Variability of black carbon deposition to the East Antarctic Plateau, 1800–2000 AD

Bisiaux, M. M.; Edwards, Ross; McConnell, Joseph R.; Albert, M. R.; Anschütz, Helgard; Neumann, Thomas; Isaksson, Elisabeth; Penner, Joyce E.

doi:10.5194/acp-12-3799-2012

Cited by 41 publications

(53 citation statements)

References 41 publications

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“…Mass concentrations of BC in snow and ice cores in Antarctica have been reported between 100 and 950 ng L −1 by optical analysis (Chýlek et al, 1992;Grenfell et al, 1994;Warren & Clarke, 1990) and between 30 and 1,300 ng L −1 by the SP2/Nebulizer system (Bisiaux, Edwards, McConnell, Albert, et al, 2012;Bisiaux, Edwards, McConnell, Curran, et al, 2012;Khan et al, 2018). Mass concentrations of BC in snow and ice cores in Antarctica have been reported between 100 and 950 ng L −1 by optical analysis (Chýlek et al, 1992;Grenfell et al, 1994;Warren & Clarke, 1990) and between 30 and 1,300 ng L −1 by the SP2/Nebulizer system (Bisiaux, Edwards, McConnell, Albert, et al, 2012;Bisiaux, Edwards, McConnell, Curran, et al, 2012;Khan et al, 2018).…”

Section: Bc Concentrations In Snow At the Syowa Stationmentioning

confidence: 99%

“…Studies have also analyzed both BC mass and number concentrations and size distributions of Denver fresh snow and Arctic snow , Sapporo snow (Ohata et al, 2013), Arctic snow Sinha et al, 2018), Alpine surface snow, Caucasus high-elevation firn, Greenland summit firn, and Himalayan surface snow (Lim et al, 2014). On the other hand, regarding the Southern Hemisphere, limited numbers of studies show the concentrations of BC in snow in Antarctica (Chýlek et al, 1987;Grenfell et al, 1994;Khan et al, 2018Khan et al, , 2019Warren & Clarke, 1990) and BC in ice core samples (Bisiaux, Edwards, McConnell, Albert, et al, 2012;Bisiaux, Edwards, McConnell, Curran, et al, 2012;Chýlek et al, 1992;McConnell et al, 2007). Recently, Khan et al (2018) reported the BC size distribution of snow samples in western Antarctica, but no study has been reported in eastern Antarctica.…”

Section: Introductionmentioning

confidence: 99%

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Concentrations and Size Distributions of Black Carbon in the Surface Snow of Eastern Antarctica in 2011

et al. 2020

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Knowledge of black carbon (BC) concentrations and size distributions within surface snow inAntarctica is limited. However, these measurements are important to understanding global aerosol transport from combustion sources, and BC contributes to positive radiative forcing. This study analyzed the concentrations and size distributions of BC and inorganic ions in snow samples collected at the Syowa station in Antarctica from April to December 2011 and along a traverse route to an inland (Mizuho) station. The BC size distributions in snow were bimodal with mass median diameters of~140 and~690 nm. We also estimated the mass median diameter from unimodal distributions and found smaller diameters than were reported by other studies. The mass concentrations of BC in snow were higher in inland samples than in Syowa samples. Among Syowa samples, the BC concentrations in December (2117.3 ng L −1 on average) were higher than in other periods (288.2 ng L −1 on average). The December samples experienced ambient temperatures above 0°C, and the atmospheric BC concentrations did not increase simultaneously. Inorganic ions originated from the ocean and decreased with increasing distance from the coastal area. We conclude that the BC concentrations in surface snow increased mainly by postdeposition processes through the loss of water mass due to melting, evaporation, and sublimation. Our study is the first to report detailed BC concentrations and size distributions in eastern Antarctica, and the results will help to evaluate BC global transport, the snow albedo estimations in this region, and the climate impacts of BC.

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Section: Bc Concentrations In Snow At the Syowa Stationmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Concentrations and Size Distributions of Black Carbon in the Surface Snow of Eastern Antarctica in 2011

et al. 2020

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“…Here we compared the past 150 years of BC for a suite of ice cores from Antarctica (Figures 8 and S6, Table 1), and we evaluated the measured fluxes against modeled BC flux [ Lee et al, 2013] to investigate temporal and spatial variations in BC fluxes. We compared the East Antarctic Law Dome record [Bisiaux et al, 2012a[Bisiaux et al, , 2012b, the West Antarctic Pine Island Glacier (PIG), Thwaites Glacier (THW) and the divide between Pine Island and Thwaites Glaciers (DIV) [Criscitiello et al, 2014] records, and the James Ross Island (JRI) record from the Antarctic Peninsula [Mulvaney et al, 2012;Arienzo et al, 2016]. approximately 1960 to the mid-1990s.…”

Section: Long-range Transportmentioning

confidence: 99%

Holocene black carbon in Antarctica paralleled Southern Hemisphere climate

et al. 2017

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Black carbon (BC) and other biomass‐burning (BB) aerosols are critical components of climate forcing, but quantification, predictive climate modeling, and policy decisions have been hampered by limited understanding of the climate drivers of BB and by the lack of long‐term records. Prior modeling studies suggested that increased Northern Hemisphere anthropogenic BC emissions increased recent temperatures and regional precipitation, including a northward shift in the Intertropical Convergence Zone (ITCZ). Two Antarctic ice cores were analyzed for BC, and the longest record shows that the highest BC deposition during the Holocene occurred ~8–6 k years before present in a period of relatively high austral burning season and low growing season insolation. Atmospheric transport modeling suggests South America (SA) as the dominant source of modern Antarctic BC and, consistent with the ice core record, climate model experiments using mid‐Holocene and preindustrial insolation simulate comparable increases in carbon loss due to fires in SA during the mid‐Holocene. SA climate proxies document a northward shifted ITCZ and weakened SA Summer Monsoon (SASM) during this period, with associated impacts on hydroclimate and burning. A second Antarctic ice core spanning the last 2.5 k years documents similar linkages between hydroclimate and BC, with the lowest deposition during the Little Ice Age characterized by a southerly shifted ITCZ and strengthened SASM. These new results indicate that insolation‐driven changes in SA hydroclimate and BB, likely linked to the position of the ITCZ, modulated Antarctic BC deposition during most of the Holocene and suggests connections and feedbacks between future BC emissions and hydroclimate.

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“…Measurements of actual impurity concentrations in snowpacks and glaciers have been conducted on different spatial and temporal scales in natural conditions by for example Clarke and Noone (1985); McConnell et al (2007); Ming et al (2008); Xu et al (2009) ;Forsström et al (2009); Doherty et al (2010); Kaspari et al (2011);Bisiaux et al (2012); Meinander et al (2013); Svensson et al (2013); Dagsson-Waldhauserova et al (2015). Furthermore, to observe the effects of impurities on the snow, several experimental studies have been conducted (Conway et al, 1996;Brandt et al, 2011;Hadley and Kirchstetter, 2012).…”

Section: J I Peltoniemi Et Al: Reflectance Of Contaminated Snowmentioning

confidence: 99%

Soot on Snow experiment: bidirectional reflectance factor measurements of contaminated snow

et al. 2015

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Abstract. In order to quantify the effects of absorbing contaminants on snow, a series of spectral reflectance measurements were conducted. Chimney soot, volcanic sand, and glaciogenic silt were deposited on a natural snow surface in a controlled way as a part of the Soot on Snow (SoS) campaign. The bidirectional reflectance factors of these soiled surfaces and untouched snow were measured using the Finnish Geodetic Institute's Field Goniospectropolariradiometer, FIGIFIGO.A remarkable feature is the fact that the absorbing contaminants on snow enhanced the metamorphism of snow under strong sunlight in our experiments. Immediately after deposition, the contaminated snow surface appeared darker than the natural snow in all viewing directions, but the absorbing particles sank deep into the snow in minutes. The nadir measurement remained the darkest, but at larger zenith angles, the surface of the contaminated snow changed back to almost as white as clean snow. Thus, for a ground observer the darkening caused by impurities can be completely invisible, overestimating the albedo, but a nadir-observing satellite sees the darkest points, underestimating the albedo. Through a reciprocity argument, we predict that at noon, the albedo perturbation should be lower than in the morning or afternoon. When sunlight stimulates sinking more than melting, the albedo should be higher in the afternoon than in the morning, and vice versa when melting dominates. However, differences in the hydrophobic properties, porosity, clumping, or size of the impurities may cause different results than observed in these measurements.

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Variability of black carbon deposition to the East Antarctic Plateau, 1800–2000 AD

Abstract: Abstract. Refractory black carbon aerosols (rBC) from biomass burning and fossil fuel combustion are deposited to the Antarctic ice sheet and preserve a history of emissions and long-range transport from low-and mid-latitudes.

Cited by 41 publications

References 41 publications

Concentrations and Size Distributions of Black Carbon in the Surface Snow of Eastern Antarctica in 2011

Concentrations and Size Distributions of Black Carbon in the Surface Snow of Eastern Antarctica in 2011

Holocene black carbon in Antarctica paralleled Southern Hemisphere climate

Soot on Snow experiment: bidirectional reflectance factor measurements of contaminated snow

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