Below are the first 10 and last 10 pages of uncorrected machine-read text (when available) of this chapter, followed by the top 30 algorithmically extracted key phrases from the chapter as a whole.
Intended to provide our own search engines and external engines with highly rich, chapter-representative searchable text on the opening pages of each chapter. Because it is UNCORRECTED material, please consider the following text as a useful but insufficient proxy for the authoritative book pages.
Do not use for reproduction, copying, pasting, or reading; exclusively for search engines.
OCR for page 9
--> 2 Discussion of the Science Issues The topics covered in this chapter are grouped into four general areas: gas phase processes, particle-related processes, atmospheric transport, and climate impacts. For each of these general areas, the panel looks at the findings of both the NASA and European assessment reports and raises issues judged to merit most attention in light of SASS's objectives and schedule. In some cases, the issues are the same as those highlighted by SASS's strategic plan; in other cases they suggest a shift in priorities. It should be noted that research on many of these issues is progressing rapidly, and the discussions presented here can really only provide a concise snapshot of the state of the science when the panel's analyses were written. Gas-Phase Emissions, Characterization, and Chemistry A central focus of SASS investigations has been to quantify the effects of aircraft emissions, particularly NOx, on atmospheric ozone levels. (The panel's interim review of SASS contains a description of the basic processes involved in ozone photochemistry and will not be reviewed here.) Some highly uncertain issues remain, such as the lightning NOx source, and the need for more upper troposphere/lower stratosphere trace gas measurements to constrain model estimates. In recent years, though, some significant progress has been made. For instance, trace gas measurements made during field campaigns such as SUCCESS, SONEX, and STRAT2 have led to valuable new insights into the role 2 SUCCESS (Subsonic Aircraft: Contrail and Cloud Effects Special Study), SONEX (SASS Ozone and Nitrogen Oxide Experiment), STRAT (Stratospheric Tracers of Atmospheric Transport).
OCR for page 10
--> of NOx, HOx, and HCs in determining the photochemistry of ozone in the upper troposphere. Also, detailed NOx source inventories, laboratory investigations of key reactions, and emission characterization studies have helped provide input data for assessment models. The chemistry as outlined in the Brasseur et al. (1997) report is shown in somewhat more detail than that given in the Friedl (1997) report, but where comparisons can be made it appears that there is general agreement on the specific chemistry employed by both groups. It is likely that the chemical mechanisms chosen by the NASA and European groups are very similar, since both U.S. and European groups rely heavily on the two existing major kinetic data reviews, which are very similar in their recommendations (DeMore et al., 1997; Atkinson et al., 1997). In general, SASS's research objectives related to the homogeneous chemistry used in the project's modeling efforts do not appear to be missing any critical elements. However, there are some issues the panel feels may deserve more attention, as discussed in the following sections. Aircraft Emission Issues The nature and extent of the chemistry included in the assessment models should ideally be based on our knowledge of the aircraft emissions under actual flight conditions. In the absence of such knowledge, choices are made on the basis of measurements made during bench tests of aircraft engines. Observations of exhaust plume components seem to have been restricted to those components that are believed, a priori, to be important (e.g., NOx, CO, SOx, soot, aerosols). Friedl (1997) suggests strongly that this information is still very incomplete. As discussed below, there are some issues related to the emissions of hydrocarbons and nitrogen-containing compounds that may deserve particular attention; discussion of sulfur-compound emissions is reserved for the 'aerosols' section of this report. Although current jet-engine bench tests indicate that aircraft engine combustion is very efficient under many operating conditions, combustion in any engine is never "complete." Some unburned fuel is found in jet-aircraft exhaust, particularly when a fuel-rich mixture is used in the engine. Friedl (1997) notes on p. 36, "Aircraft exhaust is known to contain a large number of C2–C17 species, although the relative amounts are not well established." This means that assessments must consider the effects on ozone chemistry of unburned hydrocarbons and hydrocarbon oxidation products in the exhaust plume. Our knowledge of the hydrocarbons present in current jet fuels is reasonably good, but some important minor components remain ill-defined. JP-8 fuel, which is used in many units of the U.S. Air Force, complies with a set of specifications that are essentially identical with those of civilian aviation fuel (JA-1), except for fuel additives required by the JP-8 specification (CRC, 1984). Mayfield (1996) reports that on average the JP-8 jet fuel mixture consists of about 80.4% alkanes
OCR for page 11
--> (mostly C10 to C14), 17.9% aromatic hydrocarbons, and 0.8% alkenes. The normal (straight-chain) alkanes, n-C9H2O to n-C15H32 make up 34% of the carbon in the fuel. The properties given by Schumann et al. (1996) for European jet fuel reflect a similar composition: largely C10 to C14 alkanes and C8 to C10 alkyl-substituted benzenes and napthlenes. The atmospheric lifetime of hydrocarbons in this mass range is determined largely by reactions with OH radicals; it is relatively short for the conditions typical of the upper troposphere and lower stratosphere, but some of the initial products of oxidation of the large alkanes (e.g., the ketones) have longer lifetimes than the original alkanes. The extent of oxidation of the fuel is, among other factors, dependent on the air-to-fuel ratio used by the aircraft. To our knowledge, no analyses of trace hydrocarbon concentrations in the C10–C14 range or of their oxidation products in the air-traffic corridor have been reported. More tests for these NMHC emissions should be made in the flight corridor regions. Not only may these species serve as additional tracers for aircraft-exhaust dispersion, but they may also represent an important input into model simulations of ozone chemistry in the troposphere. These questions may be particularly relevant with respect to military aircraft, as Friedl (1997) notes that military aircraft have been calculated to account for a disproportionately large fraction (>30%) of HC and CO aircraft emissions. As suggested, further work to lower the present uncertainties in the military database is needed. This will require detailed consideration of the issues raised above and further modeling efforts devoted to the problem. An important factor in designing the atmospheric transport/chemistry models used in the NASA and European assessments (Friedl, 1997; Brasseur et al., 1997) is the degree of chemical complexity that must be included to attain a credible accuracy in atmospheric simulations. The need to use a realistic composition of hydrocarbon reactants in fuel is borne out by model-sensitivity tests, as Friedl (1997) reports on p. 82: "Removing hydrocarbon chemistry from the model reduces the sensitivity of ozone to aircraft NOx emissions appreciably (from 0.97% to 0.66% globally and annually averaged)." In view of these tests, it is surprising that Friedl concludes on p. 36, "Although the impact of NMHCs from subsonic aircraft emissions is likely to be small, no serious effort to accurately simulate these effects has been undertaken to date." More model-sensitivity studies are required to justify any conclusions about the effects on the ozone column of hydrocarbon reactions in aircraft exhaust. Similarly, one might expect that the carbon-rich aerosol observed in the plume of jet aircraft may be influenced strongly by the aromatic content of the fuel in the same fashion that aromatic hydrocarbon content of gasoline correlates with urban aerosol development (Odum et al., 1997). No published reports confirming this speculation have appeared to our knowledge. This issue should be given attention in future planning of bench tests on aircraft engine emissions. In addition to uncertainties related to hydrocarbon species, no detailed analy-
OCR for page 12
--> sis of the nitrogen-containing compounds in the current jet fuels has yet been carried out to our knowledge. Within the temperature range used for the distillation and separation of the jet aircraft fuel (~170–260°C), compounds such as alkyl-substituted pyridines (azines), pyridazenes (1,2-diazines), pyrimidines (1,3-diazines) and pyrazines (1,4-diazines) would be expected to be present, unless the jet fuel components receive some special chemical treatment to eliminate nitrogen-containing organics in the fuel preparation. The CRC Handbook of Aviation Fuel Properties (CRC, 1984) states that non-hydrocarbon compounds containing sulfur, oxygen, or nitrogen are found in low concentrations in aviation fuels. Even though the amount of nitrogen-containing species in the fuel may be small, the NOx formed from their combustion may not be a trivial contribution to total NOx emissions from the aircraft. Each nitrogen atom present in the fuel will appear as an NOx species in the exhaust, and unlike the NOx produced by the high-temperature N2-O2 combustion of air, this fuel-related NOx will probably not be altered by the combustion conditions (excess of air, fuel, temperature profile, etc.). It would be worthwhile for SASS to give more consideration to this potential source of NOx. Tropospheric Ozone Trends Current SASS studies are concerned principally with the estimation of upper-tropospheric ozone levels. An important source of upper-tropospheric ozone, however, may be the upward transport of lower-tropospheric ozone. A reasonably accurate lower-tropospheric ozone field is therefore required in models. Unfortunately, tropospheric ozone observations are not extensive today, and their interpretations differ. For instance, on p.40, Friedl (1997) states, ". . . in the lower troposphere, there are indications of ozone increases over the past 25 years in parts of northern mid-latitudes, but the increase appears to have leveled off since the mid-1980s over Europe and the United States." Yet, some of the recent studies cited by Friedl do show increasing trends, as do other observations at northern mid-latitude sites, such as those over Japan (Akimoto et al., 1994; Lee et al., 1998). In addition, Kley et al. (1994) have pointed out that in some cases the "potential ozone"([O3] + [NO2]) of an air mass, rather than [O 3] alone, may be a more appropriate indicator to use. Local emissions of NO titrate existing ozone, forming NO2, but as transport and dilution of the air mass occurs, NO2 photolysis will eventually form additional ozone. The SASS project needs to take into account the possible influence of tropospheric ozone increases in the years ahead, which would affect model results and uncertainties. Simulation of j-Values j-values describe the extent of photodissociation that occurs for any particu-
OCR for page 13
--> lar molecule as a function of the incident radiation. The accurate representation of j-values in tropospheric chemistry simulations remains a difficult problem. Brasseur et al. (1996) shows that using a diurnal cycle in j-value calculations, rather than average j-values, has a large effect (>25 %) on the calculated maximum in the NOx mixing ratio and the net ozone production rates. It thus appears to be necessary to use either the diurnal cycle or a well-calibrated algorithm to adjust the results when average j-values are used. The calculated j-values for the cloud-containing troposphere are a matter of great concern to modelers of tropospheric ozone, since the use of clear sky j-values in simulations does not reflect the reality of the often cloudy troposphere. Recently, in NASA's SONEX campaign, direct aircraft measurements of the spectral solar flux were made using well-calibrated, 360° spectroradiometers for a variety of locations within the upper troposphere, for both non-cloudy and cloudy conditions (including below-cloud, above-cloud, and in-cloud flight paths). From these measurements, realistic j-values can be calculated for the important light-absorbing molecules (e.g., O3, NO2, CH2O) for a variety of typical cloudy tropospheric conditions. The extent of cloud cover over the Earth can be estimated from suitable satellite or other databases. These data, coupled with the extensive and growing database of j-values measured for various amounts and types of clouds, should be used to develop algorithms that can estimate realistic j-values for use in the predictive modeling of the effects of aircraft emissions on the ozone column. Particle Emissions, Characterization, and Chemistry The SASS strategic plan reflects an increased recognition of the importance of aerosol-related issues, and more of its resources are now being directed toward this area. This greater emphasis reflects primarily the growing awareness of the potential influence on climate of aircraft exhaust particles, through both direct and indirect effects. PAEAN's interim review of SASS (NRC, 1997a) made a number of recommendations related to aerosols, including the following: Designate a team of researchers to examine extant datasets (U.S. and other) for the mid-troposphere, to assess the extent to which they provide a consistent picture of the aerosol and gas-phase characteristics of the free troposphere, and its regional variability. Use these datasets and other information to bound current uncertainties and sensitivities of the relationships among clouds, aerosol, and radiative effects. Evaluate and prioritize research strategies on the basis of these existing datasets and uncertainties. Increase efforts to characterize the size and properties of soot particles emitted under ambient operating conditions
OCR for page 14
--> The recent SASS and European assessment reports indicate that progress has been made in some of the above areas. However, important details still remain poorly understood. This section addresses several issues related to aerosols and contrails that require more investigation. Among them are the emission, formation, and ambient distribution of sulfate and carbon aerosols, the formation of contrails and their role in cirrus-cloud development, and the heterogeneous chemistry occurring on all of these surfaces. Sulfur Aerosols Friedl (1997) notes a major difficulty in quantitatively understanding how sulfur compounds in aircraft fuel are converted to sulfate in the aircraft engine. The sulfur content of jet-aircraft fuels varies with each fuel's specifications, but it is commonly around 200 ppm by weight or lower. As the fuel is burned in the engine, the chemically bound sulfur compounds occurring in the hydrocarbon fuel matrix form SO2, SO3, and H2SO4 and its hydrates. An experimental determination of aerosols in aircraft wakes was made in 1995, when an ER-2 aircraft was able to sample the exhaust plume of a Concorde aircraft (Fahey et al., 1995a). A huge number of aerosol particles was found in the plume with peak values ranging up to 15,000 particles/cm3 (the background concentration was approximately 6–18 particles/cm3). Heated at 192°C, a large fraction of these submicron particles was volatilized, and their composition was consistent with that of sulfuric acid. While the Concorde engine design is quite different than that of today's subsonic fleet, these studies are still relevant to SASS, as they confirmed that a large number of aerosols can be generated in the aircraft wake by the simultaneous condensation of sulfuric acid and water vapors (heteromolecular nucleation), even if the local atmosphere is under saturated with water vapor. Similar conclusions were reached by Schlager et al. (1997) when they sampled flight corridors in the troposphere and in the stratosphere, showing the similarity between supersonic and subsonic plumes with regard to aerosol formation. Several theoretical studies have been performed to predict aerosol production in aircraft wakes, including those of Miake-Lye et al. (1993, 1994), Zhao and Turco (1995), Kärcher (1995), Danilin et al. (1997), Yu and Turco (1997), and Taleb et al. (1997). The mechanism of aerosol production involves the formation of sulfuric acid in the jet regime, followed by its condensation with water vapor (heteromolecular nucleation). The rate of formation of the aerosols is generally calculated according to the "classical" theory of (binary) nucleation. When this theory is applied to aircraft wakes, nucleation rates as high as 1012/cm3 are predicted, depending on the sulfur content of the fuel. However, it has been shown that the steady-state assumption used in the classical theory is not valid (Taleb et al., 1997), and that a certain delay is needed to reach the steady state, the net effect being a reduction of the number density of the newly formed particles.
OCR for page 15
--> Other refinements to nucleation theory include the formation of hydrates in the gas phase, as well as the role of ions (Yu and Turco, 1997). So far, it seems that only binary nucleation on ions can explain the presence of "large" particles (> 9 nm) observed in the wake of the Concorde. Turco and Yu (1997) pointed out that the total number density of aerosols present in a plume, arising from the coagulation of particles and from the dispersion of the plume, can be predicted to a certain extent without knowing the detailed mechanisms of their formation. This probably applies for time scales of several minutes, but these detailed mechanisms must still be known in order to describe the interaction between soot and aerosols in the early stage of the plume. More complete data on the mode of formation and growth of the aerosols should be pursued if adequate parameterizations of the aerosols' radiative and chemical impacts are to be developed. The field observations of Fahey et al. (1995a,b) and others suggest that more than 10% of the sulfur appears in the fresh jet-exhaust plume as sulfate (presumably H2SO4 and its hydrated forms); yet modeling studies by Brown et al. (1996a), Miake-Lye et al. (1994), and Kärcher et al. (1996), which simulate the chemistry within the engine and in the plume, suggest that only 1–2% of fuel sulfur is converted to SO3 and H2SO4. This discrepancy between measurement and model may be caused in part by the difficulty of modeling the highly complex transport and combustion processes in a jet engine, or by uncertainties in the determination of the particle size distribution. The extent to which SO3 (and subsequently H2SO4) is formed should be explicable in terms of the complex kinetics of the many reactions involved, but the rate-coefficient data needed for the calculations are often not available for the temperature-pressure regimes occurring in the aircraft engines. Although this "kinetic solution" is the ultimate goal to aid our understanding of sulfur conversion, the thermodynamic properties of the sulfur gases also yield useful information. At the high temperatures occurring in the engine (~1400 K after the combustion chamber and ~600 K at the exhaust), the rates of reactions converting SO2 to SO3, and the reverse transformation of SO3 to SO 2, are fast; however, current calculations suggest that typical combustion residence times are on the order of 1–3 ms, while somewhat longer times (about 5–6 ms) may be required to establish concentrations of those species close to their equilibrium values at the particular local temperature. The fraction of SOx that appears as SO3 when equilibrium is achieved, 2SO2 + O2 ↔ 2SO3, depends on the oxygen content of the fuel-air mixture in the engine. It is difficult to know the distribution of oxygen in the gas flow in the various regions of the engine, but it is likely that during much of the transport of gases through the engine, some excess of oxygen over that required for complete oxidation of the fuel is present. If equilibrium between the sulfur oxides and oxygen is maintained over the range of temperatures approaching those found near the output of the engine exhaust—that is, the attainment of equilibrium dur-
OCR for page 16
--> ing passage through the engine is not limited by the kinetics—then the relatively large fractional conversions of SO2 to SO3 that have been observed (e.g., by Fahey et al., 1995a,b) are not unexpected. Precise knowledge of this conversion factor is desirable because it controls the aerosol formation rate and the sulfate loading of the atmosphere. Incomplete reaction-rate data, as well as factors peculiar to the engine design (the effects of engine walls on the combustion, the extent of carbonaceous aerosols present, time of flow through the various chambers in the engine, and the temperature profile of the flowing gases), complicate calculation of the changes occurring in the fuel-air mixture. Such calculations are important, however, for understanding the extent of sulfur conversion to SO3 and H2SO4 in the engine. To carry them out, it may be necessary to determine experimentally the missing rate-coefficient data for the potentially important SO2 oxidation steps. Some of the reactions that may be important in establishing the conversion of SO2 to SO3 in the jet engine are: (1) O + SO2 (+ M) → SO3 (+ M) (2) O + SO3 (+ M) → SO2 + O2 (+ M) (3) HO2 + SO2 (+ M) → OH + SO3 (+ M) (4) OH + SO2 (+ M) → HOSO2 (+ M) (5) HOSO2 + O2 → HO2 + SO3 (6) SO3 + H2O (+ H2O) → H2SO4 (+ H2O) Reaction rate coefficients for most of these reactions are poorly known and are difficult to obtain for the range of temperatures and pressures encountered in the jet engine. Yet, these data are required to derive more meaningful theoretical estimates of the extent of sulfur conversion to SO3 in the engines. Finally, it should be noted that the relative significance of this aircraft-related particle production must be assessed in terms of other natural processes that also produce high concentrations of new aerosols over extensive spatial scales. High concentrations (several thousand to tens of thousands per cm3) of recently formed nuclei, associated with cloud outflow, have been observed at altitudes of 8–10 km. Such regions have been reported to extend over hundreds of kilometers, for outflow from deep convection near the Intertropical Convergence Zone (Clarke, 1993). More recently, outflow from lower clouds in mid-latitudes has been shown to produce similarly high particle concentrations in the daytime, by photochemistry linked to high sulfuric acid production near these clouds (Clarke et al., 1998a,b). Soot Emissions The SASS interim assessment indicates that considerable progress has been made in understanding various aspects of the emission of soot particles from
OCR for page 17
--> aircraft. Soot has many characteristics that are not fully understood, however, and they may have important implications for heterogeneous chemical processes and for aerosol nucleation, growth, evolution, and role as cloud condensation nuclei (CCN). Soot can provide a surface for the conversion or deposition of sulfates, which in turn can influence the growth of the aerosol and uptake of water. It will be important to estimate the contribution of water uptake to measured (or inferred) aerosol properties, since in many cases aerosol size and composition reflect the concentration of aqueous solution and frozen droplets in equilibrium at ambient relative humidity. Thus, soot, sulfates, and water must be considered as an integral system in the assessment of aerosol effects. While measurements of tropospheric aerosol and soot are increasing, the uncertainties related to the impacts of these particles are not necessarily decreasing. The uncertainties persist in part because of the difficulty of measuring and identifying the soot component of aircraft emissions under the appropriate conditions. Some data and suggestions presented in the recent literature are inconclusive and, at times, contradictory. More data will be needed to confirm the existing observations and to determine the significance of aircraft soot emissions relative to other sources of soot. Some recent publications are discussed below to illustrate the complexity of the role soot aerosol may play and the many related uncertainties. In a 1995 paper, Blake and Kato drew several conclusions that are relevant to aircraft soot emissions: ''(i) During volcanically quiescent periods, the calculated total surface area of black carbon soot aerosol is of the same order of magnitude as that of the background sulfuric acid aerosol . . . (ii) mass balance calculations suggest that aircraft soot injected at altitude does not represent a significant source of condensation nuclei for sulfuric acid aerosols. . . . (iii) The measured latitudinal distribution of this soot (from 90°N to 45°S) at 10- to 11-km altitude is found to co-vary with commercial air traffic fuel use, suggesting that aircraft fuel combustion at altitude is the principal source. . . ." The first conclusion is justified only if the surface area of the soot is calculated on the assumption that the carbon chains are made up of 20-nm isolated spheres that are not collapsed upon themselves. This value may not accurately describe the average condition. Similarly, evidence suggests that a significant amount of the soot surface becomes coated by other species as the plume evolves; yet, the second conclusion is based on a technique that cannot detect the presence of soot inside the sulfate particle. Finally, the third conclusion is based on a very limited dataset collected over a small altitude range and does not account for the fact that the observed soot aloft also co-varies with major surface sources of continental aerosol advected from Asia at altitudes as high as 12 km over the Pacific (Menzies and Tratt, 1997). While Blake and Kato deduce from their uniformly low measurements of upper-troposphere tropical soot that biomass burning does not constitute a significant soot-aerosol source at altitude in the tropics, growing bodies of data (e.g., from PEM-Tropics) suggest that those low
OCR for page 18
--> measurements may not be adequately representative; pollution layers are often vertically stratified, and thus may not be representatively sampled if measurements are made over a narrow altitudinal range. Two interesting conclusions are drawn in a recent paper by Pueschel et al. (1997). The first is that a strong gradient in black carbon aerosol (BCA) exists between the northern and southern hemispheres, indicating mixing times longer than lower-stratospheric residence times. The second conclusion is that BCA is generally observed to 20 km altitude, so if subsonic commercial aircraft are the major source of lower-stratospheric BCA, a mechanism must exist that transports BCA from flight levels below 12 km up to 20 km. The possibility exists that a significant fraction of the soot observed near tropopause levels may arise from biomass burning, and may be quite unrelated to aviation. High concentrations of carbon aerosols (both black carbon and organic) have been observed to be convected over extensive regions of the tropics (Andreae and Crutzen, 1997). In the 1995 NASA PEM-Tropics experiment, biomass-burning plumes were observed at 8–10 km altitude over the remote South Pacific, clearly revealing that strong biomass-burning sources exist. Measurement of specific markers to help isolate and identify these "alternate" soot sources (e.g., CO/ethyne ratios, which are quite different for emissions from biomass burning and from aircraft) should be incorporated into future sampling strategies. Interpreting the limited measurements of soot currently available is difficult, especially when their sparseness is coupled with recognized sampling uncertainties (Penner and Novakov, 1996). While it is clear that aircraft do introduce soot aerosol into the free troposphere, the contribution of their emissions relative to that from other sources remains highly uncertain. Reducing this uncertainty, and putting aircraft measurements of soot in the context of this uncertainty, should remain a priority of the SASS program. Aerosol Size Distribution "Measured concentrations of volatile particles in commercial aircraft wakes are large and show significant unexplained variability." This statement, or something like it, has appeared repeatedly in various papers and documents, with particular reference to the high particle-number concentrations observed behind the Concorde by Fahey et al. (1995a,b). Many of these studies make assumptions about the aerosol mass (presumably related to carbon and sulfur emissions in the fuel) associated with the number concentration of particles observed. In most cases, some estimate of the relationship of mass to number is made, but the uncertainties in these assumptions are often poorly established and are often not properly propagated through the calculations. To its credit, the Friedl (1997) report has provided (pp. 34–35) loose bounds on this assessment that suggest a globally averaged enrichment of CCN spanning two orders of magnitude, from 0.8 to 77 cm-3; these values, however, range from insignificant to probably important. We
OCR for page 19
--> agree with that report's conclusion that more focused research is needed to reduce these uncertainties. It should be emphasized that the key to reducing these uncertainties will be careful characterization of the aerosol size distribution, from about 3 nm up to 3000 nm or larger. This precision is necessary because a few large particles can dominate aerosol mass in the presence of smaller particles, while the number of smaller particles may actually exceed the large particles in number by several orders of magnitude. For aerosol/cloud issues, it is generally the aerosol number that determines cloud droplet number and the associated radiative effects. For interpretation of specific chemical conversion rates or fuel emission scenarios, it is the aerosol mass that is important. Last, the available aerosol surface area, which is often dominated by aerosols of intermediate sizes, determines heterogeneous chemical properties that are important to a multitude of processes, including the growth and evolution of aerosols. The issue of mass and number interpretations comes up in the comparison of emission inventories for soot in the SASS assessment. On page 32 of Freidl (1997) it is argued that "in the worst case, aircraft are only responsible for <0.5% of the total global soot emissions." Even if this figure is correct on a mass basis, most emission indices for soot are obtained for combustors that generally emit larger carbon-soot particles than aircraft engines and, thus, fewer particles for a given amount of soot mass. Hence, the number of soot particles emitted by aircraft engines could be much larger than the 0.5% mentioned. Similarly, in discussion of the possible role of soot as a condensation site for sulfuric acid and its potential contribution to CCN, we are most interested in the number concentration of soot particles. Any comparisons of aircraft soot-emission indices with those of other sources can be misleading if both are mass-based when aerosol number is the concern. The interpretation of fundamental processes related to the production of aerosol from aircraft requires that the entire aerosol size spectrum be fully characterized and its dynamic evolution understood. The integral properties of the size distribution (total number, surface, volume) are of limited use and provide no opportunity to evaluate the evolution of the size distribution. Consequently, it is important that future measurements and model assessments include adequate determinations of, or realistic parameterizations of, the complete size spectrum. Need for an Aerosol Climatology At present, the effects of tropospheric aerosols are the largest uncertainties in quantifying climate forcing due to anthropogenic changes in the composition of the atmosphere. The main reason for these uncertainties is a lack of understanding of the contribution of the natural background aerosol to the total particle burden of the troposphere, which makes it difficult to evaluate the relative importance of any additions. The new SASS strategic plan calls for building an aerosol
OCR for page 20
--> climatology database. Such a database will be fundamental to putting any assessment of aviation-related aerosol radiative effects or influences on tropospheric chemistry in perspective. Providing a representative aerosol climatological database for the free troposphere will be a significant effort. It will have to build on careful assimilation of data from as many aircraft datasets as possible (NASA-GLOBE, NASA-PEM Tropics; NASA-TRACE, ACE-1, ACE-2, and others), which are large and diverse and will take time to assemble. At the same time, they will probably not provide full global and temporal coverage. In situ measurements can fail to capture the complex aerosol distribution (which often occurs as layers or 'rivers' of aerosol). Hence, whenever possible, such datasets will need to be integrated with satellite and lidar data in order to improve our understanding of the structure of aerosol fields in the troposphere. Because significant amounts of surface aerosol can at times be carried aloft into transport paths that coincide with major air corridors, the interpretation of differences in aerosol type found inside and outside of air corridors will require care. PAEAN recognizes that the establishment of a representative aerosol climatology may be beyond the scope of SASS's current mandate and resources; however, studies currently active under NASA's OES (in particular, through the Global Aerosol Climatology Project), as well as other programs outside of NASA, already include measurement efforts that can contribute directly to the needed climatology. Closer collaboration with these programs would be highly desirable. The panel also recognizes that compiling datasets from different sources is not a straightforward process. Other programs may not be measuring all the parameters that are most important to SASS's analyses, and the complicating factors raised in the previous section (such as particle mass vs. number) must be carefully considered with any aerosol datasets. Yet, it seems well worth the effort to try to meet such challenges. This collaborative approach may be the only currently available means of collecting the data necessary to fully evaluate the relative importance of aircraft particle emissions. Contrail Formation Contrails may be formed entirely from direct emission of precursor substances, or may result from the emissions of smaller particles that modify or enhance natural cirrus. Compared to natural cirrus clouds, crystals in aged contrails have a greater number density and smaller size (Gayet et al., 1996). There is a wide range of independent evidence that contrails occur both alone and in combination with natural cirrus clouds and that their spatial extent may reach synoptic scales over many regions of Earth (Sassen, 1997; Sausen et al., 1997). Contrails interact with natural cirrus to stabilize the cirrus, slowing its sedimentation and thus increasing its lifetime. Unlike acidic aerosols, which are always found in aircraft wakes, contrails
OCR for page 21
--> form only when the ambient meteorological conditions are favorable. Contrails appear when the hot water vapor emitted by the engines mixes with moist ambient air. Appleman (1953) derived a criterion for contrail formation, assuming that during the mixing process water vapor must reach saturation. This condition restricts the formation of contrails to the troposphere, although they have been observed in the stratosphere under very cold conditions. Appleman's criterion has often been used to predict threshold conditions of contrail formation; it is unable to predict their lifetime though, because it does not take into account the kinetics of particle growth or evaporation. Discrepancies have been found between observed and computed threshold conditions for contrail formation (Busen and Schumann, 1995), indicating that the details of the formation mechanisms are not fully understood. The main question is which nucleation mechanism is activated. Since the saturation ratio of water vapor is not large enough to induce homogeneous nucleation of water vapor, heterogeneous nucleation on existing particles must take place. Several pathways of contrail formation have been considered, including heterogeneous nucleation of water vapor on frozen H2SO4/H2O aerosols, on soot, and on soot coated with H2SO4. This last case can occur either by adsorption of H2SO4 from the gas phase or by coagulation of soot particles and supercooled H2SO4-H2O aerosols. In addition, observations from the SUCCESS campaign indicate that ambient aerosols, including mineral particles, may play an important role in contrail formation (Twohy and Gandrud, 1998; Jensen et al., 1998). Studies by Busen et al. (1998) indicate that fuel sulfur content (FSC) has little effect on the formation of visible contrails or on the threshold conditions for contrail formation. Further studies of contrail formation mechanisms would be worthwhile, as this uncertainty limits our ability to assess contrail chemical and radiative impacts. Heterogeneous Chemistry Participants in AEAP and the European assessment programs recognize the importance of including heterogeneous chemistry in their modeling efforts. However, implementing chemical modules that incorporate the possible reactions is difficult and introduces significant uncertainties. Only a few heterogeneous reactions, occurring on polar stratospheric cloud (PSC) particles and sulfuric-acid aerosols, have been identified and sufficiently quantified to allow inclusion in both assessment programs. Discussed below are the heterogeneous processes that may be of particular importance to subsonic aircraft impacts on atmospheric chemistry. N2O5-Aerosol Reactions The importance of including in models the reactions of N2O5 on moist aerosols [N2O5 + H2O (in aerosols) → 2HNO3] is clear from the studies of Dentener
OCR for page 22
--> and Crutzen (1993). Their tropospheric simulations, which include reaction of N2O5 with aqueous aerosols (using an uptake coefficient of 0.1), show yearly global average decreases in the concentration of tropospheric NOx of as much as 50% and of O3 by 9%. These reactions are most important during the winter months. For instance, the calculations of Dentener and Crutzen (1993) indicate that, for January in the troposphere north of 45° N, more than 90% of all NOx is removed by this heterogeneous reaction. These results are relatively insensitive to the assumed value of the uptake coefficient. All experimental measurements are in relatively good agreement on the magnitude of the uptake coefficient for aqueous sulfuric acid aerosols, and the dependence of this value on temperature and relative humidity (Fried et al., 1994). Experimental estimates of the uptake coefficient for aqueous ammonium sulfate and ammonium bisulfate aerosols, common to the lower troposphere, show some scatter, but all lie within the range 0.02–0.1 (Hu et al., 1997). Both the U.S. and European scientists recognize the importance of the N2O5 + H2O reaction, and it is included in some current global atmospheric models. Probably the biggest problem in including this reaction in models lies in estimating the magnitude of the moist aerosol surface area and its geographical distribution and seasonal variation. This again emphasizes a need for better aerosol data and a plausible aerosol climatology if these uncertainties are to be reduced. Removal of HO2 and OH Radicals in Heterogeneous Reactions Other potentially important heterogeneous reactions involve two key participants in atmospheric chemistry, the HO2 and OH radicals. Laboratory experiments show that reactions that remove each of these species on sulfuric acid, ammonium sulfate, and other aerosols have significant mass accommodation coefficients (> 0.2). Such reactions could provide a source of highly reactive species that promote solution phase reactions in aerosols or in cloud water, and they can act as a significant sink for HO2 and OH. These important chain-carrying radicals are key participants with hydrocarbons and NOx in promoting ozone generation in the troposphere (Mozurkewich et al., 1987; Hanson et al., 1992; Cooper and Abbatt, 1996). It is stated on p. 38 of Friedl (1997) that the HO2 and OH reactions have not yet been well enough characterized to be included in models of the upper troposphere. However, this lack of characterization should not exclude their use in model sensitivity tests of the effects of aircraft emissions on upper tropospheric and lower stratospheric ozone. A series of sensitivity tests should be made with current models in which these reactions are included with a range of aqueous aerosol concentrations and uptake coefficients that cover the range of experimental values. The absence of these reactions from the current assessment models should be factored into estimates of the overall uncertainties by the NASA and European assessment studies.
OCR for page 23
--> Reactions on Soot Particles O3, NO2, HNO3 and other good oxidizing agents, in theory, can react readily with black carbon aerosols. However the ozone-carbon reaction is relatively slow for upper tropospheric temperatures (Stephens et al., 1989), and the oxidation of the surface layer strongly inhibits subsequent reaction. Lary et al. (1997) point out that the reduction of HNO3, NO2, and O3 on carbon aerosols may be an important effect of increased air traffic that has not been considered to date. If these are important, then a significant lower stratospheric ozone loss mechanism could exist. The amount of carbon aerosol emitted by aircraft engines has been estimated experimentally, but it is currently not known what fraction of the aerosol is quickly coated by H2SO4 or other adsorbed material, which would lower the available free-carbon surface area of the aerosols. Kärcher (1997) has considered the possible role of aircraft exhaust soot in promoting heterogeneous reactions (involving HNO2, SO2, and NO2) in aircraft plumes. He suggests that rapid heterogeneous reaction of exhaust NO2 with soot might explain why the observed NO2 values in the Concorde plume were a factor of 2 lower than indicated by a photochemical steady-state approximation, and considers it likely that soot particles absorb oxidized sulfur gases at emission and collect volatile H2SO4/H2O in the plume. If the aerosol is covered with sulfuric acid or other material that can absorb water from the air, the resulting aqueous solution can promote reactions at the solid-liquid interface. Active sites can be regenerated if the reaction product is soluble in water and leaves the aerosol surface. As mentioned earlier, it is not yet clear whether the abundance of carbon aerosols in the upper troposphere and lower stratosphere is significantly increased by aircraft exhaust emissions. If this is indeed the case, it is important to determine experimentally the possible extent of alteration of the ozone column due to heterogeneous reactions involving those aerosols (whether coated with H2SO4 or uncoated). Reactions Between Halogenated Species on Cirrus Clouds Raman lidar measurements of ozone, water vapor, and cirrus cloud optical properties over northern Germany (Reichardt et al., 1996) showed decreased ozone levels in the upper troposphere in the presence of ice-cloud layers. Borrmann et al. (1997) observed elevated ClO levels in and near cirrus clouds near the tropopause; they suggested that heterogeneous chemistry might be generating active chlorine species, ClO and Cl, from relatively inactive ClONO2 and HCl (and also HOCl with HCl). Similar reactions have been observed in the arctic "ozone hole" (HCl + ClONO2 → Cl2 + HNO3). Upon dissociation by sunlight, Cl2 can initiate the catalytic cycles that destroy O3 From their modeling studies, Solomon et al. (1997) conclude that cirrus clouds, occurring with sufficient frequency and spatial extent, could influence
OCR for page 24
--> chemical composition and ozone depletion in the region near the tropopause. While the presence of cirrus clouds near the tropopause plays only a small role in determining the total ozone column trends (less than 1.5% change in computed column ozone at mid-latitudes in these calculations of Solomon et al.), they are of particular importance in determining the changes in ozone at the tropopause and hence the radiative forcing. Solomon et al. note that emissions from aircraft (contrails and chemical effluents) could influence cirrus cloud distributions and frequency. Clearly, if there were to be variability or trends in the frequency of occurrence of cirrus clouds or in their distribution, this could add substantially to their impact on the ozone layer. As our knowledge of the influence of aircraft emissions on contrail formation and the possible enhancement of cirrus cloud formation improves, the resulting effects on the ozone column should be tested in the modeling studies. Atmospheric Dynamical Processes Atmospheric dynamics, operating over a vast range of spatial scales, includes many process that must be understood in order to properly assess the impacts of aircraft exhaust. In particular, since aircraft emissions are deposited primarily in the upper troposphere and lower stratosphere, cross-tropopause transport processes may significantly affect aviation's impacts in both regions. Stratosphere-troposphere exchange directly affects the distribution of aircraft emissions and indirectly affects the chemical impact of these emissions by influencing the composition of the background atmosphere. At low latitudes, gas and particulates are convectively transported from the troposphere upward to the stratosphere. Downward transport occurs at higher latitudes through tropopause folding, and isentropic transport occurs through sub-tropical tropopause breaks. There are indications of distinct hemispheric asymmetries and seasonal variations in these cross-tropopause processes. In the last few years, our understanding of the large-scale transport processes has improved significantly. These developments are discussed in detail in Holton et al. (1995), as well as in the panel's recent interim review of AESA (NRC, 1998). However, the smaller-scale details of cross-tropopause transport are still not well enough known to permit appropriate representation in models. Additional balloon and/or aircraft campaigns designed to probe the tropical and subtropical tropopause regions, and measurements of a variety of long-lived tracers in these regions may provide the data needed to help understand these transport processes. This issue needs to be an important focus of AEAP analyses, but little mention is made of it in the SASS strategic plan. The issue is relevant to both the subsonic and the supersonic components of AEAP; thus it is important that SASS and AESA sort out this common concern with whatever type of collaboration will be most effective.
OCR for page 25
--> Climate Impacts Gases and particles emitted by jet aircraft can affect climate in numerous ways, through both direct and indirect radiative forcing. Some of the most uncertain and potentially important of these processes are discussed below. Discussion of climate modeling is reserved for the following chapter. Effects of Radiatively Active Gases As discussed in the NASA assessment (Friedl, 1997), it may turn out to be very difficult to quantify the climatic effects of directly emitted combustion gases (such as CO2 and water vapor) through observational studies; however, provided the magnitude of the emissions can be reliably predicted, there is some hope that their effects can be estimated with reasonable accuracy through model computations. A more indirect and uncertain problem is that some combustion gases such as NOx can change ozone chemistry in the upper troposphere/lower stratosphere region, which in turn can have significant climatic impacts. Estimating the magnitude of these impacts requires keeping at least three factors in mind: (i) ozone loss in the upper troposphere/lower stratosphere region may be linked to heterogeneous chemistry on cirrus cloud particles (Borrman et al., 1997); (ii) although the ozone changes in this region may have a minor influence on the total ozone column, such changes may be quite important to radiative forcing of the climate system (Solomon et al., 1997); and (iii) there are possible feedbacks through ozone loss/temperature decrease/cirrus formation to consider. Understanding the ozone changes in this altitude range will be critical to assessing climate forcing and response; however, modeling or observing such perturbations in the region around the tropopause is very difficult because large variations occur in both transport patterns and concentrations of key species. Effects of Particles and Contrails The direct radiative forcing caused by jet aircraft soot and sulfur emissions is thought to be relatively insignificant. However, contrails and injected aerosols can modify the abundance and microphysical properties of cirrus clouds, which in turn can have significant climatic impacts. Yet, these cloud-related effects are very difficult to quantify because of the large uncertainties about ice-crystal formation mechanisms and physical properties. To model the radiative effects of contrails and injected aerosols, one needs to know particle shape, size distribution, and refractive index. During the recent SUCCESS campaign, a great deal was learned about ice crystal size and shape characteristics (for example, see Lawson et al., 1998; Goodman et al., 1998; Liou et al., 1998; Sassen and Hsueh, 1998), and about the role of ice nuclei in cirrus ice formation (Chen et al., 1998;
OCR for page 26
--> Rogers et al., 1998, De Mott et al., 1998). Yet, even if these physical properties were fully characterized, it is quite difficult to compute the optical properties of such varied particles. The growth of contrails into extensive, diffuse "contrail-cirrus" was clearly documented by geostationary satellite observations during the SUCCESS mission (Minnis et al., 1998). Many earlier investigators had noted this link between aircraft activity and enhanced cirrus-cloud coverage (for example, Machta and Carpenter, 1971; Chagnon, 1981. It has been suggested that contrails are responsible for a 2% increase of cloudiness above the United States between the years 1950 and 1988 (Angell, 1990); similar findings were also reported by Liou et al. (1991) above Salt Lake City, and by Bakan et al. (1994) over Europe. Since the physical properties of contrails appears to be quite different from naturally occurring cirrus clouds, the mechanisms that link contrails to climate may be very different from those operating in the natural, unperturbed system. The balance between the albedo and greenhouse effects of contrails determines the net radiative forcing, and this may be a function of a wide range of environmental factors. The uncertainty in the net forcing is substantial and may be of opposite sign in different atmospheric regimes. The chemistry and physics underlying this complex issue are discussed in many of the SUCCESS papers cited above as well as several other recent articles (see, e.g., Andronache and Chameides, 1997; Baker, 1997; Sassen, 1997; Szyrmer and Zawadzki, 1997; Travis et al., 1997). Although the current understanding of direct and indirect effects of aircraft particle injections is discussed at some length in the NASA report, a cohesive and well-articulated plan for how to proceed is generally lacking. In view of the complexity of the problem, this is perhaps not surprising. Some effort should be directed toward exploiting the possibility of using new remote-sensing capabilities to study these aerosol/cloud/contrail issues; any such studies should be validated through comparison to in situ measurements whenever possible. In the near term however, given the complexity of the problem and the limited resources available through the SASS program, back-of-the-envelope calculations may have to provide the guidance for how to proceed. These should be used to put plausible bounds on potential effects and to point to areas of sensitivity. In conjunction with emerging data from SUCCESS and other recent large programs (ACE-1, PEM, etc.) efforts should be made to gauge aircraft perturbations against other major natural and anthropogenic inputs (biomass burning, urban pollution) that can impact tropospheric aerosol size, concentration, composition, and cloud nucleating capability. An understanding of both absolute and relative effects caused by aerosol emissions from aircraft will need to be developed further.
Representative terms from entire chapter: