Temporal variation of 7Be and 210Pb size distributions in ambient aerosol

Winkler, R.; Dietl, F.; Frank, G.; Tschiersch, J.

doi:10.1016/s1352-2310(97)00333-6

Cited by 93 publications

(54 citation statements)

References 21 publications

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“…The increase in 210 Pb is associated with the crustal origin of mineral dust where it occurs as a typical geochemical tracer deriving both from an intrinsic component in equilibrium with the parent 226 Ra and from the indirect form produced by the 222 Rn emitted by rocks and soils usually known as excess or unsupported 210 Pb known for being highly particle-reactive and typically associated with the aerosol accumulation mode (Papastefanou and Ioannidou, 1995;Winkler et al, 1998;Gaffney et al, 2004;Ioannidou et al, 2005).…”

Section: Resultsmentioning

confidence: 99%

An outstanding Saharan dust event at Mt. Cimone (2165 m a.s.l., Italy) in March 2004

Brattich

Riccio

Tositti

et al. 2015

Atmospheric Environment

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Section: Resultsmentioning

confidence: 99%

An outstanding Saharan dust event at Mt. Cimone (2165 m a.s.l., Italy) in March 2004

Brattich

Riccio

Tositti

et al. 2015

Atmospheric Environment

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“…Such a simple approach excludes the complexity in the estimation calculations. With the measurements of 10 Be/ 7 Be, further analysis is expected to obtain more pronounced tracing signals for the air mass originated from the stratosphere or the upper troposphere.…”

Section: Discussionmentioning

confidence: 99%

“…As the source of 7 Be or 210 Pb differs prominently, the aerosol particle absorbing 7 Be in the upper atmosphere perhaps should have longer residence time than that of 210 Pb aerosol particles before two particles collision-coalescence. Winkler et al [10] reported that the aerodynamic size of 7 Be-bearing particles is usually 0.1 μm greater than that of 210 Pb-bearing particles in summer, and 7 Be-bearing particles resided longer in the atmosphere with the growth of particle coagulation. Therefore, the wet scavenging efficiency for the two isotopes-bearing particles may not be exactly same [11].…”

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confidence: 99%

Source characteristics of O3 and CO2 at Mt. Waliguan Observatory, Tibetan Plateau implied by using 7Be and 210Pb

Zheng

Wan

Tang

2010

Sci. China Earth Sci.

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The weekly averages of near-surface 7 Be, 210 Pb, O 3 , and CO 2 concentrations at the Global Atmospheric Watch Observatory, Mt. Waliguan (101.98°E, 36.287°N, 3810 m a.s.l.), from October 2002 to January 2004 are presented. With the establishment of the new datasets of DCCW (Differential Concentrations in Contiguous Weeks) of 7 Be, 210 Pb, and O 3 , CO 2 (Δ 7 Be, Δ 210 Pb, ΔO 3 , ΔCO 2 , respectively, the impacts of upper-level downward transports and land-surface emissions on O 3 and CO 2 concentrations are implied by 7 Be and 210 Pb being as independent tracers. The relations among Δ 7 Be, Δ 210 Pb, and ΔO 3 , ΔCO 2 are examined statistically and compared. The results indicate that with the DCCWs, the interferences with the tracing significance of 7 Be and 210 Pb from the seasonal wet scavenging of atmospheric aerosol are greatly reduced, and the weighting sources of O 3 or CO 2 variations are more pronounced. Basically, the variability of surface O 3 is controlled predominately by air mass transported from the upper atmosphere levels while the emission from the Continent Boundary Layer (CBL) has an obvious input for CO 2 . The relation between Δ 210 Pb and ΔO 3 reflects that influences of CBL emission are generally positive/negative for surface O 3 budget in summer/winter, and the relation of Δ 7 Be and ΔCO 2 also reveals that upper level downward transport has positive/negative inputs for CO 2 in summer/winter. With the highly correlated relations between 7 Be and O 3 , a quantitative estimation is made of the stratospheric contributions to the budget of surface O 3 at WLG: the monthly averages of stratospheric O 3 range from 6 × 10 −9 to 8 × 10 −9 (volume mixing ratio) in April and from June to August, and 2 × 10 −9 to 4 × 10 −9 in the remaining months. For the ultimate sources of the baseline concentration of surface O 3 , which consist of only stratospheric transport and tropospheric photochemistry production, the contribution from stratospheric transport is estimated to be about 20 × 10 −9 from May to July, and (12-15) × 10 −9 in the remaining months, and the total relative contribution rate is about 35% to 40%. Differential Concentrations in Contiguous Weeks (DCCW), Continent Boundary Layer (CBL) emission, downward transport from stratosphere, natural trace, WLGCitation:

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“…[6] estimated the (AMAD) of 210 Pb of 0.53 μm and [7] 0.56 μm. 210 Pb has been extensively used to determine the mean residence time of atmospheric aerosols [8], to trace chemical compound that may have broadly similar source distributions, for example sulphur [9], and to study the transport of continental aerosols across the sea or into Polar Regions [10,11].…”

Section: Introductionmentioning

confidence: 99%

Variations of²¹⁰Pb concentrations in surface air at Thessaloniki, Greece (40°N)

Ioannidou

Kotsopoulou

Karanatsiou

et al. 2012

EPJ Web of Conferences

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Atmospheric concentrations of 210 Pb were measured over the year 2009 in ground level air at Thessaloniki, Northern Greece (40 • 62 N, 22• 95 E). The mean activity concentrations of 210 Pb in surface air have been found to be 671 ± 213 μBq m −3 . The highest values of monthly atmospheric concentrations of 210 Pb were observed in the autumn and the lowest in the spring period. The higher values of 210 Pb during autumn were attributed to frequent inversion conditions of the surface layers, resulting in an enrichment of radon and its decay products in surface air. The lower values during the winter months might be due to the low emanation of radon from the frozen or snow-covered soil. The minima of 210 Pb concentrations during spring might reflect on higher washout during this period, which results in less emanation of radon from saturated with water soil, resulting in less production of 210 Pb near ground-level air. The relative high values during summer are probably due to the higher 222 Rn exhalation from the ground and due to the higher air mixing within the troposphere, which has as a result to carry down to the surface layer 210 Pb whose origin is older air masses which entered into the free troposphere. *

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Temporal variation of 7Be and 210Pb size distributions in ambient aerosol

Cited by 93 publications

References 21 publications

An outstanding Saharan dust event at Mt. Cimone (2165 m a.s.l., Italy) in March 2004

An outstanding Saharan dust event at Mt. Cimone (2165 m a.s.l., Italy) in March 2004

Source characteristics of O3 and CO2 at Mt. Waliguan Observatory, Tibetan Plateau implied by using 7Be and 210Pb

Variations of²¹⁰Pb concentrations in surface air at Thessaloniki, Greece (40°N)

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Temporal variation of 7Be and 210Pb size distributions in ambient aerosol

Cited by 93 publications

References 21 publications

An outstanding Saharan dust event at Mt. Cimone (2165 m a.s.l., Italy) in March 2004

An outstanding Saharan dust event at Mt. Cimone (2165 m a.s.l., Italy) in March 2004

Source characteristics of O3 and CO2 at Mt. Waliguan Observatory, Tibetan Plateau implied by using 7Be and 210Pb

Variations of210Pb concentrations in surface air at Thessaloniki, Greece (40°N)

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Variations of²¹⁰Pb concentrations in surface air at Thessaloniki, Greece (40°N)