3. Aerosols and Radiation
3.1.
Aerosol Monitoring
E. Andrews (Editor), D. Delene,
D. Jackson, A. Jefferson, J. Ogren, P. Sheridan, and
J. Wendell
3.1.1.
Scientific Background
Aerosol
particles affect the radiative balance of Earth both
directly, by scattering and absorbing solar and terrestrial radiation, and
indirectly, through their action as cloud condensation nuclei (CCN) with
subsequent effects on the microphysical and optical properties of clouds. Evaluation of the climate forcing by aerosols,
defined here as the perturbation of the Earth's radiation budget induced by the
presence of airborne particles, requires knowledge of the spatial distribution
of the particles, their optical and cloud-nucleating properties, and suitable
models of radiative transfer and cloud physics. Obtaining a predictive relationship between
the aerosol forcing and the physical and chemical sources of the particles
additionally requires knowledge of regional and global-scale chemical
processes, physical transformation, and transport models for calculating the
spatial distributions of the major chemical species that control the optical
and cloud-nucleating properties of the particles. Developing and validating these various models
requires a diverse suite of in situ and remote observations of the aerosol
particles on a wide range of spatial and temporal scales.
Aerosol
measurements began at the CMDL baseline observatories in the mid-1970s as part
of the Geophysical Monitoring for Climatic Change (GMCC) program. The objective of these "baseline"
measurements was to detect a response, or lack of response, of atmospheric
aerosols to changing conditions on a global scale. Since the inception of the program,
scientific understanding of the behavior of atmospheric aerosols has improved
considerably. One lesson learned is that
residence times of tropospheric aerosols are generally less than 1 week, and
that human activities primarily influence aerosols on regional/continental
scales rather than global scales. In
response to this increased understanding, and to more recent findings that
anthropogenic aerosols create a significant perturbation in the Earth's radiative balance on regional scales [Charlson
et al., 1992; National Research Council, 1996], CMDL expanded its
aerosol research program to include regional aerosol monitoring stations. The goals of this regional-scale monitoring
program are: (1) to characterize means, variabilities,
and trends of climate-forcing properties of different types of aerosols, and
(2) to understand the factors that control these properties.
No single approach to observing the atmospheric aerosol can provide the necessary data for monitoring all the relevant dimensions and spatial/temporal scales required to evaluate climate forcing by anthropogenic aerosols. In situ observations from fixed surface sites, ships, balloons, and aircraft can provide very detailed characterizations of the atmospheric aerosol but on limited spatial scales. Remote sensing methods from satellites, aircraft, or from the surface can determine a limited set of aerosol properties from local to global spatial scales, but they cannot provide the chemical information needed for linkage with global chemical models. Fixed ground stations are suitable for continuous observations over extended time periods but lack vertical resolution. Aircraft and balloons can provide the vertical dimension, but not continuously. Only when systematically combined can these various types of observations produce a data set where point measurements can be extrapolated with models to large geographical scales where satellite measurements can be compared to the results of large-scale models, and where process studies have a context for drawing general conclusions from experiments conducted under specific conditions.
Measurements of atmospheric aerosols are used in three fundamentally different ways for aerosol/climate research: algorithm development for models and remote-sensing retrievals, parameter characterization, and model validation. Laboratory and field process studies guide the development of parameterization schemes and the choice of parameter values for chemical transport models that describe the relationship between emissions and concentration fields of aerosol species. Systematic surveys and monitoring programs provide characteristic values of aerosol properties that are used in radiative transfer models for calculating the radiative effects of the aerosols, and for retrieving aerosol properties from satellites and other remote sensing platforms. And finally, monitoring programs provide spatial and temporal distributions of aerosol properties that are compared to model results to validate the models. Each of these three modes of interaction between applications and measurements requires different types of data and entails different measurement strategies. Ogren [1995] applied the thermodynamic concept of “intensive” and “extensive” properties of a system to emphasize the relationship between measurement approach and applications of aerosol observations.
Intensive
properties do not depend on the amount of aerosol present and are used as
parameters in chemical transport and radiative
transfer models (e.g., atmospheric residence time, single-scattering
albedo). Extensive properties vary
strongly in response to mixing and removal processes and are most commonly used
for model validation (e.g., mass concentration, optical depth). Intensive properties are more difficult and
expensive to measure than extensive properties because they generally are
defined as the ratio of two extensive properties. As a result, different measurement strategies
are needed for meeting the data needs of the various applications. Measurements of a few carefully chosen
extensive properties, of which aerosol optical depth and species mass
concentrations are prime candidates, are needed in many locations to test the
ability of the models to predict spatial and temporal variations on regional to
global scales and to detect changes in aerosol concentrations resulting from
changes in aerosol sources. The higher
cost of determining intensive properties suggests a strategy of using a limited
number of highly instrumented sites to characterize means and variabilities of intensive properties for different regions
or aerosol types, supplemented with surveys by aircraft and ships to
characterize the spatial variability of these parameters. CMDL's regional aerosol monitoring program is
primarily focused on characterizing intensive properties.
CMDL's measurements provide ground truth for satellite observations and global models, as well as key aerosol parameters for global-scale models (e.g., scattering efficiency of sulfate particles and hemispheric backscattering fraction). An important aspect of this strategy is that the chemical measurements are linked to the physical measurements through simultaneous, size-selective sampling that allows the observed aerosol properties to be connected to the atmospheric cycles of specific chemical species [e.g., Quinn et al., 2001].
3.1.2. Experimental Methods
Extensive aerosol properties monitored by CMDL include condensation nucleus (CN) concentration, aerosol optical depth (d), and components of the aerosol extinction coefficient at one or more wavelengths (total scattering (ssp), backwards hemispheric scattering (sbsp), and absorption (sap)). At the regional sites, size-resolved impactor and filter samples (submicrometer and supermicrometer size fractions) are obtained for gravimetric and chemical (ion chromatograph) analyses. All size-selective sampling, as well as the measurements of the components of the aerosol extinction coefficient at the regional stations, is performed at a low, controlled relative humidity (<40%) to eliminate confounding effects due to changes in ambient relative humidity. Data from the continuous sensors are screened to eliminate contamination from local pollution sources. At the regional stations the screening algorithms use measured wind speed, direction, and total particle number concentration in real-time to prevent contamination of the chemical samples. Algorithms for the baseline stations use measured wind speed and direction to exclude data that are likely to have been locally contaminated.
Prior to 1995, data from the baseline stations were manually edited to remove spikes from local contamination. Since 1995 an automatic editing algorithm has been applied to the baseline data in addition to manual editing of local contamination spikes. For the baseline stations (Barrow, Alaska (BRW), Mauna Loa, Hawaii (MLO), American Samoa (SMO), and South Pole, Antarctica (SPO), as well as Sable Island (WSA)), data are automatically removed when the wind direction is from local sources of pollution (such as generators and buildings) as well as when the wind speed is less than a threshold value (0.5-1 m s-1). In addition, at MLO data for upslope conditions (1800-1000 UTC) are excluded since the airmasses do not represent “background” free tropospheric air for this case. A summary of the data-editing criteria for each station is presented in Table 3.1.
Integrating nephelometers are used to determine the light scattering coefficient of the aerosol. These instruments operate by illuminating a fixed sample volume from the side and observing the amount of light that is scattered by particles and gas molecules in the direction of a photomultiplier tube. The instrument integrates over scattering angles of 7-170°. Depending on the station, measurements are performed at three or four wavelengths in the visible and near-infrared. Newer instruments allow determination of the hemispheric backscattering coefficient by using a shutter to prevent illumination of the portion of the instrument that yields scattering angles less than 90°. A particle filter is inserted periodically into the sample stream to measure the light scattered by gas molecules, which is subtracted from the total scattered signal to determine the contribution from the particles alone. The instruments are calibrated by filling the sample volume with CO2 gas, which has a known scattering coefficient.
The
aerosol light absorption coefficient is determined with a continuous light
absorption photometer. This instrument
continuously measures the amount of light transmitted through a quartz filter
while particles are being deposited on the filter. The rate of decrease of transmissivity,
divided by the sample flow rate, is directly proportional to the light
absorption coefficient of the particles.
Newer instruments (Particle Soot
Absorption Photometers (PSAP), Radiance Research,
Particle number concentration is determined with a CN counter that exposes the particles to a high supersaturation of butanol vapor. This causes the particles to grow to a size where they can be optically detected and counted. The instruments in use have lower particle-size detection limits of 10-20 nm diameter.
Summaries of the extensive measurements obtained at each site are given in Tables 3.2 and 3.3. Table 3.4 lists the intensive aerosol properties that can be determined from the directly measured extensive properties. These properties are used in chemical transport models to determine the radiative effects of the aerosol concentrations calculated by the models. Inversely, these properties are used in algorithms for interpreting satellite remote-sensing data to determine aerosol amounts based on measurements of the radiative effects of the aerosol.
3.1.3. Annual Cycles
The annual cycles of aerosol optical properties for the four baseline and three regional stations are illustrated in Figures 3.1 and 3.2, respectively. The data are presented in the form of box and whisker plots that summarize the distribution of values. Each box ranges from the lower to upper quartiles with a central bar at the median value, while the whiskers extend to the 5th and 95th percentiles. The statistics are based on hourly averages of each parameter for each month of the year; also shown are the annual statistics for the entire period of record. The horizontal line represents the annual median, so measurements above and below the median can easily be discerned. The annual cycles for the baseline stations are based on data through the end of 2001 except at SMO where scattering measurements were only made from 1977 – 1991.
In
general, changes in long-range transport patterns dominate the annual cycles of
the baseline stations. For BRW, the high
values of CN, ssp, and sap are observed
during the arctic haze period when anti-cyclonic activity transports pollution
from the lower latitudes of
For
MLO, the highest ssp and sap
values occur in the springtime and result from the long-range transport of
pollution and mineral dust from
Based
on only 4-7 years of measurements, the annual cycles for the regional stations
are less certain than those of the baseline stations. The proximity of the regional sites to North
American pollution sources is apparent in the results, with monthly median
values of ssp
that are up to two orders of magnitude higher than values from the baseline
stations. The Bondville site (BND),
situated in a rural agricultural region, displays an autumn high in sap
and a low in wo
that coincide with anthropogenic and dust aerosols emitted during the harvest [Delene and Ogren,
2001]. As evident in the lower ssp
and sap
values, the
3.1.4. Long-term Trends
Long-term trends in CN concentration, ssp,
sap, wo, and å are plotted in Figures 3.3 and 3.4 for the baseline
observatories. The monthly means are
plotted along with a linear trend line fitted to the data. The aerosol properties at BRW exhibit an
annual decrease in ssp of about 2% per year since 1980. This reduction in aerosol scattering has been
attributed to decreased anthropogenic emissions from
In contrast to the reduction in ssp at BRW, CN concentrations, which are most sensitive to particles with diameters <0.1 mm, have increased since 1976. There is an offset in CN concentration starting in 1998 that corresponds to a change to a new CN sampling inlet. Similarly the step increases in CN concentration in late 1991 at MLO and 1989 at SPO are due to replacement of the CN counter with a butanol-based instrument with a lower size detection limit. The reason for the decrease in CN and increase in å at SMO is not readily apparent, but it could stem from changes in long-term circulation patterns.
Previous reports describing the aerosol data sets include: BRW: Bodhaine [1989, 1995]; Quakenbush and Bodhaine [1986]; Bodhaine and Dutton [1993]; Barrie [1996]; Delene and Ogren [2001]; MLO: Bodhaine [1995]; Delene and Ogren [2001]; SGP: Delene and Ogren [2001]; Sheridan et al. [2001]; Bergin et al. [2000]; SMO: Bodhaine and DeLuisi [1985]; SPO: Bodhaine et al. [1986, 1987, 1992]; Bergin et al. [1998]; WSA: McInnes et al. [1998]; Delene and Ogren [2001].
3.1.5. Special Studies
NOAA’s Climate Monitoring and Diagnostics Lab (CMDL) has
measured both aerosol light scattering (since 1974) and aerosol light absorption
(since 1990) at Mauna Loa (MLO). In Spring 2000 new light scattering and
absorption instruments were installed at
It is important to assess how measurements from these instruments compare in order to maintain data consistency for the entire measurement period. The MLO and MLN systems were operated simultaneously for approximately 1 year (Spring 2000 – Spring 2001). One year of simultaneous light scattering and three months of light absorption (the aethalometer broke in August 2000) measurements from the co-located instruments are compared.
The comparison procedure was:
Figure 3.5 shows that, on an hourly basis, there is excellent correlation between the nephelometer measurements (R2=0.94), and the instruments agree fairly well – the slope is 1.1. This agreement is also seen when the data are separated for upslope (polluted) and downslope (cleaner) conditions. Because the two instruments appear to be in good agreement, the old nephelometer was removed during annual maintenance in May 2001.
The
comparison between the PSAP and the aethalometer (Figure 3.6) was over a much
shorter time period: May 2000 - early August 2000. In early August the aethalometer feed
sprocket was replaced, and after the replacement, measurements from the two
instruments became completely uncorrelated (R2=0.02). Prior to the feed sprocket replacement, the
absorption measurements show that the PSAP measured absorption coefficients ~3x
higher than the aethalometer although the instruments were fairly well
correlated. (R2~0.6). The difference between the two instruments
suggests that the assumed BC absorption efficiency of 10 m2 g-1 may not be
appropriate for
Carbonaceous particles in the atmosphere are generally thought to contain up to two major classes of carbon; these are organic carbon (OC) and black carbon (BC, also called elemental carbon, EC). Visible light absorption by atmospheric aerosols is typically dominated by particles containing BC. The mass measurement of BC in atmospheric aerosol samples has most often been performed by thermal evolved gas analysis [e.g., Cachier et al., 1989] or thermal optical reflectance (TOR) methods [e.g., Chow et al., 1993]. The light absorption coefficient (sap) of aerosol samples has been determined using optical (usually filter-based) instruments, such as the aethalometer [e.g., Bodhaine, 1995], the Particle Soot Absorption Photometer (PSAP) [e.g., Bond et al., 1999], or photoacoustic techniques [e.g., Arnott et al., 1999]. All of these measurement techniques depend directly on the amount of aerosol sampled for the analysis, and all have associated measurement uncertainties, artifacts, interferences, and other problems that must be taken into account.
A measure of the efficiency with which atmospheric aerosols absorb visible radiation is desirable for model inputs and other applications. The aerosol light absorption efficiency, a, is defined as:
a = sap / mC (1)
where sap is measured in Mm-1, and mC is the mass concentration of absorbing carbon in mg m-3. The parameter a has also been called the specific attenuation cross-section, the specific absorption coefficient, and the BC mass absorption coefficient in previous studies. Over the past two decades, reported values of a have ranged from ~1 to 25 m2 g-1. Most of the variability in a has been attributed to differences in aerosol composition, shape, size, mixing state (i.e., internal vs. external), and amount of scattering material present. The challenge for researchers is to determine what portion of the variability in a is caused by instrument uncertainty or differences in measurement methods and what portion is due to real differences in the studied aerosols.
In this study we report on a new method of determining the a of graphitic carbon (GC), a specific and dominant component of BC. We have used the PSAP instrument to obtain the sap of aerosol samples collected during the Indian Ocean Experiment (INDOEX) in early 1999. The PSAP is a filter-based instrument in which aerosol particles are continuously deposited onto a filter. A transmittance measurement is made through the particle deposit and simultaneously compared with an identical measurement through a second, particle-free filter. Through careful calibration of the raw transmittance signals against derived absorption from an extinction cell – nephelometer system [Bond et al., 1999], a measurement of suspended-state aerosol absorption is obtained.
For the analysis of GC mass, we collaborated with colleagues at the Institute for Tropospheric Research (IFT) in Leipzig, Germany. The Raman instrument used in this study to quantify GC mass was a Bruker IFS 55 spectrometer equipped with a FRA-106 Raman module in a backscatter configuration. Calibration of the Raman spectrometer for GC mass on the PSAP filters was performed as documented in Mertes et al. [2001] with a commercially available carbon black standard (Monarch 71, Cabot Corporation, Boston, Massachusetts). The atmospheric concentration of GC can then be calculated from the GC filter mass by using the volume of air sampled through the PSAP filters.
Our investigation has two advantages over previous studies. First, the GC responsible for light absorption and not the thermographic EC is used. Thus, a quantifiable, dominant component of light absorbing carbon is obtained. Second, the correlation between sap and mC is analyzed from identical aerosol samples (i.e., the same particles), so any variability between samples does not come from examining different populations of particles in the two analyses.
The
INDOEX Intensive Field Phase (IFP) was conducted during February and March
1999. The site for our measurements was
the Kaashidhoo Climate Observatory (KCO), on the
island of Kaashidhoo in the Republic of
Maldives. During this period of the
winter monsoon, dry winds from the northeast sweep over the area. These winds bring very polluted air from
Figure
3.7 shows a time series of sap
plotted alongside GC concentration.
Overall, there was good agreement between the two parameters over the
course of the IFP. The initial portion
of the experiment (through DOY 70) was a period of higher aerosol
concentrations at KCO punctuated by two rainfall events that removed aerosols
from the atmosphere. From DOY 71 through
nearly the end of the IFP, light absorption coefficients were relatively lower,
but still several times larger than at typical rural, midcontinental
sites in the
Figure 3.8 shows sap plotted against GC. In this analysis, we have grouped the PSAP filters according to their filter loading and have removed one obvious outlier from the “Medium Loading” category. The PSAP manufacturer’s manual states that absorption measurements should be reliable as long as the filter transmittance (Tr, or I/I0) remains above 0.5. The calibrations recommended by Bond et al. [1999], however, were performed using PSAPs with Tr values maintained above 0.7, so this grouping of lightly loaded filters is the only one in which the Bond et al. [1999] PSAP calibration corrections can be applied reliably. The slope of the linear least squares regression line through the lightly loaded filters equates to an a of 9.7 m2 g-1, with a very small offset and an R2 value of 0.86. The filters with higher GC loadings show regression slopes between roughly 9.0 and 10.4, but with significant y-intercepts. These zero offsets may be due to uncertainties in the nonlinear filter loading corrections used in the PSAP instrument. While GC currently is thought to be the major aerosol absorber of visible radiation, other forms of carbonaceous material (e.g., amorphous C, organic C) need to be studied in a similar manner to quantify their contributions to visible light absorption by aerosols.
In Situ Aerosol Profile
Measurements over the Southern Great Plains CART Site
The objective of this project is to obtain a statistically significant data set of in-situ measurements of the vertical distribution of aerosol properties (e.g., light scattering and absorption). The measurements will be used to answer the following scientific questions:
The data are obtained by flying an
instrumented light aircraft (Cessna C-172N) over the Southern Great Plains
(SGP) site in
There
is good agreement (R2 = 0.82) between lowest level leg and surface extinction
(sext = sap + ssp) values, indicating submicrometer
aerosol (predominantly scattering aerosol) in the 150 m above the surface is
well-mixed. Much of the variability in
the parameters measured at the surface site appears to be captured by the
weekly profiling flights. The comparison is not as good (R2 = 0.49) for
single-scattering albedo, which is due to measured differences in absorption
between the surface and the lowest flight level. These observed differences
appear to be real because side-by-side tests of the two particle soot
absorption photometers show good agreement (within 8%). Comparison of other derived properties
at the lowest flight level with surface properties are excellent for
backscatter fraction and green-blue Ångström
exponent, but less so for the green-red Ångström
exponent.
Figure 3.9 shows the medians and ranges (as indicated by percentiles) of a representative extensive aerosol optical property (extinction) and a representative intensive aerosol optical property (single-scattering albedo) at STP, low RH, and Dp < 1 mm, obtained at the surface and during vertical profiling flights. The line in the center of the box represents the median, while the edges of the box give the 25th and 75th percentiles, and the whiskers extend to the 5th and 95th percentiles. The values for extensive properties (extinction, absorption, and scattering coefficients) vary by up to a factor of 3, while the medians for intensive aerosol properties (single scattering albedo, backscatter fraction, Ångström exponent) are much less variable (less than 10% variation). Figure 3.9 suggests that the median values of the extensive properties tend to decrease with altitude from the surface upward. Such behavior is expected as distance from the ground-based sources of aerosol particles increases. The median values of the intensive properties do not display a strong dependence with altitude.
More indicative of the overall variability of the aerosol are the ranges of the parameters as indicated by the percentiles in Figure 3.9. Extensive properties can differ by up to two orders of magnitude between flights and even between individual levels of the same flight. The intensive properties, while still displaying a range of values, vary at most by an order of magnitude (i.e., green-red Ångström exponent, level 3660 m) but more commonly by less than a factor of two. The parameter ranges display different tendencies with height. Extensive properties become less variable at higher altitudes, due to consistently low concentrations of aerosol particles. Conversely, intensive properties become more variable with altitude for a similar reason: low concentrations of aerosol particles result in more noise when calculating the values of these parameters.
The surface measurements are representative of the frequency distributions aloft, particularly for intensive properties such as albedo (Figure 3.9). However, the correlations between column average and surface values (not shown) are lower (e.g., extinction R2 = 0.65; albedo R2 = 0.30) than correlations between lowest flight level and surface values. Thus, while surface aerosol measurements are statistically representative of the air aloft, they may not be representative of day-to-day variations in the column.
Measurements from the profile flights can also be compared with measurements by remote sensing instruments located at SGP (i.e., the Cimel sun/sky radiometer and the multi-filter rotating shadowband radiometer (MFRSR)). After incorporating corrections for supermicrometer, upper tropospheric, and stratospheric aerosol particles, comparison of aerosol optical depth (AOD) (Figure 3.10) calculated from aircraft measurements with AOD obtained from the remote sensing instruments shows fair correlation (R2 ~ 0.5 Cimel, R2 ~ 0.8 MFRSR), although the aircraft AODs are lower than those derived from the radiation instruments, with an offset in the range of -0.03 or -0.04.
Long-term surface measurements can represent statistical distribution of aerosol properties aloft. However, day-to-day variability between the surface and aloft may not always be captured and causes a poor relationship between surface and column average quantities. Comparison of the in-situ and remote sensing instruments shows fair correlation for AOD although the aircraft AOD is consistently lower than that of the remote sensing instruments.
Measurements of Aerosol Optical
Properties From a Surface Site in
An
intensive field campaign known as the Aerosol Characterization Experiment
(ACE-Asia) took place in April 2001 in eastern
This
large field study was a multi-platform, international effort with scientific
measurements being recorded from land-based sites, ships, aircraft, and
satellites. Scientists from
As part of this effort, CMDL conducted in situ measurements of the aerosol optical properties as well as full column measurements of the solar radiation at Kosan, South Korea. The ground-based measurements included aerosol scattering coefficient as a function of particle size, wavelength, and relative humidity and the aerosol absorption coefficient as a function of size. These observations provide a direct measure of the surface aerosol extinction of visible radiation. For full column measurements of the atmosphere, radiometers from CMDL measured the total, direct, and diffuse (scattered light by aerosol) solar radiation. These observations can be used to derive the AOD or amount of solar radiation attenuated by aerosols and the aerosol forcing efficiency.
The aerosol scattering coefficient was highly variable during the campaign, ranging between 20 and 250 Mm-1. Spring in Korea is known as the dust season when southeasterly winds bring dust to the region from the Gobi Desert. Several such events (note particularly DOY 101-104 and DOY 110) are apparent from the data (Figure 3.11). On these days over 60% of the aerosol scattering was in the total size mode as indicated by the low values of the ratio of the submicrometer to total aerosol scattering coefficients (Figure 3.11c). The aerosol single- scattering albedo during the dust events declined slightly to ~0.80 for total aerosol and as low as 0.63 for submicrometer aerosol. Most of the aerosol absorption during the campaign was in the submicrometer particles. The aerosol hygroscopic growth factor (f(RH)= ssp(RH=85)/ssp(RH=40)), a measure of the increase in scattering due to aerosol water uptake, was relatively high during the dust events, ranging from 1.5 to 2.5. The low single-scattering albedo and high hygroscopic growth factor indicate the aerosol at the site was composed of not only dust but also likely had absorbing elemental and hygroscopic species such as sulfate, oxidized organics, and sea salt.
Mean
aerosol optical properties from Kosan as well as from two other anthropogenically-perturbed sites are given in Table 3.6.
Although all three sites receive anthropogenic aerosol, there are significant
differences in the aerosol optical properties between the sites, demonstrating
the importance of long term, regional measurements at a variety of locations. Kosan, South Korea, and Kaashidhoo,
Republic of Maldives are anthropogenically perturbed marine sites, and
Bondville, Illinois, is an anthropogenically perturbed continental site. The
aerosol scattering coefficient from Kosan is higher than either the Kaashidhoo or the Bondville site, indicating a high aerosol
loading in eastern Asia during the spring.
Kosan and Kaashidhoo have higher light
absorption coefficients than Bondville, consistent with a larger contribution
of combustion aerosol (e.g., from biomass burning or limited pollution control
on vehicles and industries). In keeping
with the higher absorption coefficients at Kosan and Kaashidhoo,
those sites have lower single-scattering albedo
values than Bondville, with Kaashidhoo
being significantly lower than Kosan.
The f(RH) value at Kosan was significantly higher than at Kaashidhoo or Bondville.
The f(RH) at Kosan did not correlate well with sea salt aerosol, but was
likely high due to extensive mixing with polluted air masses containing sulfates
and nitrates from both
The sunphotometers give a measure of the direct solar
irradiance in seven narrow band wavelength channels. Preliminary data from these instruments
(screened for clouds) give a measure of the AOD. On days with the highest
pollution, the AOD for 500-nm radiation was as high as 0.7, and on days with
clean marine air the value dropped to a low of 0.1. During the major dust event on DOYs 101 to 104 the AOD was 0.45 to 0.7, indicating
relatively low sunlight levels from a heavy loading of aerosol. Figure 3.12 shows both the AOD at 500 nm and
the aerosol Ångström exponent, a measure of the
aerosol size, for a 3-month period from March 31 to
Systematic Variation of Aerosol
Optical Properties
Aerosol optical properties measured over several years at BND, SGP, WSA, and BRW have been analyzed to determine the importance of the variability in aerosol optical properties to direct aerosol radiative forcing calculations and to investigate whether systematic relationships exist between various aerosol optical properties (sap, wo, b, å, and aerosol radiative forcing (DF/d)) and the amount of aerosol present (measured by ssp). Systematic relationships among aerosol properties can be used to check for consistency among measured and modeled climatologies. Also, systematic relationships can be used in model parameterization to reduce uncertainties resulting from insufficient knowledge of aerosol properties. The performance of different models can be evaluated with measurements, and if models predict the parameters that are observed, the measurements can be used to validate the models.
Knowledge concerning systematic relationships among aerosol properties can be useful in reducing uncertainties in remotely sensed data because they can be used to make better assumptions about unknown aerosol properties. Remer and Kaufman [1998] illustrated the importance of using a dynamic model where aerosol properties vary with aerosol load for the inversion of remote sensing data. The reason for using a dynamic aerosol model is to represent systematic changes in one aerosol property as another property changes. Due to their importance and usefulness, systematic relationships among aerosol optical properties were investigated at the four surface sites. Figure 3.13 shows systematic relationships among low relative humidity (<40%) aerosol optical properties (sap, wo, b, and DF/d) and the aerosol load (measured as ssp at 550-nm wavelength). The mean aerosol optical properties were calculated over ssp intervals of 10 Mm-1 with the corresponding maximum standard error for each station given in the graph. The standard errors are considerably smaller than the changes over 10-Mm-1 bins, which implies a high level of significance to the relationships. The sap does not increase as rapidly as the ssp, resulting in a systematic increase in wo as ssp increases at all four stations. All four stations also show a systematic decrease in b as ssp increases. In terms of DF/d, the relationship between b and ssp acts to offset the relationship between wo and ssp. The b-ssp relationship results in a decrease in the magnitude of the DF/d as ssp increases, while the wo-ssp relationship results in an increase in the magnitude of the DF/d as ssp increases. For SGP and WSA, the b-ssp relationship is more important and results in a decrease in the magnitude of DF/d as ssp increases. For BND, the wo-ssp relationship is more important for ssp less than 40 Mm-1 and results in an increase in the magnitude of DF/d as ssp increases; however above 40 Mm-1 b-ssp relationship is more important and results in a decrease in the magnitude of DF/d as ssp increases. Similarly at BRW, the relative importance of one relationship compared to the other determines how DF/d changes as ssp increases.
Figure
3.14 illustrates two systematic relationships, one between å and ssp and the
other between Rsp and å. The strong relationship between Rsp and å indicates that the å is sensitive to
changes in the relative amount of submicrometer
scattering aerosol. At BND and
SGP there is a drop in å as ssp drops below 30 Mm-1, while at
WSA and BRW the å
increases as the ssp
drops below 30 Mm-1. Above 30
Mm-1 all four stations show a fairly constant å with increasing ssp.
This systematic relationship suggests that during low aerosol
concentration events, the continental sites (BND and SGP) have more relatively
larger particles present, while the marine sites (WSA and BRW) have more
relatively smaller particles present.
The å-ssp
relationship at BND and SGP (Figure 3.14a) is consistent with the relationship
between the Ångström exponent and aerosol optical
thickness (derived from Sun/sky scanning spectral radiometer measurements) for
the mid-Atlantic region of the eastern
Systematic relationships exist between various aerosol properties (sap, wo, b, DF/d, and å) and ssp and also between å and Rsp. These systematic relationships are qualitatively similar among the four stations; however, the quantitative relationships are different at each station, which is indicative of the occurrence of different aerosol types and size distributions at each station. Systematic relationships and the regional, yearly, weekly, and daily variations in optical properties can be used to check for consistency between climatologies based either on observations or models. The existence of systematic changes in aerosol optical properties with changes in aerosol concentration indicate that care should be taken when using average values in algorithms to retrieve aerosol properties, such as optical depth, from satellite data. An algorithm that uses a static representation for aerosol optical properties will have a systematic bias in derived values.
3.1.6 References
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M.H., R.S. Halthorne, S.E. Schwartz, J.A. Ogren, and
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LIST OF TABLES
Table 3.1 Data Editing Summary for NOAA Baseline and Regional Stations
Table 3.2. CMDL Baseline Aerosol Monitoring Stations (Status as of December 2001)
Table
3.3. CMDL Regional Aerosol Monitoring Sites (Status as of December 2001)
Table 3.4. Intensive Aerosol Properties Derived From CMDL Network
Table 3.5 Instrument inventory at Mauna Loa Observatory
Table 3.6 Means and standard deviations of aerosol optical properties of anthropogenically-influenced aerosols at 550 nm
LIST OF FIGURES
Fig. 3.1. Annual cycles for baseline stations at BRW, MLO, SMO, and SPO showing statistics for condensation nuclei (CN) concentration, total scattering coefficient (ssp), Ångström exponent (å), absorption coefficient (sap) and single scattering albedo (wo). Statistics representing the entire period are given in the last column (ANN), with the horizontal line representing the median value.
Fig. 3.2. Annual cycles for regional stations at BND, WSA, and SGP showing statistics for annual absorption coefficient (sap), total scattering coefficient (ssp), Ångström exponent (å),) and single-scattering albedo (wo). Statistics representing the entire period are given in the last column (ANN), with the horizontal line representing the median value.
Fig. 3.3. Long-term trends for baseline stations of monthly averaged condensation nuclei concentration and total scattering coefficient at 550 nm. A simple linear fit is given for the scattering coefficient but is omitted for the condensation nuclei since instrument changes make a trend line inappropriate.
Fig. 3.4. Long-term trends for baseline stations of monthly averaged Ångström exponent (550/700 nm), absorption coefficient, and single scattering albedo. A simple linear fit to the data is shown.
Fig. 3.5. Comparison of scattering measured by new nephelometer (bspG MLN) with scattering measured by old nephelometer (bspG MLO) for 550 nm wavelength. The solid black line shows the fit when the y-intercept is forced through the origin; the dashed line is the 1:1 line.
Fig. 3.6. Comparison of absorption measured by PSAP (bap MLN) with absorption measured by aethalometer (bap MLO). The solid black line shows the fit when the y-intercept is forced through the origin; the dashed line is the 1:1 line.
Fig. 3.7. Time series of absorption and graphitic carbon measured at KCO during February-March 1999.
Fig. 3.8. Comparison of GC and absorption coefficient. The solid dark line is the fit to the heavy loading data; the gray line is the fit to the medium loading data; and the dashed black line is the fit to the light loading data. One outlier has been removed from the ‘Medium Loading’ data set.
Fig. 3.9. Statistical plots of vertical profiles of extinction (left) and albedo (right) over the SGP site. Black box-whiskers are from aircraft flights. Gray box-whiskers are surface measurements.
Fig. 3.10. Comparison of AOD measured by aircraft with AOD derived from remote sensing instruments at SGP.
Fig. 3.11. Time series of aerosol measurements from Kosan during ACE-Asia in 2001: a) total absorption and scattering coefficients, b) submicrometer and total single-scattering albedo, c) submicrometer fraction of aerosol absorption and scattering, and d) total aerosol hygroscopic growth factor. All values are reported for a wavelength of 550 nm.
Fig. 3.12. Aerosol optical depth measured at 500 nm and aerosol Ångström exponent from the 412/862-nm wavelength pair.
Fig. 3.13. (a) Mean aerosol light absorption coefficient (sap), (b) single-scattering albedo (wo), (c) hemispheric backscatter fraction (b), and (d) forcing efficiency (DF/d) versus the aerosol light scattering coefficient (ssp) for BND, SGP, WSA, and BRW. Plots are based on all valid hourly averaged aerosol measurements (>50% 1–min data within the hour) for systems with TSI 3563 nephelometers. The mean values were calculated over 10-Mm-1 ssp bins. The maximum standard error (sample standard deviation /square root of the number of points) at each station is given in the text boxes.
Fig. 3.14. (a) Mean angstrom exponent (å) versus aerosol light scattering coefficient (ssp) and (b) sub micrometer scattering fraction (Rsp) versus Ångström exponent for BND, SGP, WSA, and BRW. Plots are based on all valid hourly averaged aerosol measurements (>50% 1–min data within the hour) for systems with TSI 3563 nephelometers. The å values were calculated over 10-Mm-1 ssp bins and the mean Rsp was calculated from 0.25-Ångström exponent bins. The maximum standard error (sample standard deviation /square root of the number of points) at each station is given in the text boxes.
TABLE 3.1.
Data-Editing Summary for NOAA Baseline and
Regional Stations
Station |
Editing |
Clean Sector
|
South Pole |
a,b,c |
0° < WD < 110°, 330°<WD < 360° |
Samoa |
a,b,c |
0° < WD < 165°, 285°<WD < 360° |
Mauna
Loa |
a,b,c,d |
90° < WD < 270° |
Barrow |
a,b,c |
0° < WD < 130° |
Sable
Island |
a,b,c |
0° < WD < 35°, 85° < WD < 360° |
Southern
Great Plains |
a |
|
Bondville |
a |
|
a: Manual removal of local contamination spikes;
b: Automatic
removal of data not in clean sector;
c: Automatic
removal of data for low wind speeds;
d: Removal
of data for upslope wind conditions;
WD: Wind
direction.
TABLE 3.2. CMDL Baseline Aerosol Monitoring Stations
(Status as of December 2001)
Category |
Baseline
|
Baseline
Free Troposphere |
Baseline
Marine |
Baseline
Antarctic |
Location |
Point Barrow |
|
|
South Pole |
Designator |
BRW |
MLO |
SMO |
SPO |
Latitude |
71.323ºN |
19.539ºN |
14.232ºS |
89.997ºS |
Longitude |
156.609ºW |
155.578ºW |
170.563ºW |
102.0ºE |
Elevation
(m) |
8 |
3397 |
77 |
2838 |
Responsible
Institute |
CMDL |
CMDL |
CMDL |
CMDL |
Status |
Operational,
1976 |
Operational,
1974 Major upgrade, 2000 |
Operational,
1977 |
Operational,
1974 |
Sample
RH |
RH
<40% |
RH
<40% |
Uncontrolled |
Uncontrolled |
Sample
Size Fractions |
D<1
µm D<10
µm |
D<1
µm D<10
µm |
Uncontrolled |
Uncontrolled |
Optical
measurements |
ssp(3l), sbsp(3l), sap(1l) |
ssp(3l), sbsp(3l), sap(1l), d(6l) |
None |
ssp(4l) |
Microphysical
|
CN
concentration |
CN
concentration |
CN
concentration |
CN
concentration |
Chemical measurements |
Major ions, mass |
None |
None |
None |
TABLE 3.3. CMDL Regional Aerosol Monitoring Sites
(Status as of December 2001)
Category |
Perturbed
Marine |
Perturbed
Continental |
Perturbed
Continental |
Location |
Sable Island, Nova Scotia, Canada |
Bondville, Illinois |
Lamont, Oklahoma |
Designator |
WSA |
BND |
SGP |
Latitude |
43.933ºN |
40.053ºN |
36.605ºN |
Longitude |
60.007ºW |
88.372ºW |
97.489ºW |
Elevation
(m) |
5 |
230 |
315 |
Responsible
Institute |
CMDL |
CMDL |
CMDL |
Collaborating
Institute(s) |
AES
|
University
of Illinois, Illinois State Water Survey |
DOE/ARM |
Status |
Operational,
August 1992 Inactive, April 2000 |
Operational,
July 1994 |
Operational,
July 1996 Chemistry added, February 2000 |
Sample
RH |
RH
<40% |
RH
<40% |
RH
<40% |
Sample
size fractions |
D<1
µm, D<10 µm |
D<1
µm, D<10 µm |
D<1
µm, D<10 µm |
Optical measurements |
ssp(3l), sbsp(3l) sap(1l) |
ssp(3l), sbsp(3l), sap(1l) |
ssp(3l),sbsp(3l), sap(1l), d(7l) |
Microphysical
|
CN
concentration |
CN
concentration |
CN,
n(D) concentration |
Chemical measurements |
Major ions, mass |
Major ions, mass |
Major ions, mass |
TABLE 3.4.
Intensive Aerosol Properties Derived From CMDL Network
Properties |
Description |
å |
The
Ångström exponent, defined by the power-law sspµl-å, describes the
wavelength-dependence of scattered light.
In the figures below, å is calculated from measurements at 550 and 700 nm
wavelengths. Situations where the
scattering is dominated by submicrometer particles
typically have values around 2, while values close to 0 occur when the
scattering is dominated by particles larger than a few microns in
diameter. |
wo |
The
aerosol single-scattering albedo, defined as ssp/(sap + ssp), describes the relative
contributions of scattering and absorption to the total light extinction. Purely scattering aerosols (e.g., sulfuric
acid) have values of 1, while very strong absorbers (e.g., elemental carbon)
have values around 0.3. |
g, b |
Radiative transfer models commonly require one of two
integral properties of the angular distribution of scattered light (phase
function): the asymmetry factor g or the hemispheric backscatter
fraction b. The asymmetry factor is the cosine-weighted
average of the phase function, ranging from a value of -1 for entirely
backscattered light to +1 for entirely forward-scattered light. The hemispheric backscatter fraction b is defined as sbsp/ssp. |
f(RH) |
The
hygroscopic growth factor, defined as ssp(RH=85)/ssp(RH=40), describes the
humidity dependence of scattering on relative humidity (RH). |
aI |
The mass scattering efficiency for species i, defined as
the slope of the linear regression line relating ssp and the mass
concentration of the chemical species, is used in chemical transport models
to evaluate the radiative effects of each chemical
species predicted by the |
TABLE 3.5.
Instrument Inventory at Mauna Loa Observatory
Instrument |
Period
of Operation |
Station |
Comments |
MRI nephelometer |
1974 - Spring 2000 |
MLO |
4 wavelengths, no size cut |
MRI
nephelometer (operating at 1 wavelength due to instrument problems) |
Summer
1982 - Spring 1984 |
MLO |
1
wavelength (550 nm), no size cut |
MS Electron nephelometer |
Spring
1994 - Spring 2001 |
MLO |
3
wavelengths, no size cut |
Magee
Scientific aethalometer |
1990
- present |
MLO |
Broadband,
no size cut Specific
absorption of 10 m2/g used to convert [BC] to sap |
TSI
nephelometer (model
number 3563) |
Spring
2000 - present |
MLN |
3
wavelengths, total and back scatter, 1-and 10-mm size cuts |
Radiance Research particle soot absorption
photometer (PSAP) |
Spring
2000 - present |
MLN |
565-nm
wavelength, 1-and 10- mm size cuts |
TABLE 3.6.
Means and Standard Deviations of Aerosol Optical Properties of Anthropogenically Influenced Aerosols at 550 nm.
Aerosol |
Kosan |
Kaashidhoo |
Bondville |
Property |
( |
(KCO) |
(BND) |
sspa |
92 (53) |
73 (28) |
54 (43) |
sapa |
12
(8) |
16
(9) |
4
(3) |
wo |
0.87
(0.05) |
0.82
(0.03) |
0.92
(0.06) |
f(RH) |
2.2
(0.5) |
1.7
(0.1) |
1.7
(0.4)b |
Fsspc |
0.61
(0.16 ) |
0.67
(0.08) |
0.86
(0.09) |
Fsapc |
0.83 (0.09) |
0.84 (0.06) |
0.92 (0.38) |
aValues are for total (Dp <10 mm) aerosol.
bRood, personal communication[2002]
cFssp and Fsap are the submicrometer fractions of aerosol scattering and
absorption, respectively.
|
|
Figure 3.1
|
|
Figure 3.2
Figure 3.3
Figure 3.4
Fig. 3.5
Fig. 3.6
Fig. 3.7.
Fig. 3.8.
Fig. 3.9.
Fig. 3.10
Fig. 3.11a.
Fig. 3.11b.
Fig. 3.11c
Fig. 3.11d
Fig. 3.12
Fig. 3.13a
Fig. 3.13b
Fig. 3.13c
Fig. 3.13d
Fig. 3.14a
Fig. 3.14b