Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites
Objectives. To analyze data on aerosol optical thickness (AOT) in the atmosphere over some Ukraine and Antarctic AERONET (AErosol RObotic NETwork) sites. To determine and compare direct aerosol radiative forcing (DRF) typical values using the data from midlatitude and Antarctic AERONET sites. Мета....
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| Опубліковано в: : | Український антарктичний журнал |
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Національний антарктичний науковий центр МОН України
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| Назва журналу: | Digital Library of Periodicals of National Academy of Sciences of Ukraine |
| Цитувати: | Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites / G. Milinevsky, Yu. Yukhymchuk, A. Grytsai, V. Danylevsky, Yu. Wang, V. Choliy // Український антарктичний журнал. — 2019. — № 1 (18). — С. 128-138. — Бібліогр.: 37 назв. — англ. |
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Digital Library of Periodicals of National Academy of Sciences of Ukraine| _version_ | 1860261806346338304 |
|---|---|
| author | Milinevsky, G. Yukhymchuk, Yu. Grytsai, A. Danylevsky, V. Wang, Yu. Choliy, V. |
| author_facet | Milinevsky, G. Yukhymchuk, Yu. Grytsai, A. Danylevsky, V. Wang, Yu. Choliy, V. |
| citation_txt | Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites / G. Milinevsky, Yu. Yukhymchuk, A. Grytsai, V. Danylevsky, Yu. Wang, V. Choliy // Український антарктичний журнал. — 2019. — № 1 (18). — С. 128-138. — Бібліогр.: 37 назв. — англ. |
| collection | DSpace DC |
| container_title | Український антарктичний журнал |
| description | Objectives. To analyze data on aerosol optical thickness (AOT) in the atmosphere over some Ukraine and Antarctic AERONET (AErosol RObotic NETwork) sites. To determine and compare direct aerosol radiative forcing (DRF) typical values using the data from midlatitude and Antarctic AERONET sites.
Мета. Проаналізувати дані щодо аерозольної оптичної товщини (АОТ) в атмосфері на деяких пунктах мережі AERONET (AErosol RObotic NETwork) в Україні та Антарктиці. Для визначення та порівняння типових значень аерозольного прямого радіаційного форсингу (ПРФ) використати типові дані середньоширотної та двох антарктичних пунктів AERONET.
|
| first_indexed | 2025-12-07T18:56:14Z |
| format | Article |
| fulltext |
128
Cite: Milinevsky G., Yukhymchuk Yu., Grytsai A., Danylevsky V.,
Wang Yu., Choliy V. Preliminary comparison of the direct aerosol ra-
diative forcing over Ukraine and Antarctic AERONET sites. Ukrai-
nian An tarctic Journal, 2019. № 1(18), 128—138.
UDC 551.510.42
G. Milinevsky 1, 2, 3, 4, *, Yu. Yukhymchuk 4, 5, A. Grytsai 3, V. Danylevsky 3, Yu. Wang 2, V. Choliy 3
1 National Antarctic Scientific Center, Ministry of Education and Science of Ukraine,
16 Taras Shevchenko Blvd., Kyiv, 01601, Ukraine
2 College of Physics, International Center of Future Science, Jilin University, 2699 Qianjin Str., Changchun, 130012, China
3 Taras Shevchenko National University of Kyiv, 64/13, Volodymyrska St., Kyiv, 01601, Ukraine
4 Main Astronomical Observatory of Ukraine, National Academy of Sciences of Ukraine,
27 Akad. Zabolotnogo Str., Kyiv, 03143, Ukraine
5 Institute of Physics, National Academy of Sciences of Ukraine, 46 Nauka Ave, Kyiv, 03028, Ukraine
* Corresponding author: genmilinevsky@jlu.edu.cn, genmilinevsky@gmail.com
PRELIMINARY COMPARISON OF THE DIRECT AEROSOL RADIATIVE
FORCING OVER UKRAINE AND ANTARCTIC AERONET SITES
ABSTRACT. Objectives. To analyze data on aerosol optical thickness (AOT) in the atmosphere over some Ukraine and Antarctic
AERONET (AErosol RObotic NETwork) sites. To determine and compare direct aerosol radiative forcing (DRF) typical values
using the data from midlatitude and Antarctic AERONET sites. Methods. Retrieval and visualization of the AERONET aerosol
optical thickness and radiative forcing, data analysis and interpretation of the data. Radiative forcing evaluation using Global At-
mospheric ModEl (GAME) and the AERONET operational product. Results. Aerosol optical thickness measurements are con-
sidered using observations by sun/sky photometers that are part of the AERONET sites in Ukraine (Kyiv) and at two additional sites
in Antarctica (Vechernaya Hill and ARM_McMurdo sites). According to the 2015–2018 measurements at the Vechernaya Hill and
ARM_McMurdo sites, the AOT values are small and are in the range of 0.05–0.1 at the 340 nm wavelength. In contrast, the cor-
responding AOT values from Kyiv observational site are reached 0.3–0.5 and sometimes higher. Using these AOT values from Kyiv
site and the urban aerosol types, the aerosol direct radiative forcing has been evaluated by the GAME code. The top of atmosphere
(TOA) DRF assessment using GAME suggests the instantaneous values of –5.7 W m–2 over vegetation surface for AOT equal 0.1.
Conclusions. The AERONET derived aerosol optical thicknesses over Kyiv site show the mean value of 0.3 at 340 nm; the values
over two Antarctic sites are in range of 0.03 to 0.06. Calculations using a numerical code (GAME) suggested the associated TOA
instantaneous DRF of –6 W m–2 to –14 W m–2 over the Kyiv site. The values calculated as part of the AERONET Kyiv site opera-
tional product are about –20 W m–2 (BOA) and about –10 W m–2 (TOA) during 2018.
Keywords: aerosol optical thickness, aerosol radiative forcing, AERONET, GAME code.
ISSN 1727-7485. Український антарктичний журнал. 2019, № 1 (18)
INTRODUCTION
Aerosol particles of natural and anthropogenic origin
play an essential role in climate formation and climate
change (Boucher et al., 2013; Larsen et al., 2014; Me-
nut et al., 2015; IPCC, 2019). They affect the energy
balance of the atmosphere in two ways: (1) through
the scattering and absorption of sunlight directly by
aerosol particles (direct effect) and (2) by influencing
the formation processes and the physical characte ris-
tics of clouds, since aerosol particles become water
vapor condensation nucleus under appropriate atmo-
sphe ric conditions (indirect effect). But quantita ti ve-
ly, these radiation effects are estimated with very
significant errors due to the significant lack of data
on the spatial-temporal distribution of aerosol con tent
in the atmosphere and on the characteristics of parti-
cles (Boucher et al., 2013; Larsen et al., 2014; Foun-
tou lakis et al., 2019). Studies using remote ground-
based and satellite lidar systems, as well as direct in
situ measurements at different altitudes from aircraft
(Boucher et al., 2013), indicate that the aerosol is
129ISSN 1727-7485. Український антарктичний журнал. 2019, № 1 (18)
Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites
concentrated the boundary layer of the tro po sphe-
re (below 1–3 km). Under the influence of tur bu-
len ce and various meteorological phenomena, the
concentration and characteristics of the particles are
very variable in space and time. The prediction of
aerosol characteristics is also complicated by the short
lifetime of some components, including precursor
gases, which may be involved in aerosol formation
(SO
x
, NO
x
, and other substances). Composition of
these volatile atmospheric components depends on
the geographical distribution of their sources and
meteorological conditions. On the basis of measure-
ments during the 1990–2015 period and the use of
different simulation methods, it was concluded that
atmospheric aerosol and ozone create positive ra-
dia tive forcing, the value of which globally reaches
+0.2 W m–2. In Europe, the maximum value for the
same time interval is +4.0 W m–2, in Asia it equals to
–3.0 W m–2 (Myhre et al., 2017).
The climatic effects of the aerosol depend on both
the physical and chemical parameters of the aerosol
particles associated with their origin. For example, 30%
of all aerosol-related effects are caused by mi neral dust.
It is a key component of the aerosol that acts on the
climate through interaction with ra dia ti on, clouds,
affects ecosystems, in clu ding human health, alters
the vertical profile of temperature and cloud cover
(Kudo et al., 2016). Dust and climate assessments on
the global and regional scale are connected with sig-
nificant uncer tainties related to its high concentra-
tions in the sparse explored regions (Ridley et al.,
2016). In addition, for example, solid dust particles
can be carried over a distance of more than 2500 km
by the wind (Pey et al., 2013; Salvador et al., 2014).
Powerful volcanoes can produce sig ni ficant climatic
effects on a global scale releasing the aerosols in the
stratosphere (Hansen et al., 2005; Waquet et al., 2014).
In recent decades, the regional distribution of at-
mospheric aerosol has changed markedly. This is mai-
nly due to the reduction of sulfur dioxide emissions
in the US and Europe to improve air quality. At the
same time, there is an increase in the amount of
aerosol at south and east of Asia (Myhre et al., 2017),
which, for example, creates negative aerosol radiative
forcing (RF) to –4.0 W m–2 over India.
Biomass burning has become one of the major
sources of aerosol replenishment (Wu et al., 2018;
Andreae, 2019). The particles resulting from the
combustion are small in diameter (30 – 100 nm), but
their size may vary. This is due to the fact that the
aerosol undergoes rapid physical and chemical
transformations (typically from minutes to hours).
The change in particle size occurs through coagulation
and condensation of organic material on existing
particles (Laing et al., 2016). This aerosol consists
predominantly of organic carbon and black carbon,
which absorbs solar radiation (Kudo et al., 2016)
including some inorganic material as well (Vakkari et
al., 2014). The sources of this type of aerosol are
concentrated predominantly in the tropical zone fo-
rests, taiga and urban areas of the Northern Hemi-
sphere, where occasional fires of vegetation occur, as
well as biomass and hydrocarbon combustion for
economic purposes, in industry, vehicles. So, in
September 2015, due to the forest fires and burning
of peatlands, thick aerosol clouds in the form of
smoke particles arrived in the atmosphere over Kyiv
(Bovchaliuk et al., 2017). The optical thickness of the
aerosol was so large that at altitudes higher than 500 m
the atmosphere became opaque to the aerosol lidar
CE370 (under normal atmospheric transparency
conditions, this lidar can provide the measurements
up to a height of 15 km). The smoke screen was also
clearly visible on satellite images. Extensive forest
fires in central Russia during the summer of 2010
(Chubarova et al., 2012; Pere et al., 2014; Galytska et
al., 2018), cause both significant increases in the
aerosol content and changes of aerosol characteristics
in the atmosphere over Eastern Europe. Similar
events lead to an increase in the relative black carbon
content among aerosols and raise their ability to
absorb sunlight.
On the other hand, there are remote regions, in
particular the Antarctic, where the content and cha-
rac teristics of aerosols in the atmosphere are signi-
ficantly different than in the above-mentioned regions,
and therefore the climate effects caused by them are
also different. Surface albedo in Polar Regions exce-
eds 0.85 that can cause positive BOA aerosol forcing
due to multiple scattering (Tomasi et al., 2007). First
130 ISSN 1727-7485. Ukrainian Antarctic Journal. 2019, № 1 (18)
G. Milinevsky, Yu. Yukhymchuk, A. Grytsai, V. Danylevsky, Yu. Wang, V. Choliy
AOT measurements in the Antarctica have been pro-
vided in the summer 1950/51 (Maudheim, Norway).
Measurements of optical parameters were carrying
out during 1960–1980s at several Antarctic stations
(Mirny, South Pole, McMurdo, Molodezhnaya) with
the sun photometer and pyrheliometer. Background
values at 500 nm changed in the range 0.01–0.05
increasing after strong volcanic eruptions, to 0.12
after El Chichon and to 0.30 after Pinatubo (Tomasi
et al., 2007). Evident AOT trends in the Antarctica
were not found out (Tomasi et al., 2012).
This paper compares the regional differences in
the magnitude of the direct radiative forcing (DRF)
basing on aerosol optical thickness at the mid-latitude
site and at the Antarctic coastal sites. For comparison,
measurements at three AERONET sites were used:
the Kyiv site (N50°21′50′′, E30°29′49′′) in Ukraine,
the Vechernaya Hill site (S67°39′36′′, E46°09′28′′) and
the ARM_McMurdo site (S77°50′56′′, E166°43′47′′)
in Antarctica.
DATA AND METHODS
1. Radiative forcing
The effectiveness of the aerosol impact on the climate
is evaluated using the concept of radiative forcing. The
concept proposes a quantitative estimate of chan ges
that the aerosol makes to the energy balance of the
Earth’s climate system, affecting the total flux of
electromagnetic radiation at the boundary of this
system. Radiative forcing is defined as the perturbation
introduced by a particular component of the atmos-
phere into the difference between the flux of solar
radiation entering the climate system and the ra dia-
tion flux of the Earth’s atmosphere leaving it (Co-
mmi ttee on Radiative Forcing, 2005; Larsen et al.,
2014). The total radiation flux is determined at the
boundary of the Earth’s climate system as the diffe-
rence between the incoming flux of solar radiation Φ
S
coming into this system and the outgoing radiation
flux of the Earth’s surface and atmosphere Φ
E
leaving
it (Committee on Radiative Forcing, 2005):
( )E
S
S A
E
−=Φ 1
4
,
where
E
S
– is the solar constant (the total radiative
energy flux outside of the Earth atmosphere (Brasseur
and Solomon 2005), A
E
is the Earth’s albedo; the flux
per unit surface is considered. The radiation flux from
Earth is determined by the Stefan–Boltzmann law:
4
EE Tσ=Φ ,
where σ – is the Stefan–Boltzmann constant, and T
E
is the effective temperature of the Earth’s climate
system. The total flux at the boundary of the climate
system is defined as the difference between ingoing
and outgoing radiation flux:
ES Φ−Φ=Φ .
In the case of energy equilibrium Φ = 0. If the
equilibrium is disturbed, then the change in total flux
can be estimated:
ΔΦ = ΔΦ
S
– ΔΦ
E
.
Obviously, changes in this flux can be caused by
both changes in the ascending and the descending
energy fluxes. This change, which occurs in the cli-
mate system due to external factors, is called radiative
forcing. These factors can change the radiation flux
from the Sun, albedo and/or the effective temperatu-
re of the climate system. Positive radiative forcing
causes the system to heat up, while a negative one
causes it to cool down.
The direct radiative forcing produced by aerosol
particles is determined by the optical properties of
these particles, their albedo and phase function. The
aerosol DKF depends on the aerosol particles concent-
ration, size, composition, morphology as well as on
the solar zenith angle. In addition, the aerosol DRF
depends on the ratio between the scattering and
absorption capacity of the particles in the aerosol layer.
If the absorption capacity of the aerosol layer in-
crea ses in comparison with the scattering, then the
DRF can change from negative to positive and the
aerosol layer begins to heat the atmosphere. The
absorption properties depend on the size of the aero-
sol particles and their surface albedo. In addition, if the
aerosol layer consists of a mixture of different mate-
rials, which scatter and absorb light, then this heating
or cooling effect is also dependent on how these par-
σ
131ISSN 1727-7485. Український антарктичний журнал. 2019, № 1 (18)
Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites
ticles with opposite properties are mixed. Thus, sulfa-
tes of anthropogenic origin, for which the single-sca-
tte ring albedo is close to 1, lead to negative radiative
forcing (cooling), whereas black carbon aerosols (soot)
have the single-scattering albedo less than 1 due to
their large absorption effect.
Dust particles also provide heating of the atmo sphe-
re, absorbing both shortwave and longwave ra dia tion.
Since the effect of aerosols depends on altitude, the
resulting forcing at the conventional upper boundary
of the atmosphere (about 100 km a.s.l.) is calculated.
This parameter is known as TOA (Top Of the Atmo-
sphere), which describes the climatic role of aerosols.
To estimate changes at the surface, calculations are
performed at the bottom of the atmosphere, BOA
(Bottom Of the Atmosphere). Total effect at diffe rent
altitudes can be calculated as well. Global means of
the aerosol radiative forcing in Liao et al. (2004)
were retrieved as –0.72 W/m2 (TOA), and –4.04
W/m2 (BOA).
2. AERONET Data.
Aerosol radiative forcing estimates are based on gro und-
based measurements, first and foremost, the AERONET
(International Network of Automatic Solar Photo-
meters (Aerosol Robotic NETwork, https://aeronet.
gsfc.nasa.gov/)), which provides ground-based remote
sensing observations of the optical atmospheric cha-
racteristics by standardized CIMEL318 sun-pho to me-
ters (Holben et al., 1998; Giles et al., 2019). AERONET
sun-photometers measure the optical thickness of
the atmosphere caused by aerosols (AOT) at obser-
vations in individual narrow wavebands of the solar
spectrum in the range of 340 to 1640 nm (in some
sun-photometer modifications up to 1020 nm only).
The wavelengths of the sun-photometers are chosen
to avoid absorption the solar radiance by the at mos-
phe re constituens (except Rayleigh scattering) such
as oxygen, water vapor, ozone, etc. Measurements
are made at times co rresponding to the certain solar
zenith angle. The sun-photometer also measures the
distribution of sky brightness along the Sun’s almu-
cantarate and along height circle at specified wave-
lengths using two separate optical channels (Holben
et al., 1998; Giles et al., 2019).
The spectral AOT measured by a sun-photometer
is designated on the basis of the Beer–Bouguer–
Lambert law:
,
where E(λ) – measured spectral luminosity, E
0
(λ) –
spectral out-of-atmospheric luminosity, τ(λ) – spec-
tral optical thickness of the atmosphere towards
the Sun (Brasseur and Solomon, 2005). Aerosol op-
tical thickness is defined as the integral of the ex ti n-
c tion coefficient σ(z) between two points with alti-
tudes (z
1
, z
2
) in the atmosphere (Brasseur and Solo-
mon, 2005):
AOTλ = ∫
z1
z2
σ(λ, z)dz.
The optical thickness of the atmosphere is the sum
of its components:
τλ = τmol, λ + τaer, λ,
where τmol, λ, τaer, λ — optical thicknesses for molecules
and aerosols at wavelength λ. In addition, τ
mol, λ in clu-
des the sum of the optical thicknesses of all significant
molecular constituents of the atmosphere (oxygen,
nitrogen, carbon dioxide) (Brasseur and Solomon,
2005). These parameters in the AERONET algorithm
are determined by the conditions for the standard
atmosphere according to special measu re ments
(Hol ben et al., 1998; Giles et al., 2019). The total
uncertainty in AOT for the AERONET measurements
under cloud-free conditions is 0.01 at 440 nm (Hol-
ben et al., 1998).
When calculating the radiation fluxes, both direct
solar and diffuse radiation from the celestial
hemisphere are taken into account. These calculations
are performed over a wide spectral range from 0.2 to
4.0 μm (Dubovik and King, 2000). The spectrum-in-
tegrated solar radiation flux near the Earth’s surface,
weakened by an aerosol:
Ф(t, θ, ϕ) = ∫ Φ
0
(t, λ, θ, ϕ) · exp[–AOT(t, λ, θ, ϕ)] · dλ,
where AOT(t, λ, θ, ϕ) — is the spectral optical
thickness of the aerosol measured at time t in the
location with coordinates θ, ϕ; Φ
0
(t, λ, θ, ϕ) — is the
radiation flux at the upper limit of the atmosphere
(about 100 km). The fluxes at different altitudes are
λ2
λ1
132 ISSN 1727-7485. Ukrainian Antarctic Journal. 2019, № 1 (18)
G. Milinevsky, Yu. Yukhymchuk, A. Grytsai, V. Danylevsky, Yu. Wang, V. Choliy
calculated using special atmospheric optical propa-
gation models and related algorithms, including the
GAME algorithm (Halthore et al., 2005; Dubuisson
et al., 1996; Dubuisson et al., 2006).The GAME
(Global Atmospheric ModEl) model used to calculate
radiatiev fluxes and direct radiative forcing generated
by aerosols and water vapor (Bassani et al., 2012;
Garcia et al., 2012). In the GAME code, the radiative
fluxes and heating rate of the atmosphere are calcu-
lated for atmosphere divided by 50 flat homogeneous
layers in the spectral range from 0.2 to 3 microns. In
calculation we assume cloudless conditions and typi-
cal albedo for vegetation surface for Kyiv site. It also
accounts for Rayleigh scattering and employs standared
Fig. 1. AOT at 380 nm for observations of the AERONET net-
work (solid curve with vertical lines showing standard devia-
tion) and ac cor ding to the lidar observations at 520 nm (solid
curve with diamonds)
AOD, 3 Sep, 2015
6 8 10
Time, UTC
12 14
1.6
1.4
1.2
1.0
0.8
0.6
0.4
0.2
0.0
A
O
D
Fig. 2. The energy flux dependence on the altitude for different AOT values: a — incoming flux, b — outgoing flux from the
surface, c — their difference, d — the radiative dependence on the altitude
a
c
b
d
120
100
80
60
40
20
0
120
100
80
60
40
20
0
120
100
80
60
40
20
0
120
100
80
60
40
20
0
A
lt
it
u
d
e
,
k
m
A
lt
it
u
d
e
,
k
m
A
lt
it
u
d
e
,
k
m
A
lt
it
u
d
e
,
k
m
900
–1000 –900 –800 –700 –50 0 50 100 150 200
1000 1100 1200 1300 1400 290 300 310 320 330 340 350 360 370
Flux down, W/m2
Net flux, W/m2 Net flux
AOT 0.0
— Net flux
AOT
, W/m2
Flux up, W/m2
AOT 0.0
AOT 0.4
AOT 0.6
AOT 0.08
AOT 0.0
AOT 0.4
AOT 0.6
AOT 0.08
AOT 0.4
AOT 0.6
AOT 0.08
AOT 0.0
AOT 0.4
AOT 0.6
AOT 0.08
133ISSN 1727-7485. Український антарктичний журнал. 2019, № 1 (18)
Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites
atmospheric gas profiles (Dubuisson et al., 1996;
2006). Due to the preliminary DRF evaluation task
for aerosol particles parameters (single scattering
albedo, size distribution, etc.), the standard values
were used for urban aerosol. The calculation software
used in this paper was provided by the Laboratory of
Atmospheric Optics, University of Lille, France. More
details on the DRF computational packagescan be fo-
und in (Derimian et al., 2012; 2016; Garcia et al., 2012).
RESULTS
The DRF results obtained in this paper are the cal-
culations of the instantaneous direct radiative forcing.
For a better understanding of the effect of significant
aerosol concentrations in the atmosphere on the
radiative forcing, calculations were made for different
values of aerosol optical thickness values: no aerosol
in the atmosphere (AOT = 0), pure at mos phere with
Table 1. Average values of the instantaneous
radiative forcing at AOT of 0.1, 0.4, 0.8
АОT 0.1 0.4 0.8
Radiative forcing, Wm—2 –5.7 –12.4 —
Fig. 3. Aerosol optical thickness at 340 and 675 nm for the AERONET Vechernaya Hill and ARM_McMurdo sites
0.5
0.4
0.3
0.2
0.1
0
0.25
0.2
0.15
0.1
0.05
0
0.25
0.2
0.15
0.1
0.05
0
0.5
0.4
0.3
0.2
0.1
0
A
O
T
,
3
4
0
n
m
A
O
T
,
3
4
0
n
m
A
O
T
,
6
7
5
n
m
A
O
T
,
6
7
5
n
m
Vechernaya Hill, level 2.0
McMuro, level 2.0
Vechernaya Hill, level 2.0
McMuro, level 2.0
Day of year
Day of year
Day of year
Day of year
100
100
100
100
200
200
200
200
300
300
300
300
2016
2017
2018
2015
2016
2015
2016
2016
2017
2018
134 ISSN 1727-7485. Ukrainian Antarctic Journal. 2019, № 1 (18)
G. Milinevsky, Yu. Yukhymchuk, A. Grytsai, V. Danylevsky, Yu. Wang, V. Choliy
a minimum aerosol contamination (АОТ = 0.08, 0.1),
average pollution (AOT = 0.4) and ab nor mally high
values for the region of Ukraine (Mili nevsky et al.,
2014; Milinevsky and Danylevsky, 2018). A significant
aerosol pollution was observed in the at mosphere
over Kyiv, for example, during forest fires in Septem-
ber 2015 (Fig. 1) with AOT = 0.6 ÷ 1.3 at 440—380 nm
(Bov chaliuk et al., 2017).
The circles in Fig .1 show the results of the AOT
measurements that were used to further calculate the
radiative forcing. Analyzing the data of simultaneous
lidar measurements, we see that in September 3,
2015, the extinction coefficient at 520 nm becomes
high – more than 0.3 km–1, while on August 8 these
values are within 0.06 km–1. The values larger than 0.3
km–1 are ob ser ved at a time when significant smoke
was registered (Bovchaliuk et al., 2017). The extinction
coefficient shows how a light intensity decreases due
to absorption and scattering. According to Bovchaliuk
et al., (2017) above 4 km extinction goes to zero, which
means that the absorption and scattering processes
have small effect on the intensity of the emitted light.
The aerosol effect on radiative forcing was estima-
ted using the GAME numerical code. The GAME
Fig. 4. The radiative forcing according to AERONET database for sites Kyiv, Vechernaya Hill (2018) and ARM_McMurdo
(2015 and 2016). Radiative forcing is given on the BOA (dotted line) and the TOA (black line)
Kyiv, 2018, level 2.0
R
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,
W
/m
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Vechernaya Hill, 2018, level 1.5
20
0
–20
–40
–60
–80
–2
–4
–6
–8
–10
–12
0
–5
–10
–15
–20
–25
–30
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–2
–4
–6
Day of year
Day of year Day of year
Day of year
200
340 350 360
40100
330 100 200 300
200
320 0
0300 60 80
McMuro, 2015, level 1.5 McMuro, 2016, level 1.5
135ISSN 1727-7485. Український антарктичний журнал. 2019, № 1 (18)
Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites
code computes the radiative fluxes taking into account
various components. In general, as less energy rea ching
the surface (ingoing radiative flux), less is emitted
into the space (outgoing radiative flux) as shown in
Fig. 2, a, b. The results of simulation of the diffe-
rence between the outgoing radiation flux from the
Earth’s surface and coming from the Sun are shown
in Fig. 2
Table 1 shows the average values of instantaneous
radiative forcing for different aerosol optical thickness
(AOT).
Increasing the aerosol content leads to an increase
in the DRF, with a corresponding sign. The cha-
racteristic values of the aerosol optical thickness in
the atmosphere over Antarctica do not exceed 0.1,
which is illustrated in Fig. 3. In the atmosphere above
the Kyiv station at 340 nm wavelength AOT values
are in the range 0.3–0.5, and sometimes larger.
Therefore, the direct aerosol forcing by the data at
Antarctic stations are lower substantially. However,
in the Antarctic atmosphere, aerosol optical thickness
values of up to 0.3–0.4 are rare recorded, which has
seen by observations at the Vechernaya Hill and ARM_
McMurdo AERONET sites.The albedo of the Earth
surface is important for radiation forcing calculations
because the larger albedo produced greater the energy
flux reflected from the surface. The GAME algorithm
allows to calculate the aerosol radiative forcing under
various types of the surface, for example, vegetation
and snow conditions.
Values of the instantaneous aerosol radiative for-
cin g at BOA and TOA are available as part of the
AERONET operational product.The relevant data of
the aerosol DRF for the AERONET Kyiv, Vechernaya
Hill and ARM_McMurdosites are presented in Fig. 4.
The data shows that the radiative forcing is almost
exclusively negative, meaning cooling of the surface-
atmosphere system. The typical RF values for the
atmosphere above the AERONET Kyiv site (at the
BOA the DRF is about –22 W m–2 and at the TOA
the DRF is about –10 W m–2) are larger than the
DRF for the atmosphere above the Antarctic sites.
Note the sparce data from the Antarctic AERONET
sites are due to the high Sun zenith angle and weather
conditions. For comparison, the results of AERONET
radiative forcing calculations for the ARM_McMurdo
site for 2015 – 2016 show the typical values of ra-
diative forcing at the BOA of –4 ÷ –8 W m– 2 and at
the TOA –2 ÷ –6 W m–2 (Fig. 4).
CONCLUSIONS
The study presents a preliminary comparison of
AERONET derived AOT in the atmosphere over Kyiv
site and over two Antarctic sites (Vechernaya Hill,
ARM_McMurdo). The average AOT at 340 nm spect-
ral wavelength in Kyiv was found to be of 0.3, but in
some episodes can even exceed 0.5 (Milinevsky et al.,
2014; Milinevsky and Danylevsky, 2018). For the
Antarctic atmosphere, typically low AOT values of
about 0.05–0.1 were found. The data for the Antarctic
AERONET station are available for austral summer
period only. The values of the radiative forcing at the
TOA for the Antarctica sites are from –2 W m–2 to –6
W m–2, while the average AOT is 0.05. To provide the
comprehensive investigation of the direct radiative
forcing level in the Antarctic atmosphere, the all
available data from AERONET sites will be studied.
The future prospects for this investigation will include
the composition of aerosol over mid-latitude and
Antarctic sites, as well as aerosol size distribution,
single scattering albedo and clouds fraction.
Acknowledgements. This work was supported in part
by State Institution National Antarctic Scientific Cen-
ter, Ministry of Education and Science of Ukraine,
by Main Astrono mical Observatory NAS of Ukraine,
and by Taras Shev chenko National University of Kyiv
project 19BF051-08. The most preparation works on
the paper have been done in College of Physics,
Inter national Center of Future Science, Jilin Uni-
versity. We thank Philippe Dubuisson from Labora-
toired’ Optique Atmosphérique (LOA) for pro viding
the GAME software and valuable consultations. We
thank also Brent Holben (NASA/GSFC) for ma na-
ging the AERONET program and sites, principal
inves tigators Anatoli Chaikovsky and Philippe Go-
loub (LOA) of the Vechernaya Hill site, principal in-
vestigator Rick Wagener and site manager Paul Or-
tega of the ARM_McMurdo site, and all observers
136 ISSN 1727-7485. Ukrainian Antarctic Journal. 2019, № 1 (18)
G. Milinevsky, Yu. Yukhymchuk, A. Grytsai, V. Danylevsky, Yu. Wang, V. Choliy
from AERONET sites Vechernaya Hill and ARM_
McMurdo for their hard work in Antarctica. We thank
Yevgeny Derimian (LOA) for valuable comments and
suggestions that allow im pro ving the text of the pa-
per. The high quality of AERONET/PHOTONS da-
ta of Kyiv site was provided by CIMEL sun-photo-
meter calibration performed at LOA, suppor ted by
ACTRIS-2 project with funding from the Euro pe an
Union’s Horizon 2020 research and innovation prog-
ram under grant agreement No 654109.
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138 ISSN 1727-7485. Ukrainian Antarctic Journal. 2019, № 1 (18)
G. Milinevsky, Yu. Yukhymchuk, A. Grytsai, V. Danylevsky, Yu. Wang, V. Choliy
Г. Міліневський1,2,3,4*, Ю. Юхимчук4,5, А. Грицай3, В. Данилевський3, Ю. Ванг2, В. Чолій3
1 Національний антарктичний науковий центр МОН України,
бульв. Тараса Шевченка, 16, м. Київ, 01601, Україна
2 Коледж фізики, Міжнародний центр науки майбутнього,
Цзилінський університет, вул. Цянцин, 2699, м. Чанчунь, 130012, Китай,
3 Київський національний університет імені Тараса Шевченка,
вул. Володимирська, 64/13, м. Київ, 01601, Україна
4 Головна астрономічна обсерваторія НАН України,
вул. Академіка Заболотного, 27, м. Київ, 03143, Україна
5 Інститут фізики НАН України, пр. Науки, 46, м. Київ, 02000, Україна
* Автор для кореспонденції: genmilinevsky@jlu.edu.cn, genmilinevsky@gmail.com
ПОПЕРЕДНІ ПОРІВНЯННЯ ПРЯМОГО АЕРОЗОЛЬНОГО РАДІАЦІЙНОГО ФОРСИНГУ
ЗА ДАНИМИ СТАНЦІЙ AERONET В УКРАЇНІ ТА АНТАРКТИЦІ
РЕФЕРАТ. Мета. Проаналізувати дані щодо аерозольної оптичної товщини (АОТ) в атмосфері на деяких пунктах
мережі AERONET (AErosol RObotic NETwork) в Україні та Антарктиці. Для визначення та порівняння типових зна-
чень аерозольного прямого радіаційного форсингу (ПРФ) використати типові дані середньоширотної та двох антарк-
тичних пунктів AERONET. Методи. Визначення та візуалізація даних AERONET щодо оптичної товщини аерозолю
та радіаційний форсинг, проведення аналізу та інтерпретації цих даних. Обчислення радіаційного форсингу за допо-
могою алгоритму Глобальна атмосферна модель (Global Atmospheric ModEl, GAME). Результати. Розглянуто вимірю-
вання аерозольної оптичної товщини за спостереженнями за допомогою аерозольних сонячних фотометрів мережі
AERONET в Україні (пункт Київ) та у двох пунктах спостережень в Антарктиді (Гора Вечірня та АРМ_МакМердо
(ARM_McMurdo)). Відповідно до вимірювань 2015–2018 рр. визначено, що за даними пунктів Гора Вечірня та АРМ_
МакМердо значення AOT є невеликими і знаходяться в діапазоні 0.05–0.1 на довжині хвилі 340 нм. На відміну від
вимірювань в Антарктиці, на пункті AERONET Київ відповідні значення AOT сягають понад 0.3–0.5. Використову-
ючи значення AOT з пункту Київ було оцінено прямий аерозольний радіаційний форсинг за допомогою алгоритму
GAME. Розрахунки за GAME визначають аерозольний ПРФ на рівні –5.7 Вт м–2 над поверхнею з рослинністю, коли
оптична товщина аерозолю дорівнює 0.1. Висновки. Оптична товщина аерозолю за даними AERONET в атмосфері
над пунктом Київ має середнє значення AOT, що дорівнює 0.3 (340 нм), значення АОТ над двома антарктичними
пунктами знаходяться в межах від 0.03 до 0.06. Оцінки з використанням чисельного коду (GAME) дають величини
ПРФ від –6 Вт м–2 до –14 Вт м–2 над пунктом Київ. Значення, обчислені в рамках оперативного продукту AERONET
за даними пункту Київ, становлять близько –20 Вт м–2 (нижня границя атмосфери) та близько –10 Вт м–2 (верхня
границя атмосфери) протягом 2018 року.
Ключові слова: аерозольна оптична товщина, радіаційний форсинг, AERONET, алгоритм Глобальна атмосферна мо-
дель (GAME)
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| id | nasplib_isofts_kiev_ua-123456789-168301 |
| institution | Digital Library of Periodicals of National Academy of Sciences of Ukraine |
| issn | 1727-7485 |
| language | English |
| last_indexed | 2025-12-07T18:56:14Z |
| publishDate | 2019 |
| publisher | Національний антарктичний науковий центр МОН України |
| record_format | dspace |
| spelling | Milinevsky, G. Yukhymchuk, Yu. Grytsai, A. Danylevsky, V. Wang, Yu. Choliy, V. 2020-04-29T17:25:10Z 2020-04-29T17:25:10Z 2019 Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites / G. Milinevsky, Yu. Yukhymchuk, A. Grytsai, V. Danylevsky, Yu. Wang, V. Choliy // Український антарктичний журнал. — 2019. — № 1 (18). — С. 128-138. — Бібліогр.: 37 назв. — англ. 1727-7485 https://nasplib.isofts.kiev.ua/handle/123456789/168301 551.510.42 Objectives. To analyze data on aerosol optical thickness (AOT) in the atmosphere over some Ukraine and Antarctic AERONET (AErosol RObotic NETwork) sites. To determine and compare direct aerosol radiative forcing (DRF) typical values using the data from midlatitude and Antarctic AERONET sites. Мета. Проаналізувати дані щодо аерозольної оптичної товщини (АОТ) в атмосфері на деяких пунктах мережі AERONET (AErosol RObotic NETwork) в Україні та Антарктиці. Для визначення та порівняння типових значень аерозольного прямого радіаційного форсингу (ПРФ) використати типові дані середньоширотної та двох антарктичних пунктів AERONET. This work was supported in part by State Institution National Antarctic Scientific Center, Ministry of Education and Science of Ukraine, by Main Astrono mical Observatory NAS of Ukraine, and by Taras Shev chenko National University of Kyiv project 19BF051-08. The most preparation works on the paper have been done in College of Physics, Intern ational Center of Future Science, Jilin University. We thank Philippe Dubuisson from Laboratoired’ Optique Atmosphérique (LOA) for pro viding the GAME software and valuable consultations. We thank also Brent Holben (NASA/GSFC) formanaging the AERONET program and sites, principal invest igators Anatoli Chaikovsky and Philippe Goloub (LOA) of the Vechernaya Hill site, principal investigator Rick Wagener and site manager Paul Ortega of the ARM_McMurdo site, and all observers from AERONET sites Vechernaya Hill and ARM_ McMurdo for their hard work in Antarctica. We thank Yevgeny Derimian (LOA) for valuable comments and suggestions that allow im pro ving the text of the paper. The high quality of AERONET/PHOTONS data of Kyiv site was provided by CIMEL sun-photometer calibration performed at LOA, supported by ACTRIS-2 project with funding from the European Union’s Horizon 2020 research and innovation program under grant agreement No 654109. en Національний антарктичний науковий центр МОН України Український антарктичний журнал Геокосмічні дослідження Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites Попередні порівняння прямого аерозольного радіаційного форсингу за даними станцій AERONET в Україні та Антарктиці Article published earlier |
| spellingShingle | Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites Milinevsky, G. Yukhymchuk, Yu. Grytsai, A. Danylevsky, V. Wang, Yu. Choliy, V. Геокосмічні дослідження |
| title | Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites |
| title_alt | Попередні порівняння прямого аерозольного радіаційного форсингу за даними станцій AERONET в Україні та Антарктиці |
| title_full | Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites |
| title_fullStr | Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites |
| title_full_unstemmed | Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites |
| title_short | Preliminary comparison of the direct aerosol radiative forcing over Ukraine and Antarctic AERONET sites |
| title_sort | preliminary comparison of the direct aerosol radiative forcing over ukraine and antarctic aeronet sites |
| topic | Геокосмічні дослідження |
| topic_facet | Геокосмічні дослідження |
| url | https://nasplib.isofts.kiev.ua/handle/123456789/168301 |
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