Frequent ultrafine particle formation and growth in Canadian Arctic marine and coastal environments

Collins, Douglas B.; Burkart, Julia; Chang, Rachel Y.-­W.; Lizotte, Martine; Boivin-Rioux, Aude; Blais, Marjolaine; Mungall, Emma L.; Boyer, Matthew; Irish, Victoria E.; Massé, Guillaume; Kunkel, Daniel; Tremblay, Jean‐Éric; Papakyriakou, Tim; Bertram, Allan K.; Bozem, Heiko; Gosselin, Michel; Levasseur, Maurice; Abbatt, Jonathan P. D.

doi:10.5194/acp-17-13119-2017

Cited by 55 publications

(87 citation statements)

References 110 publications

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“…The values of

\overset{δ_{P}}{true}

and

\overset{δ_{P}}{true}

were nearly zero below an altitude of 4 km, especially during the summer months;

\overset{δ_{P}}{true}

had minimum values in July and August (Figure b), corresponding to the largest lidar‐observed

\overset{β_{M 532}}{true}

values (Figure a). Observations in the Arctic boundary layer have shown active particle formation during the summer (Collins et al, ; Freud et al, ; Tunved et al, ). At higher altitudes, Scheuer et al () reported a sharp increase in the mixing ratio of sulfate ions in free tropospheric fine aerosol particles over the Arctic during March.…”

Section: Discussionmentioning

confidence: 99%

Seasonal Variations in High Arctic Free Tropospheric Aerosols Over Ny‐Ålesund, Svalbard, Observed by Ground‐Based Lidar

et al. 2018

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Free tropospheric aerosols over the high Arctic were observed by lidar for about 4 years from March 2014 at Ny-Ålesund (78. 9°N, 11.9°E). Vertical profiles of aerosol backscattering coefficients at two wavelengths, 532 and 1,064 nm, and depolarization ratio at one wavelength, 532 nm, are derived from these observations. The aerosol backscattering coefficient, the particle depolarization ratio, and the color ratio (the ratio of the backscattering coefficients at the two wavelengths) are roughly proportional to mass concentration, nonsphericity, and size of the aerosol particles, respectively. The aerosol backscattering coefficients indicate that monthly averaged concentration of aerosols was largest in the lowest free troposphere at about 1 km in altitude and was an order of magnitude less at an about 10 km in altitude and that the concentration of aerosols was highest from late spring to summer and lowest from late summer to fall. The depolarization ratio was less than a few percent in the troposphere during the four observed years. The depolarization ratio and the color ratio were greatest from winter to spring and smallest from summer to fall. The maxima in the monthly averaged nonsphericity and size precede the maxima in the monthly averaged concentration by a few months, indicating a seasonal change in the morphology or the characteristics of the aerosol particles. The small particle depolarization ratio of less than a few percent is consistent with previous findings that Arctic free tropospheric aerosol particles in spring are composed of a mixture of liquid phase sulfate and soot particles.Space-borne instruments, such as the Cloud-Aerosol Lidar with Orthogonal Polarization (CALIOP) onboard the Cloud-Aerosol Lidar and Infrared Pathfinder Satellite Observation (CALIPSO) satellite or the Stratospheric Gas Experiment (SAGE), provide observations of the global distribution of aerosols, including in the Arctic region, and their temporal variations. Observations of the Arctic region from space, however, are significantly affected by its unique condition of having very different background solar radiation levels

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“…The values of

\overset{δ_{P}}{true}

and

\overset{δ_{P}}{true}

were nearly zero below an altitude of 4 km, especially during the summer months;

\overset{δ_{P}}{true}

had minimum values in July and August (Figure b), corresponding to the largest lidar‐observed

\overset{β_{M 532}}{true}

Section: Discussionmentioning

confidence: 99%

Seasonal Variations in High Arctic Free Tropospheric Aerosols Over Ny‐Ålesund, Svalbard, Observed by Ground‐Based Lidar

et al. 2018

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“…Some observations in productive marine areas of the Canadian Arctic Archipelago have indicated higher growth rates (Burkart, Hodshire, et al, ; Collins et al, ). Two years of ship‐based observations indicated a mean apparent growth rate of 4.3 ± 4.1 nm/hr, with some events of ≥10 nm/hr (Collins et al, ). The impact of Arctic anthropogenic emissions from petroleum extraction has been shown to influence particle growth rates; at Utqiaġvik air masses from Prudhoe Bay showed a higher mean growth rate (2.7 ± 2.5 nm/hr) and more frequent particle formation compared to clean marine air masses (1.8 ± 1.5 nm/hr; Kolesar et al, ).…”

Section: Regional Arctic Processesmentioning

confidence: 99%

Processes Controlling the Composition and Abundance of Arctic Aerosol

Willis

Leaitch

Abbatt

2018

Reviews of Geophysics

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143

154

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The Arctic region is a harbinger of global change and is warming at a rate higher than the global average. While Arctic warming is driven by increases in anthropogenic greenhouse gases' in combination with local feedback mechanisms, short‐lived climate forcing agents, such as tropospheric aerosol, are also important drivers of Arctic climate. Arctic aerosol‐climate impacts vary seasonally as a result of the interplay between aerosol and different cloud types, available solar radiation, sea ice, surface albedo, Arctic and lower latitude removal processes, and atmospheric transport patterns. Photochemistry and efficient wet aerosol removal have low impact in winter but become important in spring to summer, dramatically altering aerosol chemical composition, and driving the size distribution from a pronounced accumulation mode toward a dominance of smaller particles. Retreating sea ice, increasing solar insolation and warmer temperatures in summer result in enhanced emissions from Arctic marine and terrestrial ecosystems, and anthropogenic sources, with impacts on the composition of gas and particle phases. Fractional cloud cover reaches a maximum in Arctic summer, in parallel with decreasing sea ice extent and surface albedo. This seasonal variation corresponds to significant changes in the net cloud radiative effect; changes that are affected by aerosol. This review summarizes our current knowledge of processes that control Arctic aerosol properties. We highlight both natural and anthropogenic processes that will be impacted by current and future sea ice loss. Efforts are needed to better constrain aerosol removal rates, characterize aerosol precursors, and constrain the seasonality and magnitude of aerosol‐cloud‐climate impacts.

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“…Melt pond water temperatures and salinities varied between 0.21 and 1.86 • C and between 0.2 and 8.5, respectively. Chl a concentrations were (Cox and Weeks, 1983;Petrich and Eicken, 2010).…”

Section: Physical Chemical and Biological Characteristics Of The Mementioning

confidence: 99%

“…Clean Arctic air masses allow ultrafine (5-20 nm diameter) particle formation and the potential growth of secondary marine organic aerosols (including DMS-derived particles) into CCN (Willis et al, 2016). Hence, the Arctic is a favourable terrain for new particle formation from biogenic DMS Rempillo et al, 2011;Collins et al, 2017;Giamarelou et al, 2016;Mungall et al, 2016;Willis et al, 2016).…”

Section: Introductionmentioning

confidence: 99%

Dimethyl sulfide dynamics in first-year sea ice melt ponds in the Canadian Arctic Archipelago

et al. 2018

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Abstract. Melt pond formation is a seasonal pan-Arctic process. During the thawing season, melt ponds may cover up to 90 % of the Arctic first-year sea ice (FYI) and 15 to 25 % of the multi-year sea ice (MYI). These pools of water lying at the surface of the sea ice cover are habitats for microorganisms and represent a potential source of the biogenic gas dimethyl sulfide (DMS) for the atmosphere. Here we report on the concentrations and dynamics of DMS in nine melt ponds sampled in July 2014 in the Canadian Arctic Archipelago. DMS concentrations were under the detection limit (< 0.01 nmol L −1 ) in freshwater melt ponds and increased linearly with salinity (r s = 0.84, p ≤ 0.05) from ∼ 3 up to ∼ 6 nmol L −1 (avg. 3.7 ± 1.6 nmol L −1 ) in brackish melt ponds. This relationship suggests that the intrusion of seawater in melt ponds is a key physical mechanism responsible for the presence of DMS. Experiments were conducted with water from three melt ponds incubated for 24 h with and without the addition of two stable isotope-labelled precursors of DMS (dimethylsulfoniopropionate), (D6-DMSP) and dimethylsulfoxide ( 13 C-DMSO). Results show that de novo biological production of DMS can take place within brackish melt ponds through bacterial DMSP uptake and cleavage. Our data suggest that FYI melt ponds could represent a reservoir of DMS available for potential flux to the atmosphere. The importance of this ice-related source of DMS for the Arctic atmosphere is expected to increase as a response to the thinning of sea ice and the areal and temporal expansion of melt ponds on Arctic FYI.

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Frequent ultrafine particle formation and growth in Canadian Arctic marine and coastal environments

Cited by 55 publications

References 110 publications

Seasonal Variations in High Arctic Free Tropospheric Aerosols Over Ny‐Ålesund, Svalbard, Observed by Ground‐Based Lidar

Seasonal Variations in High Arctic Free Tropospheric Aerosols Over Ny‐Ålesund, Svalbard, Observed by Ground‐Based Lidar

Processes Controlling the Composition and Abundance of Arctic Aerosol

Dimethyl sulfide dynamics in first-year sea ice melt ponds in the Canadian Arctic Archipelago

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