Radiative and chemical implications of the size and composition of aerosol particles in the existing or modified global stratosphere

. The size of aerosol particles has fundamental effects on their chemistry and radiative effects. We explore those effects using aerosol size and composition data in the lowermost stratosphere along with calculations of light scattering. In the size range between about 0.1 and 1.0 µm diameter (accumulation mode), there are at least two modes of particles in the lowermost stratosphere. The larger mode consists mostly of particles produced in the stratosphere and the smaller mode consists mostly of particles transported from the troposphere. The stratospheric mode is similar in the Northern and Southern 15 hemispheres whereas the tropospheric mode is much more abundant in the Northern Hemisphere. The two modes have very different roles for radiative effects on climate and for heterogeneous chemistry. Because the larger particles are more efficient at scattering light, most of the radiative effect in the lowermost stratosphere is due to stratospheric particles. In contrast, the tropospheric particles can have more surface area, at least in the Northern Hemisphere. The surface area of tropospheric particles could have significant implications for heterogeneous chemistry because these particles, which are partially 20 neutralized and contain organics, do not correspond to the surfaces used for laboratory studies of stratospheric heterogeneous chemistry. The purity of sulfuric acid particles in the stratospheric mode shows that there is limited production of secondary organic aerosol in the stratosphere, especially in the Southern Hemisphere. Out of eight sets of flights sampling the lowermost stratosphere (four seasons and two hemispheres) there were three with large injections of specific materials: volcanic, biomass burning, or dust. We then extend the analysis of size-dependent properties to particles considered for intentional climate 25 modification. There is no single size that will simultaneously optimize the climate impact relative to the injected mass, infrared heating, potential for heterogeneous chemistry, and undesired changes in direct sunlight. In addition, light absorption in the far ultraviolet is identified as an issue requiring more study for both the existing and potentially modified stratosphere.

at lower altitudes means that the majority of the mass of stratospheric aerosol is in the lowermost stratosphere, below the maximum in mixing ratio (Yu et al., 2016).
Various trends have been reported for the background stratospheric aerosol at times not influenced by major volcanic eruptions. 35 Deshler et al. (2006) concluded there was little long-term change in background stratospheric aerosol from 1971 to 2004. Hofmann et al. (2009 found an increasing trend after Friberg et al. (2014) found an increasing trend from 1999 to 2008. There has been recognition that moderate volcanic eruptions frequently influence the stratospheric aerosol and true nonvolcanic "background" concentrations are not necessarily present just because there has been no Pinatubo-scale eruption (Solomon et al., 1996). Different altitudes may exhibit different trends (Khaykin et al., 2017). Moderate 40 volcanic eruptions tend to mask trends in the non-volcanic background (Kremser et al., 2016). The data shown here reinforce the notion of modest but frequent perturbations to the lower stratosphere.
The overall circulation of air in the stratosphere, with rising air in the tropics and descending air in the extratropics, is mostly fed by air entering at the tropical tropopause. The lowermost stratosphere is a region at middle and high latitudes between the 45 local tropopause and slightly above the altitude of the tropical tropopause. Air in this lowermost stratosphere is affected by both downward motion in the extratropical stratosphere and adiabatic mixing with the troposphere (Holton et al., 1995). The tropospheric influence can extend as high as about 450 K potential temperature (Rosenlof et al., 1997). All of the data described here are in the lowermost stratosphere and show the influence of both air from higher in the stratosphere and air from the troposphere. 50 The chemical composition of particles in the lower stratosphere has been measured by several techniques. Impactor samples collected from the CARIBIC platform have been quantitatively analyzed for N, O, S, K, Fe, and other elements (Nguyen and Martinsson, 2007;Friberg et al, 2014). The moles of oxygen were approximately four times sulfur plus about 0.2 times carbon, indicating SO4 in sulfate and sulfuric acid plus some contribution from oxygenated organics. Much of the detailed information 55 on the chemical composition of aerosols in the lower stratosphere has come from the Particle Analysis by Laser Mass Spectrometry (PALMS) instrument (Murphy et al., 1998). These data show that most particles larger than about 110 nm fall into three distinct types: sulfuric acid with or without meteoric metals and mixed organic-sulfate particles from the troposphere (Murphy et al., 2014). Because the pure sulfuric acid particles do not contain biomass burning residues, they are not simply tropospheric particles that have lost organics after entering the stratosphere . Recent data from another 60 single particle mass spectrometer have found comparable abundances of sulfuric acid particles with meteoric metals (Schneider et al. discussion). https://doi.org/10.5194/acp-2020-909 Preprint. Discussion started: 22 September 2020 c Author(s) 2020. CC BY 4.0 License.
We extend the previous results to show that the mixed organic-sulfate particles from the troposphere are generally smaller than both types of sulfuric acid particles. We then show how this size difference has significant implications for light scattering and 65 heterogeneous chemistry.

Methods
This paper includes data in the lowermost stratosphere from the Atmospheric Tomography (ATom) mission with deployments 70 in four seasons during 2016 to 2018. Although the ATom mission was not specifically designed to sample the stratosphere, it encountered stratospheric air in both the Northern and Southern Hemispheres during its regular vertical profiles. Stratospheric air was encountered periodically at altitudes greater than 8 km and latitudes poleward of 30 degrees north or 40 degrees south ( Figure S1). Because the NASA DC8 aircraft has a ceiling of about 12 km, stratospheric air was always associated with low tropopauses, sometimes in tropopause folds. We therefore use ozone rather than altitude as the primary definition of how far 75 into the stratosphere measurements were taken. Any high ozone below 6 km altitude was excluded.
Size distributions for accumulation-mode particles were measured using two modified commercial laser optical particle spectrometers, an ultra-high sensitivity aerosol spectrometer (UHSAS; Droplet Measurement Technologies, Longmont, USA) from 0.07 -0.6 µm diameter and a laser aerosol spectrometer (LAS, TSI Inc., St. Paul, USA) from 0.6 to ~4.8 µm diameter 80 (Kupc et al., 2018;Brock et al., 2019). The diameters are based on calibration by ammonium sulfate particles. The size resolution of the reported data is 20 bins per decade of particle size. Data are recorded at 1s intervals although averaging is needed in the stratosphere to improve counting statistics for particles in the LAS size range (Brock et al., 2019).
Particle composition was measured with the Particle Analysis by Laser Mass Spectrometry (PALMS) instrument (Thomson 85 et al., 2000;Froyd et al. 2019). A pressure-controlled aerodynamic focusing inlet brings particles into a vacuum where they cross two continuous laser beams. The transit time between the beams measures the aerodynamic diameter of each particle.
The aerodynamic diameters are under vacuum conditions with most particles much smaller than the mean free path at the inlet exhaust; however transition flow corrections are considered. Transit times were calibrated to known particle sizes before and after every field deployment. A 193 nm pulse from an excimer laser is triggered when a particle arrives at the second laser 90 beam. Either positive or negative ions are analyzed with a time-of-flight mass spectrometer. The polarity was switched every few minutes. Most of the data shown here are from positive ion spectra. Negative ion spectra do not distinguish sulfuric acid with and without meteoric metals because the metal ions only appear in the positive ion spectra.
The optical size distributions are combined with the PALMS single-particle composition data for particles larger than 100 nm 95 to create size distributions that are resolved by composition. This requires converting the PALMS aerodynamic diameters to correspond to the optical diameters (Froyd et al., 2019). The composition-resolved size distributions presented here use wider https://doi.org/10.5194/acp-2020-909 Preprint. Discussion started: 22 September 2020 c Author(s) 2020. CC BY 4.0 License. size bins than the native optical particle counter resolution but narrower size bins than the standard ATom products (Froyd et al., 2019). The narrower bins are possible because of improved statistics after averaging over all of the data within a specific band of ozone and latitude, even if those data were not contiguous in time. 100 For the purpose of this study particles are classified into four basic categories: sulfuric acid with and without meteoric metals, mixed organic-sulfate particles, and other particles including dust. Example spectra are shown in Murphy et al. (2014). When appropriate further distinctions can be made, such as separating biomass burning particles from other mixed organic-sulfate particles. 105 Calculations of light scattered back to outer space are made for an optically thin layer uniformly spread over a sunlit hemisphere as described in Murphy (2009), except that these calculations use an atmospheric transmittance appropriate for approximately 11 km altitude (Arvesen, 1969). Changing the solar spectrum over the entire range from top-of-atmosphere to surface gives qualitatively similar results. At the low relative humidities in the stratosphere, water uptake is less important for optical 110 properties than it is in the troposphere. The mean relative humidity for the ATom data at ozone > 250 ppbv was less than 10%. A sectional aerosol model (CARMA) coupled with the NSF/DOE Community Earth System Model (CESM) is used in the study to simulate the composition and size distributions of stratospheric aerosols (Yu et al., 2015;Toon et al., 1988). CESM-CARMA tracks two external-mixed groups of aerosols. The first group consists of pure sulfate particles (formed through 115 nucleation and condensation of water vapor and sulfuric acid) with 20 size bins ranging from 0.4 nm to 2.6 µm in diameter; the second group consists of internal mixed aerosols (containing condensed sulfate, organics, black carbon, salt and dust) with 20 size bins from 0.1 µm to 17 µm. The model is run at a horizontal resolution of 1.9° (latitude) x 2.5° (longitude). It has 56 vertical layers from the surface to 1.8 hPa with a vertical resolution of ~1 km near tropopause. 120 3 Composition-resolved size distributions in the stratosphere Figure 1 shows the composition-resolved size distributions measured in the lowermost stratosphere for the four ATom deployments, separated by the Northern and Southern Hemisphere. The data are for ozone between 250 and 400 ppbv. This range of ozone is chosen to be definitely in stratospheric air and to include data from both hemispheres on all four deployments. 125 On each panel the thick black line is the size distribution from the optical particle counters. At each size the fraction of particle types from PALMS is shaded. A number of features in Figure 1 are worthy of comment.
The volume distributions show a peak near 400 nm diameter and another peak, or at least a shoulder, near 180 or 200 nm. Indeed, without the composition it would be difficult to be sure that there were two separate modes. For example, the Wyoming particle counters used on stratospheric balloon flights (Deshler et al., 2003) do not clearly resolve the modes.
The 400-nm mode is from sulfuric acid particles produced in the stratosphere, especially those with meteoric metals. The size of these meteoric-sulfuric particles is extremely consistent through both hemisphere and the four deployments ( Table 1). The 135 primary source of sulfuric acid in the stratosphere, oxidation of carbonyl sulfide, is similar in the two hemispheres. The meteoric-sulfuric particles also have a narrow size distribution, with a typical geometric standard deviation of about 1.4 when fit with a log-normal distribution. This is consistent with condensational growth, which tends to lead to narrow size distributions. Sulfuric acid particles without meteoric material have more diverse sizes except for the volcanically influenced ATom1 Southern Hemisphere, when the sulfuric acid particles had a narrow size distribution very similar to the meteoric-140 sulfuric particles.
The smaller mode near 200 nm is from mixed organic-sulfate particles that have mixed into the stratosphere. The mass spectra of particles in the smaller mode are essentially identical to those of particles in the upper troposphere. Comparing the Northern and Southern Hemispheres in Figure 1, the concentration of the smaller mode is larger in the Northern Hemisphere. The upper 145 troposphere in the Southern Hemisphere has generally lower aerosol concentrations, so mixing in a given amount of tropospheric air will bring in fewer particles than the same amount of mixing in the Northern Hemisphere.
Of the eight cases in Figure 1, three have much higher aerosol concentrations than the others, for three very different reasons. The ATom1 Southern Hemisphere had a large and very narrow mode of pure sulfuric acid particles. These were most likely 150 produced from SO2 injected into the stratosphere by the Calbuco eruption in April 2015, about 16 months before the measurements. The ATom3 Northern Hemisphere had a large tropospheric organic-sulfate contribution. More detailed composition shows that these included a large fraction of biomass burning particles. A separate paper is in preparation about this event. The ATom4 Northern Hemisphere had both a large contribution from organic-sulfate particles and a remarkable amount of dust at and above the tropopause. Concentrations at the tropopause often reached several micrograms per standard 155 cubic meter. The dust was very widespread: it was measured over both the north Atlantic and Pacific Oceans over more than 40 degrees of latitude. This may be Asian dust and pollution carried to high altitude in an event similar to that described by Huang et al. (2008). The ATom4 and Huang et al. events were both in May. A separate paper is also planned about this dust event.
160 Figure 2 shows the CESM/CARMA model results for the ATom2 flights for the same 250-400 ppbv range of ozone as the data in Figure 1. ATom2 is chosen because neither hemisphere was perturbed by volcanic sulfate, biomass burning, or dust.
The model reproduces the tropospheric mode well in the Northern Hemisphere but overestimates it in the Southern Hemisphere. The model reproduces the total volume of stratospheric particles well in both hemispheres but the modeled https://doi.org/10.5194/acp-2020-909 Preprint. Discussion started: 22 September 2020 c Author(s) 2020. CC BY 4.0 License. diameter of these particles is too small. A possible reason is that the model does not include meteoric smoke particles on which 165 sulfuric acid can condense. That is, the model treats both the meteoric-sulfuric and sulfuric acid particles observed by PALMS as a single type. Figure S2 compares the Northern Hemisphere ATom data to Wilson et al. (2008). Consistent with the ATom observations, the tropospheric particle mode at about 200 nm is in some cases distinct from the larger stratospheric mode. Figure 3 shows composition-resolved size distributions further into the stratosphere with ozone between 500 and 850 ppbv. 170 Only the Northern Hemisphere during ATom2 and ATom4 had significant amounts of PALMS data in this ozone range. For ATom2, the primary difference at higher ozone was more meteoric-sulfuric particles, a result also found by Schneider et al. (discussion). The large mixing event of dust and other tropospheric particles during ATom2 barely affected "altitudes" of more than 500 ppbv ozone.

Vertical profiles
The shaded regions in Figure 1 can be integrated over all sizes to give the volume associated with each type of particle, then multiplied by a density to give the mass. Figure 4 shows vertical profiles of the mass concentrations for the meteoric sulfuric particles and organic-sulfate particles. As expected for their sources, the concentration of meteoric-sulfuric particles increases 180 with altitude and the concentration of organic-sulfate particles decreases with altitude. The concentration of the meteoricsulfuric particles is fairly consistent between hemispheres and deployments. In contrast, the concentration of organic-sulfate particles was larger in the Northern Hemisphere that the Southern Hemisphere and varied considerably between deployments.
It is worth noting that the highest concentration of tropospheric particles in each hemisphere, ATom3 for the Southern Hemisphere and ATom4 for the Northern Hemisphere, were both local springtime. 185 Figure 5 shows the ratio of the C + peak, an indicator of organic content, to two peaks indicative of sulfate or sulfuric acid. The top axis gives an approximate mass fraction of organics adapted from calibrations described by Froyd et al. (2019). The vertical axis of ozone serves as a measure of distance into the stratosphere. That the stratospheric and tropospheric particle compositions remain distinct implies that there is very limited redistribution of semi-volatile organics between particles. Like 190 most upper tropospheric particles, the organic-sulfate particles contain on average about 40 to 80 organic material by mass.
There is little variation with ozone, indicating a long lifetime for the organic material as well as little uptake of sulfuric acid.
The latter is consistent with most of the sulfuric acid coming from carbonyl sulfide above 20 km rather than SO2 near the tropopause (Kremser et al., 2016;Rollins et al., 2017).

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There is some limited uptake of organics onto the stratospheric particles, although the maximum organic concentration is still much less than for tropospheric particles. Meteoric-sulfuric particles definitely formed in the stratosphere, so any significant https://doi.org/10.5194/acp-2020-909 Preprint. Discussion started: 22 September 2020 c Author(s) 2020. CC BY 4.0 License. organic content indicates net uptake of organics. Their organic content grows as the particles descend to the lowermost stratosphere and the upper troposphere.

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The meteoric-sulfuric particles contain much less than 1% organic mass at altitudes with ozone greater than 500 ppbv and as much as 2 to 4% near the tropopause in the Northern Hemisphere. Such limited formation of secondary organic mass in the lowermost stratosphere is consistent with previous PALMS measurements .
A new finding from ATom is that there is a very distinct and consistent difference between the hemispheres in the small amount 205 of organic content that does form in the meteoric-sulfuric acid particles. Since the particles start from similar formation processes much higher in the stratosphere, we conclude that there is more condensable or reactive organic vapor in the Northern Hemisphere lower stratosphere. This could be either gas phase species mixed from the troposphere or semi-volatile organics transferring from organic-sulfate particles.

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Adding a few percent mass to the meteoric-sulfuric particles represents a very small amount of organic vapor. Without knowing uptake coefficients the amount of vapor cannot be determined uniquely, but a representative calculation is that one or two pptv of an organic gas-phase species with molecular weight of about 100 daltons that reacts with sulfuric acid on every collision would add few percent mass to a 450 nm particle in a few months. The same order of magnitude can be obtained by noting from Figure 4 that at 200 ppbv ozone there is about 100 ng standard m -3 of meteoric sulfuric particles. 1% by mass of these 215 particles corresponds to about a part per trillion by mass of air. We conclude that an order of magnitude for highly condensable organic vapor in the lowermost stratosphere is a few parts per trillion in the Northern Hemisphere and less in the Southern Hemisphere. A less reactive or condensable organic molecule could be present at a correspondingly higher concentration.

Radiative and chemical implications 220
The different sizes of the sulfuric acid and organic-sulfate particles lead to substantial differences in their radiative and chemical effects. Important properties are the amount of infrared heating, the amount of light scattered, implications for photolysis, the surface area available for heterogeneous chemistry, and the mass sedimentation rate.

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A key part of the radiative implications is the efficiency of light scattering as a function of particle size. Figure 6 shows the mass scattering efficiency as a function of particle size averaged over the solar spectrum and a sunlit Earth. Calculations are for a real refractive index of 1.45 and minimal absorption. Atmospheric extinction is determined by the solid total scattering curve. Much of the light scattered by particles continues downward to the Earth and so does not directly affect climate.
Separating out the light scattered to outer space (dashed curve) gives a maximum that is slightly broader and shifted to smaller 230 sizes than light extinction. Over much of the size range of particles that scatter light efficiently, only about 1/5 of the light that https://doi.org/10.5194/acp-2020-909 Preprint. Discussion started: 22 September 2020 c Author(s) 2020. CC BY 4.0 License.
is scattered goes to outer space; the remainder becomes diffuse light. This is a reason for the large increases in diffuse light (with decreases in direct sunlight) after volcanic eruptions (Murphy, 2009).
The top panel of Figure 7 replots the chemically resolved size distribution for ATom2 in the Northern Hemisphere. This was 235 chosen as an example because it is similar to several other locations and seasons such as ATom1 Northern Hemisphere and ATom3 Southern Hemisphere. There was more sampling time in the ATom2 Northern Hemisphere stratosphere so the particle statistics are better, with about 10,000 particles. In Figure 7 the two sulfuric acid particle categories have been combined. Of the particles larger than 0.1 µm diameter, about 39% of the volume was organic-sulfate particles from the troposphere and 61% sulfuric acid particles from the stratosphere (including both those with and without meteoric metals). The percentage 240 contribution to each parameter in Figure 7 by stratospheric aerosol will be somewhat larger at ambient conditions because sulfuric acid has some water uptake even at <10% relative humidity. Ambient sulfuric acid particles may have roughly 5 to 15% larger diameters than measured in the warm aircraft cabin.

Infrared heating 245
An important property for stratospheric particles is their absorption and emission of infrared radiation. Infrared properties are more important for stratospheric aerosol than very low-altitude aerosol because the latter are close to the surface temperature and so absorb and emit similar amounts of energy.

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Infrared absorption by stratospheric particles is important for two reasons. First, it heats the stratosphere around the particles.
Changes in circulation due to infrared heating were responsible for significant changes in ozone after the Pinatubo eruption (Labitzke and McCormick, 1992;Pitari and Rizi, 1993). The heating-induced changes in ozone were as large or larger than those due to heterogeneous chemistry. There are additional feedbacks on the circulation after changes in infrared heating due to changes in ozone and water vapor (Visioni et al., 2017). Infrared heating is largest in the lower stratosphere where the 255 temperature contrast with the surface is greatest (Lacis, 2015). Second, infrared absorption by stratospheric particles offsets some or even all of the shortwave cooling of the Earth. For sulfuric acid particles similar to those after the Pinatubo eruption, longwave heating offset roughly 25% of the shortwave cooling (Hansen et al., 2005). This increases to about 50% for large injection rates because larger particles (>0.6 um) become 260 increasingly less efficient at scattering sunlight to outer space ( Figure 6) compared to their volume (Niemeier and Timmreck, 2015). Alumina with the size distribution from rocket emissions was calculated to cause net warming (Ross and Sheaffer, 2014 For wavelengths much larger than the particles, absorption and emission are approximately proportional to total particle 265 volume (and the material) and do not depend on particle size (van de Hulst, 1981). Therefore, net thermal infrared heating is insensitive to the size of particles and will approximately follow the volume distribution in the top panel of Figure 7. For ATom2, most of the volume distribution was composed of particles of stratospheric origin, but that was not always the case ( Figure 1). The infrared effects of the tropospheric particles found in the lower stratosphere are hard to assess. Longwave radiative heating depends not only on the strength of the absorption bands but also on their overlap with atmospheric windows 270 in the infrared spectrum. The presence of a significant fraction of organic material has unknown implications for infrared heating.

275
The middle panel in Figure 7 shows the size distribution weighted by the amount of sunlight scattered to outer space, which is relevant for shortwave climate effects. Weighting the size distribution by the light extinction would shift the peak just slightly further to larger particles. Because of their size, the sulfuric acid particles contribute a greater fraction of the light scattering than their mass fraction. In fact, comparing Figures 1 and 6, the most abundant size of the sulfuric acid particles in the lower stratosphere was close to the maximum in light scattering to outer space per unit mass. The ATom mission was during a time 280 with small volcanic influence. In contrast, particles shortly after the Pinatubo eruption had volume mean diameters greater than 0.7 µm (Wilson et al., 2008; Figure S2), large enough that their mass scattering efficiency decreased.

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Particle size can affect heterogeneous chemistry. Reactions with sulfuric acid particles that are important to stratospheric chemistry span the range from reactions that occur in the interior of liquid particles and hence are proportional to volume to reactions that occur on the surface and hence are proportional to surface area (Hanson et al., 1994). Heterogeneous chemistry can be especially important within or at the edge of the polar vortex (Solomon et al., 2015;Stone et al., 2017).

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The bottom panel of Figure 7 shows the size distribution weighted by surface area rather than volume. For these conditions surface reactions are closely proportional to surface area; gas-phase diffusion is a minor correction. For the case shown in Figure 7, the organic-sulfate particles from the troposphere are about half of the surface area in the lowermost stratosphere. This is significant because whereas stratospheric heterogeneous chemistry on sulfuric acid has been extensively studied, little is known about the same reactions on organic-sulfate particles. 295 The organic-sulfate particles differ from the sulfuric acid particles in important ways. Most obviously, they contain a high proportion of organics that may participate in new chemistry with halogen radicals. Iodine in particular may react with organic https://doi.org/10.5194/acp-2020-909 Preprint. Discussion started: 22 September 2020 c Author(s) 2020. CC BY 4.0 License. aerosols Pechtl et al., 2007). Although not fully neutralized, the organic-sulfate particles are not nearly as acidic as the relatively pure sulfuric acid particles. This can be determined from acid cluster peaks in the PALMS 300 mass spectra. Some chlorine activation reactions that lead to ozone destruction are acid-catalyzed (Burley and Johnston, 1992) and therefore may be slower on partially neutralized particles. The organic-sulfate particles also contain less water -sulfuric acid is extremely hygroscopic compared to other species at the low relative humidities in the stratosphere. The availability of condensed water for heterogeneous reactions could be further reduced if the organic-sulfate particles are glassy at the low temperatures and humidity in the stratosphere (Krieger et al., 2012;Price et al., 2014). 305

Sedimentation
Sedimentation is a key process in the stratospheric aerosol budget (Wilson et al., 2008). It is more important than in the stratosphere than it is near ground level partly because particles fall faster at lower air density. A bigger reason sedimentation 310 is important in the stratosphere is the relevant time scale: a fall speed of a kilometer per month would be unimportant in the lower troposphere but can control the residence time of a particle in the stratosphere. Particles larger than about 1 µm diameter have sedimentation rates greater than 10 km yr -1 in the lower stratosphere. On Figure 7, the sedimentation flux as a function of size would be slightly more skewed to large diameters than the light scattering panel. For the case shown in Figure 7 the sulfuric acid particles have roughly twice the volume of the organic-sulfate particles. Their source strength must be somewhere 315 between about twice as large as the tropospheric particles (if loss is controlled by bulk air motion) and three times as large (if loss is controlled by sedimentation).

320
Absorption and scattering of ultraviolet light are distinct from that of visible light because of the impact on photolysis rates.
Light scattering by stratospheric aerosol changes the path length of light in the stratosphere, which in turn changes photolysis rates (Huang and Massie, 1997;Pitari et al., 2015). The calculations are complex because Rayleigh scattering in the ultraviolet leads to strong effects from multiple scattering (Bian and Prather, 2002), especially at twilight or if a scattering aerosol layer is located above gas-phase absorption (Davies et al., 1993;Anderson et al., 1995). In addition, the long path lengths magnify 325 the importance of any absorption of ultraviolet light by aerosols.
The scattering of ultraviolet light peaks at smaller particle sizes than for sunlight. This means that the smaller troposphericorganic particles contribute substantially to the scattering of ultraviolet light. The relative contributions to scattering of light at < 240 nm are fairly similar to the surface area panel in Figure 7 except that sizes smaller about 80 nm and larger about 600 330 nm contribute less to UV scattering than they do to surface area.
One important wavelength band is 200 to 242 nm, where photolysis of O2 is responsible for formation of ozone and photolysis of N2O produces odd nitrogen (NOy). (Brasseur and Solomon, 1986). For purely scattering particles, changes in photolysis in this wavelength range are reduced by large cancellations in direct and diffuse light (Michelangeli et al., 1989). Light scattering 335 by the El Chichon volcanic cloud was estimated to reduce O2 photolysis by about 10% (Michelangeli et al., 1989). The overall effect of scattering seems to be to reduce ozone formation (Pitari et al., 2015).
Unlike pure scattering particles, absorbing particles would not have a similar partial cancellation between direct and diffuse sunlight. Huang and Massie (1997) examined the effect of substituting ash, with visible and UV absorption, for non-absorbing 340 sulfuric acid in a simple model of photolysis after a volcanic eruption. There are competing effects on the ozone column because both JO2 and JO3 are reduced by UV absorption, with one reducing and the other increasing ozone (Pitari and Rizi, 1993). The individual effects were several percent of the ozone column with the net impact difficult to assess because their simple model did not include NOx or halogen chemistry. The imaginary refractive index of the organic-sulfate particles at wavelengths below 242 nm is not known but could easily be large enough to lead to significant absorption compared to 345 scattering.

Relevance to volcanic or intentional aerosol injection
Sulfur dioxide is periodically injected into the stratosphere by major volcanic eruptions, leading to an increase in sulfuric acid 350 aerosol. One such example is visible in the ATom1 Southern Hemisphere panel in Figure 1. There have also been numerous proposals for, and studies of, injecting material into the stratosphere for the purpose of solar radiation management (National Research Council, 2015). Regardless of the desirability of such actions, some of the calculations presented above on the optical properties and potential for heterogeneous chemistry have implications for added material whether it be from volcanoes or deliberate intervention. 355

Complex controls on particle size
The previous sections demonstrate that particle size is important for many of the properties relevant to climate and chemical effects. In the real world, one cannot instantly fill a box with monodisperse particles of a chosen size, the way one might in a 360 model. It is important to understand what controls the size distribution of particles in the stratosphere and how will it change with additional aerosol or precursors such as sulfur dioxide. The mean diameter in the stratosphere is not a single number but varies with the aerosol loading, altitude, and latitude (English et al., 2012).
The size of particles in the unperturbed or perturbed stratosphere can be understood in two complementary ways. The first 365 way, a top-down approach, says that for a given mass of stratospheric aerosol, the more particles there are, the smaller they https://doi.org/10.5194/acp-2020-909 Preprint. Discussion started: 22 September 2020 c Author(s) 2020. CC BY 4.0 License. must be. The second way, a bottom-up approach, considers how the size of each particle is set by a balance of growth and removal processes in the stratosphere.
For the top-down approach, one must consider at least three sources of particle number in the stratosphere. Particles come 370 down from the mesosphere, up from the troposphere, and new particles can form in the stratosphere (Murphy et al., 2014). The meteoric source of particles to the stratosphere is mostly "smoke" consisting of material that evaporated from ablating meteoroids and condensed into new particles high in the atmosphere. Much of this material descends near the winter poles (Bardeen et al., 2008). Second, tropospheric particles provide an important source of stratospheric particles below 20 km altitude (Yu et al., 2016). The fate of tropospheric particles entering the stratosphere is poorly represented in most models. 375 New particle formation is also important for the stratosphere. The pure sulfuric acid category in Figure 1 is probably from growth of particles formed in (or at the edge of) the stratosphere. One formation region is near the tropical tropopause with upward transport into the stratosphere (Brock et al., 1995;English et al., 2011). There is probably also formation of new sulfuric acid particles higher in the stratosphere over the winter poles (Wilson et al., 1989), although this must be distinguished from meteoric smoke descending in the same regions (Curtius et al., 2005). 380 Adding sulfuric acid or its precursors will have complex effects on new particle formation, with more vapor to condense but also more surface area sink. In contrast, injected solid particles would provide a surface sink for background sulfuric acid from oxidation of carbonyl sulfide, likely reducing new particle formation. This implies that injected solid particles would probably change the size of the natural sulfuric acid particles in the stratosphere. Sufficiently small injected solid particles might reach 385 high altitudes where existing sulfuric acid particles have evaporated (Weisenstein et al., 2015;Jones et al., 2016). There could be unknown effects if they were later entrained in descending air in the winter polar regions.
The bottom-up approach considers how the size of stratospheric particles is determined by a balance of growth and removal processes. Particles grow by coagulation and by condensation of sulfuric acid and other species. Coagulation in the unperturbed 390 stratosphere is slow except for special situations such as shortly after new particle formation (Brock et al., 1995;Hamill et al., 1997). Coagulation increases non-linearly with aerosol concentration so it becomes more significant after volcanic eruptions (Pinto et al., 1989) or large injection scenarios (Weisenstein et al., 2015). In these cases, coagulation helps drive the extra mass primarily to larger particles rather than more numerous particles (Heckendorn et al., 2009;Niemeier and Timmreck, 2015).
Both sedimentation and downward motion are important removal processes (Wilson et al, 2008). 395 One implication of having multiple sources of particles in the stratosphere is that there is no single response to injected material.
It is only in the last few years that stratospheric models have incorporated multiple sources of particles along with detailed microphysics (Pitari et al. 2014;Yu et al., 2016;Mills et al., 2017). There is still considerable uncertainty in quantitatively https://doi.org/10.5194/acp-2020-909 Preprint. Discussion started: 22 September 2020 c Author(s) 2020. CC BY 4.0 License.
understanding the size of particles in the current stratosphere, let alone after a perturbation. Figure 2 demonstrates that a 400 detailed microphysics model of the stratosphere did not grow the sulfuric acid particles to large enough sizes.

Impacts on the stratosphere as a function of size
The preceding section suggests that the ultimate size of particles is not something that can simply be chosen when injecting 405 aerosol particles or their precursors; instead it is also strongly influenced by subsequent particle formation and growth processes in the stratosphere. Even solid particles may coagulate or grow by condensation of sulfuric acid and not retain their original size. Despite this, it is of interest to examine the impact of particle size on the relative magnitude of effects. Figure 8 shows an estimate of net cooling compared to particle volume, surface area, and sedimentation rate.

410
The shortwave effect is modified to include longwave effects by adapting a calculation in Lacis et al. (1992), who showed that heating exceeded shortwave cooling for several different types of particles when their diameters were more than about 4 µm.
Since infrared absorption is almost independent of size, an approximate net cooling was estimated by subtracting a constant from the calculated shortwave scattering to space ( Figure 6) such that the net was zero at 4 µm diameter. Subtracting this amount is only approximate but the patterns in Figure 8 are not sensitive to the exact crossing point. The relative sedimentation 415 curve in Figure 8 also varies slightly with altitude but again the patterns are similar.
The size that has the least infrared absorption for a given amount of shortwave climate impact is about 0.5 µm diameter (filled circles). Larger or smaller particles will be less effective at cooling the Earth and will cause more stratospheric circulation changes for a given amount of cooling. Sufficiently large (> 4 µm) or small (< 0.1 µm) particles cause net heating of the Earth 420 (Lacis et al., 1992). Even for the optimal size, the infrared heating due to deliberate injections of sulfuric acid or its precursors into the stratosphere would cause significant changes in circulation (Aquila et al., 2014).
The potential for increased heterogeneous chemistry would be reduced by using larger particles with less surface area. Particles with a diameter of about 1 µm have the largest cooling effect for a given surface area (open circles). These larger particles, 425 however, have high sedimentation rates (downward triangles) and limited stratospheric lifetimes. For a given climate impact, the mass flux due to sedimentation is minimized by particles with a diameter of about 300 nm. The least diffuse light is created by the smallest particles ( Figure 6). The exact sizes of the various maxima depend on the refractive index and density. However, the patterns of which variables are maximized at larger or smaller sizes will be similar.
The title of Solomon et al. (2011) includes the phrase "the persistently variable 'background' stratospheric aerosol". The ATom data presented here add new meaning to that phrase. Out of eight samplings of the lowermost stratosphere, three exhibited much higher aerosol concentrations for three different reasons: a volcanic eruption, biomass burning aerosol, and transport of 435 dust and other near-surface particles. None of these events were targeted during the flights. Such variations in the stratospheric aerosol layer are important for both heterogeneous chemistry (Solomon et al., 1996) and climate (Solomon et al., 2011).
There are important differences in the aerosol in the lower stratosphere between the Northern and Southern Hemispheres. A smaller amount of tropospheric aerosol in the Southern Hemisphere stratosphere indicates that the tropospheric particles are 440 mixing into the lower stratosphere within each hemisphere rather than entering in rising air in the tropics and splitting into the two hemispheres. Sulfuric acid particles in the Southern Hemisphere also acquire less organic content. This suggests that there are lower concentrations of gas-phase organics in the Southern Hemisphere. One of several possible formation routes is that small organic compounds such as acetone and formaldehyde can react with concentrated sulfuric acid to form polymers that stay in the aerosol (Iraci and Tolbert, 1997;Williams et al., 2010). Other routes would be if low-volatility organic molecules 445 were formed in the gas phase or evaporated from the tropospheric particles and recondensed on the sulfuric acid particles.
Even in the Northern Hemisphere, only low part-per-trillion range concentrations of gas-phase organics are required to explain the very small amounts of organics taken up by the sulfuric acid particles.
The data here add support to the concept of Yu et al. (2016) that tropospheric particles comprise a significant fraction of the 450 aerosol in the lowermost stratosphere. Such tropospheric particles offer a route for anthropogenic influence on the stratosphere. The Yu et al. model also correctly predicts that tropospheric particles are smaller than sulfuric acid particles formed in the stratosphere (Figure 2).
Absorption of ultraviolet light means that impurities should be considered when assessing deliberately added materials. For 455 example, absorption appropriate for optical-quality sapphire should probably not be used when evaluating proposals to add industrial quantities of alumina to the stratosphere. Even part-per-million impurities in alumina increase absorption in the ultraviolet (Innocenzi et al., 1990). Compared to many materials, sulfuric acid has extremely low absorption in the ultraviolet (Noziere and Esteve, 2005;Dykema et al., 2016).

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The broad distribution of particle sizes in the unperturbed stratosphere is the superposition of several narrower distributions.
Single particle types, particularly meteoric-sulfuric acid particles, can have narrow size distributions (lognormal standard deviation ~1.4).
Multiple formation mechanisms for stratospheric particles imply that the size of particles after a volcanic or intentional 465 injection may be difficult to predict. Yet an accurate prediction of size is important: The diameter must be known to perhaps https://doi.org/10.5194/acp-2020-909 Preprint. Discussion started: 22 September 2020 c Author(s) 2020. CC BY 4.0 License. 25% to accurately estimate tradeoffs between climate impact and side effects (Figure 8). A state-of-the-art microphysical bin model underestimates the size of stratospheric sulfuric acid particles, indicating that we do not fully understand what controls the size of particles in the stratosphere. The size difference has significant impacts on properties: the modeled particles have about 65% of the climate impact per unit mass as the observations, 160% of the surface area, and sediment about 60% as fast. 470 There is no single diameter that produces the largest shortwave climate impact with the fewest side effects (Figure 8). To the extent that one could control the size of particles after an intentional injection, any chosen size involves tradeoffs. Particles smaller than about 0.6 µm diameter have more surface area for possible heterogeneous chemistry. Particles larger than about 0.4 µm require more injected mass and produce more diffuse light. For a given amount of scattered sunlight, either sufficiently 475 large or small particles have more infrared absorption and hence more impacts on stratospheric circulation. Most of the mass of particles after the Mt. Pinatubo eruption was larger than 0.6 µm diameter (Brock et al., 1993;Wilson et al. 2008), a size range with relatively little surface area compared to their climate impact. The heterogeneous chemistry observed after Mt.
Pinatubo may therefore underestimate what might happen with intentionally added material.  Phys., 12, 4775-4793, doi:10.5194/acp-12-4775-2012Phys., 12, 4775-4793, doi:10.5194/acp-12-4775- , 2012.       Figure S3 shows the percentage contributions of various particle types to these processes for other deployments. Scaling to net thermal infrared heating gives nearly identical relative contributions as volume in the top panel. Scaling to sedimentation rate gives a similar shape to the 810 middle panel.       where D is the diameter and a is a scaling factor. Each fit is for a specific component. Fits were not attempted for 830 "other" particles (mostly dust) because they did not generally show a defined mode. Italics indicate a poor fit to a lognormal shape.