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Ionic composition of atmospheric aerosol and wet deposition in Novosibirsk region
~ Pergamon
J. AtroJoi SCI., Vol. 21, 5uppl. I, pp . 5111-5112, 1996
PU: 80021-8502(96)00128-0
Copynghl il:l 1996 Elsevier Science Ltd Printed in Greet Britain. All righta reserved oo21·g502/96 $15.00 + 0.00
IONIC COMPOSITION OF ATMOSPHERIC AEROSOL AND WET DEPOSITION IN NOVOSIBIRSK REGION. B.S.Smolyakov, L.APavluik, K.P.Koutsenogii,* and V.I.Makarov*. Institute of Inorganic Chemistry, Institute of Chemical Kinetics and Combustion* of SB RAN, 630090 Novosibirsk, Russia. KEYWORDS
Aerosol;Wet Deposition; Ionic Composition;Acidity. Vast expanse of Siberia, playing the detectable role to global processes of atmospheric transfere, is still scantify known in regard to the chemical composition and acidity of atmospheric components. Presented studies are a part of a complex project " Siberian aerosols" and continue the studies performed by us in 1992 in Novosibirsk region. In 1994-96 the observations were carried out at the follows sites: site N21 near village Zavyalovo, 90 krn to the South-South-West from Novosibirsk; site N2 2 near Akademgorodok, 30 km to the South-South- East from Novosibirsk. Aerosol sampling was performed using AFA-CA filters. Volumetric rate was 13 m 3/h, sampling time was 24 h. After exposition a part of filter is placed in deionized water (510 cm 3) for 24 h. Rain samples were analysed just after rainfall, snow samples were studied after thawing. We used: ion chromatographic technique for analysis of F ,Cl ,
N0 3
,
SO~
; ion selective electrodes
conductometric titration for
(Ca 2
for determination of pH , NH., Na , K ;
+ Mg 2 ) and potentiometric titration for
determination of HCO 3' Specific electric conductivity, Xexp, of water samples was measured, too. The data of analysis were used to calculate the balance of rAn anions and I:Cat cations as well as Xeal. TIle discrepancy between ~l and LCat was no more than 15%, and between Xexp and leal no more than 20%. This testifies to the fact that the ion analysed are the main fraction of the ion composition of wet depositions (WD) and of water soluble part of aerosol (WSPA).For rain depositions (site N2 1, 32 samples in 1994, 25 samples in 1995) the values of pH varied from 4.5 to 7.2 ,for snow depositions (site N2 2, 33 samples inI994-95,19 samples in 1995-96) these varied from 4.65 to 7.4 ,and the mean values were 5.53, 5.25, 5.76 and 5.71, respectively. For discrete WD samples, more acidity, as a rule, agrees with less Xexp. The values of pH of WDPA varied from 5.0 to 6.3 at mean values 5.5 both in summer and in winter. This indicate to the absence of constant factors of WD "acidification" at observation sites. It is interesting to correlate the ion composition of aerosol and wet deposition obtained in synchronous observations. TIlls correlation has much potential for yielding infomlation about processes of its formation and atmospheric transfer. For this purpose we will consider the contribution of each ion to total composition in terms of equivalent concentration. Sill
S112
Abstracts of the 1996 European Aerosol Conference
The distribution of ions (without H+ and HCO-3 ) in WD and WCPA are tabulated below as percentages of equivalent of given ion to 1:Cat or 1:An, respectively. Summary ion concentration, 1: (mg-eqv/dm! for WD, and ug-eqv/m! for WCPA), and a portion (%) ofWCPA in total aerosol mass, B, are shown, too. Ionic composition of WCPA and WD in Novosibirsk region is different from usual continental one. Sulphate dominates in WCPA, but not in WD, which contain a great portion of CI- and NO; . A part of lithophylic Ca 2+, Mg 2+, N a + among cations is much above than of NH; -ion for WCPA both in summer and in winter and for WD (snow) in winter. Table. Ionic composition of WD and WCPA in sites winter. Sites Period
Ca 2+
N21 and N2 2 in summer and in SO;-
1:
B
wet depositions (WD) 31.2 12.8 3.5 29.5 20.2
43.8
193
-
NH+4
Na+
K+
F- C1- NO;
+M g 2+ N21
N22 N21 N22 N~l
N!l
N22 N22
summer 1994 winter 1994-95 summer 1995 winter 1995-96 24.0613.07.95 21.0807.09.95 18.0802.09.95 29.1128.12.95
16.4
33.5
8.7
16.8
55.9
15.1
3.9 40.9 30.7
23.1
331
-
18.1
41.9
21.5
12.1
1.9 24.7 17.9
54.3
198
-
50.6
11.6
31.5
6.2
3.6 35.8 19.4
39.0
301
-
44.7
1.9
35.7
12.0
48.9
3.3
3.0
47.7
21.0
24.3
37.2
11.6
45.7
aerosols lWCPA) 45.4 8.4 2.4 7.6 16.8
73.1
0.218 14.2
4.7 16.2
76.2
0.102 9.1
7.0
1.7 12.2 6.6
79.6
0.125 10.5
5.4
1.8
4.2 14.5
79.6
0.169 30.6
It is believed that these features are due to the atmospheric transfere of mineral salts from some South-West regions where the intense processes of the saline soils scattering occure.
REFERENCES Koutsenogii KP.(1994) Opt.atm. i okean. 7, NQ8, 1015-1019 Koutsenogii KP., Bufetov N.S. et al. (1994) Meteorolog. i gidrolog., N28, 38-43 Smolyakov B.S., Pavluik L.A., et al. (1996) Opt. atm. i okean lin press;'
J. AtroJoi SCI., Vol. 21, 5uppl. I, pp . 5111-5112, 1996
PU: 80021-8502(96)00128-0
Copynghl il:l 1996 Elsevier Science Ltd Printed in Greet Britain. All righta reserved oo21·g502/96 $15.00 + 0.00
IONIC COMPOSITION OF ATMOSPHERIC AEROSOL AND WET DEPOSITION IN NOVOSIBIRSK REGION. B.S.Smolyakov, L.APavluik, K.P.Koutsenogii,* and V.I.Makarov*. Institute of Inorganic Chemistry, Institute of Chemical Kinetics and Combustion* of SB RAN, 630090 Novosibirsk, Russia. KEYWORDS
Aerosol;Wet Deposition; Ionic Composition;Acidity. Vast expanse of Siberia, playing the detectable role to global processes of atmospheric transfere, is still scantify known in regard to the chemical composition and acidity of atmospheric components. Presented studies are a part of a complex project " Siberian aerosols" and continue the studies performed by us in 1992 in Novosibirsk region. In 1994-96 the observations were carried out at the follows sites: site N21 near village Zavyalovo, 90 krn to the South-South-West from Novosibirsk; site N2 2 near Akademgorodok, 30 km to the South-South- East from Novosibirsk. Aerosol sampling was performed using AFA-CA filters. Volumetric rate was 13 m 3/h, sampling time was 24 h. After exposition a part of filter is placed in deionized water (510 cm 3) for 24 h. Rain samples were analysed just after rainfall, snow samples were studied after thawing. We used: ion chromatographic technique for analysis of F ,Cl ,
N0 3
,
SO~
; ion selective electrodes
conductometric titration for
(Ca 2
for determination of pH , NH., Na , K ;
+ Mg 2 ) and potentiometric titration for
determination of HCO 3' Specific electric conductivity, Xexp, of water samples was measured, too. The data of analysis were used to calculate the balance of rAn anions and I:Cat cations as well as Xeal. TIle discrepancy between ~l and LCat was no more than 15%, and between Xexp and leal no more than 20%. This testifies to the fact that the ion analysed are the main fraction of the ion composition of wet depositions (WD) and of water soluble part of aerosol (WSPA).For rain depositions (site N2 1, 32 samples in 1994, 25 samples in 1995) the values of pH varied from 4.5 to 7.2 ,for snow depositions (site N2 2, 33 samples inI994-95,19 samples in 1995-96) these varied from 4.65 to 7.4 ,and the mean values were 5.53, 5.25, 5.76 and 5.71, respectively. For discrete WD samples, more acidity, as a rule, agrees with less Xexp. The values of pH of WDPA varied from 5.0 to 6.3 at mean values 5.5 both in summer and in winter. This indicate to the absence of constant factors of WD "acidification" at observation sites. It is interesting to correlate the ion composition of aerosol and wet deposition obtained in synchronous observations. TIlls correlation has much potential for yielding infomlation about processes of its formation and atmospheric transfer. For this purpose we will consider the contribution of each ion to total composition in terms of equivalent concentration. Sill
S112
Abstracts of the 1996 European Aerosol Conference
The distribution of ions (without H+ and HCO-3 ) in WD and WCPA are tabulated below as percentages of equivalent of given ion to 1:Cat or 1:An, respectively. Summary ion concentration, 1: (mg-eqv/dm! for WD, and ug-eqv/m! for WCPA), and a portion (%) ofWCPA in total aerosol mass, B, are shown, too. Ionic composition of WCPA and WD in Novosibirsk region is different from usual continental one. Sulphate dominates in WCPA, but not in WD, which contain a great portion of CI- and NO; . A part of lithophylic Ca 2+, Mg 2+, N a + among cations is much above than of NH; -ion for WCPA both in summer and in winter and for WD (snow) in winter. Table. Ionic composition of WD and WCPA in sites winter. Sites Period
Ca 2+
N21 and N2 2 in summer and in SO;-
1:
B
wet depositions (WD) 31.2 12.8 3.5 29.5 20.2
43.8
193
-
NH+4
Na+
K+
F- C1- NO;
+M g 2+ N21
N22 N21 N22 N~l
N!l
N22 N22
summer 1994 winter 1994-95 summer 1995 winter 1995-96 24.0613.07.95 21.0807.09.95 18.0802.09.95 29.1128.12.95
16.4
33.5
8.7
16.8
55.9
15.1
3.9 40.9 30.7
23.1
331
-
18.1
41.9
21.5
12.1
1.9 24.7 17.9
54.3
198
-
50.6
11.6
31.5
6.2
3.6 35.8 19.4
39.0
301
-
44.7
1.9
35.7
12.0
48.9
3.3
3.0
47.7
21.0
24.3
37.2
11.6
45.7
aerosols lWCPA) 45.4 8.4 2.4 7.6 16.8
73.1
0.218 14.2
4.7 16.2
76.2
0.102 9.1
7.0
1.7 12.2 6.6
79.6
0.125 10.5
5.4
1.8
4.2 14.5
79.6
0.169 30.6
It is believed that these features are due to the atmospheric transfere of mineral salts from some South-West regions where the intense processes of the saline soils scattering occure.
REFERENCES Koutsenogii KP.(1994) Opt.atm. i okean. 7, NQ8, 1015-1019 Koutsenogii KP., Bufetov N.S. et al. (1994) Meteorolog. i gidrolog., N28, 38-43 Smolyakov B.S., Pavluik L.A., et al. (1996) Opt. atm. i okean lin press;'