr can form BrCl, promoting the formation of reactive chlorine through a non-autocatalytic cycle that can also contribute to ozone loss. Key controls on the plume chemistry are described by Roberts et al. [29] and include the following: the halogen emission flux, the primary volcanic aerosol emission that catalyses key heterogeneous (gas-aerosol) reactions of reactive halogens, and the rate of plume-air mixing that entrains oxidants including ozone into the plume. A high-temperature near-vent chemistry generates radicals that act to “kick-start” the downwind plume chemistry, thereby accelerating the (low-temperature) formation of BrO.
Comparison of the box/1D model simulations to plume observations enables testing of the underlying model mechanisms and is an important first step towards assessing regional-to-global-scale tropospheric impacts from volcanic halogen emissions. In such comparisons, the data is typically scaled to SO2 that acts as a quasi-plume-tracer over short time-scales. This enables to distinguish between plume chemistry and dilution effects. The model simulations were able to reproduce the observed magnitude and trends in volcanic BrO/SO2 downwind from Mt Etna [25,26,29], and to broadly capture the magnitude of reported OClO/SO2 [30]. Recent studies have also demonstrated a modelling capability to reproduce ozone depletion observed in the Mt Redoubt (AK, USA) plume [23] and at Mt Etna (Italy) [24]. Other model-predicted impacts of volcanic plume reactive halogen chemistry in the troposphere include depletion of HOx and NOx (the latter converted into nitric acid) [25] and conversion of inert mercury to a more reactive and easily deposited form [26]. A regional modelling study by Jourdain et al. [27] also highlighted the potential for volcanic plume reactive halogens to undergo secondary transport to the stratosphere (e.g., via convective events) for further impacts. However, uncertainties remain in our understanding of the very complex volcanic plume chemistry given the model parameter-space is vast and is constrained by rather few observations, particularly regarding the impacts of volcanic plume halogens on tropospheric ozone. This study presents field-measurements of ozone in the Halema‘uma‘u and Pu‘u ‘Ō‘ō plumes of Kīlauea (HI, USA) on 3 September 2007 and 19 July 2008, respectively, and compares them to reported observations at Mt Etna and Mt Redoubt. As a low halogen emitter, Kīlauea provides a useful “end-member” to complement the existing case-studies of the higher halogen emitters Mt Etna and Mt Redoubt, [23,24].
The goals of this study are: (i) to quantify the H2S emission alongside SO2 (i.e., H2S/SO2 ratio) enabling the prediction of cross-sensitivity on the Aeroqual ozone measurement; (ii) to measure ozone in the crater-rim plume; (iii) to measure ozone in the chemically more evolved downwind plume; and (iv) to interpret the ozone observations in the context of volcanic plume halogen chemistry and tropospheric ozone depletion reported in volcanic plumes globally.
Section 2 below outlines the challenges to measuring ozone in volcanic plumes; Section 3 describes the instruments and field-deployment; Section 4 presents the ozone measurements made at Kīlauea; and Section 5 discusses these observations in a wider volcanic plume chemistry context.

2. Challenges to In-Situ Measurement of Ozone in the Near-Source Volcano Plume

2.1. Interferences of Volcanic Gases on the Ozone Measurement

Ozone is present in the background troposphere at mixing ratios of tens of nmol/mol (or ppbv). Two main in-situ approaches to measuring atmospheric ozone are ultra-violet (UV) spectroscopy on ground-based or aircraft platforms (with instruments often operating at 254 nm, within the Hartley ozone absorption band) and the ozone (electrochemical) balloon sonde. A challenge to measuring ozone in volcanic plumes is the presence of other interfering gases at much higher abundances (e.g., µmol/mol or ppmv) than typically occur in the background atmosphere. These can induce positive or negative interferences to yield an erroneously high or low ozone measurement, respectively.
Specifically, volcanic SO2 induces a negative interference on electrochemical cell measurements of ozone. For example, ozone-sondes launched into the Eyjafjallajӧjkull 2010 eruption plume over Europe detected severely disturbed profiles [31], but the low ozone signal could not be quantifiably attributed to volcanic plume chemistry due to the interference from SO2. Volcanic SO2 induces a positive interference on UV spectroscopic measurements of ozone due to its absorption at 254 nm. This interference can be automatically corrected in dual channel instruments that contain a second (ozone scrubbed) channel, or may be subtracted in data post-processing using co-measured SO2, provided that the plume is sufficiently dilute [23]. Several airborne measurements of ozone in volcanic plumes have been reported; ozone concentrations were observed below ambient levels in a study of volcanic plumes predominantly from Alaska [32]. Ozone was depleted by at least a third compared to background, reaching up to 90% depletion in the 1980 Mount St. Helens eruption plume, during both ash-rich and ash-poor (passive degassing following the eruption) conditions [33,34]. Oppenheimer et al. [35] reports ozone depletion up to 35% with respect to background in the Mt Erebus (Antarctica) plume, alongside measurements of volcanic sulfur and nitrogen species, but also with some evidence for a very rapid (and unexplained) near-source reduction in SO2. Instrumented aircraft campaigns by Vance et al. [36] and Schumann et al. [37] measured ozone depletion alongside volcanic SO2 and other gases and particles in the 2010 Eyjafjallajokull eruption plume dispersed over Europe. Volcanic BrO was also observed in the downwind plume. However, the total volcanic bromine emission from Eyjafjallajokull was not well monitored. Finally, an instrumented aircraft campaign spatially mapped ozone depletion alongside SO2 in the 2010 Mt Redoubt eruption plume over 2–20 km downwind [27]. In this study, Kelly et al. also quantified the volcanic bromine emission by filterpack (HBr/SO2 = 4.1 × 10−3 mol/mol), enabling interpretation of the observations and a comparison to an atmospheric box model. Their study captured a rapid decrease in ozone in the near-downwind plume reaching up to tens of ppbv O3 loss, followed by a slow (partial) recovery in the dispersing plume. This demonstrated the need to characterise plume ozone-depleting chemistry over short spatial-timescales very near to the source. To do so, diffusion tubes were installed on Mt Etna flanks by Vance et al. [36], who reported an ozone depletion signature that was anti-correlated with SO2. However, corrosion problems prevented a measurement very close to the crater-rim. Some initial measurements were also made using a UV ozone instrument with CrO3 scrubber [36]. This approach was significantly furthered by Surl et al. [24], whose novel observations quantified the rate of ozone depletion through measurements on Mt Etna’s flanks. Their approach involved a portable single-channel UV spectroscopic instrument combined in series with CrO3 scrubbers to remove SO2 from the air inlet, with the ozone losses on the scrubber quantified and treated in the data post-processing. This enabled—for the first time—quantification of ozone depletion in very near-to-source plumes containing tens of ppmv of volcanic SO2 that was co-measured by small electrochemical sensor (Multi-Gas instrument). The volcanic bromine emission was also characterised during the field-campaign (HBr/SO2 = 6.13 × 10−4 mol/mol). Through observations made at up to several hundred meters distance from the summit emission source (equivalent to up to a few minutes travel time), Surl et al. [24] derived a linear equation for ozone loss in Mt Etna’s near-source plume as a function of travel time downwind from the summit craters, finding a gradient of ΔO3/ΔSO2 = (−1.02 ± 0.07) × 10−5 s−1 and intercept of (−6.2 ± 0.05) × 10−4 mol/mol. The non-zero intercept suggests that some depletion of ozone had already occurred before the gases reached the crater-rim. The ozone depletion rate (gradient) has been compared to atmospheric 1D and box model simulations by Surl et al. [24] and Roberts et al. [30].
Here, we used an Aeroqual instrument (WO3 sensor; Aeroqual Limited, Auckland, New Zealand) to measure ozone in the Kīlauea volcanic plumes (Halema‘uma‘u and Pu‘u ‘Ō‘ō, HI, USA). The instrument is much less sensitive to interference from volcanic SO2 than other methods, see Table 1. However, the sensor exhibits other cross-sensitivities as listed in Table 1. The most important cross-sensitivity for volcanic plumes is that of H2S at −2.5% that needs to be considered in data post-processing. The importance of this interference depends on the magmatic conditions specific to each volcano. Fumarolic emissions are H2S-rich (e.g., Vulcano, with H2S/SO2 molar ratios of ~1 [38]). Oxidized magma emissions are H2S-poor and dominated by SO2 (e.g., Masaya, Mt Etna, Kīlauea with H2S/SO2 molar ratios of just a few percent [39]). The H2S-poor nature of the Kīlauea volcanic emission is further verified by our in-situ real-time sensing of H2S and SO2 alongside ozone (see Results). Alongside our field-measurements of ozone, the bromine content of Kīlauea emissions was characterized by Mather et al. [40], finding HBr/SO2 = 2.9 × 10−5 mol/mol.

2.2. Intermittent Plume Exposure and Sensor Response Times

In-situ measurements of SO2 at the volcano crater-rim typically exhibit a high temporal variability. Rapid variations in local gas concentrations are often observed near to the volcanic source due to the complex local wind fields that advect the volcanic gases towards and away from the sensors. To characterize the emissions, the correlation in the time-series from two sensors (e.g., SO2 and H2S) is analyzed to derive a gas ratio, e.g., H2S/SO2. However, the response times of Multi-Gas and other sensors are not all identical, which can introduce uncertainty in the volcanic gas measurement [42]. Rapid variations in gas concentrations are also a challenge to the Aeroqual instrument that makes measurements of ozone at one-minute resolution. As mentioned in Section 2.1 above, the instrument sensor is sensitive to other gases, including (volcanic) H2S. These cross-sensitivities have been individually quantified by Aeroqual in laboratory experiments at constant gas abundance, Table 1. However, field-deployment of the Aeroqual instrument at volcanoes can expose it to time-varying abundances of volcanic gases. Very large and rapid temporal variations in interfering gas abundances may lead to anomalous values in the ozone measurement that are difficult to correct in data post-processing (see Section 3, Materials and Methods). A potential solution is to attempt to perform measurements under conditions of more sustained exposure to the volcanic plume. Such conditions are rather uncommon due to the local wind-field conditions near-to-source and because buoyant volcanic plumes tend to become elevated above ground. Here, we present in-situ observations of SO2, H2S, and ozone in the near-source and near-downwind Kīlauea (Halema‘uma‘u and Pu‘u ‘Ō‘ō, HI, USA) plumes obtained during two rare periods of relatively sustained plume exposure (>10 min at “plume strengths” of 5–10 ppmv SO2) on 3 September 2007 and 19 July 2008.

3. Materials and Methods

The Aeroqual portable ozone monitor is a hand-held instrument for measuring ozone at low mixing ratios at one-minute resolution using a tungsten oxide (WO3) sensor. The range is 0 to 150 ppbv and a reported resolution of 1 ppbv, accuracy <±5 ppbv (datasheets: www.Aeroqual.com [41]). The WO3 sensor is highly sensitive to ozone, but a major challenge to its use for atmospheric ozone measurements is sensitivity drift. The Aeroqual instrument uses propriety software to correct for WO3 sensitivity drift that involves different phases of sensor operation during the one-minute measurement period. Cross-sensitivities to the ozone measurement are reported by Aeroqual for fixed gas concentrations (such as for H2S, Table 1), however, the interferences caused by time-varying gas exposure under time-varying sensor operation are more complex to characterize or quantitatively account for in data post-processing. Therefore, this study focuses on Aeroqual measurements during some (rare) periods of relatively sustained plume exposure, and relies on co-measurements of SO2 and H2S to aid interpretation of the Aeroqual ozone observations.
Volcanic gases were measured at 1 Hz resolution using the pumped Multi-Gas system described by Roberts et al. [43] that includes Alphasense Ltd (Essex, UK) electrochemical sensors SO2-AF and H2S-A1 to measure SO2 and H2S respectively. Reported resolution of the sensors is <0.1 ppmv (SO2), <0.05 ppmv (H2S), and response time is <35 s (www.Alphasense.com [44]). The sensor current output was converted into ppmv mixing ratio time-series using sensitivities and cross-sensitivities determined from laboratory calibrations prior to the fieldwork. The H2S-A1 sensor exhibits a positive interference to SO2 that was subtracted in the data post-processing (using SO2 simultaneously measured by the SO2-AF sensor and calibration (cross)-sensitivities). Further details on the instrument and data analysis are provided by Roberts et al. [43].
Kīlauea volcano was emitting three plumes during the fieldwork: an emission from the Halema‘uma‘u summit crater (measured prior to the 2008 appearance of a lava-lake), the emission from Pu‘u ‘Ō‘ō (east rift zone vents), and an emission resulting from lava contact with sea-water (not sampled). Field-measurements were made at relatively sustained plume exposure on 3 September 2007 to sample Halema‘uma‘u crater-rim emissions and on 19 July 2008 sampling grounding plume downwind from Pu‘u ‘Ō‘ō, on chain of craters road. This latter site is about 10 km distance from the Pu‘u ‘Ō‘ō vent emission source. Linear regressions were performed to determine H2S/SO2 and ΔO3/ΔSO2 using robust-fit algorithms that yield similar results to least-squares but are less affected by outliers. The reported linear model trends exhibit p-values < 0.05 that indicate significant explanatory power. The R2 coefficient of determination (ratio of the explained variation to the total variation) was calculated using coefficients of correlation and is also provided in the Results.

4. Results

4.1. Volcanic SO2, H2S, and Ozone Measured in the Halema‘uma‘u Crater Rim Emission Plume

Time-series of volcanic SO2 and H2S gas abundances measured at Halema‘uma‘u crater-rim are well-correlated (p-value < 0.05 and R-squared = 0.52), and linear-regression finds a H2S/SO2 molar ratio of 0.030, see Figure 1. This result confirms the low H2S content of the Kīlauea plume, although the H2S/SO2 molar ratio is somewhat higher than has been reported previously [39]. This might reflect changing magmatic conditions over time. The scatter in the data is most likely due to instrument response times [41]. Nevertheless, a H2S measurement is still possible, due to the relatively sustained exposure (e.g., around 10 ppmv SO2 for tens of minutes). The statistical uncertainty in the gas ratio is very low (<10−3) due to the very large number of data points. The actual measurement uncertainty is probably somewhat higher as discussed in Section 4.2.
The volcanic SO2 time-series was filtered to make one-minute averaged data and these are compared to the ozone time-series (1 min resolution) in Figure 2. The measured ozone abundance fluctuates around 20 to 40 ppbv with a few (anomalous) zero data points. No clear trend is visible in the time-series although a scatter plot of the SO2, and ozone data show a weak anti-correlation (p-value < 0.05 and R-squared = 0.13). The gradient of the linear regression is −0.72 (±0.13) × 10−3 mol/mol. This measured ΔO3/ΔSO2 closely matches the predicted Aeroqual instrument response to a 2.5% H2S interference for volcanic plume with H2S/SO2 = 0.03 mol/mol (−2.5/100 × 0.03 = −0.75 × 10−3 mol/mol). Accounting for the H2S interference leads to the deduction in that actual in-plume ozone concentrations were very close to ambient levels in the emission plume at Halema‘uma‘u crater rim.

4.2. Volcanic SO2, H2S, and Ozone Measured in the Near-Downwind Plume from Pu‘u ‘Ō‘ō

Time-series of volcanic SO2 and H2S gas abundances measured in the plume ~10 km downwind from Pu‘u ‘Ō‘ō are also well-correlated (p-value < 0.05 and R-squared = 0.50), and linear-regression finds a H2S/SO2 molar ratio of 0.034, Figure 3. Visually, the data appear less scattered compared to those in Figure 1, reflecting improved instrument performance when exposed to more slowly fluctuating gas concentrations. However, instrument noise becomes important at these low H2S abundances in relatively dilute plume, leading to similar R2 as for Figure 1. The gas ratio is slightly higher than found for the crater-rim emissions from the Halema‘uma‘u (H2S/SO2 = 0.030 mol/mol) which could be due to (i) slight differences in the H2S/SO2 emitted from Pu‘u ‘Ō‘ō and Halema‘uma‘u despite their common magma source; (ii) partial atmospheric oxidation of SO2 in the Pu‘u ‘Ō‘ō plume by up to 14% (this would indicate a relatively fast in-plume SO2 oxidation); or (iii) uncertainty in the Multi-Gas measurement.
The one-minute averaged SO2 time-series is compared to the ozone measurement (at 1 min resolution) in Figure 4. The measured ozone abundance fluctuates between 30 and 50 ppbv. The last 20 min of the time-series appear mostly plume-free (low SO2) so show the natural variability in ozone abundance. There were no (anomalous) zero data points. A clear tendency (seen particularly in the first 50 min) is that ozone decreases in conjunction with maximum peaks in SO2. A scatter plot of the SO2 and ozone data confirms this anti-correlation (p-value < 0.05 and R-squared = 0.30). The R2 is higher than found at the crater-rim (Figure 2), i.e., the anti-correlation of ozone to SO2 explains a greater ratio of the variation in ozone compared to total variation for the Pu‘u ‘Ō‘ō downwind plume measurements than for that of the Halema‘uma‘u crater-rim measurements. The gradient of the linear regression is −1.15 (±0.18) × 10−3 mol/mol. This measured ΔO3/ΔSO2 exceeds the Aeroqual instrument response to volcanic H2S calculated as −0.84 × 10−3 mol/mol for a plume with H2S/SO2 molar ratio of 0.034. Accounting for the negative H2S interference on measured ozone at H2S/SO2 = 0.034 suggests an actual in-plume ΔO3/ΔSO2 of −0.31 (±0.18) × 10−3 mol/mol.
A source of uncertainty in the ozone depletion measurement is variation in background ozone, which appears to descend then ascend during the time-period, and also exhibits short-term variability. Additional uncertainties can arise from uncertainty in the interference from H2S, for example, an error of ±0.005 in the measured H2S/SO2 molar ratio would induce an uncertainty in the detected ΔO3/ΔSO2 of ±0.125 × 10−3 mol/mol, whilst an error of ±0.01 would induce an uncertainty in ΔO3/ΔSO2 of ±0.25 × 10−3 mol/mol. Nevertheless, results from the crater-rim observations suggested that H2S/SO2 measured by the Multi-Gas sensors is fully consistent with the expected interference. In summary, the data show that ozone in the downwind Pu‘u ‘Ō‘ō plume was likely slightly depleted below ambient levels but only by a small magnitude.

5. Discussion and Conclusion: Ozone Depletion from Halogen-Poor to Halogen-Rich Volcanic Plumes

Measurements of ozone in volcanic plumes are challenging. This study demonstrates the need to consider the interference of H2S on Aeroqual measurements of ozone, the need for sustained plume exposure (as 1 min measurements can be affected by rapid changes in gas concentration), and also illustrates natural variability in background ozone that can act to mask an observable ozone depletion signature. Nevertheless, the Aeroqual measurements provide a useful constraint on the magnitude of ozone depletion in the Kīlauea volcanic plumes at short distances from the source. In particular, the observations provide a valuable end-member example that quantifies ozone in the plume of a low halogen emitter. This contrasts to studies to date that mostly focused on volcanic plumes with higher halogen contents. To interpret the field-data, ozone depletion is scaled relative to co-measured SO2 in order to distinguish between chemistry and plume dilution effects, and it is interpreted in terms of distance or travel time downwind and the bromine emission.
For the Kīlauea plumes, ozone was shown to be close to ambient levels during plume exposures of up to 10 ppmv SO2 at the Halema‘uma‘u crater-rim, and they were only slightly depleted in the grounding plume at around 10 km downwind from Pu‘u ‘Ō‘ō (e.g., by up to 2 ppbv measured at 5–8 ppmv SO2). The measurements indicate that the volcano emission has only a limited impact on tropospheric ozone, as might be expected for a low halogen emitter. This contrasts with findings for higher halogen emitters. A study of Mt Etna plume ozone by Surl et al. [24], for example, found 11 ppbv ozone depletion measured in plume exposure of 9 ppmv SO2 at just 300 m downwind. Surl et al. [24] also suggest that ozone in the Mt Etna crater-rim plume was depleted below background, finding from their near-source field-campaign that ΔO3/ΔSO2 = (−1.02 ± 0.07) × 10−5 s−1 with an intercept of (−6.2 ± 0.05) × 10−4 mol/mol. A much greater depletion of tropospheric ozone (tens of ppbv ozone loss in plume of 1 ppmv SO2) was observed by Kelly et al. [23] through spatial mapping of the Mt Redoubt 2009 eruption plume. The ΔO3/ΔSO2 data from Kelly et al. [23] is shown in Figure 5 as a function of distance downwind for two flight campaigns. A smaller ozone depletion was observed in August compared to June 2009. We focus our comparison on the June 2009 data for which the volcanic halogen emission was also quantified (just one day prior to the aircraft campaign) that yields a linear regression in ΔO3/ΔSO2 of (−7.2 ± 1.3) × 10−3 mol/mol km−1, with intercept close to zero (within statistical uncertainty). Table 2 summarizes these field measurements and interconverts ΔO3/ΔSO2 per unit travel time or per distance downwind using available or estimated wind-speeds. Not shown in Table 2 are aircraft studies of the 2010 Eyjafjallajӧkull eruption plume over Europe [36,37] that found large ozone depletions in the far-field dispersed plume but which are difficult to interpret because the halogen emission was poorly constrained and the assumption of SO2 as a quasi-plume-tracer (in ΔO3/ΔSO2) may not be valid.
Figure 6 presents the ΔO3/ΔSO2 scaled to distance or travel time downwind (i.e., rate of ozone depletion) as a function of Br/S in the volcano emission for the three case studies of Table 2 (Kīlauea, Mt Etna, and Mt Redoubt). The data show that ozone depletion is a non-linear function of the bromine emission; greater ozone loss occurs for a higher Br/S emission, as expected. However, the rate of ozone depletion for the volcano with the highest Br/S emission (Mt Redoubt) is disproportionately slow, i.e., the Mt Redoubt plume is found to be less efficient at destroying tropospheric ozone than would be expected. This non-linearity is initially a surprising result given the role of volcanic bromine in the depletion of tropospheric ozone through a “bromine explosion” that is autocatalytic (i.e., self-enhancing). A potential reason could be the complete titration of plume ozone (thereby preventing any further ozone depletion), but this is ruled out based on the measurements of Kelly et al. [23]; ozone in the Mt Redoubt plume was reduced to less than ambient levels but was not fully depleted. Instead, an explanation is provided by atmospheric box modelling of the near-source plume chemistry. Model studies point to non-linearities in the conversion of emitted HBr into reactive bromine species, depending on the bromine content of the emissions [24,29]. For high Br/S emissions, not all of the emitted HBr may become converted into reactive bromine. This was shown in a model sensitivity study by Roberts et al. [29] for Mt Etna that predicts HBr is rapidly and fully converted into reactive forms over tens of minutes for an emission with HBr/SO2 molar ratio of 7.4 × 10−4, but HBr is more slowly and only partially (~50% after one hour) converted into reactive bromine for an emission with a higher HBr/SO2 molar ratio of 2.4 × 10−3. Furthermore, the model simulation of the Mt Redoubt 2009 eruption plume by Kelly et al. [23] predicts that only 30% of emitted HBr was converted into reactive forms, for an emission with even higher HBr/SO2 molar ratio of 4.1 × 10−3. However, another difference between the plumes is the emission flux, with 4.3 kg/s SO2 flux for Mt Redoubt and ~20 kg/s SO2 flux for the Mt Etna simulation. The net conversion of emitted volcanic HBr into reactive bromine reflects the balance of plume chemistry processes (that form reactive halogens from HBr and that can re-form HBr from reactive halogens) as a function of plume properties such as gas flux, aerosol, plume-air mixing, etc., and is also a function of time. For plumes younger than one minute, recent observations by Rüdiger et al. [45] suggest reactive bromine accounts for less than 44% of total bromine, consistent with the models. The modeled plume Br-speciation predicted by Roberts et al. [23] and [29] are shown in Figure 7, illustrating the proportion of emitted HBr converted into reactive bromine during the first hours of plume chemical evolution. These model outputs are used to re-evaluate the non-linear trend in Figure 6. When the Br/S content of the emissions is adjusted to reflect the modeled plume “reactive bromine”/S (e.g., reduced to 30% of the total emitted Br/S for Mt Redoubt: open triangle, Figure 6), there is more linearity (broadly proportional trend) between the volcanic (reactive) bromine/S and the rate of plume ozone depletion. It is nevertheless expected that other variables, e.g., aerosol and plume-air mixing rate, may affect ΔO3/ΔSO2 depending on the volcanic-meteorological setting.
In conclusion, chemistry in the near-source volcanic plume exerts an important influence on the fate of volcanic halogens entering the troposphere. Plume chemistry converts the volcanic HBr emission into reactive bromine, causing the depletion of tropospheric ozone. Measurements of ozone in the near-source volcanic plume are challenging to make but they can provide useful observational constraints on the volcanic plume halogen chemistry. This study presents observations of ozone in the volcanic plumes from Kīlauea, a low-halogen emitter. Ozone was close to ambient levels in crater-rim Halema‘uma‘u emissions and only slightly depleted in the plume 10 km downwind from Pu‘u ‘Ō‘ō. This contrasts with observations of much larger ozone depletion (tens of ppbv) in the near-source and near-downwind plumes of two higher halogen emitters: Mt Etna and Mt Redoubt [23,24]. The available observations combined with numerical modelling of the plume chemistry suggest that the volcanic Br/S emission and its (partial or complete) conversion into reactive bromine are key controls in the depletion of tropospheric ozone downwind from the volcano. Characterizing the near-source volcanic plume chemistry is thus an essential step to quantifying the fate and downwind impacts of volcanic emissions to the atmosphere.

Acknowledgments

This work was funded by the Orleans Labex VOLTAIRE (VOLatils-Terre Atmosphère Interactions—Ressources et Environnement) ANR-10-LABX-100-01, and a UK NERC studentship, and acknowledges MDPI for the invitation to cover publication fees. I would like to thank the following people for very useful discussions on volcano science, sensors, and ozone observations: Clive Oppenheimer, Rod Jones, John Saffell (Alphasense Ltd., Essex, UK), Peter Kelly, Luke Surl; field-collaborators Tamsin Mather and Mel Witt; and the Hawai‘i Volcano Observatory. I also thank the editor P. Sellitto and two anonymous reviewers.

Conflicts of Interest

The authors declare no conflict of interest. The founding sponsors had no role in the design of the study; in the collection, analyses, or interpretation of data; in the writing of the manuscript, and in the decision to publish the results.

References

  1. Carn, S.A.; Fioletov, V.E.; McLinden, C.A.; Li, C.; Krotkov, N.A. A decade of global volcanic SO2 emissions measured from space. Sci. Rep. 2017, 44095. [Google Scholar] [CrossRef] [PubMed]
  2. Stoffell, M.; Khodri, M.; Corona, C.; Guillet, S.; Poulain, V.; Bekki, S.; Guiot, J.; Luckman, B.H.; Oppenheimer, C.; Lebas, N.; et al. Estimates of volcanic-induced cooling in the Northern Hemisphere over the past 1500 years. Nat. Geosci. 2015, 8, 784–788. [Google Scholar] [CrossRef]
  3. Sellitto, P.; Zanetel, C.; di Sarra, A.; Salerno, G.; Tapparo, A.; Meloni, D.; Pace, G.; Caltabiano, T.; Briole, P.; Legras, B. The impact of Mount Etna sulfur emissions on the atmospheric composition and aerosol properties in the central Mediterranean: A statistical analysis over the period 2000–2013 based on observations and Lagrangian modelling. Atmos. Environ. 2017, 148, 77–88. [Google Scholar] [CrossRef]
  4. Berthet, G.; Jégou, F.; Catoire, V.; Krysztofiak, G.; Renard, J.B.; Bourassa, A.E.; Degenstein, D.A.; Brogniez, C.; Dorf, M.; Kreycy, S.; et al. Impact of a moderate volcanic eruption on chemistry in the lower stratosphere: Balloon-borne observations and model calculations. Atmos. Chem. Phys. 2017, 17, 2229–2253. [Google Scholar] [CrossRef]
  5. Ivy, D.J.; Solomon, S.; Kinnison, D.; Mills, M.J.; Schmidt, A.; Neely, R.R., III. The influence of the Calbuco eruption on the 2015 Antarctic ozone hole in a fully coupled chemistry-climate model. Geophys. Res. Lett. 2017, 44, 2556–2561. [Google Scholar] [CrossRef]
  6. Aiuppa, A.; Baker, D.R.; Webster, J.D. Halogens in volcanic systems. Chem. Geol. 2009, 263, 1–18. [Google Scholar] [CrossRef]
  7. Carn, S.; Clarisse, L.; Prata, A.J. Multi-decadal satellite measurements of global volcanic degassing. J. Volcanol. Geotherm. Res. 2016, 311, 99–134. [Google Scholar] [CrossRef]
  8. Theys, N.; Van Roozendael, M.; Dils, B.; Hendrick, F.; Hao, N.; De Mazière, M. First satellite detection of volcanic bromine monoxide emission after the Kasatochi eruption. Geophys. Res. Lett. 2009, 36. [Google Scholar] [CrossRef] [Green Version]
  9. Theys, N.; De Smedt, I.; Van Roozendael, M.; Froidevaux, L.; Clarisse, L.; Hendrick, F. First satellite detection of volcanic OClO after the eruption of Puyehue-Cordón Caulle. Geophys. Res. Lett. 2014, 41, 667–672. [Google Scholar] [CrossRef]
  10. Schönhardt, A.; Richter, A.; Theys, N.; Burrows, J.P. Space-based observation of volcanic iodine monoxide. Atmos. Chem. Phys. 2017, 17, 4857–4870. [Google Scholar] [CrossRef]
  11. Rose, W.I.; Millard, G.A.; Mather, T.A.; Hunton, D.E.; Anderson, B.; Oppenheimer, C.; Thornton, B.F.; Gerlach, T.; Viggiano, A.A.; Kondo, Y.; et al. Atmospheric chemistry of a 33–34 hour old volcanic cloud from Hekla Volcano (Iceland): Insights from direct sampling and the application of chemical box modeling. J. Geophys. Res. 2006, 111, D20206. [Google Scholar] [CrossRef]
  12. Millard, G.A.; Mather, T.A.; Pyle, D.M.; Rose, W.I.; Thornton, B. Halogen emissions from a small volcanic eruption: Modeling the peak concentrations, dispersion, and volcanically induced ozone loss in the stratosphere. Geophys. Res. Lett. 2006, 33, L19815. [Google Scholar] [CrossRef]
  13. Lurton, T.; Jégou, F.; Berthet, G.; Renard, J.-B.; Clarisse, L.; Schmidt, A.; Brogniez, C.; Roberts, T. Model simulations of the chemical and aerosol microphysical evolution of the Sarychev Peak 2009 eruption cloud compared to in-situ and satellite observations. Atmos. Chem. Phys. Discuss. 2017. [Google Scholar] [CrossRef]
  14. Bobrowski, N.; Honninger, G.; Galle, B.; Plat, U. Detection of bromine monoxide in a volcanic plume. Nature 2003, 423, 273–276. [Google Scholar] [CrossRef] [PubMed]
  15. Boichu, M.; Oppenheimer, C.; Roberts, T.J.; Tsanev, V.; Kyle, P. On bromine, nitrogen oxides and ozone depletion in the tropospheric plume of Erebus volcano (Antarctica). Atmos. Environ. 2011, 45, 3856–3866. [Google Scholar] [CrossRef] [Green Version]
  16. Lübcke, P.; Bobrowski, N.; Arellano, S.; Galle, B.; Garzón, G.; Vogel, L.; Platt, U. BrO/SO2 molar ratios from scanning DOAS measurements in the NOVAC network. Solid Earth 2014, 5, 409–424. [Google Scholar] [CrossRef]
  17. Hörmann, C.; Sihler, H.; Bobrowski, N.; Beirle, S.; de Vries, M.P.; Platt, U.; Wagner, T. Systematic investigation of bromine monoxide in volcanic plumes from space by using the GOME-2 instrument. Atmos. Chem. Phys. 2013, 13, 4749–4781. [Google Scholar] [CrossRef]
  18. Bobrowski, N.; von Glasow, R.; Aiuppa, A.; Inguaggiato, S.; Louban, I.; Ibrahim, O.W.; Platt, U. Reactive halogen chemistry in volcanic plumes. J. Geophys. Res. 2007, 112, D06311. [Google Scholar] [CrossRef]
  19. General, S.; Bobrowski, N.; Pöhler, D.; Weber, K.; Fischer, C.; Platt, U. Airborne I-DOAS measurements at Mt. Etna: BrO and OClO evolution in the plume. J. Volcanol. Geotherm. Res. 2015, 300, 175–186. [Google Scholar] [CrossRef]
  20. Gliß, J.; Bobrowski, N.; Vogel, L.; Pöhler, D.; Platt, U. OClO and BrO observations in the volcanic plume of Mt. Etna—Implications on the chemistry of chlorine and bromine species in volcanic plumes. Atmos. Chem. Phys. 2015, 15, 5659–5681. [Google Scholar] [CrossRef] [Green Version]
  21. Donovan, A.; Tsanev, V.; Oppenheimer, C.; Edmonds, M. Reactive halogens (BrO and OClO) detected in the plume of Soufrière Hills Volcano during an eruption hiatus. Geochem. Geophys. Geosyst. 2014, 15, 3346–3363. [Google Scholar] [CrossRef] [Green Version]
  22. Oppenheimer, C.; Tsanev, V.I.; Braban, C.F.; Cox, R.A.; Adams, J.W.; Aiuppa, A.; Bobrowski, N.; Delmelle, P.; Barclay, J.; McGonigle, A.J. BrO fomation in volcanic plumes. Geochim. Cosmochim. Acta 2006, 70, 2935–2941. [Google Scholar] [CrossRef]
  23. Kelly, P.J.; Kern, C.; Roberts, T.J.; Lopez, T.; Werner, C.; Aiuppa, A. Rapid chemical evolution of tropospheric volcanic emissions from Redoubt Volcano, Alaska, based on observations of ozone and halogen-containing gases. J. Volcanol. Geotherm. Res. 2013, 259, 317–333. [Google Scholar] [CrossRef]
  24. Surl, L.; Donohoue, D.; Aiuppa, A.; Bobrowski, N.; von Glasow, R. Quantification of the depletion of ozone in the plume of Mount Etna. Atmos. Chem. Phys. 2015, 15, 2613–2628. [Google Scholar] [CrossRef] [Green Version]
  25. Roberts, T.J.; Braban, C.F.; Martin, R.S.; Oppenheimer, C.; Adams, J.W.; Cox, R.A.; Jones, R.L.; Griffiths, P.T. Modelling reactive halogen formation and ozone depletion in volcanic plumes. Chem. Geol. 2009, 263, 151–163. [Google Scholar] [CrossRef]
  26. Von Glasow, R. Atmospheric chemistry in volcanic plumes. Proc. Natl. Acad. Sci. USA 2010, 107, 6594–6599. [Google Scholar] [CrossRef] [PubMed]
  27. Jourdain, L.; Roberts, T.J.; Pirre, M.; Josse, B. Modeling the reactive halogen plume from Ambrym volcano and its impact on the troposphere with the CCATT-BRAMS mesoscale model. Atmos. Chem. Phys. 2016, 16, 12099–12125. [Google Scholar] [CrossRef]
  28. Von Glasow, R.; Bobrowski, N.; Kern, C. The effects of volcanic eruptions on atmospheric chemistry. Chem. Geol. 2009, 263, 131–142. [Google Scholar] [CrossRef]
  29. Roberts, T.J.; Martin, R.S.; Jourdain, L. Reactive halogen chemistry in Mt Etna’s volcanic plume: The influence of total Br, high temperature processing, aerosol loading and plume-air mixing (volcanic emissions flux). Atmos. Chem. Phys. 2014, 14, 11201–11219. [Google Scholar] [CrossRef] [Green Version]
  30. Roberts, T.J.; Vignelles, D.; Liuzzo, M.; Giudice, G.; Aiuppa, A.; Coltelli, M.; Salerno, G.; Chartier, M.; Couté, B.; Berthet, G.; et al. The primary volcanic aerosol emission from Mt Etna: Size-resolved particles with SO2 and role in plume reactive halogen chemistry. Geochim. Cosmochim. Acta 2018, 222, 74–93. [Google Scholar] [CrossRef]
  31. Flentje, H.; Claude, H.; Elste, T.; Gilge, S.; Köhler, U.; Plass-Dülmer, C.; Steinbrecht, W.; Thomas, W.; Werner, A.; Fricke, W. The Eyjafjallajökull eruption in April 2010—Detection of volcanic plume using in-situ measurements, ozone sondes and lidar-ceilometer profiles. Atmos. Chem. Phys. 2010, 10, 10085–10092. [Google Scholar] [CrossRef] [Green Version]
  32. Stith, J.L.; Hobbs, P.V.; Radke, L.F. Airborne particle and gas measurements in the emissions from six volcanoes. J. Geophys. Res. 1978, 83, 4009–4017. [Google Scholar] [CrossRef]
  33. Fruchter, J.S.; Robertson, D.E.; Evans, J.C.; Oslen, K.B.; Lepel, E.A.; Laul, J.C.; Abel, K.H.; Sanders, R.W.; Jackson, P.O.; Wogman, N.S.; et al. Mount St. Helens ash from the 18 May 1980 eruption: Chemical, physical, mineralogical and biological properties. Science 1980, 209, 1116–1125. [Google Scholar] [CrossRef] [PubMed]
  34. Hobbs, P.V.; Tuell, J.P.; Hegg, D.A.; Radke, L.F.; Eltgroth, M.W. Particles and gases in the emissions from the 1980–1981 volcanic eruptions of Mt. St. Helens. J. Geophys. Res. 1982, 87, 11062–11086. [Google Scholar] [CrossRef]
  35. Vance, A.; McGonigle, A.J.S.; Aiuppa, A.; Stith, J.L.; Turnbull, K.; von Glasow, R. Ozone depletion in tropospheric volcanic plumes. Geophys. Res. Lett. 2010, 37, L22802. [Google Scholar] [CrossRef]
  36. Schumann, U.; Weinzierl, B.; Reitebuch, O.; Schlager, H.; Miniki, A.; Forster, C.; Baumann, R.; Saile, T.; Graf, K.; Mannstein, H.; et al. Airborne observations of the Eyjafjalla volcano ash cloud over Europe during air space closure in April and May 2010. Atmos. Chem. Phys. 2011, 11, 2245–2279. [Google Scholar] [CrossRef] [Green Version]
  37. Oppenheimer, C.; Kyle, P.; Eisele, F.; Crawford, J.; Huey, G.; Tanner, D.; Saewung, K.; Mauldin, L.; Blake, D.; Beyersdorf, A.; et al. Atmospheric chemistry of an Antarctic volcanic plume. J. Geophys. Res. 2010, 115, D04303. [Google Scholar] [CrossRef]
  38. Aiuppa, A.; Federico, C.; Giudice, G.; Gurrieri, S. Chemical mapping of a fumarolic field: La Fossa Crater, Vulcano Island (Aeolian Islands, Italy). Geophys. Res. Lett. 2005, 32, L13309. [Google Scholar] [CrossRef]
  39. Gerlach, T.M. Volcanic sources of tropospheric ozone-depleting trace gases. Geochem. Geophys. Geosyst. 2004, 5, Q09007. [Google Scholar] [CrossRef]
  40. Mather, T.A.; Witt, M.L.I.; Pyle, D.M.; Quayle, B.M.; Aiuppa, A.; Bagnato, E.; Martin, R.S.; Sims, K.W.W.; Edmonds, M.; Sutton, A.J.; et al. Halogens and trace metal emissions from the ongoing 2008 summit eruption of Kīlauea volcano, Hawai`I. Geochim. Cosmochim. Acta 2012, 83, 292–323. [Google Scholar] [CrossRef]
  41. Aeroqual Limited. Datasheets for Aeroqual Series 500 Portable Ozone Instrument. Available online: https://www.aeroqual.com/product/series-500-portable-ozone-gas-monitor (accessed on 24 January 2018).
  42. Roberts, T.J.; Saffell, J.R.; Dawson, D.H.; Oppenheimer, C.; Lurton, T. Electrochemical sensors applied to pollution monitoring: Measurement error and gas ratio bias—A volcano plume case study. J. Volcanol. Geotherm. Res. 2014, 281, 85–96. [Google Scholar] [CrossRef]
  43. Roberts, T.J.; Braban, C.; Oppenheimer, C.; Martin, R.S.; Saffell, J.R.; Dawson, D.; Freshwater, R.A.; Griffiths, P.T.; Jones, R.L. Electrochemical sensing of volcanic plumes. Chem. Geol. 2012, 332–333, 74–91. [Google Scholar] [CrossRef]
  44. Alphasense Sensor Technology Company. Datasheets for Alphasense SO2-AF and H2S-A1 Sensors. Available online: http://www.alphasense.com/index.php/safety/downloads/ (accessed on 24 January 2018).
  45. Rüdiger, J.; Bobrowski, N.; Liotta, M.; Hoffman, T. Development and application of a sampling method for the determination of reactive halogen species in volcanic gas emissions. Anal. Bioanal. Chem. 2017, 409, 5975–5985. [Google Scholar] [CrossRef] [PubMed]
Geosciences 08 00068 g001 550
Figure 1. Volcanic plume SO2 and H2S abundances measured at 1 Hz resolution in the crater-rim emissions from Halema‘uma‘u on 3 September 2007. These two volcanic gas time-series are well-correlated; a scatter plot with linear regression yields the H2S/SO2 molar ratio of 0.030 mol/mol. p-value < 0.05 and R-squared = 0.52.
Figure 1. Volcanic plume SO2 and H2S abundances measured at 1 Hz resolution in the crater-rim emissions from Halema‘uma‘u on 3 September 2007. These two volcanic gas time-series are well-correlated; a scatter plot with linear regression yields the H2S/SO2 molar ratio of 0.030 mol/mol. p-value < 0.05 and R-squared = 0.52.
Geosciences 08 00068 g001
Geosciences 08 00068 g002 550
Figure 2. Volcanic plume SO2 and ozone abundances measured at 1 min resolution in the crater-rim emissions from Halema‘uma‘u on 3 September 2007. The data show a degree of scatter (with some zero ozone observations that are likely instrument anomalies) and weak anti-correlation between measured ozone and SO2. The linear regression has gradient ΔO3/ΔSO2 = −0.72 (± 0.13) × 10−3 mol/mol with intercept corresponding to 35 nmol/mol ambient ozone. p-value < 0.05 and R-squared = 0.13. Dashed lines denote regression trend with coefficients ±2× standard error (95% CI).
Figure 2. Volcanic plume SO2 and ozone abundances measured at 1 min resolution in the crater-rim emissions from Halema‘uma‘u on 3 September 2007. The data show a degree of scatter (with some zero ozone observations that are likely instrument anomalies) and weak anti-correlation between measured ozone and SO2. The linear regression has gradient ΔO3/ΔSO2 = −0.72 (± 0.13) × 10−3 mol/mol with intercept corresponding to 35 nmol/mol ambient ozone. p-value < 0.05 and R-squared = 0.13. Dashed lines denote regression trend with coefficients ±2× standard error (95% CI).
Geosciences 08 00068 g002
Geosciences 08 00068 g003 550
Figure 3. Volcanic plume SO2 and H2S abundances measured at 1 Hz resolution in the grounding plume ~10 km from the Pu‘u ‘Ō‘ō emission source on 19 July 2008. These two volcanic gas time-series are well-correlated; a scatter plot with linear regression yields an H2S/SO2 molar ratio of 0.0335 mol/mol. p-value < 0.05 and R-squared = 0.50.
Figure 3. Volcanic plume SO2 and H2S abundances measured at 1 Hz resolution in the grounding plume ~10 km from the Pu‘u ‘Ō‘ō emission source on 19 July 2008. These two volcanic gas time-series are well-correlated; a scatter plot with linear regression yields an H2S/SO2 molar ratio of 0.0335 mol/mol. p-value < 0.05 and R-squared = 0.50.
Geosciences 08 00068 g003
Geosciences 08 00068 g004 550
Figure 4. Volcanic plume SO2 and ozone abundances measured at 1 min resolution in grounding plume on a chain of craters road on 19 July 2008. This location is approximately 10 km downwind of the Pu‘u ‘Ō‘ō volcanic emission source. Peak maxima in the volcanic SO2 time-series correspond to clearly defined minima in the ozone time-series. The anti-correlation between ozone and SO2 is confirmed by scatter-plot; the linear regression has gradient ΔO3/ΔSO2 = −1.15 (±0.18) × 10−3 mol/mol with intercept corresponding to 43 nmol/mol ambient ozone. Dashed lines denote regression trend with coefficients ±2× standard error (95% CI). p-value < 0.05 and R-squared = 0.30. This measured ΔO3/ΔSO2 exceeds the Aeroqual instrument response to volcanic H2S, therefore, it indicates an ozone depletion. See text for further details and quantification.
Figure 4. Volcanic plume SO2 and ozone abundances measured at 1 min resolution in grounding plume on a chain of craters road on 19 July 2008. This location is approximately 10 km downwind of the Pu‘u ‘Ō‘ō volcanic emission source. Peak maxima in the volcanic SO2 time-series correspond to clearly defined minima in the ozone time-series. The anti-correlation between ozone and SO2 is confirmed by scatter-plot; the linear regression has gradient ΔO3/ΔSO2 = −1.15 (±0.18) × 10−3 mol/mol with intercept corresponding to 43 nmol/mol ambient ozone. Dashed lines denote regression trend with coefficients ±2× standard error (95% CI). p-value < 0.05 and R-squared = 0.30. This measured ΔO3/ΔSO2 exceeds the Aeroqual instrument response to volcanic H2S, therefore, it indicates an ozone depletion. See text for further details and quantification.
Geosciences 08 00068 g004
Geosciences 08 00068 g005 550
Figure 5. Ozone depletion (scaled to co-measured SO2) in the Mt Redoubt 2009 eruption plume as a function of distance downwind during the aircraft campaigns on 21 June (black triangles) and 19 August (grey triangles) 2009. Data from Kelly et al. [23]. The gradient of the linear regression for 21 June is (−7.2 ± 1.3) × 10−3 mol/mol km−1.
Figure 5. Ozone depletion (scaled to co-measured SO2) in the Mt Redoubt 2009 eruption plume as a function of distance downwind during the aircraft campaigns on 21 June (black triangles) and 19 August (grey triangles) 2009. Data from Kelly et al. [23]. The gradient of the linear regression for 21 June is (−7.2 ± 1.3) × 10−3 mol/mol km−1.
Geosciences 08 00068 g005
Geosciences 08 00068 g006 550
Figure 6. Depletion in ozone scaled to volcanic SO2 (as a quasi-plume-tracer) and scaled with (i) km distance downwind or (ii) seconds travel time downwind, plotted as a function of the bromine/SO2 molar ratio in the emission. Data are available for three volcanic systems: Kīlauea (red circle, this study), Mt Etna (purple square, [24]), and Mt Redoubt (black triangle, [23]), in ascending order of Br/S in their emissions. Arrow and open triangle denote adjustments in the Br/S content that accounts for partial rather than full conversion of emitted HBr into reactive bromine. See text for details.
Figure 6. Depletion in ozone scaled to volcanic SO2 (as a quasi-plume-tracer) and scaled with (i) km distance downwind or (ii) seconds travel time downwind, plotted as a function of the bromine/SO2 molar ratio in the emission. Data are available for three volcanic systems: Kīlauea (red circle, this study), Mt Etna (purple square, [24]), and Mt Redoubt (black triangle, [23]), in ascending order of Br/S in their emissions. Arrow and open triangle denote adjustments in the Br/S content that accounts for partial rather than full conversion of emitted HBr into reactive bromine. See text for details.
Geosciences 08 00068 g006
Geosciences 08 00068 g007 550
Figure 7. Model simulated reactive bromine speciation in the plumes of Mt Etna and Mt Redoubt, from Roberts et al. [29], and Kelly et al. [23] illustrating varying degrees (complete, partial) of conversion of HBr into reactive bromine. Reproduced with permission from Kelly et al. [23], JVGR; published by Elsevier.
Figure 7. Model simulated reactive bromine speciation in the plumes of Mt Etna and Mt Redoubt, from Roberts et al. [29], and Kelly et al. [23] illustrating varying degrees (complete, partial) of conversion of HBr into reactive bromine. Reproduced with permission from Kelly et al. [23], JVGR; published by Elsevier.
Geosciences 08 00068 g007
Table
Table 1. Cross-sensitivities of Aeroqual ozone instrument (tungsten oxide sensor). Source: www.Aeroqual.com [41].
Table 1. Cross-sensitivities of Aeroqual ozone instrument (tungsten oxide sensor). Source: www.Aeroqual.com [41].
Test GasMixing Ratio (ppmv)Sensor Reading (ppmv)Sensitivity (%)
Ammonia (NH3)25−0.02−0.08
Butane100000
Carbon monoxide (CO)10000
Carbon dioxide (CO2)100000
Chlorine (Cl2)0.50.2−40
Ethanol20−0.02−0.1
Ethyl acetate100−0.02−0.02
Heptane10000
Hydrogen sulfide (H2S)4−0.1−2.5
Isopropanol2000
Methane (CH4)500000
Nitrogen dioxide (NO2)0.50.120
Ozone (O3)0.30.3100
Perchloroethylene5000
Propane500000
Sulfur dioxide (SO2)1000
Toluene5000
Table
Table 2. Studies of ozone depletion in volcanic plumes where the halogen emission was also reported: Br/S in the emission and ΔOzone/ΔSO2 per km downwind or per second of travel time.
Table 2. Studies of ozone depletion in volcanic plumes where the halogen emission was also reported: Br/S in the emission and ΔOzone/ΔSO2 per km downwind or per second of travel time.
VolcanoBr/S
(mmol/mol)		Distance
(km)		Wind Speed * m/sTime
(min)		ΔO3/ΔSO2 Per km
(km−1) × 10−3		ΔO3/ΔSO2 Per Second
(s−1) × 10−5		Reference
Mt Redoubt
2009 eruption		4.12.4–27.84.49–105−7.2 ± 1.3−3.2 ± 0.6[23]
(Figure 5 this study)
Mt Etna passive degassing 20120.6130.15–0.40~2.21–4(−4.4 ± 0.3)−1.02 ± 0.07[24]
Kīlauea plumes
2007–2008		0.029 ± 0.025~10~5~30Up to −0.03(Up to 0.02)This study (ΔO3/ΔSO2)
[40] (2012) (Br/S)
* Wind-speed reported directly by Kelly et al. [23] for the study of Mt Redoubt, calculated from the reported 380 m distance downwind equivalent to about 175 s travel time in the study of Mt Etna by Surl et al. [24], and estimated from Hilo radiosonde data for the study of Kīlauea. Values of ozone depletion rate in brackets were obtained by interconverting time and distance data using the wind-speeds of Table 2.

Share and Cite

MDPI and ACS Style

Roberts, T.J. Ozone Depletion in Tropospheric Volcanic Plumes: From Halogen-Poor to Halogen-Rich Emissions. Geosciences 2018, 8, 68. https://doi.org/10.3390/geosciences8020068

AMA Style

Roberts TJ. Ozone Depletion in Tropospheric Volcanic Plumes: From Halogen-Poor to Halogen-Rich Emissions. Geosciences. 2018; 8(2):68. https://doi.org/10.3390/geosciences8020068

Chicago/Turabian Style

Roberts, Tjarda J. 2018. "Ozone Depletion in Tropospheric Volcanic Plumes: From Halogen-Poor to Halogen-Rich Emissions" Geosciences 8, no. 2: 68. https://doi.org/10.3390/geosciences8020068

Note that from the first issue of 2016, this journal uses article numbers instead of page numbers. See further details here.

Article Metrics

Back to TopTop