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Persisting volcanic ash particles impact stratospheric SO2 lifetime and aerosol optical properties

Abstract

Volcanic ash is often neglected in climate simulations because ash particles are assumed to have a short atmospheric lifetime, and to not participate in sulfur chemistry. After the Mt. Kelut eruption in 2014, stratospheric ash-rich aerosols were observed for months. Here we show that the persistence of super-micron ash is consistent with a density near 0.5 g cm−3, close to pumice. Ash-rich particles dominate the volcanic cloud optical properties for the first 60 days. We also find that the initial SO2 lifetime is determined by SO2 uptake on ash, rather than by reaction with OH as commonly assumed. About 43% more volcanic sulfur is removed from the stratosphere in 2 months with the SO2 heterogeneous chemistry on ash particles than without. This research suggests the need for re-evaluation of factors controlling SO2 lifetime in climate model simulations, and of the impact of volcanic ash on stratospheric chemistry and radiation.

Introduction

Stratospheric volcanic aerosols have altered climate throughout Earth’s history. The major constituents of volcanic aerosols are liquid sulfate (SO42− in solution with water) originating from sulfur dioxide (SO2) injections, and volcanic rocks <2 mm in diameter, referred to as ash. It is well known that the sulfate aerosol (a.k.a. sulfuric acid aerosol) scatters incoming solar radiation back to space and cools the surface globally, while its absorption of solar and infrared light heats the stratosphere. Sulfate aerosols also provide surfaces to activate halogen species, enhancing ozone depletion. Volcanic ash is usually neglected in simulations of changes in the climate and stratospheric chemistry because large, high-density (over 2 g cm−3) particles would be short lived1.

However, observations indicate that ash can linger for long periods of time in the stratosphere. The stratospheric volcanic aerosol layer from the tropical Mt. Kelut eruption of 13 February, 2014, with Volcanic Explosivity Index (VEI) of 4, was observed for more than three months by the Cloud-Aerosol Lidar and Infrared Pathfinder Satellite Observation (CALIPSO)2. Vernier et al.2 suggested that sub-micron volcanic ash particles were partly responsible for the aerosol layer. The Airborne Tropical TRopopause EXperiment (ATTREX) aircraft observed super-micron particles in the lower stratosphere near Guam 3–4 weeks after the eruption that was very likely volcanic ash3. Kelut’s cloud is not a unique example of persisting ash-containing particles. Six to eight months after the 1991 Mt. Pinatubo eruption (VEI = 6), particles with mean radii near 0.8 µm composed of minerals coated with sulfate were observed in the Arctic lowermost stratosphere, increasing the particulate surface area up to 50-fold4. Similarly, volcanic ash was observed in the stratosphere for a year after the 1963 Mt. Agung eruption5 (VEI = 5) and for a year after the 1982 El Chichon eruption6 (VEI = 5).

The Mt. Kelut eruption is one of the few since those of Mt. Agung5 and Mt. St. Helens7 in 1980 for which ash size distributions were observed soon after the eruptions. Some of the volcanic ash particles are relatively large, have a significant fall velocity, and can remove the sulfate attached to them from the stratosphere. Some of the smaller ash particles contribute to the longer-lasting stratospheric volcanic aerosols, which can affect the radiation and chemistry for a longer time. Current simulations often assume ash has a density of ~ 2.3 g cm−3, equivalent to volcanic glass8. Such dense particles of 10 µm radius have fall velocities near 4 cm s−1 at 20 km, and fall times from 20 to 16 km of about 1 day. The lifetime of 1-µm particles of the same density is about 50 days, or slightly more than 200 days if the density is 0.5 g cm−3. Non-spherical shapes can also reduce fall velocity.

Here, we compare simulations using a sectional aerosol-climate model (detailed in “Methods”) with satellite and aircraft observations to investigate the physical processes that explain the persisting ash particles following the Kelut eruption. We analyze the ash physical properties (particle density, particle size distribution, etc.) and determine the temporal contribution of volcanic ash to the stratospheric volcanic aerosol layer. We find that the SO2 lifetime is not controlled only by hydroxyl radical (OH) as commonly assumed, but also by heterogeneous reactions on ash, a potential concern for climate and geoengineering simulations. Finally, we show that there is significant removal of sulfur (S) on falling ash. Such removal has been observed in the troposphere near volcanic vents possibly due to adsorption of S gases on the ash9,10,11,12,13,14. However, SO2 removal via heterogeneous reactions on ash in the stratosphere has been ignored in climate models, even though it is recognized in laboratory studies15,16,17,18.

Results

SO2 lifetime

Correctly constraining the volcanic SO2 emission and lifetime, as well as the physical proximity of S gases and ash particles, is important to predict the interaction between S species and ash particles. Large ash particles have large surface areas to uptake the vapor through condensational growth or heterogeneous reactions, but at the same time, they quickly fall out of the stratosphere. Ash can interact with H2SO4 gas and aerosol through several well-known microphysical processes (Methods, Fig. 1): H2SO4 gas heterogeneously nucleates on ash particles and then grows; pure sulfate aerosol particles form by homogeneous nucleation and can then coagulate with ash particles and mixed ash/sulfate particles. The longer it takes SO2 to be converted to H2SO4, the less H2SO4 vapor is available to condense onto the ash, and the fewer sulfate particles are available to coagulate on ash particles before the ash particles fall out of the stratosphere. Heterogeneous uptake of SO2 on ash can remove SO2 directly without requiring SO2 conversion to H2SO4 vapor (Methods, Fig. 1).

Fig. 1: A schematic diagram and the volcanic ash/sulfate module in the model.
figure1

a A schematic diagram of the chemistry and microphysical processes for this work; b The three aerosol groups and the main microphysical processes involved in the volcanic ash/sulfate module in the CARMA model. The red arrows indicate the processes added to the model for this study relative to English et al.42.

The SO2 oxidation process is very complicated inside a volcanic plume and cloud. Generally, in the stratosphere, it has been thought that the SO2 lifetime is determined by its reaction rate with OH. In turn, the oxidation of SO2 reduces the OH abundance. Therefore, OH chemistry must be included in any simulation of volcanic plumes and clouds. The factors that impact the SO2/OH reaction rate include the injection of H2O from the volcanic eruption, which can increase the OH concentration; the spreading of the volcanic clouds, which dilutes the SO2 concentration so OH is less impacted by the reaction with SO2; as well as light scattering by ash, sulfate, and possibly ice, which increases the path length of light through the atmosphere thereby changing photolysis rates that control the OH production rate19.

Carn et al.20 discovered a correlation between the altitude of SO2 injection and the lifetime of SO2 and possibly a related dependence of SO2 lifetime on the amount of injected SO2 and the latitude of injection. They found that large injections, such as that of Mt. Pinatubo, in the altitude range above 20 km have SO2 lifetimes near 30 days, while smaller injections near the tropopause result in lifetimes of less than a week.

To explore the influence of various factors that might alter the SO2 oxidation rate in our model, we show in Fig. 2 several simulations of SO2 evolution (lines), as well as various spacecraft observations (symbols). The dashed lines in Fig. 2 represent the SO2 burden from the simulations. As the volcanic cloud spreads, the SO2 column is reduced due to wind shear until some columns have so little SO2 that it is below the observational detection limit, but is not actually lost. Therefore, some apparent SO2 loss is actually SO2 spreading into the background. The solid lines in Fig. 2 represent the simulated SO2 burden only counting the grid cells with SO2 above the background noise level of the Ozone Monitoring Instrument (OMI) data (reasons detailed in Supplementary Note 1).

Fig. 2: The volcanic SO2 burden.
figure2

The satellite observations are shown in symbols and the simulations are shown in lines. IASI is the Infrared Atmospheric Sounding Interferometer. ARIS is Atmospheric Infrared Sounder on board NASA’s aqua satellite. OMI is Ozone Monitoring Instrument upper tropospheric and stratospheric SO2 column data. The dashed lines and solid lines in the same color refer to the same simulations, but the solid lines show the simulated SO2 burdens counting only the grid cells where SO2 is above OMI noise level (0.2 Dobson Unit (DU), while the dashed lines show the simulated total SO2 burden without accounting for observational bias due to signal to noise ratio. The boundaries of the green shaded area are two extreme estimations of simulated SO2 burden of the SO2onAsh case considering the observational uncertainty. The lower boundary only counts the grid cell with the gridbox average SO2 higher than the detection limit (a.k.a. five times OMI noise level). The upper boundary assumes the simulated SO2 occupies only a part of the model grid cell equivalent to the five adjacent pixel threshold of OMI and compares that with the OMI detection limit. The fraction is not smaller than 5 OMI observation pixels. For details of applying observational uncertainties to the modeled results refer to Supplementary Note 1. The descriptions of the model cases are given in Table 1. γ stands for uptake efficiency; sc stands for saturation coverage.

Mills et al.21 assumed an injection of 0.3 Tg of SO2 from Kelut, and computed an SO2 lifetime of 26 days. However, the satellite observations in Fig. 2 report that the SO2 lifetime after the Kelut eruption is about a week. Considering the SO2 merging into the background with signals below instrumental detection limits, our simulations suggest the actual SO2 lifetime is ~2 weeks. The Reference case in Fig. 2 and Table 1 shows that reducing the injected amount of SO2 from 0.3 Tg to 0.2 Tg does not impact the SO2 lifetime found by Mills et al.21. The Base case explores the effect on the SO2 lifetime by altering three factors to be closer to the Microwave Limb Sounder (MLS) observed SO2 and H2O. First, we used an initial injection into a 10˚ latitude × 2˚ longitude band so that we could pick up enough wind shear to reproduce the spreading patterns and concentrations observed by the OMI satellite (Supplementary Note 2; Supplementary, Figs. 13). Second, we used a lower SO2 injection height than suggest by Mills et al.21 based on MLS observations (Table 1). Third, we used a water injection of ~0.26 Tg which is near the upper limit allowed by MLS (Table 1). We included these three factors together because their effects are each small, in total they shorten the lifetime by 4 days relative to the Mills et al.20 lifetime of 26 days. With three tests tracking the three factors individually, we found the larger geographic injection area for SO2 contributes 2 days to lifetime reduction, the lower injection height contributes 2 days, and the observed H2O injection causes no significant reduction.

Table 1 The model cases and the parameters related to SO2 injection, as well as the SO2 lifetime of each case.

Figure 2 shows that none of the simulations just described reproduce the satellite observations of SO2. Supplementary Fig. 4 illustrates the OH field 1 day after the eruption from the Base case. As may be seen OH in the volcanic cloud is depleted by ~1 pptv relative to surrounding air. Basically, OH is converted to HO2, so that the ratio of OH to HO2 is changed. The slow down of the SO2/OH reaction due to depletion of OH has been suggested in models22 and seen in oxygen isotopic data during historical moderate and large eruptions23,24,25. One possible way to increase OH, and thereby reduce the SO2 lifetime is to assume that a large injection of H2O occurred. In order to fit the observed SO2 trend, we need to inject 26 Tg of H2O (the LrgH2O case in Table 1, not shown in Fig. 2), 100 times more than the water vapor observed (Table 1). Also, injecting huge amounts of water dilutes the sulfate aerosols making them unrealistically large. The LrgH2O case increases the OH to 1.8 pptv, which is about 0.5 pptv higher than the surrounding air (Supplementary Fig. 4). Another possible way to change OH is to mimic the effect of aerosol scattering light on OH production rate. We empirically increase the OH photolysis rate by 50 times for the first 3 days (the LrgOH case in Table 1, not shown in Fig. 2) in order to fit the observed SO2 trend. However, such a drastic increase of OH is unlikely to be caused only by scattering. Both the LrgH2O and the LrgOH cases are implausible explanations to shorten the lifetime of SO2 for this eruption.

In addition to the SO2 gas-phase reaction with OH, laboratory experiments report SO2 reacting on volcanic ash and mineral dust15,16,17,18,26,27 (Supplementary Note 3). In general, the laboratory data show a rapid initial SO2 uptake, that saturates over time. We are able to estimate the uptake efficiency using the rate of decline of the SO2 concentration mostly during the first day, and the saturation coverage using the time at which the SO2 loss stops being controlled by the heterogeneous loss, after about one day (Supplementary Note 3). During this time about 20 % of the initial SO2 has been removed from the gas phase. We find the uptake efficiency, γ, is about 3 × 10−3, and the saturation coverage is about 3 × 1016 molecules cm−2 assuming a geometric surface area of spherical ash particles. This saturation coverage is equivalent to ~13% of SO2 on mixed particles by mass in our simulation, for the particle size with the largest surface area, ~2 µm. These numbers will be useful to climate modelers simulating volcanic clouds and assuming spherical particles, but because we assumed the particles are spherical they are not directly comparable to laboratory studies which often measure the Brunauer, Emmett and Teller (BET) surface area of volcanic ash samples. The surface area of real volcanic ash varies case by case and is expected to be larger than the spherical assumptions. The true γ value should be reduced by the amount the true surface area exceeds that of an equal mass sphere. For our example of an oblate spheroid particle discussed below, the surface area is 1.4 times greater, so the γ value would be about 2 × 10−3, but the true surface area is likely larger because of other features such as surface roughness and/or secondary phases, which can raise specific surface area by one or two orders of magnitude18,28,29,30. Usher et al.18 reported an initial uptake efficiency in the range 7.0 × 10−5 to 5.1 × 10−4 for their mineral samples studied in the laboratory assuming the BET surface area of the particles. Other studies have reported lower initial uptake efficiencies in the 10−6 range26,27. Maters et al.15 used a Knudsen cell to measure the initial uptake efficiency of SO2 on dacite glass to be 1.3 × 10−2 at ~250 K assuming the geometric surface area of the sample holder. Our derived values for Kelut ash assuming the geometric surface area of the particles falls between these laboratory studies. Several papers in the literature report saturation coverage of SO2 on the mineral dust or ash ranging from 1011 to 9 × 1014 molecules cm−2 assuming the BET surface area using different laboratory technologies under different exposure times, pressures, RH, and SO2 concentrations13,15,16,17,18,31,32. Likewise, if we scale down our saturation coverage limit by 1 or 2 orders of magnitude, the value falls between these laboratory data. Several different combinations of uptake efficiency and saturation coverage can also explain the observed SO2 burden (Supplementary Fig. 5). Supplementary Fig. 5 indicates that as we increase the uptake efficiency, we can decrease the saturation coverage to fit the observation. Supplementary Fig. 5 suggests a reasonable saturation coverage, assuming spherical particles and the geometric surface area, is in the 1016 molecules cm−2 range, and γ is in the 10−3 to 10−2 range.

Figure 2 displays the SO2onAsh case with γ = 3 × 10−3 and saturation coverage of 3 × 1016 molecules cm−2. After saturation, we set the SO2 uptake efficiency to zero. Figure 2 shows the modeled actual SO2 lifetime, in which all SO2 in the gas phase is counted and the heterogenous reaction is included, is 17 days (blue dash line). We apply the OMI observational uncertainties on the SO2onAsh case (blue solid line and green shaded area). The uncertainties increase quickly and overlap the Reference case and Base case after 10 days, which is consistent with the end time of the OMI observations when the satellite is no longer able to observe SO2.

In the following sections, we continue to use results from both the Base case and the SO2onAsh case to explore the similarity and the differences of volcanic aerosol properties and ash/S interactions between cases with longer and shorter SO2 lifetime.

The persisting ash-containing volcanic aerosol layer

CALIPSO observed the aerosol backscatter to be larger than 0.01 km−1sr−1 above Mt. Kelut two hours after the eruption. Afterward, the backscatter decayed over more than 1 month as illustrated in Fig. 3. Vernier et al.2 used depolarization data to show that the non-spherical particle signal is close to zero 110 days after the eruption. Vertically, the volcanic aerosol had a three-layer pattern the first day after the eruption. After that, CALIPSO only detected one obvious layer near 18–21 km. Generally, the altitude of the volcanic aerosol layer to the east of Kelut was lower (17–19.5 km) and the ash layer to the west was higher (18–20 km), indicating wind shear caused the volcanic aerosol layers at different altitudes to move in different directions.

Fig. 3: the volcanic ash layer altitudes and the total backscatter coefficient.
figure3

a the volcanic ash layer altitudes from CALIPSO and two model cases. b The total backscatter coefficient (aerosol + Rayleigh). We pick the largest total backscatter in the vertical profiles and its corresponding altitude on the selected segments to define the altitudes in panel a and the values in (b) (dots and circles). The dashed lines are the zonal average backscatter from CALIPSO (black) and two model cases (red and blue). CALIPSO does not have observations from 21 Feb to 23 Feb and from 25 Feb to 2 March. The blue dotted line represents the approximate background backscatter from air plus the background sulfate aerosol. The gray error bars represent the standard deviation of the dotted CALIPSO data. The gray shaded area shows the modeled average values are within 20% of CALIPSO averaged values. The standard deviation of the CALIPSO zonal average values is over a factor of 200%.

In order to match the simulated backscatter coefficient values and the vertical distributions with CALIPSO observations, we use the method described by Vernier et al.2 to choose the orbit segments in which CALIPSO observed the volcanic aerosol layers on each day. For each segment, we average the total backscatter (Rayleigh + all types of aerosols) to create a vertical profile. In Fig. 3, we pick the altitudes and the values with the largest total backscatter in the vertical profiles from CALIPSO (black) and the simulations (red and blue) from 13 Feb to 4 March. The altitudes of the simulated ash layers are consistent with the CALIPSO observed altitudes when we use an initial injection height from 72 to 52 hPa (18.5–20.5 km). The altitude differences between the simulations and observations in Fig. 3 can be caused by the mismatch of the vertical resolution of the model, which is about 1 km in the stratosphere, and the CALIPSO data, which is about 60 m. The backscatter data from CALIPSO (black) decreases rapidly in the first few days and then decreases more slowly. The simulated values decrease more slowly from day 1 to day 5 than the observations. However, the Base and the SO2onAsh cases are generally within the standard deviation of the observed values after day 6. We conducted several tests with various initial size distributions and particle number densities, but they all show similar decreases in backscatter with time.

It is tricky to compare simulations with the CALIPSO data in the first few days. CALIPSO may have missed volcanic aerosol layers in the first few days because the orbit may not have crossed narrow layers. The mesoscale winds are also important for aerosol spreading in the first couple of days, but are not well represented in the model due to the coarse horizontal resolution as we discuss in the Supplementary Note 2 and Supplementary Fig. 1.

After 20 days, the volcanic aerosols are generally well spread in longitude. Figure 3 also shows the zonal average backscatter from CALIPSO (black dash line) and compares it with the simulated zonal average backscatter (red and blue dash line). These three lines correspond to an of altitude 19.5 km and a latitude range of 0–6˚ S, where both the observations and the simulations have the largest zonal average backscatter signals 20 days after the eruption. After 40 days, the differences between the simulated values (red and blue dash lines) and the observation (black dash line) are <20% and all of them are slightly higher than the background (background aerosol+rayleigh) backscatter, indicating the presence of the volcanic aerosols.

Particle size distribution

Instruments onboard the NASA Global Hawk measured the size distributions of volcanic ash near Guam above 16.5 km altitude during ATTREX flights from 6 March to 12 March, 20–25 days after the eruption3. Measurement details are described in Woods et al.33 and Jensen et al.3. These observations constrain the input ash size distribution and the particle density or shape. As noted by Durant et al.8, volcanic particles are not spherical and particle densities are determined by the particle compositions. Densities of glassy volcanic particles are around 2.3 g cm−3, while those for pumice are about 0.6 g cm−3. The ash particle density and shape are important to the simulations of sub- and super-micron-sized mixed particles because they affect the fall velocity, which is large enough for the super-micron-sized particles to experience significant sedimentation in 20 days. A spherical particle with a radius of 5 µm with a particle density of 0.6 g cm−3 falls at about the same speed as a particle of 2.3-µm radius with a particle density of 2.3 g cm−3. Highly oblate shapes have effects on fall speeds comparable to spherical shapes with similarly lower densities. Our model tests (Supplementary Fig. 6) indicate particles with length/diameter ratios of 0.3 only reduce the fall velocity by 8% compared with the equivalent-volume spherical particle, while highly oblate particles with length/diameter ratio of 0.1 can reduce the fall velocity by 30%.

We ran simulations assuming various mass burdens in three ash size modes and/or with various ash particle densities to find the best choices to match the ATTREX observations (detailed in “Methods”). Figure 4 shows the simulations of the volume size distributions of pure sulfate (blue) and mixed particles (orange) in the Base and SO2onAsh cases compared with ATTREX data from two FCDP probes (black and purple). Modeled ash particles are spherical with various densities of 0.5 and 2.3 g cm−3 (Fig. 4). The simulation results in Fig. 4 (blue and orange) are sampled near 170˚ E and 8˚ S on 10 March from 16.5 to 18.5 km. This location matches the ATTREX flight path on 9 March and 10 March. We find the particle density is the main controller of the size distribution on 10 Mar (25 days after the eruption). Decreasing the particle density from 2.3 g cm−3 (Fig. 4c) to 0.5 g cm−3 (Fig. 4a) significantly improves the observed (black and purple) and simulated (orange) particle size distribution agreement around 5 µm, and also limits the particle numbers near 0.8 µm as shown in Supplementary Fig. 7. The size distribution of the base case and the SO2onAsh case are very similar. Note that the actual mixed particle densities are slightly different from the ash particle densities because of the mixing with sulfate. The mixed particle densities for these three panels in Fig. 4 are 0.52, 0.57, and 2.25 g cm−3. The balance between mode 1 (~0.5 µm) and mode 2 (~1.5 µm) in the initial size distribution (see Methods) is also relatively important. If we put the majority of mass in mode 1, the particles do not have enough time to grow/coagulate and reproduce the size distribution above 5 µm on 10 March. We also show the number size distribution for each case in Supplementary Fig. 7, which shows an agreement with the observation assuming an ash density of 0.5 g cm−3. Note that, in reality, ash particles are usually non-spherical with a non-porous structure or with a porosity dominated by macropores (diameters > 50 nm)29. Our conclusion is that the non-spherical, porous or aggregate shaped particles have the same fall velocities as spherical particles with densities of 0.5 g cm−3.

Fig. 4: The particle volume size distributions near Guam.
figure4

The particle volume size distributions from the simulated pure sulfate (blue), mixed particles (orange) and the two ATTREX FCDP probe observations (black and purple) around 16.5–18.5 km near Guam about 25 days after the eruption. No pure ash remains at this time. Panel a is the Base case assuming ash density of 0.5 g/cm3; b the SO2onAsh case assuming ash density of 0.5 g/cm3; c the Base case assuming ash density of 2.3 g/cm3.

Figure 5 shows the evolution of the normalized size distribution of the mixed particles as a function of time. The Base case and the SO2onAsh case show the volume density of mixed particles peaks near 2–5 µm in radius after day 11 and the large particles (above 5 µm in radius) fall out through the time period. Comparing the Base case and the Nocoag case, we show that the sub-micron particles coagulate into larger radii particles especially in the first ten days. Coagulation of mixed particles with ash and pure sulfates is the key process needed to produce the evolution of the size distribution of the mixed particles. After 11 days, the shape of the size distribution does not change very much. Supplementary Fig. 9 shows the pure sulfate size distribution evolution. Condensational growth and coagulation increase the pure sulfate size from 0.1 to 0.3 µm in a month.

Fig. 5: The normalized mixed particle volume size distribution at 61 hPa.
figure5

The normalized mixed particle volume size distribution at 61 hPa (19.5 km) for the Base case, the SO2onAsh case, and the Nocoag case. The Nocoag case shows the simulation without coagulation between mixed particles and pure sulfates or between mixed particles and ash. The values are picked at the location with the largest mass mixing ratio of mixed particles on the days specified on top of the figure. The un-normalized distributions are shown in Supplementary Fig. 8.

Impact of volcanic ash on sulfate burden

Volcanic ash can accumulate S species by uptaking H2SO4 gas, sulfate aerosols, and SO2 gas. Large volcanic ash particles fall out of the stratosphere quickly, which reduces the stratospheric sulfate burden. Here, we investigate the stratospheric S/ash interactions in three simulations (Fig. 6) from 33˚S to 16˚N: the Noashemission case (blue), the Base case (black), and the SO2onAsh case (red). They use the same SO2 injection. First, neither the Noashemission case nor the Base case, with a S residence time of 22 days, consider SO2 reactions on ash. The difference of S burden (Fig. 6a) between them is minor indicating the sulfate and H2SO4 gas is not effectively removed directly by ash since the SO2 lifetime is long compared with the super-micron ash removal time. As we include the SO2 reacting on ash surfaces, the sulfate produced by reactions on the ash stays with the ash particle and is removed effectively. After two months, the stratospheric S burden is reduced to 67% of its original value in the case with the heterogeneous reaction compared to 77% with the Noashemission case and the Base case. The amount of S removed is 43% larger with heterogeneous chemistry than without. Figure 6b shows that SO2 reaction on ash (red) produces sulfate faster than SO2 oxidation to sulfate in the gas phase (black and blue). The SO2 reacting on ash surfaces also affects the ash burden evolution (Fig. 6c) but the impact is a change of <8% of the ash mass in 2 months. The difference can be caused by the slightly different densities and effective radii of the mixed particles between the two model cases.

Fig. 6: The stratospheric S burden and ash burden between 33˚S to 16˚N.
figure6

a The stratospheric S burden from the Noashemission case (blue), the Base case (black), and the SO2onAsh case (red) between 33˚S to 16˚N; b the condensed phase (solid) and the gas phase (dotted) S burden. The gas S burden of the Noashemission case and the base case are nearly identical; c The stratospheric ash burden. The stratospheric background S burden is ~0.052 Tg within this area.

Figure 7 shows the contribution of ash and sulfate to the backscatter coefficient and mass mixing ratio in the SO2onAsh case from 72 hPa to 52 hPa (19.5–21.5 km). The Mixed particle is the main contributor to the backscatter (Fig. 7b). Inside the mixed particle, the ash is the major component (6c). Ash contributes 60% of the mixed particle mass 60 days after the eruption (6e). The 40 % of the mixed particle that is sulfate has two origins: about 20% of sulfate inside the particle is from SO2 reacting on ash surface and the other 20% is from coagulation with pure sulfate and H2SO4 gas growth on ash surface (6e). The majority of sulfate is in the form of pure sulfate rather than the mixed sulfate after 30 days of the eruption (6f). This dominance of pure sulfate indicates that SO2 oxidation to H2SO4 in the gas phase followed by nucleation into pure sulfate is the dominant sulfate production processes at this time since the heterogeneous reaction of SO2 on ash has shut down. We also see similar contribution patterns of ash and sulfate to the total backscatter and mixing ratio in the Base case as shown in Supplementary Fig. 10. Note that the sulfate percentage in the mixed particle increases much slower in Supplementary Fig. 10e than in Fig. 7e. The slower increase explains why the ash cannot reduce the S burden effectively in the base case. Therefore, we conclude that the ash particles are the main component of the persisting volcanic aerosol layer following this eruption.

Fig. 7: The composition evolution from the SO2onAsh case.
figure7

The data are picked from the maximum total backscatter at three different pressure levels from 72 to 52 hPa. a the maximum total backscatter (aerosol + Rayleigh) in red and Rayleigh backscatter in blue; b the backscatter contribution from the mixed particle and pure sulfate respectively; c the mass mixing ratio of ash and sulfate (H2SO4 + water) inside the mixed particles; d the mass mixing ratio of pure sulfate; e the weight percent of sulfate inside the mixed particle. The blue dots are the sulfate coming from SO2 reacting on ash and the red dots are the total sulfate percentage (blue dots + sulfate from coagulation/growth); f the weight percent of pure sulfate in total sulfate (blue) and the weight percent of sulfate in mixed particle in total sulfate (red). The Base case compositions are shown in Supplementary Fig. 10.

Discussion

Our investigation of volcanic ash using the Whole Atmosphere Community Climate Model provides new insight into the role of volcanic ash in climate change. First, our simulations, combined with CALIPSO and ATTREX data, indicate that the persisting volcanic aerosol layer after the 2014 Mt. Kelut eruption is primarily composed of ash (Fig. 7 and Supplementary Fig. 10), which is likely low density as well as being non-spherical and super-micron sized (Fig. 4 and Supplementary Fig. 7). Our estimate of ash density from the simulations is about 0.5 g cm−3, which corresponds to pumice8. This low density is much smaller than assumed in most model simulations. However, the particle shape may also impact the fall velocity. We conclude that density and shape combine to produce a fall velocity equivalent to spherical particles with a density of 0.5 g cm−3, but we cannot determine the relative importance of shape and density. The typical ash/sulfate mixed particle size is over 10 times larger than the size of the typical stratospheric background sulfate aerosol (~0.1 µm). Observations from several large volcanic eruptions also show persisting volcanic debris4,5,6, with volcanic ash sizes similar to that of the Mt. Kelut eruption. Simulations of large eruptions that include the small size mode of ash discussed in the Methods are needed to determine the contribution of ash to observed cooling at the surface. Sulfate coated ash may have a larger surface area than sulfate alone, which may influence stratospheric heterogeneous ozone chemistry34.

We find that volcanic S can be removed from the gas phase by volcanic ash more rapidly than considered in climate models that have ignored heterogeneous reactions of SO2 on ash. We find that neglecting the uptake of SO2 on ash minimizes the calculated effect of ash on removing volcanic S by sedimentation in a small volcanic eruption. However, SO2 reacts on ash, as shown by laboratory experiments15,16,17,18. Simulations considering these reactions give a shorter SO2 lifetime, agreeing better with observations following the Mt. Kelut eruption. We distribute the initial eruption plume over an extended area in order to capture the observed wind shear and plume transport. However, we find that more confined injections do not impact our conclusion that heterogeneous reactions of SO2 on ash are important. We also find that some of the short lifetimes reported following smaller eruptions20 may be caused by satellites missing some SO2 due to signal to noise issues as the debris layer spreads out. The SO2/ash reactions enhance the S/ash interactions and favor more sulfate removal by ash. While our simulations are focused on a relatively small eruption, Guo et al35,36 reported that half of the SO2 released to the stratosphere in the Pinatubo eruption was converted to sulfate within 3 days of the eruption.

Further studies of the heterogenous chemical reaction of SO2 on ash following other large and small eruptions are warranted since the ratio of ash to SO2 injections is variable. Also, climate models with higher resolution can reproduce the spread of volcanic ash and SO2 better. Finally, climate models need to better quantify the contribution of volcanic ash particles to the energy balance and heterogeneous ozone loss.

Methods

Model setup

We use the specified dynamics (SD) version of the Whole Atmosphere Community Climate Model (WACCM) version 4.037,38 coupled with the Community Aerosol and Radiation Model for Atmospheres (CARMA)39,40,41,42,43,44,45. The CARMA model has been used to treat many different types of stratospheric aerosols in global model frameworks: sulfate aerosol42, volcanic sulfate aerosol45,46, polar stratospheric clouds43,44 as well as noctilucent clouds and micrometeorites39,41. The model horizontal resolution is 1.9˚ latitude × 2.5˚ longitude. The vertical resolution is about 1 km in the lower stratosphere.

For this study, we further develop the sulfate aerosol and micrometeorite model employed by English et al.42 and Bardeen et al.39 to be able to simulate volcanic ash particles and their interactions with pure sulfate particles. The model considers 22 particle mass bins for each type of particle covering particle radii from ~0.088 to ~63 µm for ash particles and for mixed particles, and from ~0.34 to ~72 µm for pure sulfate aerosol. In total there are 66 particle bins being advected. The sulfate density depends on the water fraction of the particle. The ash density varies from 0.5 g cm−3 to 2.3 g cm−3 for different test cases. The mixed particles contain non-volatile ash as well as H2SO447, along with liquid water that is assumed to be in equilibrium with atmospheric humidity. In the model, the particle density is variable, so the actual radius values covered are variable. The main microphysical processes (Fig. 1) include heterogeneous nucleation of H2SO4 gas on ash particles; homogeneous nucleation of H2SO4 gas48; coagulation of sulfate particles, ash particles and mixed particles; the growth and evaporation of H2SO4 and H2O on/from sulfate aerosol and mixed particles; particle sedimentation and dry deposition. The WACCM model deals with S chemistry21,42, particle transport by winds and wet scavenging. Figure 1 also shows the main SO2 chemistry we are considering in this paper: SO2 uptake on ash and SO2 reaction with OH. SO2 aqueous phase chemistry is also important for tropospheric volcanic SO2 oxidation but is not included here since liquid water is not expected in the stratosphere14,49, and since we focus on SO2 and stratospheric volcanic cloud evolution days and months after the eruption. However, including the effects of these tropospheric reactions on the volcanic plume and cloud would be valuable to better understand the total sulfate deposition on ash, some of which occurs before the ash enters the stratosphere9,10,11,12,13.

Observational data

The Cloud-Aerosol Lidar with Orthogonal Polarization (CALIOP) instrument on board the CALIPSO satellite measures the backscatter at 532 and 1064 nm50. We use the CALIPSO L1B nighttime total backscatter coefficient data at 532 nm. In the stratosphere, the vertical resolution can be as high as 60 m from 15 to 20 km and 180 m from 20 km above. For nighttime observations, the uncertainty due to noise is estimated to be typically smaller than 1%.

The ATTREX field campaign applied the Fast Cloud Droplet Probe (FCDP)33,51,52 to measure the forward scattered light from individual particles. The instrument retrieves particle sizes ranging from 1 to 50 μm diameter. We use the size distribution data published by Jensen et al.3 from two onboard FCDP probes: the stand-alone FCDP and the Hawkeye probe. The particles were mainly detected during flights between 6 March and 12 March and between 16.5 and 18.5 km.

The OMI reported volcanic SO2 column data starting 14 February, one day after the Mt. Kelut eruption. We use the OMI L2 data that only counts the upper tropospheric and stratospheric SO2 columns. The background noise level of this dataset is 0.2 DU.

The MLS onboard NASA’s Earth Observing System (EOS) Aura satellite observes H2O concentrations. We use the MLS v4.2 H2O data as a reference for volcanic water injection on Feb. 13th, 2014. We refer to the water mixing ratio from 82 hPa to 31 hPa (~17 km to 23 km) near Mt. Kelut.

The volcanic emission references

Volcanic eruptions inject various particles and gases into the atmosphere, such as ash, H2O, CO2, SO2, HCl, H2S, etc. For this study, we constrain the SO2 and volcanic ash emissions. Several satellite observations provide estimates of SO2 injection on 13 February varying from 0.12 Tg to 0.8 Tg available at Global Sulfur Dioxide Monitoring Home Page. However, the ash masked the SO2 and made it difficult to determine the injection of SO2. Neely and Schmidt53 compiled a database of climatically relevant volcanic SO2 emissions since 1990. It suggests an injection of 0.3 Tg of SO2 uniformly mixed from ~17 to 26 km on 13 Feb, 2014 at 7.93˚S and 112.31˚E. We use this database as a reference for the injection height and inject over 6 h, following Mills et al.21. But we find the best estimate of the SO2 injection is 0.2 Tg based on comparing simulations with the OMI data.

Kristiansen et al.54 constrained the ash emission for particle radii from 1.4 to 14 µm with a total injection of 0.38 Tg into the stratosphere based on the ash retrieved from Japan’s second Multifunctional Transport Satellite (MTSAT 2) on Feb 13 and 14. We apply a different approach to constrain the ash emission for the global modeling framework which focuses more on the long-lived sub- and super-micron-sized volcanic ash. We use a 3-mode set of lognormal size distributions for our initial ash emission estimation (Fig. 8). The first mode has a mean radius of 0.476 µm and a variance of 0.535 based on aircraft size distributions measured in the Mt. St. Helens volcanic cloud of 19807. The second mode has a mean radius of 1.5 µm and a variance of 0.5 fitting the Kelut retrieval of Kristiansen et al.54. The third mode is centered at 20 µm with a variance of 0.8. This mode is suggested from ash deposits near Mt. St. Helens8. Even larger ash particles were likely injected8, but these would have such short lifetimes that they are neglected here.

Fig. 8: The initial size distribution of ash.
figure8

The gray line represents mode 1 and fits the black triangles by Farlow et al.7. The blue line represents mode 2 and fits the black line by Kristiansen et al.54. The yellow line represents mode 3 based on Durant et al.8. The red solid line is the sum of the three modes and is the number size distribution used for initial injection of ash. We also show a red dotted line and a red dash line representing the area size distribution and volume size distribution for the initial ash injection.

We vary the total mass of ash, the percentage of the particle mass in each of the three size modes, the ash particle density, the altitude range of the injection, and the geographic location of the injection to best agree with CALIPSO satellite and ATTREX aircraft data. The best estimation of ash emission in the Base case is detailed in Table 2.

Table 2 The Ash parameters in the Base case and the SO2onAsh case.

We calculate the backscatter at 532 nm of gas (Rayleigh), pure sulfate aerosol using a T-matrix code55 and spherical ash and mixed particles56. The refractive indexes are assumed to be 1.32 for pure sulfate57, and 1.55 + 0.001i for mixed particles and ash58. We interpolate the simulated results onto CALIPSO orbits. We find the best ash emission size distribution for the injection as shown in Fig. 8 and Table 2.

Code availability

The CESM/CARMA model is available on the CESM trunk to any registered user at www.cesm.ucar.edu.

Data availability

The satellite data in Fig. 2 are from Global Sulfur Dioxide Monitoring Home Page [https://so2.gsfc.nasa.gov/]. The CALIPSO data and the OMI data are available at https://search.earthdata.nasa.gov. The ATTREX data are available at [https://espoarchive.nasa.gov/]. The Integrated Global Radiosonde Archive data are available at [https://www.ncdc.noaa.gov/]. The MLS data are available at [https://mls.jpl.nasa.gov/]. The main data generated during this study are available at [https://osf.io/8cpd3/] with a permanent https://doi.org/10.17605/OSF.IO/8CPD3. Additional information is available from the corresponding author on reasonable request.

References

  1. 1.

    Niemeier, U. et al. Initial fate of fine ash and sulfur from large volcanic eruptions. Atmos. Chem. Phys. 9, 9043–9057 (2009).

    ADS  CAS  Google Scholar 

  2. 2.

    Vernier, J.-P. et al. In situ and space-based observations of the Kelud volcanic plume: The persistence of ash in the lower stratosphere: persistence of volcanic ash. J. Geophys. Res.: Atmospheres 121, 11,104–11,118 (2016).

    Google Scholar 

  3. 3.

    Jensen, E. J. et al. Ash particles detected in the tropical lower stratosphere. Geophys. Res. Lett. 45, 11,483–11,489 (2018).

    Google Scholar 

  4. 4.

    Pueschel, R. F. et al. Physical and optical properties of the Pinatubo volcanic aerosol: Aircraft observations with impactors and a Sun-tracking photometer. J. Geophys. Res.: Atmospheres 99, 12915–12922 (1994).

    ADS  Google Scholar 

  5. 5.

    Mossop, S. Volcanic dust collected at an altitude of 20 km. Nature 203, 824–827 (1964).

    ADS  Google Scholar 

  6. 6.

    Shapiro, M. A., Schnell, R. C., Parungo, F. P., Oltmans, S. J. & Bodhaine, B. A. El Chichon volcanic debris in an Arctic tropopause fold. Geophys. Res. Lett. 11, 421–424 (1984).

    ADS  CAS  Google Scholar 

  7. 7.

    Farlow, N. H. et al. Size distributions and mineralogy of ash particles in the stratosphere from eruptions of Mount St. Helens. Science 211, 832 (1981).

    ADS  CAS  PubMed  Google Scholar 

  8. 8.

    Durant, A. J., Rose, W. I., Sarna-Wojcicki, A. M., Carey, S. & Volentik, A. C. M. Hydrometeor-enhanced tephra sedimentation: Constraints from the 18 May 1980 eruption of Mount St. Helens. J.Geophys. Res.: Solid Earth 114, B03204 (2009).

  9. 9.

    Rose, W. I. Jr Scavenging of volcanic aerosol by ash: atmospheric and volcanologic implications. Geology 5, 621–624 (1977).

    ADS  CAS  Google Scholar 

  10. 10.

    Witham, C. S., Oppenheimer, C. & Horwell, C. J. Volcanic ash-leachates: a review and recommendations for sampling methods. J. Volcanol. Geotherm. Res. 141, 299–326 (2005).

    ADS  CAS  Google Scholar 

  11. 11.

    Delmelle, P., Lambert, M., Dufrêne, Y., Gerin, P. & Óskarsson, N. Gas/aerosol–ash interaction in volcanic plumes: new insights from surface analyses of fine ash particles. Earth Planet. Sci. Lett. 259, 159–170 (2007).

    ADS  CAS  Google Scholar 

  12. 12.

    Ayris, P. et al. SO2 sequestration in large volcanic eruptions: High-temperature scavenging by tephra. Geochimica et. Cosmochimica Acta 110, 58–69 (2013).

    ADS  CAS  Google Scholar 

  13. 13.

    Schmauss, D. & Keppler, H. Adsorption of sulfur dioxide on volcanic ashes. Am. Mineralogist 99, 1085–1094 (2014).

    ADS  Google Scholar 

  14. 14.

    Martin, E. Volcanic plume impact on the atmosphere and climate: O-and S-isotope insight into sulfate aerosol formation. Geosciences 8, 198 (2018).

    ADS  Google Scholar 

  15. 15.

    Maters, E. C., Delmelle, P., Rossi, M. J. & Ayris, P. M. Reactive uptake of sulfur dioxide and ozone on volcanic glass and ash at ambient temperature. J. Geophys. Res.: Atmospheres 122, 10–077 (2017).

    Google Scholar 

  16. 16.

    Urupina, D. et al. Uptake and surface chemistry of SO2 on natural volcanic dusts. Atmos. Environ. 217, 116942 (2019).

    CAS  Google Scholar 

  17. 17.

    Huang, L., Zhao, Y., Li, H. & Chen, Z. Kinetics of heterogeneous reaction of sulfur dioxide on authentic mineral dust: effects of relative humidity and hydrogen peroxide. Environ. Sci. Technol. 49, 10797–10805 (2015).

    ADS  CAS  PubMed  Google Scholar 

  18. 18.

    Usher, C. R., Al-Hosney, H., Carlos-Cuellar, S. & Grassian, V. H. A laboratory study of the heterogeneous uptake and oxidation of sulfur dioxide on mineral dust particles. J. Geophys. Res.: Atmospheres 107, ACH 16–1 (2002).

    Google Scholar 

  19. 19.

    Landgraf, J. & Crutzen, P. J. An efficient method for online calculations of photolysis and heating rates. J. Atmos. Sci. 55, 863–878 (1998).

    ADS  Google Scholar 

  20. 20.

    Carn, S. A., Clarisse, L. & Prata, A. J. Multi-decadal satellite measurements of global volcanic degassing. J. Volcanol. Geotherm. Res. 311, 99–134 (2016).

    ADS  CAS  Google Scholar 

  21. 21.

    Mills, M. J. et al. Global volcanic aerosol properties derived from emissions, 1990–2014, using CESM1(WACCM). J. Geophys. Res.: Atmospheres 121, 2332–2348 (2016).

    ADS  CAS  Google Scholar 

  22. 22.

    Mills, M. J. et al. Radiative and chemical response to interactive stratospheric sulfate aerosols in fully coupled CESM1(WACCM). J. Geophys. Res.: Atmospheres 122, 13,061–13,078 (2017).

    CAS  Google Scholar 

  23. 23.

    Pinto, J. P., Turco, R. P. & Toon, O. B. Self-limiting physical and chemical effects in volcanic eruption clouds. J. Geophys. Res.: Atmospheres 94, 11165–11174 (1989).

    ADS  Google Scholar 

  24. 24.

    Bekki, S. Oxidation of volcanic SO2: a sink for stratospheric OH and H2O. Geophys. Res. Lett. 22, 913–916 (1995).

    ADS  CAS  Google Scholar 

  25. 25.

    Savarino, J., Bekki, S., Cole-Dai, J. & Thiemens, M. H. Evidence from sulfate mass independent oxygen isotopic compositions of dramatic changes in atmospheric oxidation following massive volcanic eruptions. J. Geophys. Res.: Atmospheres 108, 4671 (2003).

  26. 26.

    Ullerstam, M., Johnson, M. S., Vogt, R. & Ljungström, E. DRIFTS and Knudsen cell study of the heterogeneous reactivity of SO2 and NO2 on mineral dust. Atmos. Chem. Phys. 3, 2043–2051 (2003).

    ADS  CAS  Google Scholar 

  27. 27.

    Park, J. & Jang, M. Heterogeneous photooxidation of sulfur dioxide in the presence of airborne mineral dust particles. Rsc. Adv. 6, 58617–58627 (2016).

    CAS  Google Scholar 

  28. 28.

    Riley, C. M., Rose, W. I. & Bluth, G. J. S. Quantitative shape measurements of distal volcanic ash. J. Geophys. Res.: Solid Earth 108, 2504 (2003).

  29. 29.

    Delmelle, P., Villiéras, F. & Pelletier, M. Surface area, porosity and water adsorption properties of fine volcanic ash particles. Bull. Volcanol. 67, 160–169 (2005).

    ADS  Google Scholar 

  30. 30.

    Paque, M., Detienne, M., Maters, E. & Delmelle, P. Smectites and zeolites in ash from the 2010 summit eruption of Eyjafjallajökull volcano, Iceland. Bull. Volcanol. 78, 61 (2016).

    ADS  Google Scholar 

  31. 31.

    Kulkarni, D. & Wachs, I. E. Isopropanol oxidation by pure metal oxide catalysts: number of active surface sites and turnover frequencies. Appl. Catal. A: Gen. 237, 121–137 (2002).

    CAS  Google Scholar 

  32. 32.

    Goodman, A., Li, P., Usher, C. & Grassian, V. Heterogeneous uptake of sulfur dioxide on aluminum and magnesium oxide particles. J. Phys. Chem. A 105, 6109–6120 (2001).

    CAS  Google Scholar 

  33. 33.

    Woods, S. et al. Microphysical properties of tropical tropopause layer cirrus. J. Geophys. Res.: Atmospheres 123, 6053–6069 (2018).

    ADS  Google Scholar 

  34. 34.

    Solomon, S. et al. Emergence of healing in the Antarctic ozone layer. Science 353, 269–274 (2016).

    ADS  CAS  PubMed  Google Scholar 

  35. 35.

    Guo, S., Rose, W. I., Bluth, G. J. S. & Watson, I. M. Particles in the great Pinatubo volcanic cloud of June 1991: the role of ice. Geochem., Geophys., Geosyst. 5, Q05003 (2004).

  36. 36.

    Guo, S., Bluth, G. J. S., Rose, W. I., Watson, I. M. & Prata, A. J. Re-evaluation of SO2 release of the 15 June 1991 Pinatubo eruption using ultraviolet and infrared satellite sensors. Geochem., Geophys., Geosyst. 5, Q04001 (2004).

  37. 37.

    Garcia, R. R., Marsh, D. R., Kinnison, D. E., Boville, B. A. & Sassi, F. Simulation of secular trends in the middle atmosphere, 1950–2003. J. Geophys. Res.: Atmospheres 112, D09301 (2007).

  38. 38.

    Marsh, D. R. et al. Climate Change from 1850 to 2005 Simulated in CESM1(WACCM). J. Clim. 26, 7372–7391 (2013).

    ADS  Google Scholar 

  39. 39.

    Bardeen, C. G., Toon, O. B., Jensen, E. J., Marsh, D. R. & Harvey, V. L. Numerical simulations of the three-dimensional distribution of meteoric dust in the mesosphere and upper stratosphere. J. Geophys. Res. 113, D17202 (2008).

  40. 40.

    Toon, O. B., Turco, R. P., Westphal, D., Malone, R. & Liu, M. A Multidimensional Model for Aerosols: Description of Computational Analogs. J. Atmos. Sci. 45, 2123–2144 (1988).

    ADS  Google Scholar 

  41. 41.

    Bardeen, C. G. et al. Numerical simulations of the three‐dimensional distribution of polar mesospheric clouds and comparisons with Cloud Imaging and Particle Size (CIPS) experiment and the Solar Occultation For Ice Experiment (SOFIE) observations. J. Geophys. Res.: Atmospheres 115, D10204 (2010).

  42. 42.

    English, J. M., Toon, O. B., Mills, M. J. & Yu, F. Microphysical simulations of new particle formation in the upper troposphere and lower stratosphere. Atmos. Chem. Phys. 11, 9303–9322 (2011).

    ADS  CAS  Google Scholar 

  43. 43.

    Zhu, Y. et al. Development of a polar stratospheric cloud model within the Community Earth System Model: assessment of 2010 Antarctic winter. J. Geophys. Res.: Atmospheres 122, 10,418–10,438 (2017).

    Google Scholar 

  44. 44.

    Zhu, Y. et al. Development of a polar stratospheric cloud model within the Community Earth System Model using constraints on Type I PSCs from the 2010–2011 Arctic winter: 3-D model of polar stratospheric clouds. J. Adv. Modeling Earth Syst. 7, 551–585 (2015).

    ADS  Google Scholar 

  45. 45.

    Zhu, Y. et al. Stratospheric aerosols, Polar Stratospheric Clouds, and polar ozone depletion after the Mount Calbuco eruption in 2015. J. Geophys. Res.: Atmospheres 123, 12,308–12,331 (2018).

    Google Scholar 

  46. 46.

    English, J. M., Toon, O. B. & Mills, M. J. Microphysical simulations of large volcanic eruptions: Pinatubo and Toba: microphysics of Pinatubo/Toba Eruptions. J. Geophys. Res.: Atmospheres 118, 1880–1895 (2013).

    ADS  Google Scholar 

  47. 47.

    Ayers, G. P., Gillett, R. W. & Gras, J. L. On the vapor pressure of sulfuric acid. Geophys. Res. Lett. 7, 433–436 (1980).

    ADS  CAS  Google Scholar 

  48. 48.

    Zhao, J. & Turco, R. P. Nucleation simulations in the wake of a jet aircraft in stratospheric flight. J. Aerosol Sci. 26, 779–795 (1995).

    ADS  CAS  Google Scholar 

  49. 49.

    Galeazzo, T., Bekki, S., Martin, E., Savarino, J. A. & Arnold, S. R. Photochemical box modelling of volcanic SO2 oxidation: isotopic constraints. Atmos. Chem. Phys. 18, 17909–17931 (2018).

  50. 50.

    Winker, D. M., Hunt, W. H. & McGill, M. J. Initial performance assessment of CALIOP. Geophys. Res. Lett. 34, L19803 (2007).

  51. 51.

    Lawson, P., Gurganus, C., Woods, S. & Bruintjes, R. Aircraft Observations of Cumulus Microphysics Ranging from the Tropics to Midlatitudes: Implications for a “New” Secondary Ice Process. J. Atmos. Sci. 74, 2899–2920 (2017).

    ADS  Google Scholar 

  52. 52.

    McFarquhar, G. M. et al. Importance of small ice crystals to cirrus properties: Observations from the Tropical Warm Pool International Cloud Experiment (TWP-ICE). Geophys. Res. Lett. 34, L13803 (2007).

  53. 53.

    Neely, R. R. III & Schmidt, A. VolcanEESM: Global volcanic sulphur dioxide (SO2) emissions database from 1850 to present - Version 1.0. Centre for Environmental Data Analysis https://doi.org/10.5285/76ebdc0b-0eed-4f70-b89e-55e606bcd568 (2016).

  54. 54.

    Kristiansen, N. I., Prata, A. J., Stohl, A. & Carn, S. A. Stratospheric volcanic ash emissions from the 13 February 2014 Kelut eruption: KRISTIANSEN ET AL. Geophys. Res. Lett. 42, 588–596 (2015).

    ADS  CAS  Google Scholar 

  55. 55.

    Mishchenko, M. I. & Travis, L. D. Capabilities and limitations of a current FORTRAN implementation of the T-matrix method for randomly oriented, rotationally symmetric scatterers. J. Quant. Spectrosc. Radiat. Transf. 60, 309–324 (1998).

    ADS  CAS  Google Scholar 

  56. 56.

    Meng, Z. et al. Single-scattering properties of tri-axial ellipsoidal mineral dust aerosols: a database for application to radiative transfer calculations. J. Aerosol Sci. 41, 501–512 (2010).

    ADS  CAS  Google Scholar 

  57. 57.

    Luo, B., Krieger, U. K. & Peter, T. Densities and refractive indices of H2SO4/HNO3/H2O solutions to stratospheric temperatures. Geophys. Res. Lett. 23, 3707–3710 (1996).

    ADS  CAS  Google Scholar 

  58. 58.

    Ball, J. G. C. et al. Measurements of the complex refractive index of volcanic ash at 450, 546.7, and 650 nm. J. Geophys. Res.: Atmospheres 120, 7747–7757 (2015).

    ADS  Google Scholar 

Download references

Acknowledgements

The work at the University of Colorado was supported by NASA grant NNX16AQ37G, NASA grant 80NSSC19K1276, and National Science Foundation (NSF) grant PLR1643701. We thank Dr. Mingxuan Wu from the University of Wyoming for providing the CALIPSO orbit data to help to convert model output in the CALIPSO orbit format. We thank Dr. Ping Yang, Dr. Bingqi Yi, and Jiachen Ding for their help with the particle optical properties. We appreciate discussions with Darya Urupina, Dr. Russ Schnell, graduate student Margot Clyne, Professor Anja Schmidt, and Dr. Anna Kristiansen. WACCM is a component of NCAR’s Community Earth System Model, CESM, which is supported by NSF and the Office of Science of the U.S. Department of Energy. We acknowledge high-performance computing support from Cheyenne (doi:10.5065/D6RX99HX) provided by NCAR’s Computational and Information Systems Laboratory (CISL), sponsored by the NSF. Data storage supported by the University of Colorado Boulder “PetaLibrary”.

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O.B.T., E.J., and Y.Z. discussed the hypothesis. Y.Z., O.B.T., and M.T. wrote the manuscript. M.T. summarized the laboratory study. E.J. S.W. provided the ATTREX data. Y.Z., P.Y., C.B., and M.M. participated in the model development. Y.Z. performed the model simulation and analyzed the observational data. All the authors edited the manuscript.

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Correspondence to Yunqian Zhu.

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Zhu, Y., Toon, O.B., Jensen, E.J. et al. Persisting volcanic ash particles impact stratospheric SO2 lifetime and aerosol optical properties. Nat Commun 11, 4526 (2020). https://doi.org/10.1038/s41467-020-18352-5

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