# Overview: Recent advances in the understanding of the northern Eurasian environments and of the urban air quality in China-a Pan-Eurasian Experiment (PEEX) programme perspective

Hanna K. Lappalainen, Tuukka Petäjä, Timo Vihma, Jouni Räisänen, Alexander Baklanov, Sergey R. Chalov, Igor Esau, Ekaterina Ezhova, Matti Leppäranta, Dimitry V. Pozdnyakov, et al.

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## ► To cite this version:

Hanna K. Lappalainen, Tuukka Petäjä, Timo Vihma, Jouni Räisänen, Alexander Baklanov, et al. Overview: Recent advances in the understanding of the northern Eurasian environments and of the urban air quality in China-a Pan-Eurasian Experiment (PEEX) programme perspective. Atmospheric Chemistry and Physics, 2022, 22 (7), pp.4413-4469. 10.5194/acp-22-4413-2022. hal-03673629

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Submitted on 21 May 2022

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# Overview: Recent advances in the understanding of the northern Eurasian environments and of the urban air quality in China – a Pan-Eurasian Experiment (PEEX) programme perspective

Hanna K. Lappalainen<sup>1,36</sup>, Tuukka Petäjä<sup>1</sup>, Timo Vihma<sup>2</sup>, Jouni Räisänen<sup>1</sup>, Alexander Baklanov<sup>3</sup>, Sergey Chalov<sup>4</sup>, Igor Esau<sup>5,44</sup>, Ekaterina Ezhova<sup>1</sup>, Matti Leppäranta<sup>1</sup>, Dmitry Pozdnyakov<sup>6,23</sup>, Jukka Pumpanen<sup>7</sup>, Meinrat O. Andreae<sup>8,41,42</sup>, Mikhail Arshinov<sup>9</sup>, Eija Asmi<sup>2</sup>, Jianhui Bai<sup>10</sup>, Igor Bashmachnikov<sup>6</sup>, Boris Belan<sup>9</sup>, Federico Bianchi<sup>1</sup>, Boris Biskaborn<sup>11</sup>, Michael Boy<sup>1</sup>, Jaana Bäck<sup>12</sup>, Bin Cheng<sup>2</sup>, Natalia Chubarova<sup>4</sup>, Jonathan Duplissy<sup>1,43</sup>, Egor Dyukarev<sup>13</sup>, Konstantinos Eleftheriadis<sup>14</sup>, Martin Forsius<sup>15</sup>, Martin Heimann<sup>16</sup>, Sirkku Juhola<sup>19</sup>, Vladimir Konovalov<sup>17</sup>, Igor Konovalov<sup>18</sup>, Pavel Konstantinov<sup>4,32</sup>, Kajar Köster<sup>12</sup>, Elena Lapshina<sup>20</sup>, Anna Lintunen<sup>1,12</sup>, Alexander Mahura<sup>1</sup>, Risto Makkonen<sup>2</sup>, Svetlana Malkhazova<sup>4</sup>, Ivan Mammarella<sup>1</sup>, Stefano Mammola<sup>21,22</sup>, Stephany Buenrostro Mazon<sup>1</sup>, Outi Meinander<sup>2</sup>, Eugene Mikhailov<sup>23,24</sup>, Victoria Miles<sup>5</sup>, Stanislav Myslenkov<sup>4</sup>, Dmitry Orlov<sup>4</sup>, Jean-Daniel Paris<sup>25</sup>, Roberta Pirazzini<sup>2</sup>, Olga Popovicheva<sup>26</sup>, Jouni Pulliainen<sup>2</sup>, Kimmo Rautiainen<sup>2</sup>, Torsten Sachs<sup>27</sup>, Vladimir Shevchenko<sup>28</sup>, Andrey Skorokhod<sup>29</sup>, Andreas Stohl<sup>30</sup>, Elli Suhonen<sup>1</sup>, Erik S. Thomson<sup>31</sup>, Marina Tsidilina<sup>38</sup>, Veli-Pekka Tynkkynen<sup>33</sup>, Petteri Uotila<sup>1</sup>, Aki Virkkula<sup>2</sup>, Nadezhda Voropay<sup>34</sup>, Tobias Wolf<sup>5</sup>, Sayaka Yasunaka<sup>35</sup>, Jiahua Zhang<sup>36</sup>, Yubao Qiu<sup>36</sup>, Aijun Ding<sup>37</sup>, Huadong Guo<sup>36</sup>, Valery Bondur<sup>38</sup>, Nikolay Kasimov<sup>4</sup>, Sergej Zilitinkevich<sup>1,2,45,†</sup>, Veli-Matti Kerminen<sup>1</sup>, and Markku Kulmala<sup>1,39,40</sup>

<footnote n="1"><sup>1</sup>Institute for Atmospheric and Earth System Research/Physics, Faculty of Science, University of Helsinki, Helsinki, P.O. Box 64, 00014, Finland</footnote>

<footnote n="2"><sup>2</sup>Finnish Meteorological Institute, 00101 Helsinki, Finland</footnote>

<footnote n="3"><sup>3</sup>Science and Innovation Department, World Meteorological Organization, WMO, Geneva, Switzerland</footnote>

<footnote n="4"><sup>4</sup>Faculty of Geography, Lomonosov Moscow State University, 1 Leninskiye gory, Moscow, 119991, Russia</footnote>

<footnote n="5"><sup>5</sup>Nansen Environmental and Remote Sensing Center/Bjerknes Centre for Climate Research, Bergen, Norway</footnote>

<footnote n="6"><sup>6</sup>Nansen International Environmental and Remote Sensing Centre, Nansen Centre, NIERSC, 14th Line 7, office 49, Vasilievsky Island, 199034, St. Petersburg, Russia</footnote>

<footnote n="7"><sup>7</sup>Department of Environmental and Biological Sciences, P.O. Box 1627 (Address: Yliopistonranta 1 E), 70211 Kuopio, Finland</footnote>

<footnote n="8"><sup>8</sup>Max Planck Institute for Chemistry, Mainz, Germany</footnote>

<footnote n="9"><sup>9</sup>V. E. Zuev Institute of Atmospheric Optics (IAO) SB RAS, Tomsk, 634055, Russia</footnote>

<footnote n="10"><sup>10</sup>LAGEO, Institute of Atmospheric Physics, Chinese Academy of Sciences (IAP-CAS), Beijing, 100029, China</footnote>

<footnote n="11"><sup>11</sup>Alfred Wegener Institute, Helmholtz Centre for Polar and Marine Research, Potsdam, Germany</footnote>

<footnote n="12"><sup>12</sup>Institute for Atmospheric and Earth System Research/Forest Sciences, Faculty of Agriculture and Forestry, P.O. Box 64, 00014, University of Helsinki, Helsinki, Finland</footnote>

<footnote n="13"><sup>13</sup>Institute of Monitoring of Climatic Ecological Systems SB RAS, Tomsk, 634055, Russia</footnote>

<footnote n="14"><sup>14</sup>ERL, Institute of Nuclear and Radiological Science & Technology, Energy & Safety, NCSR Demokritos, Attiki, Greece</footnote>

<footnote n="15"><sup>15</sup>Finnish Environment Institute SYKE, Latokartanonkaari 11, 00790 Helsinki, Finland</footnote>

<footnote n="16"><sup>16</sup>Max Planck Institute for Biogeochemistry, Jena, Germany</footnote>

<footnote n="17"><sup>17</sup>Institute of Geography RAS, Moscow, Russia</footnote>

<footnote n="18"><sup>18</sup>Institute of Applied Physics, Nizhny Novgorod, Russia</footnote>
<sup>19</sup>Faculty of Biological and Environmental Sciences,
P.O. Box 64, 00014, University of Helsinki, Helsinki, Finland

<sup>20</sup>Yugra State University, Khanty-Mansiysk, 634012, Russia

<sup>21</sup>Finnish Museum of Natural History (LUOMUS), University of Helsinki, 00100 Helsinki, Finland

<sup>22</sup>Molecular Ecology Group (MEG), Water Research Institute (IRSA), National Research Council of Italy,
(CNR), Verbania Pallanza, 28922, Italy

<sup>23</sup>St. Petersburg State University, 7/9 Universitetskaya nab, St. Petersburg, 199034, Russia

<sup>24</sup>Multiphase Chemistry and Biogeochemistry Departments, Max Planck Institute for Chemistry,
55020 Mainz, Germany

<sup>25</sup>Laboratoire des Sciences du Climat et de l'Environnement, IPSL CEA-CNRS-UVSQ,
91190 Gif-sur-Yvette, France

<sup>26</sup>Institute of Nuclear Physics, Lomonosov Moscow State University, 119991, Moscow, Russia

<sup>27</sup>GFZ German Research Centre for Geosciences, Telegrafenberg, Potsdam, Germany

<sup>28</sup>Shirshov Institute of Oceanology, Russian Academy of Sciences, Moscow, Russia

<sup>29</sup>A. M. Obukhov Institute of Atmospheric Physics, 119017, Moscow, Russia

<sup>30</sup>Department of Meteorology and Geophysics, University of Vienna, Vienna, Austria

<sup>31</sup>Department of Chemistry & Molecular Biology, University of Gothenburg, 41296, Göteborg, Sweden

<sup>32</sup>Peoples' Friendship University of Russia (RUDN), Laboratory of Smart technologies for sustainable development of urban environment under global changes, Moscow, Russian Federation

<sup>33</sup>Aleksanteri Institute, University of Helsinki, Helsinki, Finland

<sup>34</sup>V B Sochava Institute of Geography SB RAS, Irkutsk, 664033, Russia

<sup>35</sup>Japan Agency for Marine-Earth Science and Technology (JAMSTEC), Yokosuka, Japan

<sup>36</sup>Aerospace Information Research Institute, Chinese Academy of Sciences, Beijing, 100094, China

<sup>37</sup>Joint International Laboratory of Atmospheric and Earth System sciences (JirLATEST),
Nanjing University, Nanjing, China

<sup>38</sup>Institute for Scientific Research of Aerospace Monitoring "AEROCOSMOS", Moscow, 105064, Russia

<sup>39</sup>Aerosol and Haze Laboratory, Beijing Advanced Innovation Center for Soft Matter Sciences and
Engineering, Beijing University of Chemical Technology (BUCT), Beijing, China

<sup>40</sup>Guangzhou Institute of Geography, Guangzhou Academy of Sciences, Guangzhou, China

<sup>41</sup>Department of Geology and Geophysics, King Saud University, Riyadh, Saudi Arabia

<sup>42</sup>Scripps Institution of Oceanography, UCSD, La Jolla, CA, USA

<sup>43</sup>Helsinki Institute of Physics, University of Helsinki, 00014 Helsinki, Finland

<sup>44</sup>Institute for Physics and Technology, Norwegian Arctic University – University in Tromsø,
9037, Tromsø, Norway

<sup>45</sup>Department of Cryosphere, Tyumen State University, Tyumen, 625003, Russia

†deceased, 15 February 2021

**Correspondence:** Hanna K. Lappalainen (hanna.k.lappalainen@helsinki.fi) and Veli-Matti Kerminen
(veli-matti.kerminen@helsinki.fi)

Received: 22 April 2021 – Discussion started: 19 May 2021

Revised: 26 October 2021 – Accepted: 5 November 2021 – Published: 6 April 2022

**Abstract.** The Pan-Eurasian Experiment (PEEX) Science Plan, released in 2015, addressed a need for a holistic system understanding and outlined the most urgent research needs for the rapidly changing Arctic-boreal region. Air quality in China, together with the long-range transport of atmospheric pollutants, was also indicated as one of the most crucial topics of the research agenda. These two geographical regions, the northern Eurasian Arctic-boreal region and China, especially the megacities in China, were identified as a "PEEX region". It is also important to recognize that the PEEX geographical region is an area where science-based policy actions would have significant impacts on the global climate. This paper summarizes results obtained during the last 5 years in the northern Eurasian region, together with recent observations of the air quality in the urban environments in China, in the context of the PEEX programme. The main regions of interest are the Russian Arctic, northern Eurasian boreal forests (Siberia) and peatlands, and the megacities in China. We frame our analysis against research themes introduced in the PEEX Science Plan in 2015. We summarize recent progress towards an enhanced holistic understanding of the land-atmosphere-ocean systems feedbacks. We conclude that although the scientific knowledge in these regions has increased, the new results are in many cases insufficient, and there
are still gaps in our understanding of large-scale climate-Earth surface interactions and feedbacks. This arises from limitations in research infrastructures, especially the lack of coordinated, continuous and comprehensive in situ observations of the study region as well as integrative data analyses, hindering a comprehensive system analysis. The fast-changing environment and ecosystem changes driven by climate change, socio-economic activities like the China Silk Road Initiative, and the global trends like urbanization further complicate such analyses. We recognize new topics with an increasing importance in the near future, especially “the enhancing biological sequestration capacity of greenhouse gases into forests and soils to mitigate climate change” and the “socio-economic development to tackle air quality issues”.

# 1 Introduction

The Earth system is facing major challenges, including climate change, biodiversity loss, ocean acidification, epidemics and energy demand on a global scale (Ripple et al., 2017). These “Grand Challenges” are highly connected and interlinked. This creates a need for an approach of a multi-disciplinary scientific programme, which could deliver science-based messages to fast-tracked policy making (Kulmala et al., 2015). The recent estimates based on observed atmospheric concentrations of CO₂ (https://gml.noaa.gov/ccgg/trends/trends_log.html, last access: 17 January 2022) and business-as-usual scenarios show that humankind should find solutions to answer the Grand Challenges (IPCC, 2021). Deep understanding of the feedbacks and interactions between the land, atmosphere and ocean domains and accounting for social aspects in the regions of substantial changes are needed for effective technical solutions, mitigation and adaption policy actions. The northern regions (> 45° N), together with the Arctic coastal zone and Siberian region in Russia, are among the most critical areas for the global climate (Smith, 2011; Kulmala et al., 2015).

The idea of the Pan-Eurasian Experiment (PEEX) (https://www.atm.helsinki.fi/peex/, last access: 17 January 2022), originating from a group of Finnish and Russian scientists and research organizations in 2012, is a bottom-up research and capacity building programme concentrating on the sustainable development of the Arctic-boreal regions of northern Eurasia under changing climate and socio-economic megatrends (Kulmala et al., 2015; Lappalainen et al., 2016). The programme was based on four interconnected parts, namely research agenda, research infrastructures, capacity building, and societal impacts (Lappalainen et al., 2014; Kulmala et al., 2016a; Lappalainen et al., 2018a, b; Kulmala, 2018). In addition to a strong involvement of the Russian partners, the PEEX China collaboration was established in 2013. China has a strong economic interest in Arctic regions (Tillman et al., 2018). Furthermore, China is already facing extensive environmental and air pollution challenges and has major interests in finding technical solutions for environmental monitoring of the Silk Road Economic Belt (SREB) programme initiated by President Xi Jinping in 2013 (Kulmala, 2018; Lappalainen et al., 2018a; Dave and Kobayashi, 2018). The

PEEX programme is an umbrella for several bilateral scientific projects and activities in Russia (e.g. Chalov et al., 2015, 2018; Esau et al., 2016; Alekseychik et al., 2017; Bobylev et al., 2018; Malkhazova et al., 2018; Kukkonen et al., 2020; Ezhova et al., 2018b; Zilitinkevich et al., 2019; Petäjä et al., 2020a, 2021; Bondur et al., 2019a, b, c, d, e, f; He et al., 2020), whereas in China the primary focus is on the development of atmospheric in situ stations and advanced air quality monitoring in megacity environments (e.g. Ding et al., 2016b; Yao et al., 2018; Wang et al., 2020). Furthermore, PEEX is closely collaborating with the Digital Belt and Road (DBAR) programme coordinated by the Institute for Digital Earth and Remote Sensing (RADI). The PEEX collaboration with DBAR is driven by a need for a novel in situ station network and ground-based data as complementary information for the remote sensing in the Silk Road economic region. Long-term development of a Station Measuring the Earth Surface and Atmosphere Relations (SMEAR) concept could provide baselines for this (Hari et al., 2016; Kulmala, 2015, 2018; Lappalainen et al., 2018a).

The PEEX programme is motivated by the need to obtain scientific information that combines research in the Arctic and boreal environments and to understand large-scale feedbacks and interactions operating in land-atmosphere-ocean systems (Kulmala et al., 2004, 2016a; Vihma et al., 2019) and large-scale weather impacts related to the Arctic amplification (e.g. Coumou et al., 2014; Vihma et al., 2020). Some of the scientific backbones of PEEX are the previously coordinated research frameworks and their synthesis. For example, the latest comprehensive overview of the interactions between the atmosphere, cryosphere and ecosystems at northern high latitudes was performed by the Nordic Center of Excellence in the Cryosphere-Atmosphere Interactions in a Changing Arctic Climate (CRAICC) community (Boy et al., 2019). The PEEX programme can upscale the CRAICC results into a wider geographical context.

Climate change, as a main driver of environmental changes in the northern Eurasian Arctic-boreal region and China, sets environmental boundaries for the future socio-economic activities of these regions in general. The harsh climate of this region puts pressure on the ecosystems and living conditions of the local people (e.g. IPCC, 2019). PEEX introduced 15 large-scale research questions, which would help
us to fill the key gaps in our holistic understanding of land-atmosphere interactions and their connections to societies living in the northern Eurasian region (Kulmala et al., 2015; Lappalainen et al., 2018a). This approach also sets the framework of the current paper. Here we introduce the recent research progress in the large-scale scientific themes relevant to the PEEX region. The PEEX study region consists of the northern Eurasian Arctic and boreal (taiga) environments, and thus the major geographical part of the environments is located in the Russian territory. China was added to the study area in 2013 as it was seen as a locally and globally consequential region for climate change, air quality and long-term transport of atmospheric pollutants (Kulmala et al., 2015a, 2016a; Lappalainen et al., 2016, 2018a).

Here we introduce the scientific results from PEEX scientific output, review the main results from PEEX scientific papers and present an analysis of the key gaps in the current scientific understanding. We use the PEEX research agenda structure (Kulmala et al., 2015a; Lappalainen et al., 2018a) as a reference and mirror new rising themes and results against this plan. For the literature material, we used the following sources to demonstrate the results: (i) individual inputs sent by the PEEX research community, (ii) contents of the scientific papers published in the *Atmospheric Chemistry and Physics* (ACP) PEEX special issue in 2016–2019 (https://acp.copernicus.org/articles/special issue395.html, last access: 17 January 2022) and (iii) scientific outputs from PEEX-labelled projects (https://www.atm.helsinki.fi/peex/index.php/portfolio-items/projects-subprograms/, last access: 17 January 2022) and other relevant results reported by the PEEX partners. For the individual input, we asked the PEEX research community to identify the main published papers in peer-reviewed journals for each question out of their own work and to connect the work with 1 of the 15 science questions introduced in the PEEX Science Plan. Based on the abstracts, we listed “addressed research themes” over the last 5 years per PEEX key topical area (Table 1), which we review in more detail in Sect. 2. The results are first discussed with a holistic approach, and then we categorize the advances through a set of identified feedbacks and interactions within the Arctic-boreal environment. We follow up with a discussion on the need for a future research infrastructure to be able to provide relevant data and underline the future socioeconomic development of the region by setting the boundaries for proposed new science-based concepts and technical solutions.

## 2 Results

In the PEEX Science Plan, we indicated four main thematic research domains: the land system, the atmospheric system, the water system and the society with 15 thematic research areas and related large-scale research questions (Q) presented in Table 1 (Lappalainen et al., 2015). This is the

framework we re-visited and utilized in the synthesis of new results of the PEEX community brought together in this paper. Furthermore, we synthesized the results and discuss their contribution to the large-scale feedbacks and interactions in the Arctic context in the sections below.

### 2.1 Land ecosystems

#### 2.1.1 Changing land ecosystem processes (Q1)

##### High-latitude photosynthetic productivity

High-latitude terrestrial ecosystems are crucial to the global climate system and its regulation by vegetation. These ecosystems are typically temperature limited and thus also considered especially sensitive to climate warming. Better understanding of inter-annual and seasonal dynamics and resilience of the photosynthetic activity of forest vegetation as a whole is needed for the quantification of photosynthesis, or gross primary production (GPP), and for analysing the carbon balance of the boreal forests. The carbon sink and source dynamics of the boreal forests have been intensively studied during the last 5 years at the SMEAR II station in Finland (Hari and Kulmala, 2005; Hari et al., 2009). Recent results show that the Norway spruce and Scots pine ecosystems are rather resilient to a short-term weather variability (Matkala et al., 2020). Overall, the analyses by Kulmala et al. (2019) and Matkala et al. (2020) on subarctic Scots pine and Norway spruce stands at the northern timberline in Finland serve as examples of the canopy-scale dynamics, showing that these ecosystems are generally weak carbon sinks but have a clear annual variation. Kulmala et al. (2019) observed that there is a difference between tree canopy photosynthesis compared to forest floor photosynthesis, which starts to increase after the snowmelt. Thus, the models for photosynthesis should also address the snow cover period in order to better capture the seasonal dynamics of photosynthesis of the northern forests (Kulmala et al., 2019).

The abundance of tree species, stand biomass, increasing tree growth and coverage of broadleaf species may also affect biogenic volatile organic compound (BVOC) emissions from the forest floor and impact the total BVOC emissions from northern soils. At least the stand type has been shown to affect BVOC fluxes from the forest floor in a hemiboreal-boreal region (Mäki et al., 2019). As a whole, BVOCs emitted by boreal evergreen trees are connected to the photosynthetic activity with a strong seasonality and have a crucial role in atmospheric aerosol formation processes over the boreal forest zone. BVOC emissions have low rates during photosynthetically inactive winter and increasing rates towards summer (Aalto et al., 2015). High emission peaks caused by enhanced monoterpene synthesis were found in spring periods simultaneously with the photosynthetic spring recovery (Aalto et al., 2015). This suggests that monoterpene emissions may have a protective functional role for the foliage during the spring recovery state and that these emission peaks
<table><caption>**Table 1.** Systems, key topical areas, and research question introduced in the PEEX Science Plan (SP) (Kulmala et al., 2015, 2016a; Lapalainen et al., 2018a) connected to the addressed research themes over the last 5 years by the PEEX questionnaire. The addressed research themes and the results are summarized in Sect. 3.</caption><thead><tr><th>PEEX SP system</th><th>PEEX - SP key topical area</th><th>PEEX - SP research question (Q-No)</th><th>Addressed research themes during the last 5 years</th></tr></thead><tbody><tr><td>Land</td><td>Changing land ecosystem processes</td><td>How could the land regions and processes that are especially sensitive to climate change be identified, and what are the best methods to analyse their responses? (Q-1)</td><td>High-latitude photosynthetic productivity and vegetation changes (greening, brown-ing)<br/>New methodologies determining Earth sur-face characteristics</td></tr><tr><td>Land</td><td>Risk areas of permafrost thawing</td><td>How fast will permafrost thaw proceed, and how will it affect ecosystem processes and ecosystem-atmosphere feedbacks, including hydrology and greenhouse gas fluxes? (Q-2)</td><td>Soil temperature evolution<br/>Changing GHG fluxes, carbon sink-source dynamics due to permafrost thawing</td></tr><tr><td>Land</td><td>Ecosystem structural changes</td><td>What are the structural ecosystem changes and tipping points in the future evolution of the Pan-Eurasian ecosystem? (Q-3)</td><td>Changes in soil microbial activity, e.g. ef-fect of forest fires<br/>Changes in the northern soils and function-ing of the Arctic tundra in a global carbon cycling context</td></tr><tr><td>Atmosphere</td><td>Atmospheric composi-tion and chemistry</td><td>What are the critical atmospheric physical and chemical processes with large-scale climate implications in a northern context? (Q4)</td><td>Carbon (C) balance in the boreal forests; methane (CH<sub>4</sub>) balance at the Arctic; car-bon monoxide (CO), ozone (O<sub>3</sub>) in the northern Eurasian region<br/>Sources and properties of atmospheric aerosols in boreal and Arctic environments<br/>Black carbon and dust in the atmosphere and on snow at the northern high latitudes<br/>Methodological and model developments related to atmospheric chemistry and physics</td></tr><tr><td>Atmosphere</td><td>Urban air quality and megacities, atmospheric boundary layer (ABL)</td><td>What are the key feedbacks between air quality and climate at northern high latitudes and in China? (Q5)</td><td>Recent observations of air quality in China<br/>Anthropogenic emissions and environmen-tal pollution in Russia</td></tr><tr><td>Atmosphere</td><td>Weather and atmospheric circulation</td><td>How will atmospheric dynamics (synoptic-scale weather, boundary layer) change in the Arctic-boreal regions? (Q6)</td><td>Cold and warm episodes<br/>Cyclone density dynamics<br/>Circulation effect on temperature and moisture<br/>Cloudiness in Arctic<br/>ABL dynamics</td></tr><tr><td>Water</td><td>The Arctic Ocean in the climate system</td><td>How will the extent and thickness of the Arctic sea ice and terrestrial snow cover change? (Q-7)</td><td>Sea ice dynamics and thermodynamics with atmospheric and ocean dynamics<br/>Snow depth/mass and sea ice thickness<br/>Sea ice research supporting navigation<br/>Ocean floor, sediments: composition and fluxes<br/>River runoff affecting the hydrological pro-cesses in coastal marine environments in Russia</td></tr><tr><td>Water</td><td>Arctic marine ecosystem</td><td>What is the joint effect of Arctic warming, ocean freshening, pollution load and acidifica-tion on the Arctic marine ecosystem, primary production and carbon cycle? (Q-8)</td><td>Living marine organisms weaken or even subdue CO<sub>2</sub> accumulation.</td></tr></tbody></table>
<table><caption>**Table 1. Continued.**</caption><thead><tr><th>PEEX SP system</th><th>PEEX – SP key topical area</th><th>PEEX – SP research question (Q-No)</th><th>Addressed research themes during the last 5 years</th></tr></thead><tbody><tr><td>Water</td><td>Lakes and large-scale river systems</td><td>What is the future role of Arctic-boreal lakes, wetlands and large river systems, including thermokarst lakes and running waters of all size, in biogeochemical cycles, and how will these changes affect societies)? (Q-9)</td><td>Organic carbon, carbon balance, ice cover at lakes at the northern high latitudes<br>Specific characteristics of Lake Baikal and the Selenga River Delta in Russia<br>Specific characteristics of Asian water lakes</td></tr><tr><td>Society</td><td>Anthropogenic impact</td><td>How will human actions such as land use changes, energy production, the use of natural resources, changes in energy efficiency and the use of renewable energy sources influence further environmental changes in the region? (Q-10)</td><td>Mitigation, e.g. method for the natural risk assessment in Russia and new clean energy technologies</td></tr><tr><td>Society</td><td>Environmental impact</td><td>How do the changes in the physical, chemical and biological state of the different ecosystems, and the inland, water and coastal areas affect the economies and societies in the region, and vice versa? (Q-11)</td><td>Reindeer grazing effects on the ground vegetation structure and biomass</td></tr><tr><td>Society</td><td>Natural hazards</td><td>In which ways are populated areas vulnerable to climate change? How can their vulnerability be reduced and their adaptive capacities improved? What responses can be identified to mitigate and adapt to climate change? (Q-12)</td><td>Emerging zoonotic diseases<br>UV variation effects on health<br>Air pollution in different scales and environments (street level urban air pollution, transported air pollution in urban environments, air pollution at the Arctic) and related health effects</td></tr><tr><td>Feedbacks</td><td>Key topics: atmospheric composition, biogeochemical cycles: water, C, N, P, S</td><td>How will the changing cryospheric conditions and the consequent changes in ecosystems feed back to the Arctic climate system and weather, including the risk of natural hazards? (Q-13)</td><td>Research needs: quantification of the Continental Biosphere-Aerosol-Cloud-Climate (COBACC) feedback loop at different northern boreal environments<br>Gold and high region quantification of maBVOC-aerosol feedback loop at the Tabetan/Himalayan Plateau: HimHi</td></tr><tr><td>Feedbacks</td><td>Key topics: atmospheric composition, biogeochemical cycles: water, C, N, P, S</td><td>What are the net effects of various feedback mechanisms on (i) land cover changes, (ii) photosynthetic activity, (iii) GHG exchange and BVOC emissions, and (iv) aerosol and cloud formation and radiative forcing? How do these vary with climate change on regional and global scales? (Q-14)</td><td>Research needs: the Arctic greening and browning calls for a multi-disciplinary scientific approach together, improved modelling tools and new data in order to solve scientific questions related to the net effects of various feedback mechanisms connecting the biosphere-atmosphere-human activities</td></tr><tr><td>Feedbacks</td><td>Key topics: atmospheric composition, biogeochemical cycles: water, C, N, P, S</td><td>How are intensive urbanization processes changing the local and regional climate and environment? (Q-15)</td><td>Research needs: accelerating urbanization calls for studies on the effects of on air pollution, local climate and the effects these changes have on global climate. Integrated studies should lead to services for society, cities helping to mitigate hazards storms, flooding, heat waves, and air pollution episodes (see also Sect. 3.2).</td></tr></tbody></table>
may contribute to atmospheric chemistry in the boreal forest in springtime. Vanhatalo et al. (2018) studied the interplay between needle monoterpene synthase activities, their endogenous storage pools and needle emissions in 2 consecutive years at a boreal forest in Finland. They found no direct correlation between monoterpene emissions and enzyme activity or the storage pool size. Monoterpene synthase activity of needles was different depending on seasonality and needle ontogenesis. However, the pool of stored monoterpenes did not change with the needle age (Vanhatalo et al., 2018). Also, clear annual patterns of primary biological aerosol particles have been measured from a boreal forest, with late spring and autumn being the seasons of a dominant occurrence. Increased levels of free amino acids and bacteria were observed during the pollen season in the SMEAR II station in Finland, whereas the highest levels for fungi were observed in autumn (Helin et al., 2017).

Extensive measurements of Scots pine photosynthesis and modelling resulted in optimized predictions of the daily behaviour and annual patterns of photosynthesis in a subarctic forest (Hari et al., 2017). The study connected theoretically the fundamental concepts affecting photosynthesis with the main environmental drivers (air temperature and light), and the theory gained strong support through empirical testing. Understanding stomatal regulation is fundamental in predicting the impact of changing environmental conditions on photosynthetic productivity. Lintunen et al. (2020) showed that the canopy conductance and soil-to-leaf hydraulic conductance are strongly coupled and that both soil temperature and soil water content influence the canopy conductance through changes in the below-ground hydraulic conductance. In particular, the finding that the soil temperature strongly influences the below-ground hydraulic conductance in mature, boreal trees may help to better understand tree behaviour and photosynthetic productivity in cold environments. The plant photosynthetic rate is concurrently limited by stomatal and non-stomatal limitations, and recent modelling (Hölttä et al., 2017) and empirical (Salmon et al., 2020) studies suggest that stomatal and non-stomatal controls are coordinated to maximize leaf photosynthesis; i.e. non-stomatal limitations to photosynthesis increase with a decreasing leaf water potential and/or increasing leaf sugar concentration. This new approach allows inclusion of the effects of non-stomatal limitations in models of tree–gas exchange (Fig. 1).

Due to climate warming, it seems that trees at high latitudes have been progressively decreasing their regional growth coherence in the last decades (Shestakova et al., 2019). Shestakova et al. (2019) showed results that unequivocally linked a substantial decrease in the temporal coherence of forest productivity in boreal ecosystems to a less temperature-limited growth that is concurrent with regional warming trends. This emerging pattern points, for example, to an increasing dependence of the carbon balance on local drivers and the role of forests as carbon sinks in the northern Ural region.

Vegetation GPP is the largest CO₂ flux of the carbon cycle in terrestrial ecosystems and impacts all of the carbon cycle variables (Beer et al., 2010). Ecosystem models usually overestimate GPP under drought and during spring, late autumn and winter (Ma et al., 2015). Several new methodological improvements for a better quantification and scaling of GPP have been reported (S. Zhang et al., 2018; Pulliainen et al., 2017; Kooijmans et al., 2019). The GPP, measuring photosynthesis, is crucially important for the global carbon cycle, and its accurate estimation is essential for ecosystem monitoring and simulation. Pulliainen et al. (2017) introduced a new proxy indicator for spring recovery from in situ flux data on CO₂ exchange. This made it possible to quantify the relation between spring recovery and carbon uptake and to assess changes in the springtime carbon exchange, demonstrating a major increase in the CO₂ sink. S. Zhang et al. (2018) introduced a new water-stress factor that effectively mitigates the overestimation of GPP under drought conditions, while J. H. Bai et al. (2018) and Y. Bai et al. (2018) developed a method for quantifying the evapotranspiration of crops by using a remote-sensing-based two-leaf canopy conductance model. These methods can provide novel insights into the quantification of GPP under different conditions and, in general, into the impacts of biosphere–atmosphere relations on a larger scale.

Methods for satellite-based remote sensing of photosynthesis have been developed recently based on a solar-induced chlorophyll fluorescence signal, such as the OCO-2 product that has an improved spatial resolution, data acquisition and retrieval precision as compared with earlier satellite missions with solar-induced chlorophyll fluorescence (SIF) capability, which allows for validation of the data directly against ground and airborne measurements (Sun et al., 2017). Interpretation of the solar-induced chlorophyll fluorescence signal has also been improved by many in situ studies. For example, J. Liu et al. (2019) and W. Liu et al. (2019) simulated SIF in a realistic three-dimensional birch stand reconstructed from terrestrial laser scanning data and found a large contribution of the understory layer to the remote-sensing signal.

## Vegetation changes

The normalized difference vegetation index (NDVI) is used for detecting large-scale changes in vegetation productivity. In the past decades, these changes include an increasing NDVI, called “greening”, taking place in the tundra regions, and a decreasing NDVI, called “browning”, in the northern forest regions (Miles and Esau, 2016). A deeper analysis behind these changes is needed. For example, in northern West Siberia only 18 % of the total area had statistically significant changes in productivity either towards greening or browning and having these opposite trends for different species within the same bioclimatic zone. The observed complexity of the patterns and trends in the vegetation productivity underlines the need for new studies on how forest types and different
<figure><img src="image_5.png" /><figcaption>**Figure 1.** A recent field and modelling study shows that cold soil decreases below-ground hydraulic conductance (i.e. less root water uptake) and further canopy conductance in mature, boreal trees in spring (Lintunen et al., 2020). Cold temperature also decreases sink strength (i.e. fewer sugars are needed for metabolism and growth). Low sink strength increases sugar concentration in leaves, which decreases photosynthesis due to increased stomatal and non-stomatal limitations for photosynthesis (Hölttä et al., 2017; Salmon et al., 2020).</figcaption></figure>

species are responding to climate and environmental changes in the northern environments (Miles and Esau, 2016). Also, understanding the variations in small-scale plant communities, seasonality and biogeochemical properties is needed for modelling the functioning of the Arctic tundra in global carbon cycling. Also, the rapid development of the leaf area index (LAI, leaf area per ground area, m² m⁻²) during the short growing season and the yearly climatic variation address the importance of optimal timing of the satellite data images when they are compared with the field verification data in the Arctic region (Juutinen et al., 2017).

Bondur and Vorobeyev (2015) analysed the vegetation indices and complex spectral transformations derived from processed long-term satellite data (1973–2013) for areas around the cities of Arkhangelsk and Zapolyarny (Murmansk oblast). They demonstrated that these areas are subject to a peak anthropogenic impact associated with specific industrial facilities, leading to changes in landscapes and depletion of natural ecosystems, consequently leading to the decline in the quality of life and health conditions (Bondur and Vorobeyev, 2015). Region-wide changes in the vegetation cover and changes in and around several urbanized areas in Siberia reveal robust indications of an accelerated greening near the older urban areas. Many Siberian cities have turned greener, while their surroundings have been dominated by wider browning. The observed urban greening could be associated not only with a special tending of within-city green areas, but also with urban heat islands and succession of more productive shrub and tree species growing on warmer sandy soils (Koronatova and Milyaeva, 2011; Sizov and Lobotrosova, 2016). Tundra and forest-tundra biomes are sensitive to mean summer temperatures, which increases production and greening. Taiga biomes are sensitive to precipitation and soil moisture, with increased production in wet summers (Miles et al., 2019).

## New methodologies determining Earth surface characteristics

Earth surface characteristics are fundamental knowledge for the understanding and quantification of land-atmosphere processes. The methods for determining Earth surface characteristics from satellites are improving. As an example, a method for recognition of the Earth surface types according to space images using an object-oriented classification was developed. The classification relies on Markov stochastic segmentation for object extraction and supervised classification of the objects (Gurchenkov et al., 2017). Furthermore, a prototype algorithm for hemispheric-scale detection of autumn soil freezing using spaceborne L-band passive microwave observations was developed (Rautiainen et al., 2016) and is currently an operative soil freeze and thaw product that delivers freely available data (ftp://litdb.fmi.fi/outgoing/SMOS-FTService/, last access: 17 January 2022). The CryoGrid 3 land surface model provides improved descriptions of possible pathways of ice-wedge polygon evo-
lution and describes better the complex processes affecting ice-rich permafrost landscapes (Nitzbon et al., 2019). In addition, there are new observations for validating satellite observations and permafrost models. Boike et al. (2019) introduced a new, 16-year permafrost and meteorology data set from the Samoylov Island Arctic research site, north-eastern Siberia. Terentieva et al. (2016) introduced maps used as a baseline for validation of coarse-resolution land cover products and wetland data sets at high latitudes. Other examples of available data for the model validation are “BC emissions from agricultural burns and grass fires in Siberia” by Konovalov et al. (2018) and “permafrost records at the Lena River delta” by Boike et al. (2019).

Tundra ecosystems are under pressure and intensifying permafrost thawing, plant growth and ecosystem carbon exchange under the changing climate. The heterogeneity of Arctic landscapes is an extra challenge for environmental monitoring. For example, remote-sensing methods are not able to capture variations in moss biomass, which dominates the plant biomass and controls soil properties in the Arctic. The general accuracy of landscape level predictions in the land cover type (LCT) is good, but the spatial extrapolation of the vegetation and soil properties relevant for the regional ecosystem and global climate models still needs to be improved (Mikola et al., 2018). Furthermore, for the future, we need to have a land characterization in order to perform quantification and assessment of the ecosystem services at different scales using integrative techniques and integrated field observations together with remote sensing and modelling at the landscape scale (Burkhard et al., 2009; Fu and Forsius, 2015). At smaller scales, the isotopic composition of carbon and oxygen in peat can be used for the climate reconstruction (Granath et al., 2018).

## 2.1.2 Thawing permafrost (Q2)

### Observations of ground temperature evolution

Permafrost regions of northern Eurasia are warming along with the climate (IPCC, 2019). During the Global Terrestrial Network for Permafrost reference decade, 2007–2016, the temperature at the depth of zero annual amplitude increased by $0.39 \pm 0.15$ °C in the continuous permafrost zone and by $0.20 \pm 0.10$ °C in the discontinuous permafrost zone. At the same time, the mountain permafrost warmed by $0.19 \pm 0.05$ °C. The global average of the permafrost temperature increased by $0.29 \pm 0.12$ °C (Biskaborn et al., 2019). The observed trend in the continuous permafrost zone follows the air temperature trend in the Northern Hemisphere.

The changes in the permafrost region affect climate, hydrology and ecology from local to global scales (Arneth et al., 2010; Hinzman et al., 2005). Several local studies focused on differences introduced by vegetation, soil and hydrological characteristics at the same site (Göckede et al., 2017, 2019). Göckede et al. (2017, 2019) presented findings

on shifts in energy fluxes from paired ecosystem observations in north-eastern Siberia comprising a drained and corresponding control site. Drainage disturbance triggered a suite of secondary shifts in ecosystem properties, including alterations in vegetation community structure, which in turn influenced changes in snow cover dynamics and surface energy budget. First, the drainage reduced heat transfer into deeper soil layers, which may have led to shallower thaw depths. Second, the vegetation change due to the drainage led to an albedo increase, which decreased the total energy income, or net radiation, into the system. Third, the drainage reduced water content available for evapotranspiration, which resulted in a reduced latent heat flux and increased sensible heat flux, transferring more energy back into the atmosphere. The reported effects led to surface and permafrost cooling (Göckede et al., 2019).

Kukkonen et al. (2020) compared temperature data from several shallow boreholes in the Nadym region, Siberia, and predicted permafrost evolution for different climate scenarios. The Nadym area represents a typical site located in the discontinuous permafrost zone. Kukkonen et al. (2020) found that the permafrost thawed most rapidly in low-porosity soils, whereas high-porosity soils in the top layer (e.g. peatland) retarded thawing considerably. Similarly, the depth of a seasonally frozen layer and the temperature regime of peat soils in the oligotrophic bog in the southern taiga zone of West Siberia showed significant differences between the sites with high and low levels of bog waters (Kiselev et al., 2019). Both Kukkonen et al. (2020) and Kiselev et al. (2019) results are in line with previous conclusions on the importance of volumetric water content and unfrozen water content for soil thermal properties governing heat transfer and phase change processes (Romanovsky and Osterkamp, 2000). Locally, the sites with a thin snow cover (e.g. hilltops) demonstrated a higher resistance to the thawing (Williams and Smith, 1989; Kukkonen et al., 2020). To follow up on the development of permafrost thaw in different soil types requires continuous and comprehensive observations during the coming decades.

### Changing greenhouse gas (GHG) fluxes and VOCs due to permafrost thaw

Biogenic GHG emissions are strongly connected to permafrost conditions and changes in other related environmental conditions, such as soil temperature and moisture conditions. Here we discuss recent results on the observed emissions from these permafrost perspectives and, later, in Sect. 2.2.1, address the connections between GHG fluxes and the other environmental factors, like deforestation and forest fires.

During the permafrost thaw, even small changes in the soil carbon cycle can turn a terrestrial ecosystem from a sink into a source (Schuur et al., 2008). Based on regional in situ observations of CO₂ fluxes, Natali et al. (2019) estimated
a wintertime carbon loss of 1662 Tg C yr⁻¹, which is more
than predicted by the process model estimates. Furthermore,
Natalie et al. (2019) found that even if the soil CO₂ loss
were enhanced due to winter warming, the growing season
might start earlier and onset the carbon uptake under warm-
ing climate conditions. For a better understanding of these
connections and both spatial and temporal dynamics of the
Arctic carbon cycle, we need more observations from per-
mafrost ecosystems. Additional flux measurements are ur-
gently needed to understand the variation between the cur-
rent measurements and, especially, extended measurements
on the CH₄ emissions to better quantify their role in the
carbon balance. For example, a new data assimilation sys-
tem estimates an Arctic carbon sink of –67 g C m⁻² yr⁻¹,
but this value is associated with very high uncertainties. Fur-
thermore, these estimates do not include methane, which is
even more difficult to evaluate (López-Blanco et al., 2019).
Based on the field flux measurements, the Carbon Cycle Re-
port 2018 (Schuur et al., 2018) estimated that the Eurasian
boreal wetland is a source of 14 Tg CH₄ yr⁻¹. On the other
hand, Kirschke et al. (2013) estimations, based on atmo-
spheric measurements, end up at a value of 9 Tg CH₄ yr⁻¹.
Locally, methane fluxes measured in 2005–2013 showed sig-
nificant year-to-year variations. Interestingly, the observed
variability in North America, specifically in the Hudson Bay
lowlands, appears to have been driven partly by the soil tem-
perature, while in the West Siberian lowlands the variabil-
ity was dependent on the soil moisture (Thompson et al.,
2017). The comparison of high-resolution modelling of at-
mospheric CH₄ to CH₄ observations already in 2012 from
the East Siberian Arctic Shelf (ESAS), a potentially large
CH₄ source, confirms that methane releases are highly vari-
able and inhomogeneous (Berchet et al., 2016).

Long-term flux measurements provide insight into the car-
bon sink–source dynamics. The flux measurements from the
moist tussock tundra in north-eastern Siberia indicated that
drainage influences the carbon cycle and that the tundra is
changing to a weaker CO₂ sink and CH₄ source. Another
relevant observation was that the time outside the grow-
ing season influences the carbon balance of ecosystem pro-
cesses, especially during the zero-curtain period (Kittler et
al., 2017). This is in line with similar studies in Alaska (Com-
mane et al., 2017; Euskirchen et al., 2017). Therefore, the
autumn temperature was identified as a major driving factor
describing the differences between the annual GHG fluxes.
Notably, however, the seasonal amplitudes of CO₂ concen-
trations in Siberia were found to be significantly higher than
those in the North American continent, likely due to the more
intense biological activity here (Timokhina et al., 2015a). A
recent study showed that the Siberian carbon cycle is a major
contributor to the Northern Hemisphere amplitude of CO₂
variation (Lin et al., 2020).

Observations from non-permafrost sites may give us a clue
to the future dynamics of fluxes, as the permafrost is thawing.
The chamber measurements of CH₄ and CO₂ fluxes from a

non-permafrost site in the Siberian peatland in August 2015
showed that the highest values of methane fluxes were ob-
tained in burned wet birch forest and the lowest ones in
seasonally waterlogged forests (Glagolev et al., 2018). The
fluxes can vary even between different sites of a bog, as mea-
sured by Dyukarev et al. (2019). The net ecosystem exchange
(NEE), ecosystem respiration (ER) and GPP, based on the
measured CO₂ fluxes at a ridge–hollow complex bog and
a model for ridge and hollow sites at oligotrophic bogs in
the middle taiga zone of West Siberia, showed that a 2-year-
average NEE at the hollow site was 1.7 times higher than at
the ridge site (Dyukarev et al., 2019). The ecosystem pro-
cesses are influenced by drying in tundra ecosystems. Kwon
et al. (2019) reported from Alaska that drying in the tun-
dra ecosystems increased contributions of modern soil car-
bon to the ecosystem respiration but, at the same time, de-
creased contributions of old soil carbon. These changes were
attributed mainly to modified soil temperatures at different
soil layers due to the altered thermal properties of organic
soils following drainage. Furthermore, the drainage lowered
CH₄ fluxes by a factor of 20 during the growing season, with
post-drainage changes in microbial communities, soil tem-
peratures, and plant communities also affecting the flux re-
duction in an Arctic wetland ecosystem (Kwon et al., 2017).

Voigt et al. (2016) reported that, under warming condi-
tions, the vegetated tundra in north-eastern European Russia
shifted from a GHG sink to a source. The positive warm-
ing response was dominated by CO₂; however, N₂O emis-
sions were also significant. N₂O was emitted not only from
bare peat, already identified as a strong source, but also from
vast vegetated peat areas not emitting N₂O under current cli-
mate conditions. These results can be explained by the dy-
namics between the temperature, nitrogen assimilation by
plants and soil microbial activity, with a strong impact on
the future GHG balance in the Arctic (Voigt et al., 2016; Gil
et al., 2017). Studying N₂O emissions from a typical per-
mafrost peatland in Finnish Lapland, it was concluded that
about 25 % of the Arctic territories are areas that potentially
emit nitrous oxide (Voigt et al., 2017). It seems that there is a
positive feedback mechanism between the permafrost thaw-
ing and moisture regime. Predicting the response of soils to
climate change or land use is central to understanding and
managing N₂O emissions. According to recent results, the
N₂O flux can be predicted by models that incorporate soil
nitrate concentration (NO₃⁻), water content and temperature
(Pärn et al., 2018).

In addition to CO₂ and CH₄, thawing or collapsing of
Arctic permafrost can release volatile organic compounds
(VOCs). H. Li et al. (2020) examined the release of
VOCs from thawing permafrost peatland soils sampled from
Finnish Lapland in the laboratory. The average VOC fluxes
were 4 times as high as those from the active layer and mainly
attributed to direct release of old, trapped gases from the per-
mafrost. These results demonstrate a potential for substantive
VOC releases from thawing permafrost and suggest that fu-
ture global warming could stimulate VOC emissions from the Arctic permafrost.

### 2.1.3 Ecosystem structural change (Q3)

#### Changes in microbial activity

Climate change is likely to cause an increased appearance of trees on open peatlands, but we do not know how this vegetation change will influence the below-ground microbiology and composition. Changes along bog ecotones at three Russian peatland complexes suggest that tree encroachment may reduce the trophic level of testate amoeba communities and reduce the contribution of mixotrophic testate amoebae to primary production. Thus, it seems that increased tree recruitment on open peatlands will have important consequences for both microbial biodiversity and microbially mediated ecosystem processes (Payne et al., 2016). We also need to understand better the dynamics affecting the bacteria, fungi and other related species in the ground air layer. Recent studies by Korneykova and Evdokimova (2018) and Korneikova et al. (2018) showed the influences of anthropogenic sources (copper-nickel plant) and acidic soils in Russian northern taiga and tundra on the portion of the airborne fungi and on the structure of algological and mycological complexes (Korneikova et al., 2018). New methods were reported on how to improve soil conditions, developed on all kinds of materials made or exposed by human activity that otherwise would not occur at the Earth's surface, referred to as "Techno sol engineering" (Slukovskaya et al., 2019), and how to monitor climate change impacts on the functional state of bogs by using *Sphagnum* mosses (Preis et al., 2018).

#### Effects of forest fires on soils

Forest fires, a significant environmental factor in the northern Eurasian region, change soil chemical and physical properties and may influence greenhouse gas fluxes and emissions of BVOCs. Recent results indicate that a slower post-fire litter decomposition has a clear impact on the recovery of soil organic matter following forest fires in northern boreal coniferous forests due to accumulated soil organic matter. The soil recovery is related to slow litter composition and reduced enzymatic and microbial activity (E. Köster et al., 2016).

Post-fire studies on the long-term evolution of the structure and functioning of bacterial communities are sparse. Sun et al. (2016) showed that the major drivers influencing bacterial communities are the soil temperature, pH and moisture. Furthermore, E. Köster et al. (2015) analysed long-term effects of fire on soil CO₂, CH₄ and N₂O fluxes in pine forest stands in Finnish Lapland and discussed the role of microbial biomass in this context. They did not detect significant effects of fires on CO₂ emissions or N₂O fluxes, but there was long-lasting strengthening of the CH₄ sink by the soil. Interestingly, E. Köster et al. (2018) did not find a similar

kind of long-term effect on the CH₄ sink dynamics in studies carried out in Siberia.

Forest wildfires also regulate the BVOC emissions from boreal forest floors by changing the ground vegetation. Total BVOC emissions from a forest floor were found to decrease after a forest fire and then to increase again along with the succession of forests (Zhang-Turpeinen et al., 2020). For a comparison, Bai et al. (2017) showed that biomass burning resulted in increased BVOC emission fluxes and ozone concentration above canopy in a subtropical forest in China.

### 2.2 Atmospheric system

Concerning critical atmospheric processes and large-scale climate implications, we concentrate here on greenhouse gases and aerosol particles over northern Eurasia and the Arctic, urban air quality, and issues related to the weather and atmospheric circulation. We summarize the recent measurements on the atmospheric composition relevant to sink and source dynamics in Siberia, on the sources and properties of atmospheric aerosols in Arctic-boreal environments, including black carbon and dust in the atmosphere and snow, and on the methodological and model developments related to atmospheric chemistry and physics (Q4, Sect. 2.2.1). Furthermore, we introduce new results and observations of atmospheric pollution in rural, suburban and megacity environments in China and Russia (Q5, Sect. 2.2.2). We briefly show some recent results related to synoptic-scale weather in Arctic-boreal regions, focusing on cold and warm episodes, cyclone density and atmosphere-ocean interaction, effects of circulation on temperature and moisture, cloudiness in the Arctic, and boundary-layer dynamics (Q6, Sect. 2.2.3).

#### 2.2.1 Atmospheric composition and chemistry (Q4)

##### Boreal forest carbon balance

As already discussed in Sect. 2.1.1, boreal forests as a carbon sink and the related role of forestation have been under international debate. It seems that early snowmelt increases springtime carbon uptake of the boreal forests of Eurasia and North America and shows a major advance in the CO₂ sink (Pulliainen et al., 2017). A scenario of a complete global deforestation by Scott et al. (2018), combining radiative forcing with CO₂, surface albedo and short-lived climate forcers (SLCFs), suggests that global deforestation could cause a 0.8 K warming after 100 years, with SLCFs contributing 8% of the effect. However, deforestation as projected by the RCP8.5 scenario leads to zero net radiative forcing from SLCFs, primarily due to non-linearities in the aerosol indirect effect. Tuovinen et al. (2019) showed that methane fluxes vary strongly with a wind direction in a tundra ecosystem with heterogeneous vegetation. By combining very high-spatial-resolution satellite imagery and footprint modelling, they were able to estimate the relation between the main land cover types and ecosystem level mea-
surements. CH₄ emissions originated mainly from wet fen and graminoid tundra patches, whereas the areas of bare soil and lichen acted as strong CH₄ sinks (Tuovinen et al., 2019; Tsuruta et al., 2017). Tsuruta et al. (2017) reported posterior mean global total emissions of 516 ± 51 Tg CH₄ yr⁻¹ during 2000–2012, which indicates that these emissions had increased by 18 Tg CH₄ yr⁻¹ from the period 2001–2006 to 40 Tg CH₄ yr⁻¹ from the period 2007–2012. This increase can be explained by increased emissions from the temperate region in South America and from the temperate region and tropics in Asia.

Analysis of the trends and the diurnal, weekly and seasonal cycles of CO₂ and CH₄ mixing ratios derived from the long-term data of the Japan–Russia Siberian Tall Tower Inland Observation Network showed that the frequency of identified events of elevated concentration differs for CO₂ and CH₄ and may reach up to 20% of days in some months (Belikov et al., 2019). These observations made it possible to reduce uncertainties in the biosphere surface CO₂ uptake (Kim et al., 2017). Although the CO₂ uptake in boreal Eurasia estimated by Kim et al. (2017) was about 30% lower than that obtained without the assimilation of Siberian observation data, Siberia still remains a key contributor to the terrestrial CO₂ sink in the Northern Hemisphere.

There are tendencies of a significant growth or suppression of soil CO₂ fluxes across different types of human impacts, such as forest fires, trampling, settlements, reindeer grazing and clear cuts on cryogenic ecosystems in Russia (Karelin et al., 2017). For example, Ivakhov et al. (2019) analysed CO₂ measurements during 2010–2017 and reported CO₂ concentration increases of 20 ppm in Tiksi at a coast of the Laptev Sea and of 15 ppm at the Cape Baranov station. They also detected that wildfires in Siberia can lead to a parallel increase in the CO₂ concentration in the Russian Arctic. Furthermore, the measurements showed that the atmospheric CO₂ concentration increased on average by 2.0 ppm yr⁻¹ during 2006–2013 in central Siberia, with a large inter-annual variation. The highest increases were found in 2010 and 2012 (3.6 and 4.3 ppm yr⁻¹, respectively), when large wildfires released huge amounts of CO₂ in Siberia (Timokhina et al., 2015b). Repeated wildfires in boreal forests can combust a portion of the thick organic soil layer characteristic of this ecosystem and change the forests from a carbon sink to a carbon source (Walker et al., 2019). A study on a fire chronosequence of the central Siberian permafrost soil showed that soils affected by fires over decades act as CO₂ sources and that the CO₂ emissions from these soils increased with an increasing time since the last fire (E. Köster et al., 2018). However, there were no similar effects on CH₄ emissions, with soils acting as a CH₄ sink without any connection to forest fires. In addition to CO₂, wildfires also release large amounts of other trace gases and aerosols. Emission factors of several trace gases and aerosols from Siberian fires measured from the Trans-Siberian Railway were reported by Vasileva et al. (2017). The impact of Siberian fires as elevated aerosol

concentrations was at times observed to extend up to the Arctic coast (Asmi et al., 2016).

## Arctic methane (CH₄) balance

Deep understanding of the dynamics of methane emissions in the Arctic is needed for identifying and quantifying GHG-related feedbacks and the global methane cycle (Dean et al., 2018). During the winter, methane originates mostly from anthropogenic sources, while on smaller scales emissions from the oceans, including the ESAS, can also play an important role. During the warm season, the balance is dominated by emissions from wetlands and freshwater bodies. Thonat et al. (2017) employed the CHIMERE model for an assessment of the methane cycle in the Arctic. They reported that all methane sources, except biomass burning, contributed to measurements at six study sites. That study emphasizes the importance of a joint model-measurement approach for studies of complex phenomena at large spatial scales. Accounting for OH oxidation and soil uptake, two important sinks of methane, improved the agreement between observed and modelled methane concentrations (Thonat et al., 2017). Peltola et al. (2019) upscaled CH₄ fluxes measured at 25 northern wetland sites and showed three different maps of wetland distribution, with the annual methane emissions varying from 31 to 38 Tg CH₄ yr⁻¹. (For the monthly upscaled CH₄ flux data products, see https://doi.org/10.5281/zenodo.2560163.) Multiple sources, together with different spatiotemporal dynamics and magnitudes, are influencing the total Arctic CH₄ budget and address the need for further improved assessments (Peltola et al., 2019; Thonat et al., 2017).

## Northern Eurasian carbon monoxide (CO)

Analysis of long-term trends in the atmospheric composition in remote northern Eurasia (1998–2016) showed that the total column carbon monoxide (CO) amount has been stabilized or increased in summer and autumn months (Rakitin et al., 2018). The changes in the global photochemical system, especially changes in the ratio between the sources and sinks of minor atmospheric chemical species, could explain these trends (Skorokhod et al., 2017). A comparative study (1998–2014) on the atmospheric total column CO amount in background and polluted regions of Eurasia indicated that this amount has decreased remarkably in the Moscow urban environments (3.73 % yr⁻¹ ± 0.39 % yr⁻¹) compared to the background regions (0.9 % yr⁻¹–1.7 % yr⁻¹) (P. C. Wang et al., 2018).

## Northern Eurasian ozone (O₃)

Atmospheric measurements of ozone, its precursors and other pollutants over Siberia are important for the atmospheric chemistry modelling, satellite product validation and comparisons between Siberia and other regions of the North-
ern Hemisphere. Isoprene and monoterpenes together with nitrogen oxides impact tropospheric O₃ formation and lead to an increase in the daytime ozone-forming potential (OFP) in urban environments. Bai et al. (2021) showed that O₃ may respond either positively or negatively to isoprene and monoterpene emissions depending on the level of solar radiation and atmospheric loadings of trace gases and aerosol particles. It was demonstrated that monoterpenes have a major contribution to tropospheric O₃ formation, especially in cities in Siberia with high atmospheric NOₓ concentrations (10–20 ppb) and daytime temperatures (> 25 °C) (Berezina et al., 2019). In contrast, isoprene is dominating the O₃ formation and the increasing OFP in the cities in the Far East. The isoprene-derived OFP can originate from deciduous vegetation growing in city environments or nearby regions or from an anthropogenic isoprene source. The monoterpenene-derived OFP was found to be lowest in medium-sized cities and highest in small cities (Berezina et al., 2019). The total contribution of benzene and toluene to photochemical O₃ production was found to be up to 60%–70% in urbanized environments, indicating anthropogenic pollutant sources (Skorokhod et al., 2017). In addition to atmospheric chemistry, the connection between stratospheric O₃, UV radiation and health effects needs to be addressed in the populated urban environments of Siberia. Chubarova et al. (2019b) estimated that the wintertime O₃ depletion in northern regions of Siberia is not critical, but the much larger O₃ reductions observed in the early spring can lead to dangerous levels of erythema UV radiation (see also Sect. 2.4.3, Natural hazards and UV variation).

## Sources and properties of atmospheric aerosols in boreal and Arctic environments

Atmospheric new particle formation (NPF) is the largest contributor to the number concentration of aerosol particles in the global troposphere. During the past couple of decades, NPF has been measured in more than 10 boreal forest sites (Kerminen et al., 2018). The annual frequency of NPF event days varies between about 10% and 30% in the boreal forest zone, being highest in the western part of this region and lowest on the northern edge and in the Siberian part of it. Similar high nucleation frequencies were found at two very remote sites in boreal North America (Andreae et al., 2019). In contrast, annual NPF event frequencies below 2% were reported from central Siberia (Wiedensohler et al., 2019). Similarly, in northern Siberia on the Arctic coast, NPF events were mainly connected to marine and coastal air masses and rarely observed in continental air masses (Asmi et al., 2016). Seasonally, NPF tends to be most frequent during spring, even though high NPF event frequencies can also be observed during summer or autumn. Wintertime NPF is rare throughout the boreal forest region. In the Arctic, NPF appears to be a major aerosol particle source from spring to summer, after which this source collapses during autumn

and is practically absent over the whole winter (Freud et al., 2017). Twenty years of NPF observations in a boreal forest at the SMEAR II station in Finland show a higher frequency of NPF events under clear-sky conditions in comparison to cloudy conditions (Dada et al., 2017). Also, oxidized organic vapours showed a higher concentration during the clear-sky NPF event days, whereas the condensation sinks and some trace gases had higher concentrations during the non-event days.

The overall importance of atmospheric NPF in boreal and Arctic areas depends on the growth of freshly formed particles to cloud condensation nuclei. In the boreal forest environment, both observations and model simulations indicate that the particle growth is tied strongly to the oxidation products of biogenic volatile organic compounds originating from forest ecosystems (Paasonen et al., 2018; Östrom et al., 2017). The important compound group in this respect is monoterpenes, even though sesquiterpenes were also found to have high secondary organic aerosol yields in boreal forest environments (Hellén et al., 2018). The observed particle growth rates were found to increase with an increasing particle size and to be highest in summer (Paasonen et al., 2018). The chemistry of new particle growth in the Arctic atmosphere is not well characterized, even though available observations suggest that this growth is associated mainly with biogenic emissions from high-latitude marine areas (Giamarelou et al., 2016; Heintzenberg et al., 2017; Kecorius et al., 2019).

Wildfires are an important source of particulate pollutants on a global scale and are affecting both air quality and climate (Andreae, 2019; Bondur et al., 2020). Satellite observations indicate that the annual burned area by wildfires in Russia decreased by a factor of 2.6 during 2005–2016 owing to early detection and suppression of fire sources, whereas in Ukraine the relative size of burned-out areas increased by a factor of 6–9 from 2010–2013 to 2014–2016 (Bondur et al., 2017, 2019d). For Siberia, Ponomarev et al. (2016) reported strong increases in both number and burned areas based on satellite data, with burned areas doubling from 2005 to 2016. While biomass burning emissions have been measured widely over Russia (Bondur, 2016; Bondur and Ginzburg, 2016; Bondur et al., 2019d), there is still a need for further information on the atmospheric composition of wildfire emissions and related emission ratios from the Siberian region. Fire experiments provide important information on the emission and aging characteristics of smoke aerosols (e.g. Kalogridis et al., 2018).

Luoma et al. (2019) presented a detailed trend analysis for aerosol optical properties at the SMEAR II station in Finland. They found a statistically significantly decreasing trend for the scattering coefficient and even a stronger decreasing trend for the absorption coefficient during 2006–2017. These trends are very likely indicative of decreasing influence of anthropogenic emissions, with the contribution from emissions containing black carbon decreasing even more quickly.
Measurements of carbonaceous aerosols over central Siberia during 2010–2012 showed that, in autumn and winter, high concentrations of such aerosols were caused by long-range transport from the cities located in southern and south-western regions of Siberia (Mikhailov et al., 2015a). In spring and summer, pollution levels were high due to regional forest fires and agricultural burning in the Russian–Kazakh region. The variability of the background concentration of organic aerosols correlated with the air temperature in summer, implying that biogenic sources dominated the formation of organic particles at that time of the year (Mikhailov et al., 2015b). Based on a 5-year study by Mikhailov et al. (2017), it seems that the atmospheric pollution originating from the biomass burning and anthropogenic emissions is significantly affecting the Siberian region. However, in summer precipitation is removing the pollutants from the air and leading to relatively clean atmospheric conditions in this region.

At circumpolar sites over the Arctic, aerosol optical properties were found to vary both seasonally and spatially (Schmeisser et al., 2018). Arctic haze aerosols in late winter and spring are characterized by increased concentrations of sulfate, whereas in summer rich organic chemistry seems to be associated with vegetation, local urban and shipping sources as well as secondary aerosol formation influenced by emissions from low-latitude Siberia (O. Popovicheva et al., 2019). From a longer perspective, Arctic observations show large decreases in both sulfate and black carbon concentrations since the early 1980s (Breider et al., 2017).

Observations of the elemental composition of surface aerosols on the coastal Kandalaksha Bay of the White Sea were indicative of the dominance of biogenic aerosol particles during summertime, with heavy metal concentrations in aerosols being at Arctic background levels (Starodymova et al., 2016). Increases in Ni and Cu concentrations were observed in air masses arriving from the western part of the Kola Peninsula indicative of emissions from the smelters in that region.

## Black carbon and dust in the atmosphere and snow

Black carbon (BC) is a potentially large contributor to climate forcing in the Arctic region; however, the assessment of its pollution is hampered by the lack of aerosol studies in northern Siberia (O. Popovicheva et al., 2019; O. B. Popovicheva et al., 2019). The spatial variability of Arctic BC was studied using a harmonized data set from six circumpolar Arctic observatories (Backman et al., 2017). These data suggested a significant spatial and seasonal variability (Schmeisser et al., 2018), addressing a need for more year-round data. BC observations (September 2014–September 2016) at the Hydrometeorological Observatory Tiksi at a coast of the Laptev Sea showed a seasonal variation, with the highest concentrations (up to 450 ng m⁻³) from January to March and the lowest ones (about 20 ng m⁻³) in

June and September. During winter, stagnant weather and stable atmospheric stratification resulted in the accumulation of pollution, depending also on the wind direction and air mass transport (O. Popovicheva et al., 2019).

For the Arctic, important sources of BC include industrial regions of northern Europe, gas flares of the oil fields in the North Sea and Siberia, and Siberian biomass burning (Shevchenko et al., 2015; Konovalov et al., 2018). In 2012, for example, approximately a quarter of the biogenic BC emissions from Siberia after the fire season were transported into the Arctic (Konovalov et al., 2018). Popovicheva et al. (2017) analysed the BC origins over the Russian Arctic seas together with simulated BC concentrations. Concentrations were observed to be high (100–400 ng m⁻³) over the Kara Strait, Kara Sea and Kola Peninsula and extremely high (about 1000 ng m⁻³) over the White Sea. It seems that the gas-flaring emissions from the Yamal–Khanty–Mansiysk and Nenets–Komi regions affected the measurements made over the Kara Strait (north of 70°N) region, while the near-Arkhangelsk (White Sea) region was connected to the biomass burning at mid-latitudes. Combustion in central and eastern Europe was also identified as an important BC source.

Atmospheric aging promotes an internal mixing of BC with other aerosol constituents, leading to enhanced light absorption and radiative forcing. In situ observations at Arctic stations demonstrated an absorption enhancement due to the internal mixing of BC, which is a systematic effect and should be considered for quantifying the aerosol radiative forcing in this region (Zanatta et al., 2018).

Regional modelling of the Arctic aerosol pollution showed that long-range transported anthropogenic emissions and biomass burning are the main contributors to direct aerosol radiative effects in the region (Marelle et al., 2018). However, a scenario for 2050 indicates that shipping emissions in the Arctic Ocean could become the main source of surface aerosol and local flaring as a major source of BC, as the flaring is already a major source of BC in north-western Russia. Kühn et al. (2020) assessed the effects of different BC mitigation measures on Arctic climate and showed that reducing BC emissions by the Arctic Council member states can reduce BC deposition by about 30% compared to the current situation. A full execution of recommendations by the Arctic Council member and observer countries could reduce the annual global premature deaths due to PM (particulate matter) by ~9% by 2030 (Kühn et al., 2020). Evangeliou et al. (2018) estimated the origin of elemental carbon (EC) in snow and showed that, for West Siberia, where gas flaring emissions are a major contributor, the model underestimation was significant. Furthermore, the model was evaluated by independent BC measurements in snow over the Arctic and, again, the model underestimated BC concentrations, especially in spring.

Climatically significant cryosphere effects of light-absorbing, high-latitude dust can be similar to the albedo
and melt effects of BC (Peltoniemi et al., 2015; Svensson et al., 2016, 2018; Meinander et al., 2020a, b). Iceland is the most significant source of European Arctic dust and plays a role in the cryosphere–atmosphere–biosphere interactions and feedbacks (Boy et al., 2019; Dragosics et al., 2016; Dagsson-Waldhauserova and Meinander, 2019). Dust storms from technogenic mining industry tailing dumps on the Kola Peninsula are also an important source of local atmospheric pollution for neighbouring cities, e.g. Apatity and Kirovsk (Amosov et al., 2020). Besides regional-scale dust storms from deserts in Kazakhstan, Mongolia and China are also significant sources of aerosol pollution for these regions and for northern Asia.

Methodological and model developments related to atmospheric chemistry and physics

Several methods to characterize the atmospheric chemistry were introduced or improved. Motivated by the ability of atmospheric ion measurements to identify NPF events in the atmosphere (Leino et al., 2016), a new classification method for atmospheric NPF was developed (Dada et al., 2018). The new method uses both ion and aerosol particle number concentration measurements in the size ranges of 2–4 and 7–25 nm, respectively, is complementary to the traditional event analysis, and can also be used as an automatic way of determining NPF events from large data sets. Zaidan et al. (2018b) used a mutual information approach for a variety of simultaneously monitored ambient variables, including trace gas and aerosol particle concentrations and several meteorological variables, in order to identify key factors contributing to atmospheric NPF. This method can also be used in the atmospheric studies to discover other interesting phenomena and relevant variables. The NPF is directly observed by monitoring the time evolution of ambient aerosol particle size distributions. A new machine-learning-based approach, a Bayesian neural network (BNN) classifier, points out the potential of these methods and suggests further exploration in this direction (Zaidan et al., 2018a).

The condensation sink, being proportional to the surface area of an aerosol population, is one of the major parameters controlling NPF. A simple model for the time evolution of the condensation sink in the atmosphere for intermediate Knudsen numbers was developed to describe the coupled dynamics of the condensing vapour and the condensation sink (Ezhova et al., 2018a). The model gives reasonable predictions of condensation sink dynamics during periods of particle growth by condensation in the atmosphere. A new empirical relation between the atmospheric cloud condensation nuclei (CCN) concentration and aerosol optical properties was derived (Shen et al., 2019), making it possible to estimate CCN concentrations at sites with continuous observations of aerosol optical properties.

Empirical models of solar radiation were developed and used for calibrations of solar radiometers (Bai, 2019). This

method can be used to calibrate all kinds of solar radiometers. A solar radiation model combined with ceilometer and pyranometer measurements was used to classify clouds at SMEAR II (Ylivinkka et al., 2020). It opens new possibilities for studies of aerosol–cloud interactions.

Che et al. (2016) made an inter-comparison of three satellite (AATSR Level-2) aerosol optical depth (AOD) products (SU, ADV and ORAC) over China. The SU algorithm performs very well over sites with different surface conditions in mainland China from March to October but slightly underestimates AOD over barren or sparsely vegetated surfaces in western China. The ADV product has the same precision and error distribution as the SU product. The main limits of the ADV algorithm are underestimation and applicability. The ORAC algorithm has the ability to retrieve AOD at different ranges, including high values of AOD, but its stability decreases significantly with an increasing AOD, especially when AOD > 1.0 (see also Sect. 2.2.2, Urban air quality and megacities).

One of the major problems for both interpretation of satellite data and applications of empirical models of solar radiation is related to elevated aerosol layers in the atmosphere. It was demonstrated that their origin can be attributed to a higher confidence when back trajectories are combined with lidar and radiosonde profiles (Nikandrova et al., 2018).

Black carbon measurement methods have progressed. A representative value for the multiple scattering enhancement factor, a fundamental quantity correcting atmospheric black carbon measurement using an aethalometer, was derived for the first time in the Arctic environment (Backman et al., 2017). By analysing BC measurements made with an aethalometer in Nanjing, Virkkula et al. (2015) showed that the compensation parameter of a widely used data processing method depends both on single-scattering albedo and the backscatter fraction of the aerosol (see also Sect. 2.2.2, Urban air quality and megacities). The multiple-scattering correction factor of quartz filters and the effect of filtering particles mixed in snow were estimated by Svensson et al. (2019), who applied the method for analysing light absorption and BC in snow samples taken from Finnish Lapland and the Indian Himalayas.

Measurement of atmospheric sub-10 nm particle number concentrations has been of substantial interest recently. A new high-flow differential mobility particle sizer (HF-DMPS) was built, calibrated and operated under field conditions for 1 month (Kangasluoma et al., 2018). The counting uncertainties of the HF-DMPS were reduced by about 50% as compared to the traditional DMPS. The HF-DMPS detected about 2 times more particles than the DMPS in the size range of 3–10 nm. Below 3 nm, the HF-DMPS is currently limited by the inability of diethylene glycol to condense on biogenic particles. To collect BVOC samples, a novel collection method offering portability and improved selectivity and capacity was developed. Solid-phase micro-extraction (SPME) arrow sampling (Feijó Barreira et al., 2018) can
be used for static and dynamic collection of BVOCs under the field conditions. A significant improvement in sampling capacity was observed with the new SPME arrow system over SPME fibres. A fully automated online dynamic in-tube extraction (ITEX)-gas chromatography/mass spectrometry (GC/MS) method was introduced for continuous and quantitative monitoring of volatile organic compounds in air (Lan et al., 2019). The stability and suitability of the developed system were validated with a measurement campaign, and the ITEX method provided 2–3 magnitude lower quantitation limits than established methods. Parshintsev et al. (2015) introduced a new, fast analysis method for the desorption atmospheric pressure photoionization high-resolution (Orbitrap) mass spectrometry (DAPPI-HRMS). The DAPPI results agreed with the aerosol particle number measured with an established method and were found to detect different compounds and give complementary information about the aerosol samples.

Fragmentation of molecular clusters inside mass spectrometers is a significant uncertainty source in many chemical applications. A novel model capable of quantitatively predicting the extent of fragmentation of sulfuric acid clusters was developed (Passananti et al., 2019). The fragmentation cannot be described in terms of rate constants under equilibrium conditions, because clusters accelerate under electric fields (Zapadinsky et al., 2019). A model describing an energy transfer to the cluster-internal modes caused by collisions with residual carrier gas molecules was developed. The model can be used to interpret experimental measurements done with atmospheric pressure interface mass spectrometers.

Recently, a new atmospheric observation site equipped with state-of-the-art atmospheric aerosol instrumentation was deployed in Beijing, China (Liu et al., 2020). At the Beijing University of Chemical Technology (BUCT), the Aerosol and Haze Laboratory (AHL) was established in 2018–2019, providing novel insights into air pollution in a comprehensive manner. The station hosts comprehensive instrumentation to concentrations of atmospheric trace gases, aerosol particle size distributions and mass concentrations, and particle chemical composition on the levels from molecules, clusters and nanometre- to micrometre-sized aerosol particles. For example, the first results showed increased cluster-mode particle number concentrations during NPF events, whereas during haze days accumulation-mode particle number concentrations were high (Zhou et al., 2020). The observations have enabled us to quantify number emission factors and underlined the importance of traffic (Kontkanen et al., 2020). Daytime sulfuric acid concentrations in Beijing were typically around $4.9 \times 10^6 \text{ cm}^{-3}$ (Lu et al., 2019). During these measurements, evidence was found of significant nighttime sulfuric acid production, yielding gaseous sulfuric acid concentrations of $1.0 \text{ to } 3.0 \times 10^6 \text{ cm}^{-3}$ (Guo et al., 2021). For further results, see also Sect. 2.2.2, Urban air quality and megacities.

Besides Beijing, measurements have been performed in several other locations inside the PEEX area. We used novel instrumentation to measure new particle formation and its precursors at the background Fonovaya station in the Tomsk region (Russia, Siberia), at the Värriö subarctic research station (Finland), in Ny-Ålesund (Svalbard, Norway) and on the German icebreaker, the *Polarstern*, during the MOSAIC project. As an example, the first results from Fonovaya station are shown in Fig. 2. Thanks to these deployments, in the next years we will be able to understand the identity of NPF precursors in those remote places. This will help us to elucidate the human impact on aerosol formation and thereby on aerosol-cloud interactions at high latitudes. In Siberia, we will finally understand why new particle formation occurs infrequently and hopefully also identify the human role in this phenomenon. In the Arctic, we will understand the marine influence on NPF and will find out the detailed mechanism that leads to the formation of small clusters that initiate NPF.

Model developments were made at several scales. Aerosol-radiation and aerosol-cloud interactions are among the main sources of uncertainties in climate models, and detailed information on anthropogenic aerosol number emissions is needed to improve this situation. Anthropogenic aerosol number emissions in current large-scale models are usually converted from corresponding mass emissions in pre-compiled emission inventories using very simplistic methods. In the global aerosol-climate model ECHAM-HAM, the anthropogenic particle number emissions, converted originally from the AeroCom mass emissions, were replaced with recently formulated number emissions from the Greenhouse Gas and Air Pollution Interactions and Synergies (GAINS) model (Xausa et al., 2018). However, revisions are still needed in the new particle formation and growth schemes currently applied in global modelling frameworks.

For regional and urban scales, a fully integrated/online coupled meteorology-chemistry-aerosol model, EnviroHIRLAM, was developed (Baklanov et al., 2017) and tested for several applications in Europe, the Russian Arctic and China (Shanghai) (Mahura et al., 2018, 2020). Key issues for seamless integrated chemistry-meteorology modelling for Earth system prediction were analysed and formulated (Baklanov et al., 2018), highlighting the scientific issues and emerging challenges that require proper consideration to improve the reliability and usability of these models for three main application areas: air quality, meteorology, and climate modelling. Baklanov et al. (2018) also present a synthesis of scientific progress in the form of answers to nine key questions and provide recommendations for future research directions and priorities in the development, application, and evaluation of online coupled models.

### 2.2.2 Urban air quality and megacities (Q5)

The rapid urbanization and growing number of megacities and urban agglomerations require new types of research and
<figure><img src="image_6.png" /><figcaption>**Figure 2.** Example of results from the state-of-the-art aerosol instruments NAIS and PSM displaying an NPF event at Fonovaya station, Siberia, on 22 September 2019. Particles of different polarity, NAIS (a), ions of different polarity, NAIS (b), particle number distribution at the smallest sizes, PSM (c), and number concentration of the smallest particles in different size bins, PSM (d).</figcaption></figure>

services that make the best use of science and available tech-
nology. There are urgent needs for examining what the rising
number of megacities means for air pollution and local cli-
mate and what effects these changes have on global climate
(Baklanov et al., 2016). Such integrated studies and services
should assist cities in facing hazards, such as storm surge,
flooding, heat waves and air pollution episodes, especially in
changing climates (WMO, 2019). We discuss here the recent
observation of the atmospheric pollution in China and Rus-
sia.

Air quality in China – recent observations

China is one of the regions with the highest concentrations
of fine PM2.5 in the world (J. Wang et al., 2017). This has
serious consequences for air pollution and the associated
visibility reduction (haze) and adverse health effects (Zhao
et al., 2017). The number of haze days in China has been
growing during recent decades, but detailed understanding
of the factors governing the occurrence of haze is still not
clear (Wang et al., 2019). Both NO2 and SO2 concentrations

showed increasing trends during the 2004–2012 period, and
these trends could be linked to increased power plant and
traffic missions (Wang et al., 2019). A key feature of haze
formation seems to be an increased inorganic fraction of the
aerosol, suggesting that the reduction of nitrate, sulfate and
their precursor gases would improve air quality and visibil-
ity in China (Wang et al., 2019). In northern China, PM2.5
concentrations declined over the period 2013–2017, and ap-
proximately half of the inter-annual variability in this region
was attributed to atmospheric circulation changes (M. Li et
al., 2020). The maximum daily 8 h average O3 concentra-
tions increased over most of northern China during the same
time period, with large influences again due to atmospheric
circulation on a daily basis (J. Liu et al., 2019).

Compared with most other urban environments investi-
gated so far, measurements in urban China demonstrated a
relatively frequent occurrence of atmospheric NPF, and the
observed NPF events were typically characterized by high
particle formation rates and strongly size-dependent growth
of newly formed particles (Kulmala et al., 2016b; Z. B. Wang
et al., 2017; Chu et al., 2019). Since the first reported sub-
3 nm particle measurements in China a few years ago (Xiao et al., 2015), new insights into the formation pathways of molecular clusters and their growth have been obtained, including the relative roles of gaseous sulfuric acid, amines, ammonia and organic vapours in these processes (Yao et al., 2018; Yan et al., 2021). While high pre-existing particle loadings appear to suppress NPF during severe haze periods in Chinese megacities, it is unclear how NPF is possible at all under less but still quite polluted conditions typical of these environments (Kulmala et al., 2017). Overall, the available observations suggest NPF to be a major source of aerosol particles in urban China, with potentially large effects on haze formation (Kulmala et al., 2021) and cloud properties (Chu et al., 2019).

Urban measurements of particle number size distributions give deep understanding of the sources and atmospheric processing of fine particles. The longest urban continuous record is from the SORPES station in the Yangtze River Delta (Qi et al., 2015), covering almost a decade of measurements, whereas the broadest size range (1.5 nm–1 µm) was measured in the winter Beijing atmosphere (Zhou et al., 2020). The latter study found clear differences in particle sources in different size ranges: NPF was in general the largest source of clusters and nucleation-mode (< 25 nm) particles, while traffic contributed to all the size ranges and dominated both cluster and nucleation modes on haze days. Aitken-mode (25–100 nm) particles originated mainly from local emissions, with additional contributions from regional and transported pollution as well as from the growth of nucleation-mode particles. Regional and transported pollution was identified as the main source of accumulation-mode (> 100 nm) particles.

Air pollution and chemical transformation, including annual and seasonal variations of the concentrations of atmospheric constituents, were analysed for North China for the period 2005–2015 (Y. Bai et al., 2018). A photochemical link that related the production of fine PM and $O_3$ to VOCs was detected, and this mechanism was found to be prominent in summer. An intensive measurement campaign (SORPES station, Yangtze River Delta) was carried out to investigate sulfate formation and the associated nitrogen chemistry (Xie et al., 2015). That study highlighted the effect of $NO_x$ in enhancing the atmospheric oxidizing capacity and indicated a potentially very important impact of increasing NO concentrations on particulate pollution formation and regional climate change in East Asia. In Changzhou, a highly populated city in the Yangtze River Delta, primary organic aerosol concentrations outweighed secondary ones, indicating an important role of local anthropogenic emissions in aerosol pollution (Ye et al., 2017). The measurement also showed the abundance of organic nitrogen compounds in water-soluble organic aerosol, suggesting that these compounds are likely associated with traffic emissions.

Aerosol impacts on warm cloud properties were investigated over three major urban clusters in East China and the East China Sea using multi-sensor satellite observations (Liu

et al., 2017, 2018). In addition to the amount of aerosol, evidence was provided that aerosol types and environmental conditions need to be considered to understand the relationship between cloud properties and aerosols. Aerosol–cloud interactions were found to be more complex and of greater uncertainty over land than over the ocean.

The atmospheric boundary layer (ABL) and especially its dynamic behaviour are central to the evolution of near-surface air pollution. Using atmospheric observations combined with theoretical arguments, Petäjä et al. (2016) proposed a feedback mechanism connecting ABL properties with PM. According to such a mechanism, high concentrations of PM enhance the stability of an urban boundary layer (BL), decreasing its height and thus causing further accumulation of pollution inside the BL. Ding et al. (2016a) and Z. Wang et al. (2018) demonstrated an important role of BC aerosols in this feedback using model simulations combined with observations. A tight connection between the BL height and pollutant concentration and indications of the presence of the above feedback mechanism were also found based on comprehensive observations made on a 325 m tower in Beijing (Wang et al., 2020). In order to understand these feedbacks, Kulmala (2018) and Hari et al. (2016) emphasized the crucial role of continuous, comprehensive measurements in a network of flagship stations in tackling the air pollution problem in urban China and megacities elsewhere in the world. They also introduced the so-called SMEAR concept, which consists of integrated atmospheric and ecosystem observations allowing the analysis of Earth surface–atmosphere feedbacks and interactions. The first SMEAR-type station in China, the SORPES station located in the Yangtze River Delta, has been operating since 2011 (Ding et al., 2016b).

## Anthropogenic emissions and environmental pollution in Russia

In the complex situation of the plurality of emissions, an important research task remains in the Moscow megacity environment for the assessment of the air quality and potential sources through aerosol composition analyses. Moscow aerosol pollution has been studied using a special AeroRadCity-2018 experiment (Chubarova et al., 2019a) and satellite data with the application of the new MAIAC/ MODIS aerosol algorithm with a 1 km resolution (Zhdanova et al., 2020). An advanced source apportionment for this environment was performed using combined Fourier-transform infrared spectroscopy data and statistical principal component analysis (O. Popovicheva et al., 2020a). The main principal component loadings revealed the source impacts of transport and biomass burning, biogenic, dust and secondary aerosol in spring. Identification of biomass burning-affected periods discriminated between the daily aerosol composition change with respect to air mass transport and the number of fires detected in the surrounding areas. Measurements of particulate BC were conducted at an urban background site
(Meteorological Observatory of MSU) during the spring period of 2017–2018 (O. Popovicheva et al., 2020b). The mean BC concentrations displayed significant diurnal variations, with a poorly prominent morning peak and minimum at daytime. BC mass concentrations were higher at nighttime due to the shallow boundary layer and intensive diesel traffic. The aerosol optical thickness (AOT) over Moscow showed a pronounced seasonal cycle, with a summer maximum and winter minimum (N. Y. Chubarova et al., 2016). It was found that during 2001–2014, the monthly-mean values of AOT declined by 1 % yr⁻¹–5 % yr⁻¹, and this decline was attributed to decreased emissions of aerosols and their precursors.

In general, the atmospheric environment over remote areas of Siberia and northern Asia is relatively clean compared with other surrounding regions of Asia and eastern Europe (Baklanov et al., 2013). However, air pollution from Siberian industrial centres poses significant environmental threats. For Siberian cities (e.g. Norilsk, Barnaul, Novokuznetsk), the air quality is among the worst in Russian and European cities. Similar to Arctic cities, stable atmospheric stratification and temperature inversions dominate for more than half a year. This leads to pollution accumulation near the surface, which influences ecosystems and people. Moreover, not only severe climatic conditions, but also man-made impacts on the environment in industrial areas and large cities have intensified. The impacts manifest themselves as the pollution of the environment, land use changes, hydrodynamic regimes and the local climate. Ultimately, these impacts feed back to people, affecting their health and well-being.

The Russian part of the Barents Euro-Arctic region includes severe emission “hotspots” for air pollutants. The Kola Peninsula, despite the presence of areas with undis turbed nature in the eastern part, is the most industri ally developed and urbanized region in the Russian Arc tic. The main polluters are the smelters of the Severonickel (Monchegorsk, central part of the peninsula) and Pechengan- ickel (Nickel and Zapolyarnyi near the Russian–Norwegian border) enterprises. For comparison, emissions of SO₂ from the nickel smelter alone are 5–6 times larger than the total Norwegian emissions (Sandanger et al., 2013). In 2015, No- rilsk Nickel in Siberia – the biggest mining and metallurgical complex – emitted about 1.9 million tonnes of SO₂ (GGO, 2016). With the nickel factory (located in the southern part of the city), copper factory (just to its north) and metallurgi cal plant (12 km to the east), the city of Norilsk is influenced by heavy industry no matter which way the wind blows. The Blacksmith Institute declared in 2007 that Norilsk is one of the top 10 worst-polluted places in the world. The impacts of emissions are manifested as deterioration of forest ecosystems and acidification of soils and surface waters (Derome and Lukina, 2011), even at considerable distances from the smelters. Heavy metals and alkaline pollutants contaminate areas around the sources of pollution within a few hundred kilometres, while acid sulfates can be transported over long distances (Mahura et al., 2018).

A recent analysis of the total deposition and loading on the population in north-western Russia and Scandinavian countries caused by the continuous sulfur emissions from the Cu–Ni smelters in Murmansk indicates the dominance of wet deposition, especially in wintertime (Mahura et al., 2018). North-western Russia is influenced more by the Severonikel emissions compared with countries in the Scandinavian Peninsula. The cities of the Murmansk region (Kola Peninsula) are under the highest impacts. On a yearly scale, the individual loadings on the population are at the highest level (up to 120 kg/person) in the Murmansk region, much lower (15 kg/person) in northern Norway, and lowest (< 5 kg/person) in eastern Finland, the Republic of Karelia and the Arkhangelsk region. Distinct seasonal variability was identified, with the lowest contribution during summer and the highest contribution during winter–spring in Russia, during spring in Norway, and during autumn in Finland and Sweden.

The annual yearbook, the State of Atmospheric Pollu- tion in cities in the Territory of Russia for 2018 (Roshy- dromet and GGO, 2019), states that the highest atmospheric emissions of PM were observed in Siberian and Ural cities. In Novokuznetsk and Omsk, the observed PM was highest (> 30 000 t yr⁻¹), while emissions from other cities such as Angarsk and Chelyabinsk were lower (< 20 000 t yr⁻¹). Note that in the 2015–2019 yearbooks, emissions from only sta- tionary sources were provided due to revisions (approved and implemented in November 2019 by the Russian Min- istry of Natural Resources and Ecology, MNRE) of methods applied for estimation of emissions into the atmosphere from mobile sources. Depending on source type, different meth- ods to calculate emissions are applied (MNRE, 2019). For the gaseous compounds, such as SO₂, the maximum emis- sions included were very high from Siberian cities (e.g. No- rilsk, Novosibirsk, Novokuznetsk, Omsk, Ufa, Irkutsk, An- garsk) and from north-western Russian cities (Zapolyarny, Nickel, Monchegorsk). High NO₂ emissions were observed in Novosibirsk, Omsk, Angarsk and Chelyabinsk. The CO integral urban emissions depend on a city’s size. These var- ied from less than 10 Gg yr⁻¹ (for small regional centres like Vladimir, Kursk, or Samara) to 406 and 804 Gg yr⁻¹ for large metropolitan areas such as St. Petersburg and Moscow. As a whole, an analysis of spatiotemporal variation of trace gases in the boundary layer over Russian cities indicated significant emission variations between the urban environments and re- mote sites (Elansky et al., 2016).

Cities, not being isolated systems, may distribute as much pollution to the surrounding areas as they receive from out- side them or from remote regions. The analysis of the trans- boundary atmospheric transport between Russian Siberia and bordering countries (e.g. China, Kazakhstan, and Mongo- lia) is part of a mutual risk assessment for urban areas/cities and their surroundings. For example, the city of Ulaanbaatar (Mongolia) suffers from high levels of pollution due to ex- cessive airborne particulate matter emanating from coal com-
bustion mixed with traffic emissions and resuspended soil dust, resulting in variable chemical source profiles (Gunchin et al., 2019). Long-range transport from remote sources might be an additional contributor. Moreover, there are indications that such transport of biomass burning emissions from Siberia could lead to pollution episodes and impact surface ozone as far as in western North America (Jaffe et al., 2004).

### 2.2.3 Weather and atmospheric circulation (Q6)

The observed evolution of weather and climate represents the combined effects of external forcing (changes in the concentrations of greenhouse gases and aerosols, etc.) and internal variability, related to a large extent to the atmospheric circulation. It is also affected by local factors, particularly urban heat islands in cities. Here we discuss these interconnected processes, focusing on cold and warm episodes, cyclone density and atmosphere-ocean interactions, effects of circulation on temperature and moisture, cloudiness in the Arctic, and boundary-layer dynamics relevant to the Arctic-boreal region.

#### Cold and warm episodes

The Arctic warming as well as the Arctic amplification have been associated with changes in atmospheric large-scale circulation together affecting the European winter temperatures. In large parts of Europe, severe cold (warm) winter events are significantly correlated with warm (cold) Arctic episodes (Vihma et al., 2020). Air mass trajectory analysis revealed that air masses associated with extreme cold (warm) events typically originate from over continents (sea areas). Despite Arctic and European-wide warming, winter cooling has occurred in north-eastern Europe in cases of air masses arriving from the south-east (Vihma et al., 2020).

#### Cyclone density dynamics and atmosphere-ocean interaction

Transporting large amounts of heat and moisture from mid latitudes to the central Arctic, synoptic-scale cyclones are vital for the Arctic climate system. Recent findings, based on atmospheric reanalysis, above all the global ERA-Interim reanalysis available from 1 January 1979 to 31 August 2019, are summarized below. During 1979–2016 in winter (December, January, February), the cyclone density increased in the areas around Svalbard and in the north-western Barents Sea but decreased in the south-eastern Barents Sea (Wickström et al., 2020). This is related to a shift to more meridional winter storm tracks in the Norwegian, Barents, and Greenland seas. The shift is favoured by a positive trend in the Scandinavian pattern and, in the areas north of Svalbard, by a significant increase in the eddy growth rate (Wickström et al., 2020).

Numerical model simulations of the storm activity in the White, Baltic and Barents seas were analysed for the period 1979–2015 (Myslenkov et al., 2018). A high inter-annual variability in the storm number was observed for all studied seas. No significant trends in the storm number during the period 1979–2015 were found in the studied sea areas. On average, the connection with global atmospheric circulation is stronger for the Baltic Sea than for the other two seas. Also, the future changes in wind wave climate were analysed. According to the RCP8.5 scenario, in the second part of the 21st century the number of storm events will rise in the Baltic and Barents seas.

In the Bjerknes compensation, changes in atmospheric heat transport co-occur with opposing changes in ocean heat transport. Observations and model simulations indicate a central role for ocean-atmosphere heat exchange in the Barents Sea area in maintaining this compensation in the Arctic (Bashmachnikov et al., 2018a, b).

#### Circulation effect on temperature

The effect of atmospheric circulation on temperature trends in the years 1979–2018 was studied by Räisänen (2019, 2021) using a trajectory-based method. He found that the circulation trends had reduced the annual mean warming during this period in West and central Siberia locally by over 1 °C, with a much larger cooling effect in autumn and winter (Fig. 3). His findings also confirmed a circulation-induced amplification of warming over the Barents and Kara seas, particularly in winter. However, in most areas the circulation-related temperature trends have varied strongly from month to month, leaving only a relatively small effect on the annual mean temperature trends. The residual warming obtained after subtracting the circulation effect therefore tends to have a smoother seasonal cycle than the observed temperature trends, in better agreement with the multi-model mean trends in the CMIP5 simulations (Taylor et al., 2012).

#### Circulation effect on moisture

The effects of large-scale circulation on moisture, cloud and longwave radiation occur mostly via the impact of horizontal moisture transport (Nygård et al., 2019). Evaporation is typically not efficient enough to shape those distributions, and much of the moisture evaporated in the Arctic is transported southward (Nygård et al., 2019). Strong moisture transport events avail a large part of the northwards moisture transport. The meridional net transport is only a small part of the water vapour exchange between the Arctic and mid-latitudes (Naakka et al., 2019). When a high-pressure pattern across the Arctic Ocean from Siberia to North America is lacking, the amounts of moisture, clouds and downward longwave radiation are anomalously high near the North Pole (Nygård et al., 2019). Using vertically integrated water vapour as a metric, the Arctic (north of 70°N) has experienced a robust
<figure><img src="image_7.png" /><figcaption>**Figure 3.** Linear trends of monthly mean temperature in West Siberia (55–65° N, 65–90° E) in the years 1979–2018. In (a), the red bars show the trend in the ERA5 reanalysis and the blue bars the circulation-related trend. In (b), the residual trends are shown. The error bars indicate the 5%–95% uncertainty range in the circulation-related trend and the residual trend based on inter-annual variability. Redrawn from Räisänen (2021).</figcaption></figure>

moistening trend since 1979, and in absolute numbers this trend is smallest in March and largest in August (Rinke et al., 2019). However, the relative trends are largest in winter. Although different atmospheric reanalyses are consistent in spatiotemporal trend patterns, they scatter in the trend magnitudes.

Analysis of moisture and aridity estimated using the web-GIS “CLIMATE” and the ECMWF ERA-Interim reanalysis data for southern Siberia (50–65° N, 60–120° E) from 1979 to 2010 with a 0.75° × 0.75° grid resolution showed that the mountain regions of eastern Siberia have become more arid each month during the last 30 years (Ryazanova and Voro-pay, 2017). In West Siberia, aridity increased in May and decreased in June, while in the other months positive and negative trends were found. The greatest differences in the trends of the aridity index, air temperature and precipitation were observed in July.

## Cloudiness in the Arctic

The climatology and inter-annual variability of Arctic cloudiness remain a wildcard in regional climate change projections. Both climate models and satellite data products need in situ observations for calibration and validation. Chernokulsky et al. (2017) and Chernokulsky and Esau (2019) collected and processed manual cloud observations from meteorological stations in the PEEX area. The cloud records in the Arctic have been available since the end of the 19th century. Since 1936, cloud observations have representatively covered the Eurasian Arctic. This permits reconstructions of cloud type and cloud cover climatologies as well as studies of interdecadal variability of cloudiness. A problem of special interest is related to the co-variability of the total cloud cover and sea ice concentration or extent. Both clouds and sea ice affect the surface heat balance through surface albedo, but their feedback mechanisms, dynamical impacts and climate sensitivities are different. Chernokulsky et al. (2017) found that the annual-mean total cloud cover (TCO) decreases during warmer climate periods with a lower sea ice concentration but increases over sea ice in the Barents Sea as more moisture is transported into the Arctic at higher temperatures. Furthermore, the increasing TCO reduces the deficit of the surface heat, and the intra- and inter-annual variability of TCO over solid ice is higher than that over open water (Chernokulsky et al., 2017). Long-term cloud climatological analysis based on meteorological observations of the total and low cloud cover and cloud types from the Barents Sea to the Chukchi Sea showed that significant transitions between cloud types have taken place, and especially the low-level stratus and stratocumulus types have been transformed to convective cloud types (Chernokulsky and Esau, 2019). Chernokulsky and Esau (2019) addressed how their results are relevant for understanding Arctic cloud processes and feedbacks and how new knowledge is needed to connect the changes in the Arctic radiation balance with the Arctic cloud cover-cloud type climatology.

## Boundary-layer dynamics and urban heat islands

Against the background of accelerated and amplified Arctic warming, anthropogenic heat release and metabolism of cities add up to persistent warm temperature anomalies in urbanized areas (Fig. 4). Indeed, if the climate change forcing approaches 2 W m⁻², the urban heat forcing could be 10–100 W m⁻² (Konstantinov et al., 2018). The urban heating trapped in shallow planetary boundary layers is potent to raise the local temperatures by 1 to 10 °C or even more. This local climate phenomenon is known as an urban heat island (UHI) (Esau et al., 2020). A series of in situ and satellite UHI studies in the northern cities revealed strong and persistent warm temperature anomalies in almost all of the 28 northern West Siberian cities (Miles and Esau, 2017), in 5 cities covered by the UHIARC network (Konstantinov et al.,
2018; Varentsov et al., 2018a) and in 57 Scandinavian cities (Miles and Esau, 2020). The mean wintertime temperature anomalies and the UHI intensity varied from 0.8 to 1.4 K and had extreme intensities of up to 7 K during cold anti-cyclone weather conditions. The complete data set of surface UHI intensity derived from MODIS land surface temperature (LST) data products is freely available and published in Miles (2020). Such a UHI-induced strong mediation of cold temperature spells might cause significant socio-economic and environmental impacts in the cities (Konstantinov et al., 2018, Fig. 4). A survey of other UHI studies in 11 Arctic cities and towns confirmed that even relatively small cities at high latitudes may exhibit intensive UHIs. A recent analysis confirms the important role of the surrounding temperature in explaining spatial-temporal variation of the UHI intensity (Miles and Esau, 2017). The major contribution to the UHI was revealed for water, sparse vegetation, grassland and scrubland. The mechanisms and pathways of the UHI maintenance require an involvement of numerical experiments with turbulence-resolving models to advance the understanding of the local climate features (urban heat islands – UHIARC data set; see http://urbanreanalysis.ru/uhiarc.html, last access: 18 January 2022). We would need a denser meteorological network, especially high-quality temperature data, to better understand the urban climatology and the thawing processes in urban soils and to better assess climatic trends relevant to Arctic societies and welfare (Konstantinov et al., 2018).

Urban climate anomalies may cause more extreme weather and climate phenomena in densely populated megacities. The Moscow agglomeration – the largest megacity in the boreal continental climate within the PEEX domain – demonstrates a profound effect of interactions between the UHI and urban winds, known as a cross-over effect (Varentsov et al., 2018b). The UHI creates an urban heat “dome” with near-surface air inflow into the urban central districts and air outflow at higher levels in the atmosphere. The air uplift in the urban dome is connected to the increase in summer rainfall on the lee side and over the central urban districts. Stable atmospheric stratification over rural areas is strengthened by the downwind air motions coming from the urban region.

The atmospheric boundary layer over the Arctic Ocean has been studied on the basis of tethersonde sounding observations over sea ice (Palo et al., 2017) and research aircraft observations over the open ocean and sea ice (Suomi et al., 2016). Palo et al. (2017) found that in spring and summer, the occurrence and properties of temperature inversions were controlled by the surface melt and warm air advection rather than surface net radiation. During snowmelt/ice melt, temperature inversions were frequently surface-based and equally as strong as winter inversions over the Arctic Ocean. To better understand atmospheric boundary-layer processes in the Arctic, Suomi et al. (2016) developed a method to measure wind gusts from a research aircraft. It allows wind gust

<figure><img src="image_8.png" /></figure>

**Figure 4.** The northern urban heat islands are forerunners of the global warming. Winter season future temperatures for the Arctic (60–90° N) averaged over 36 CMIP5 global climate models and expressed as departures from the means for the 1981–2005 period. The red line is the ensemble mean for RCP8.5, and the blue line is for RCP4.5. Shaded areas denote ±1 standard deviation from the ensemble mean (Overland et al., 2014 and Fig. 2.15 of AMAP, 2017). The observed surface UHIs are shown as red dots collocated with the expected future Arctic temperature anomalies; e.g. the observed wintertime urban temperature anomaly in Nadym corresponds to the regional warming as expected to be reached by 2060. Observe that the present Arctic climate is already 1.5 °C warmer than the historical normals 1960–1990.

observations at altitudes not reached by traditional weather mast observations. The observed gust factors strongly depended on the surface roughness, which differed for sea ice and the open ocean.

## 2.3 Arctic-boreal aquatic system

We discuss the recent results on Arctic sea ice dynamics and thermodynamics, snow depth and sea ice thickness, sea ice research supporting navigation, and rare elements in snow and the ocean sediments, especially from the perspective of improvements in the observation and modelling methods (Q7, Sect. 3.3.1). We introduce new results on the Arctic marine ecosystem and focus on the primary production and carbon cycle (Q8, Sect. 3.3.2). In Sect. 3.3.3 for the Arctic-boreal lakes and rivers, we discuss the browning of lakes and lake sediment with special attention to the Selenga River system of Lake Baikal (Q9).
### 2.3.1 Changing water systems, snow, sea ice and ocean sediments (Q7)

#### Sea ice and thermodynamics with atmospheric and ocean dynamics

Referring to the earlier discussion in Sect. 2.2.3 on atmospheric circulation, we address here how the sea ice dynamics closely interacts with the atmospheric and ocean dynamics. A rapid decrease in the Arctic Ocean ice cover, particularly in the Barents and Kara seas, has been taking place since the late 1970s simultaneously with the cooling of winters in central Eurasia (McCusker et al., 2016). This unexpected winter cooling is related to increasing north-easterly winds over the south-eastern flank of an anomalous high that has developed over the north-western coast of Russia (McCusker et al., 2016; Mori et al., 2019, Räisänen, 2021). However, the causality between the atmospheric circulation changes and the Arctic sea ice decrease is debated. Observations suggest a strong correlation between these two, but climate model simulations forced by reduced ice cover produce much weaker circulation changes than observed, resulting in only weak cooling in central Eurasia (Mori et al., 2014, 2019; McCusker et al., 2016). This suggests either that most models are underestimating the sensitivity of the atmospheric circulation to sea ice decrease, supported by Romanowsky et al. (2019), or that the circulation change has not been primarily caused by the decreasing sea ice. In the latter case, the correlation between the reduced ice cover and atmospheric circulation would mainly reflect the effect of circulation on sea ice. In support of this, Blackport et al. (2019) showed that reduced sea ice coincides with an anomalous heat flux from the atmosphere to the ocean and that, on the sub-seasonal timescale, anomalies in atmospheric circulation tend to precede rather than follow those in sea ice. Thus, while the reduced sea ice might partly explain the observed changes in atmospheric circulation (Mori et al., 2019), the effect of circulation on sea ice appears to be stronger than the effect of sea ice on circulation.

Considering atmosphere-ice interactions, Jakobson et al. (2019) studied the linkages between sea ice concentration (SIC), atmospheric stratification, surface roughness and wind speed at the 10 m height (W10) and 850 hPa level (W850). In all the seasons except summer, a reduction in SIC favoured reduced atmospheric stratification and aerodynamic surface roughness, which resulted in a stronger W10. The effect was strongest in autumn, and positive trends in W10 and its ratio to W850 typically occurred in regions with the strongest negative trends in SIC. The relationships were stronger on inter-annual than sub-seasonal timescales. Large-scale atmospheric circulation, characterized e.g. by the dipole anomaly (DA), has also contributed to sea ice dynamics. A positive polarity in the DA has contributed to the recent rapid loss of summer sea ice in the Pacific part of the Arctic Ocean by bringing warmer air masses from the south and transporting

more ice towards the north, enhancing the ice-albedo feedback (Lei et al., 2016). Another example of ice dynamics affecting the ice-albedo feedback was the weakened Transpolar Drift Stream in summer 2013. It reduced sea ice transport out of the Arctic Ocean and restrained ice melt because of the low air temperatures, weakened albedo feedback, and a relatively small oceanic heat flux in the central Arctic (Lei et al., 2018).

Solar radiation, being the main forcing factor for a sea ice melt in summer, is difficult to parameterize in thermodynamic models. This is due to the large variability in the optical properties of sea ice in space and time. A two-stream model provides a time-efficient parameterization of the apparent optical properties (AOPs) for ponded sea ice, accounting for both absorption and scattering, and has a potential to be implemented in sea ice thermodynamic models to explain the role of melt ponds in the summer decay of Arctic sea ice (Lu et al., 2016). This model was used to investigate the role of solar radiation in the Arctic sea ice during the melting season considering layers of melt ponds, underlying sea ice, and the ocean beneath the ice. It was found that the energy absorption profiles depend strongly on the incident irradiance and ice scattering but only weakly on the pond depth. It seems that the incident solar energy is largely absorbed by the melt pond rather than by the underlying sea ice (Lu et al., 2018a). The model was further applied to investigate the influence of a surface ice lid on the optical properties of a melt pond. The thickness of the ice lid determines the amount of solar energy absorbed. Visual inspections of the colour of refreezing melt ponds also help to judge the significance of the influence of the ice lid. This will allow for an accurate estimation of the role of surface ice lids during field investigations of the optical properties of melt ponds (Lu et al., 2018a). The modelled pond colour agrees with field observations from the Arctic sea ice in summer. The analysis of pond colour is a new potential method to obtain ice thickness in summer; however, more validation data and improvements to the radiative transfer model would be needed (Lu et al., 2018b).

#### Snow depth/mass and sea ice thickness

Snowpack on sea ice has a crucial role in insulating the sea ice from the colder atmosphere, accordingly reducing sea ice growth in winter, effectively reflecting the incoming solar radiation, reducing sea ice melt in spring and summer and contributing to its formation. The replacement of snowfall by rain strongly enhances the ice-albedo feedback in the Arctic Ocean (Dou et al., 2019). Shalina and Sandven (2018) refined the description of snow depth on sea ice in the central Arctic, providing new snow depth data for the Arctic marginal seas. High autumn and winter precipitation and thinning Arctic sea ice make snow-ice formation prevalent in the Atlantic sector of the Arctic (Merkouriadi et al., 2017).
Advances have been made in applying thermistor string-based autonomous high-resolution Snow and Ice Mass Balance Array (SIMBA) buoys to measure snow depth and ice thickness (Figs. 5 and 6). SIMBA has a lower cost, allowing deployment in large numbers (Lei et al., 2015). The determination of snow depth and ice thickness from SIMBA temperature profiles has so far been largely a manual process. A SIMBA algorithm was developed to process SIMBA data automatically (Liao et al., 2018), assuming a fixed snow-ice interface. Snow-ice formation results in the snow-ice interface moving upward. The SIMBA algorithm was further developed to tackle the moving interfaces (Cheng et al., 2020). The developed SIMBA algorithm works well under cold conditions for lakes and polar oceans. For polar oceans, the snow and ice are close to isothermal during summer, which prevents the identification of interfaces on the basis of the temperature gradient. Under such conditions, thermodynamic modelling yields valuable information on snow depth and ice thickness (Tian et al., 2017).

A challenge in sea ice thermodynamic modelling is the uncertainty in the magnitude of the oceanic heat flux at the ice base, especially for land-fast sea ice. Yang et al. (2015) applied a one-dimensional thermodynamic model to investigate impact factors in land-fast sea ice in the East Siberian Sea. The modelled snow cover was less than 10 cm, having a small influence on the ice thickness, but surface albedo and oceanic heat fluxes were critical.

Also in the terrestrial Arctic and boreal zone, there is a need for better efficiency and coverage of an in situ snow observation network. Snow cover and snow mass are fundamental parameters for global energy and water cycles, and the changes in the regional snowpack have societal impacts, like on the amount of drinking water or the capacity for hydropower generation (Bormann et al., 2018). Snow depth data in the Arctic region are available from the synoptic weather stations and snow mass data are systematically collected from the snow courses, as demonstrated in extended data (Fig. 2) by Pulliainen et al. (2020). The use of automatic and cost-effective measurements together with harmonized snow measurement practices is the way forward. A survey on harmonized snow monitoring in Europe demonstrated that crucial parameters for operational services, such as parameters characterizing precipitating and suspended snow, are measured by 74% of the European snow network contributors (COST Action ES1404), but the parameters characterizing the snow microstructural properties, electromagnetic properties and composition are currently measured by only 41%, 26% and 13%, respectively, of the network contributors (Pirazzini et al., 2018). The observations at the continental scale, so far, demonstrate a widespread snow cover retreat since the 1970s across the Northern Hemisphere, particularly in the Arctic (Derksen and Brown, 2012; Bormann et al., 2018). By contrast, the results from the mountains are mixed, and there is no consistent picture of what is happening at the regional scale (Bormann et al., 2018). Pulliainen

<figure><img src="image_9.png" /><figcaption>**Figure 5.** Trajectories of SIMBA buoys deployed in the Arctic in the period 2018–2019. Red: Chinese National Arctic Research Expedition (CHINARE) (10 buoys), green: Nansen and Amundsen Basins Observational System (NABOS) (5 buoys), dark blue: CAA-TEX (2 buoys), and light blue: MOSAIC (15 buoys). SIMBA is a thermistor string-based ice mass balance (IMB) buoy. It measures high-resolution (2 cm) vertical environment temperature (ET) profiles (four times a day) through the air–snow–sea ice–ocean column. The heating temperature (HT) measured by the thermistor string once per day is based on the use of a small identical heater on each sensor. The ET and HT data are used to derive snow depth and ice thickness. SIMBA uses the GPS module to track the buoy location. The Iridium satellite is used for data transmission. A total 15 SIMBA buoys were deployed in the Arctic Ocean during the CHINARE 2018 and NABOS 2018 field expeditions in late autumn. In 2019 17 SIMBA buoys were deployed during the CAATEX (2) and MOSAIC expeditions (15, leg 1).</figcaption></figure>

et al. (2020) provided new insight into the seasonal snow mass and its trend by using a bias-corrected GlobSnow 3.0 estimate. Pulliainen et al. (2020) were now able to demonstrate different continental trends based on the 39-year satellite record: a decrease in North America, a negligible trend in Eurasia, and a high regional variability in both areas.

## Sea ice research supporting navigation

Recent research has addressed emerging opportunities for Arctic navigation and the importance of operational sea ice analysis. Lei et al. (2015) showed trends along the Arctic Northeast Passage (NEP) and demonstrated an increase in the spatially averaged length of the open period (the ice concentration less than 50%) from 84 d in the 1980s to 114 d in the 2000s. The summer sea ice along the high-latitude sea route (HSR) north of the eastern Arctic islands has de-
<figure><img src="image_10.png" /><figcaption>**Figure 6.** SIMBA observations of the temporal evolution of the snow depth, ice thickness, and temperature profile from the ocean through snow and sea ice to air. The results were obtained by applying the algorithm by Liao et al. (2018). The black lines are snow surface (top), initial freeboard (middle) and ice base (bottom); 0 level refers to the snow–ice interface. The colours indicate the temperature in degrees Celsius.</figcaption></figure>

creased during the last decade, with the ice-free period reaching 42 d in 2012. The HSR avoids shallow waters along the coast, which eases access for deeper-draft vessels (Lei et al., 2015). Considering operational sea ice analyses for the Bohai Sea, work has been done to combine thermodynamic modelling and Earth observation (EO) data from synthetic aperture radar (SAR) and microwave radiometers (Karvonen et al., 2017). The SAR-based discrimination between sea ice and open water works well, and areas of thinner and thicker ice can be distinguished. However, a larger comprehensive training data set is needed to set up an operational algorithm for the estimation of sea ice concentration and for the weighting scheme for sea ice thickness (Karvonen et al., 2017).

Multi-decadal Arctic sea ice state estimates are important for the strategic planning of Arctic navigation. These estimates are usually based on climate models with a thermodynamic–dynamic sea ice model. An up-to-date assessment of large-scale sea ice models was with the aid of sea ice models as a climate model component, and a comprehensive review was carried out by Leppäranta et al. (2020). Specifically, Uotila et al. (2015) found that a model with the subgrid-scale sea ice thickness distribution reproduces more realistic sea ice and upper ocean, due to better-captured spring evolution, than a model with just a single sea ice thickness category. In terms of the validity of initial conditions for multi-decadal predictions, Uotila et al. (2019) analysed a set of ocean reanalysis products, including Arctic sea ice, and found that the multi-model set mean is a useful product as a state estimate. This finding increases confidence in the use of

the combination of ocean reanalysis for both initialization of multi-decadal predictions and analysis of multi-decadal variability.

## Ocean floor and sediments: composition and fluxes

A significant content of illite and muscovite among layer silicates in most of the ice-rafted sediment samples taken from selected Arctic regions suggests that sources of the sedimentary material are mainly mineralogically similar to modern bottom sediments of the East Siberian and Chukchi seas as well as presumably sediments of the eastern Laptev Sea. A significant kaolinite fraction in the samples from the North Pole area can be caused by the influx of ice-rafted fine-grained sedimentary material from the Beaufort or Chukchi seas, where kaolinite is supplied from the Bering Sea. The samples contained variable proportions of erosion products of both mafic and felsic magmatic rocks and/or sufficiently mature sedimentary rocks (Maslov et al., 2018a).

Quantification of CH₄ sources is fundamental information for the climate change mitigation (Fletcher and Schaefer, 2019). Methane stored in ocean floor reservoirs can reach the atmosphere in the form of bubbles or dissolved in water. Methane hydrates could destabilize with rising temperatures, further increasing greenhouse gas emissions in a warming climate. Subsea permafrost and hydrates in the ESAS act as a substantial carbon pool and source of methane to the atmosphere. Annual methane emissions of the region vary from 0.0 to 4.5 Tg CH₄ yr⁻¹ estimated by Berchet et al. (2016). Yasunaka et al. (2018) estimated the monthly air–sea CO₂ fluxes in the Arctic Ocean and adjacent seas located north of 60°N for the period 1997–2014 and ended up at a net annual Arctic Ocean CO₂ uptake of 180 ± 130 Tg C yr⁻¹.

The Zeppelin Observatory data for 2014 suggest that the CH₄ fluxes from the Svalbard continental platform are smaller than 0.2 Tg yr⁻¹. All estimates are in the lower range of values reported earlier (Pisso et al., 2016). Platt et al. (2018) reported a potential region with high ocean–atmosphere CH₄ fluxes located north of Svalbard but addressed how at the time of the measurements the meteorological conditions were unique, including a short episode of the highly sensitive emissions over an active seep site without a sensitivity to land-based emissions.

## River runoff affecting the hydrological processes in coastal marine environments

The Arctic Ocean, including the Hudson Bay, receives 55.6% of its river inflow from Russia, mostly via 19 large rivers (Shiklomanov and Shiklomanov, 2003). This freshwater inflow of approximately 2920 km³ yr⁻¹ (Shiklomanov et al., 2008) is associated with large sediment and heat transports, which together affect the hydrography, marine climate and ecosystems across the Siberian shelf seas (Magritsky et al., 2018). A major part of seasonal and inter-annual varia-
tions in the river runoff is anthropogenic due to regulation in large reservoirs (Georgiadi et al., 2016). In addition, Magritsky et al. (2018) detected an increased runoff trend of 5%–10%, compared to a reference period of 1936 to 1975, in most of the major Russian rivers discharging into the Arctic Ocean. This trend is mostly due to a climate-induced increase since the second half of the 1980s (Magritsky et al., 2018). However, due to gaps in the monitoring programmes, these estimates have a large uncertainty: focusing on river discharges from the six largest Eurasian rivers to the Arctic Ocean, estimates of the increase range from 7% (Peterson et al., 2002) to 1.5% (Shiklomanov and Lammers, 2009).

Permafrost thawing has resulted in releases of old carbon storages, but so far there is no clear evidence of the impact of permafrost thawing on the net emissions of CO₂ and CH₄ into the atmosphere (IPCC, 2019). A potential explanation of no or weak net increase is that a fraction of the released methane has been taken by rivers instead of being emitted into the atmosphere. Increased amounts of organic carbon in rivers impact the regional and global biochemical and methane cycles (Shakhova et al., 2007; Wild et al., 2019). With the accelerating permafrost thaw, the atmospheric emissions are also expected to increase, in particular for CO₂, but also for CH₄. Expected future changes in river ice regime are consistent with the expected changes in the duration of the cold season and accumulated negative air temperatures. Significant changes are expected for the rivers in the Kola Peninsula and the lower reaches of the Northern Dvina and Pechora rivers, whereas the lowest changes are expected for the central parts of eastern Siberia (Agafonova et al., 2017). Due to anthropogenic activities (above all industry, municipal services, and filling of reservoirs), water withdrawal from Russian Arctic rivers and related groundwater systems is approximately 20.6 km³ yr⁻¹, and it is expected to increase to 37 km³ yr⁻¹ by 2025 to 2030 (Magritsky et al., 2018). Features of these changes at the marine margin of the Lena River Delta are different compared to changes in the delta head area.

The hydrological representativeness of a glacier is a new characteristic and of practical importance for basin-wide tasks of hydrology and glaciology. For its evaluation, it is proposed to replace the seasonal air temperatures with the glacier summer mass balance (BS) or to include BS in the multiple regression equations for calculating the runoff of rivers fed by melting of snow and ice. This method can be recommended for at least some glaciers in the existing network of the World Glacier Monitoring Service (WGMS) (Konovalov et al., 2019).

### 2.3.2 Marine ecology (Q8)

#### Living marine organisms weaken or even subdue CO₂ accumulation

The important climatological role of the world's oceans is to reduce the CO₂ accumulation into the atmosphere through its absorption. This mechanism is ordinarily viable as the partial pressure of dissolved CO₂ in marine surface waters is less than the content of CO₂ in the overlying atmosphere. Due to the organic pump, a net drawdown of atmospheric CO₂ into the ocean is put into effect. It proceeds in the process of sinking of particulate organic carbon of algal origin: organically bound CO₂ is released through remineralization and further accumulated in the deep ocean. In contrast, owing to the processes of a carbonate counter pump, CaCO₃ is exported downward and, at depth, dissolves, causing a net release of CO₂ into the atmosphere (Balch et al., 2016). However, there are living marine organisms that are able to weaken or even subdue CO₂ accumulation, at least within their habitat. Among this group of marine organisms, the leading role belongs to coccolithophores. Among marine biosystems, coccolithophores (class Prymnesiophyceae) are the most productive calcifying algae (Taylor et al., 2017). They both produce particulate inorganic carbon (in the form of calcite) and promote the increase in CO₂ partial pressure (pCO₂) in the ambient marine surface waters. Thus, the biological activity of coccolithophores can exercise a direct influence on both the CO₂ flux exchange at the atmosphere-ocean interface and the marine carbonate chemistry system (CCS). The rain ratio, i.e. the ratio of particulate inorganic carbon to organic carbon, determines the intensity and direction of CO₂ flux at the atmosphere-ocean interface. In the case of coccolithophores, the rain ratio is above unity within their habitat area, which potentially can have climatic consequences but also drive alterations in marine CCSs (Balch, 2018).

Emiliania huxleyi is the most widespread coccolithophorid algal species in Earth's oceans, which, in light of the above, naturally explains why this is one of the best-studied marine algae. Of all other coccolithophores, *E. huxleyi* is probably the most successful in forming extensive blooms in worldwide marine waters ranging from oligotrophic to eutrophic. Unlike diatoms and dinoflagellates, this alga is phenomenally immune to both light limitation and very high light intensities. As high levels of incident light/irradiances enhance calcification (which is predominantly a light-dependent reaction), it is supposed that the calcification machinery enables *E. huxleyi* cells to resist photodamage by dissipating excess energy. This specialty is important in the case of nutrient-depleted waters, especially in combination with the high affinity of *E. huxleyi* for nutrients including nitrogen, but especially phosphorous. The properties of both mixotrophic nutrition and resistance, at least partially, to zooplankton grazing and virus attacks (due to a cell's coverage by calcite
scales/coccoliths) contribute to this alga's ability to sustain a variety of unfavourable conditions and retain steadfastly its ecological niche (Godrijan et al., 2020). Thus, the elabo-rate biology of *E. huxleyi* cells imparts to them the intrinsic and rather rare property of pursuing growth-maximizing and loss-minimizing life strategies. This property reveals itself through multiple manifestations, two of which are vastness and sustainability of *E. huxleyi* bloom areas. A typical bloom surface is not less than thousands of square kilometres, but in many marine environments it is far larger (Kondrik et al., 2018b). For example, in some years, the value of S in the North and Norwegian seas can be well above 100 000 km², in the Bering Sea maximum bloom area (S) values were regis-tered at 250 000 km², and particularly large *E. huxleyi* bloom areas (up to 380 000 km²) were observed in the Barents Sea (Kondrik et al., 2017). Within the subpolar and polar zones of the Northern Hemisphere, in the waters around Great Britain, in the North, Norwegian, Labrador, Greenland, Barents, and Bering seas, *E. huxleyi* blooms occur annually, although with largely varying intensities (Pozdnyakov et al., 2017). The du-ration of blooms in the North Atlantic and the Barents Sea is on average about 3–4 weeks. The moment of onset of the *E. huxleyi* bloom area maximum shifts from June–July to September–October for the seas located at the temperate, subpolar and polar latitudes of the Northern Hemisphere, re-spectively. This sequence mimics the flow pattern of the Gulf Stream. In the Bering Sea, the temporal pattern of S varia-tions reveals two periods (1998–2001 and 2018–2020) of ex-traordinarily intense *E. huxleyi* outbursts. It is hypothesized that this phenomenon was driven by massive advection of Fe-depleted North Pacific waters due to a significant weakening of the Alaska Current. The latter is supposed to be a telecon-ned aftermath of exceptionally strong El Niño events in 1996–1997 and 2017, respectively (Pozdnyakov et al., 2020).

Satellite-borne estimations made during 1998–2018 showed that *E. huxleyi* outbursts resulted in a release of particulate inorganic carbon (PIC) in the form of CaCO₃ in surface waters in amounts ranging from ~10 to sev-eral hundreds of kilotonnes. In the Barents Sea, the re-leased PIC content varied between ~100 and 250–300 kt, whereas in the Bering Sea, during the two periods of excep-tional activity, the PIC content was as high as 500 kt (Kon-drik et al., 2017). There is ample evidence that the release of PIC was accompanied by a significant increase in CO₂ partial pressure (ΔpCO₂) within the bloom area: between 1998 and 2016, the mean and maximum values of the ratio ΔpCO₂ / (ΔpCO₂)background varied in the ranges of ~ (20–40) % and ~ (30–60) %, respectively. The highest numbers were registered in the Bering and Barents seas (Kondrik et al., 2018a; D. Kondrik et al., 2019). Also, there is spaceborne evidence of the atmospheric columnar ΔCO₂ enhancement (ΔCO₂)atm over *E. huxleyi* blooms: numerous case studies in the aforementioned North Atlantic seas as well as in the Barents and Black seas proved that (ΔCO₂)atm could reach 2–3 ppm (D. V. Kondrik et al., 2019; Morozov et al., 2019).

Notwithstanding the remarkable ability of *E. huxleyi* to grow under conditions unfavourable for algae of other functional groups (e.g. diatoms, flagellates, cyanobacteria), a highly irregular pattern of the registered 2-decadal (1998–present) time series of S, PIC, and ΔpCO₂ is indicative of susceptibility of this alga’s outbursts to environmental conditions (Nissen et al., 2018; Kazakov et al., 2019; Silkin et al., 2018). Statistical prioritization of non-biogenic forcing factors (FFs) shows that the latter are sea- and time-period-specific (Pozdnyakov et al., 2019). Thus, in the Barents Sea, sea water temperature (SWT) is the highest-ranked FF, followed by PAR (photosynthetic active radiation). In the Bering Sea, beyond the aforementioned periods (1998–2001 and 2018–present), sea surface salinity (SSS) is the FF leader, with PAR as a runner-up, whereas SWT is only third in the series. Although these assessments are done without explicitly considered nutrient concentrations (NCs), implicitly NCs were among the FFs. Indeed, arguably, variations in SWT, SSS, CHL, MLD, and surface current speed/advection (tested as FFs) indirectly account for the variations in NCs as well in such CCS parameters as alkalinity and basicity (Duraraj et al., 2015; Pozdnyakov et al., 2019, and references therein).

In the long run, the steady accumulation of CO₂ into the atmosphere should closely be considered (Rivero-Calle et al., 2015). The action of a rising atmospheric CO₂ concentration is expected to proceed through a number of direct and indirect interactions (Fig. 7), both of which should ultimately cause alterations in the rain ratio. An increase in the atmospheric CO₂ concentration leads to the rising of the global temperature and further to the strengthening of stratification, intensification of irradiance within the euphotic zone and cutting of nutrient fluxes from below. Although increases in CO₂ fluxes to the surface ocean cause a reduction of pH and CO₃²⁻ levels in water, the large pool of HCO₃⁻ remains to support the calcification machinery. Thus, it will lead to the establishment of environmental conditions unfavourable for non-calcifying phytoplankton (NCP) but beneficial (or at least endurable) for coccolithophores in general and *E. huxleyi* specifically. The reduction of NCP and uncontested growth of *E. huxleyi* drives a further reduction of dissolved CO₂ consumption by other groups of phytoplankton, increase in pCO₂ in the surface ocean and intensification of CO₂ fluxes into the atmosphere. Concurrently, through a system of feedback interactions, alterations in the rain ratio are bound to affect the carbon fluxes at the water–atmosphere interface. Therefore, the scenario of further increases in atmospheric CO₂ concentrations in the future, in all probability, implies a vaster proliferation of *E. huxleyi* in the world’s oceans.

In combination with statistic-based mathematical models of *E. huxleyi* blooms (Pozdnyakov et al., 2019), the available IPCC climate models permit mid-term projections of the forthcoming changes (Gnatiuk et al., 2020). However, our knowledge of the reciprocal influence of climate change and both the structure and functioning of marine ecosystems
<figure><img src="image_11.png" /><figcaption>**Figure 7.** (a) Biological pumps resulting in (i) an atmospheric CO₂ sink and (ii) calcium carbonate transport from surface to deep ocean; (b) anticipated forward and feedback alterations in ocean ecology driven by atmospheric CO₂ increase. PIC: particulate inorganic carbon; POC: particulate organic carbon (modified after Rost and Riebesell, 2004).</figcaption></figure>

(even at the level of primary producers) is still insufficient to confidently prognose the future dynamics of the *E. huxleyi* phenomenon. More studies are required even to fully understand the mechanism of intracellular light-dependent reaction of calcification and its dependency on both seawater carbonate chemistry and environmental FFs (Vihma et al., 2019). Creation of respective multi-decadal databases (as in Kazakov et al., 2019) as well as further delivery of satellite and in situ/shipborne/laboratory data are necessary to improve our capacity to assess with certainty the climatological and ecological role of *E. huxleyi* blooms on regional and global scales (Fig. 7).

### 2.3.3 Lakes and rivers (Q9)

#### Organic carbon in lakes

Spatial variability, an essential characteristic of lake ecosystems, has often been neglected in field research and monitoring. The detected spatial “noise” strongly suggests that, besides vertical variation, the horizontal variation should also be considered in the ecosystem monitoring and, most importantly, when the role of dissolved organic carbon (DOC) in the CO₂ flux is estimated (Manasypov et al., 2015; Lepâranta et al., 2018). In natural waters with an increasing level of coloured dissolved organic matter (CDOM) concentration, the water colour is shifted towards brown. The key “permanent” landscape variables, the coverage by lakes and peatland in the catchment area, can be strongly correlated with lake elevation above the sea level. A high lake coverage indicates a low CDOM concentration, while a high peat coverage indicates the opposite (Arvola et al., 2016). For example, in Finland, recent results from inland water studies

have not shown any overall, consistent large-scale changes in CDOM concentrations over the last 101-year period (Arvola et al., 2017). Rather, CDOM changes in individual lakes have been related to changes in land use in the drainage basin. Manasypov et al. (2015) reported results from Siberian lakes, representing a discontinuous permafrost zone, and addressed how although the concentrations of most elements in the lakes are lowest in spring, the maximal water coverage of land made it a significant reservoir of DOC. The soluble metals in the water column can be easily mobilized to the hydrological network.

In very shallow freezing lakes, the volume of liquid water is much reduced due to ice growth, and rejection of nutrients and pollutants in the ice growth causes major enrichment of the water body. This has major implications for the ecosystem of these lakes (Yang et al., 2016; Song et al., 2019). Freezing rejects some 80%-90% of the impurities in freshwater lakes. On the other hand, ice cover accumulates atmospheric deposition over several months but releases them into the water body within 1 month's melting phase. Rejection of nutrients and pollutants in lake ice growth causes major enrichment of the water body in shallow lakes and notable increases in nutrient concentrations in a shallow lake during seasonal ice growth (Fang et al., 2015).

#### Lake carbon balance

Arctic and boreal lakes are an important natural source of CH₄ into the atmosphere (Bastviken et al., 2011). Methane is produced mainly in the bottom sediments and/or hypolimnion, where most of the anaerobic decomposition of organic matter takes place and then is either oxidized to CO₂ in the water column or emitted into the atmosphere.
At Kuivajärvi, a typical meso-humid lake located in south-
ern Finland, it was found that 91 % of available CH4 was
oxidized in the active CH4 oxidation zone during hypolim-
netic hypoxia (Saarela et al., 2020). In warm springs, the
early onset of thermal stratification with the cold and well-
oxygenated hypolimnion delays the period of hypolimnetic
hypoxia and thus limits the production of methane. At Kuiv-
ajärvi measured CO2 fluxes (F-CO2) showed that the lake
acted as a net source of carbon during two open-water pe-
riods (Mammarella et al., 2015). During daytime, with typi-
cally high wind speeds, shear-induced water turbulence con-
trols the water-air gas transfer efficiency, thus enhancing the
vertical diffusive fluxes across the water-air interface. How-
ever, during calm nighttime conditions, buoyancy-driven tur-
bulent mixing, associated with penetrative cooling of surface
water, controls the gas exchange, and simple wind-speed-
based transfer velocity models strongly underestimate F-CO2
(Mammarella et al., 2015). Kiuru et al. (2018) developed a
model simulating CO2 dynamics of a boreal lake in a warm-
ing climate. The simulations for 2070–2099 showed a 20 %–
35 % increase in the CO2 flux from the lake compared to the
reference period of 1980–2009.

Lake ice cover

Wei et al. (2016) studied Lake Unari (67.14° N, 25.73° E), Finnish Lapland, in the winters 1980/1981–2012/2013, and observed an increasing trend in the air temperature during the freezing season associated with an increasing trend in the water precipitation during winter. Low temperatures with less precipitation led to the formation of columnar ice, while strong winds together with heavy snowfall favoured granular ice formation. Karetnikov et al. (2017) analysed long-term ice conditions in Lake Ladoga, Russia, for the period of 1913–2015 and showed that the mean freezing and breakup dates were 26 November and 15 May, respectively, and that the annual frequency of complete freeze-over of the lake was 0.83. The period from 1990 to present was much milder than the preceding years. The annual increase in the ice concentration depended on the accumulated freezing degree days (AFDDs) and the hypsographic curve, while the ice thickness increased with the square root of an AFDD.

An analysis of a Siberian thermokarst lake located in the
Lena River Delta, characterized as a floating ice lake, showed
that the temporal dynamics and magnitude of heat fluxes and
surface energy balance closures are substantially different
depending on lake surface conditions (Franz et al., 2018).
Sensible heat and latent heat fluxes, modelled using available
heat bulk transfer models (Woolway et al., 2015; Verburg and
Antenucci, 2010; Andreas et al., 2002), tend to underestimate
the measured fluxes and show less variability over freezing
ice cover, melting ice in spring, as well as open water in
summer. However, the performance of these models also de-
pends on the accuracy of meteorological and hydrological

<figure><img src="image_12.png" /><figcaption>**Figure 8.** Field data for ice decay in Lake Kilpisjärvi in 2013 show-
ing decrease in ice thickness by surface melting and bottom melting
and increase in porosity until breakage of ice cover.</figcaption></figure>

input parameters, which should be carefully measured, espe-
cially during challenging winter conditions.

The seasonal lake ice cover is a sensitive indicator of climate variations in the Arctic (Kirillin et al., 2012; Leppäranta, 2015). To work more on this question, Lake Kilpisjärvi (surface 37.1 km², maximum depth 57 m), a tundra lake in northern Finland, has been under intensive ice-related field programmes in recent years. The research covered the whole year but was focused on the melting period in May–June. The heat budget over the ice season was dominated by the radiation balance. Turbulent fluxes were significant before the freeze-up in autumn, but in the ice season they were small. The evolution of ice thickness served as a very good approximation to the total surface heat flux (Leppäranta et al., 2017) (Fig. 8). In the melting stage, solar radiation, the strongest forcing of the water body beneath ice cover, breaks the stability and initiates convective turbulent mixing. This brings heat from the deeper water to ice, enhancing melting at the ice bottom (Kirillin et al., 2018). Thus, the common assumption of the heat flux from the water to ice being due to molecular conduction does not hold in the melting stage, but it is much higher. The ice-water interaction under lake ice has not been well covered in earlier studies of ice growth and melting.

The ice melting process was studied in detail in Lake Kilpisjärvi. The melting progressed in the upper and lower surfaces and in the interior, with proportions depending on the solar flux and optical properties of the ice and therefore being case-dependent. About one-third of the solar flux that penetrated the ice returned to the ice bottom, providing heat for melting. This was consistent with the under-ice results by Kirillin et al. (2018). In 2013 a rapid ice breakage event completed the ice breakup in a short time interval, with final breakage at the ice porosity 40%–50%. A lake ice melting model should include the thickness and porosity of ice, with porosity connected to an ice strength criterion (Leppäranta et al., 2019).
## Lake Baikal and Selenga River Delta

The Selenga River, the main tributary of Lake Baikal, has a catchment area of 450 000 km² in the boundary region between northern Mongolia and southern Siberia. This area is well known by its climate, land use and dynamic socio-economic changes which might have negative impacts on the ecosystems of Lake Baikal and thus was selected as a PEEX field laboratory within the PEEX sub-programme Selenga-Baikal Network (https://www.atm.helsinki.fi/peex/index.php/basenet/, last access: 18 January 2022). In the recent past, hydroclimatic development together with land use changes led to a contaminant influx from mining areas, and urban settlements increased. Additional hydrological modifications due to the construction of dams and abstraction-s/water diversions from the Selenga's Mongolian tributaries could lead to additional alterations (Karthe et al., 2017b). In addition to the Selenga River, a key issue for an improved understanding of regional impacts of the environmental change is to disentangle the influence of climate change from that of other pressures within the catchment (Lychagin et al., 2017). The PEEX sub-programme Selenga-Baikal Network aims at integrated field-based and modelling knowledge to develop a basin-wide conceptual framework of riverine fluxes (Kasimov et al., 2017; Karthe et al., 2019).

As a PEEX field laboratory, regional large-scale assessments made it possible to predict the comprehensive nature of hydrological and geochemical changes driven by climatic processes and human impacts. Heavy metals in water and sediments (Kasimov et al., 2020a, b) and fish communities (Kaus et al., 2017) were measured since 2011 in over 50 locations around the catchment. The mining zones are potential hotspots for increasing metal loads to downstream river systems. Several metals (Al, Cd, Fe, Mn, Pb and V) are exported from mining sites to the downstream river system, as shown by net increasing mass flows. Based on a novel partitioning coefficient approach (Table 2), contrasting patterns with domination of both particulate and dissolved phases in different parts of the basin were found. Such heterogeneity in the metal partitioning is likely to be found in many large river systems.

Multi-scale modelling ranged from the basin-wide (Malsy et al., 2017; Frolova et al., 2017) to specific sub-regions, such as particular segments of the river system (Kaus et al., 2017; Thorslund et al., 2017; Garmaev et al., 2019) or its delta (S. R. Chalov et al., 2017; S. Chalov et al., 2017; Shinkareva et al., 2019), and identified reactions of hydrogeochemical pathways to climate change. The mean flow reduction in the Selenga River was 3%–5% during the 2020s to 2030s and 4%–25% during the 2080s to 2090s, being a crucial driver of ongoing and future hydrogeochemical changes. Increases in temperatures with permafrost thaw and the expansion of agricultural, mining and urbanization processes may induce up to a 6% increase in the particulate modes and 3% in the dissolved modes of some metals in the river

system (Chalov et al., 2018). Possible changes in the number or magnitudes of high-flow events, caused by climatic or other anthropogenic factors, could influence the total sediment deposition, which was primarily found to occur during relatively short high-flow events. Such potential changes have important implications for the possible spreading of polluted sediments (Pietroń et al., 2015) and their storage in the Selenga River Delta, which is an important wetland region forming the geochemical barrier which mitigates pollution of Lake Baikal by riverine fluxes (Voropay and Kichigina, 2018; Chalov et al., 2015). The Selenga River Delta region sequesters various metals bound to Selenga River sediments (Chalov et al., 2015, Pietroń et al., 2018). The water shortage decreases the processes of suspended sediment retention in the delta. The seasonal hydrogeochemical patterns are explained by wetland inundation during floods and channel erosion or Baikal wind surge during low-flow periods (S. R. Chalov et al., 2017; S. Chalov et al., 2017).

## Asian water lakes

The largest internal drainage basins in the world are located in central Asia, with a limited availability of both surface water and groundwater (Karthe et al., 2017a). Since the 20th century, water resources of this region have been overexploited and, for example, from small Mongolian headwater streams to the mighty Aral Sea, surface waters have been partially desiccated. It seems that the implementation of the Integrated Water Resources Management and water-food-energy nexus approaches would lead to a more environmentally friendly future (Karthe et al., 2017a, b). The lake-rich Qinghai–Tibet Plateau (QTP) has recently been identified as the “Third Pole” of the Earth. Due to its high elevation and unique climate, the QTP affects the global and local climate and played an important role in the central and southern Asian water cycle (J. Zhang et al., 2018). Lake–atmosphere interactions have been quantified over open-water periods, yet little is known about the lake ice thermodynamics and heat and mass balance during the ice-covered season. A modelling study for a thermokarst lake in the QTP was performed (Huang et al., 2019a). Strong diurnal cycles were seen for all surface heat fluxes. The ice mass balance was dominated by the growth and melt at the base, but the surface sublimation was also crucial for the ice loss, accounting for up to 40% of the maximum ice thickness and 41% of the lake water loss during the ice-covered period. The strong penetration of solar radiative flux is the dominant contributor to the high value of upward sensible heat flux at the ice bottom, resulting in a relatively thin ice cover compared with the equivalent high-latitude climate.

## 2.4 Society

The anthropogenic impact has been addressed as one of the PEEX themes for the society system. The discussion on
<figure><img src="image_13.png" /><figcaption>**Table 2.** Hydrogeochemical signature of a large river system – Selenga River case study. The figure represents metal(loid) partitioning (median values) in the Selenga River basin in the upper (Mongolian) and downstream (Russian) parts between 20 July and 10 August 2011 under dominant high-water (a) and between 7 June and 10 July 2012 under dominant low-water conditions. Dark orange fill corresponds to the share of suspended forms of elements > 75 % (green), light orange to 75 %–50 %, light blue to 50 %–25 %, and dark blue to < 25 %. The figure indicates that in the large river system some metals are mostly found in dissolved form (84 %–96 % of Mo, U, B, and Sb on average), whereas many others predominantly existed in suspension (66 %–87 % of Al, Fe, Mn, Pb, Co, and Bi). A consistently increasing share of metals in suspended particulate modes (about 2–6 times) is observed under high-discharge conditions. For details and other hydrological seasons, see Kasimov et al. (2020b).</figcaption></figure>

the mitigation and adaptation, including urban infrastructure design and risk assessment, is addressed in this context (Q10, Sect. 2.4.1). The social transformations are discussed in terms of how local reindeer grazing interacts with the environment (Q11, Sect. 2.4.2). The adaptive capacity of the northern societies depends on their environment, demographic structure and economic capacity, and the environmental hazards and environmental health under a changing climate are the key research areas in this context (Q12, Sect. 2.4.3).

## 2.4.1 Anthropogenic impact (Q10)

### Mitigation

Arctic climate change generates a need for long-term planning and development of new socio-economic infrastructures, such as dams, bridges, roads and transnational and regional energy networks. For this task, new climate-based forecasting tools, cost and operational risk estimates as well as other methods and tools for an infrastructure and urban design are needed. As an example, engineering calculations for maximal discharges were provided for the Nadym River in Russia (Shevnina et al., 2017). Badina (2018) introduced a method for the natural risk assessment by using indices based on socio-economic potential data and spatial distribution of natural hazards. This method has been tested and used to identify the most vulnerable municipalities in southern Siberia. Another example of new methods is a “green factor tool” to increase the share and effectiveness of green areas in urban environments and cities. An ambitious target set in this tool could encourage or force urban developers to

aim higher with the planning of green areas and construction; however, the existing regulations challenge the use of this approach (Juhola, 2018).

The energy production is of fundamental importance for the society's functions, and new clean energy technologies are needed to hinder the climate change. The potential of hydropower production under probabilistic projections of annual runoff rate and future changes in the potential hydropower production need to be evaluated (Shevnina et al., 2019). All the Nordic countries are vulnerable to various degrees to potential cross-border impacts due to their energy sectors being highly globalized and interconnected. However, cross-border impacts are not yet properly included in Nordic climate assessments or energy strategies. The EU's new Green Deal is pivotal in this respect, as for the first time emissions along the whole supply chain (oil, gas, coal, renewables) come under scrutiny as part of a normative governance. Therefore, policy makers and energy planners should be assisted in making comprehensive vulnerability assessments that address both domestic and international climate risks (Groundstroem and Juhola, 2019).

## 2.4.2 Environmental impact (Q11)

### Reindeer (*Rangifer tarandus* L.) grazing and ground vegetation structure and biomass

Reindeer (*Rangifer tarandus* L.) grazing in the north affect the ground vegetation structure and biomass and cover of lichens. It seems that reindeer affect GHG fluxes from the forest field layer. Grazing changes affect the vegetation composition and thereby emissions (K. Köster et al., 2018).
K. Köster et al. (2017) provided detailed information on soil CO₂ effluxes, which were mostly affected by the year of measurement, time of measurement, soil temperature and the management, resulting in higher CO₂ emissions in the grazed areas. Soil moisture content did not affect the soil CO₂ efflux. For example, in Finnish Lapland the average soil CO₂ efflux values were significantly higher in 2014 compared with 2013, mainly due to differences in the soil temperature at the beginning of the season (K. Köster et al., 2017). Furthermore, grazing significantly decreased the biomass and cover of lichens and also the amount of tree regeneration. In a subarctic mature pine forest, grazing did not affect the soil temperature or soil moisture. No statistically significant effect of grazing on the soil CO₂ efflux, soil C stock or soil microbial C biomass was found. The soil microbial N biomass was significantly lower in the grazed areas compared with the non-grazed areas. It seems that in the boreal subarctic coniferous forests, grazing by reindeer can be considered “C neutral” (K. Köster et al., 2015). There is also an indication that reindeer grazing affects the boreal forest soils, e.g. their fungal community structure and litter degradation (Santalahti et al., 2018).

### 2.4.3 Natural hazards (Q12)

Under this theme, PEEX research has so far focused on environmental health issues. These include diseases, impact of UV radiation, and air pollution in urban environments. The spread of diseases caused by living pathogens is basically determined by environmental conditions. Medico-geographical assessments are usually based on identification of the links between the spread of diseases and factors of the geographical environment.

#### Naturally determined diseases

Climatic factors are deemed among the main determinants for the spread of naturally determined diseases (Malkhazova et al., 2018). Emerging zoonotic diseases are expected to be particularly vulnerable to climate and biodiversity disturbances. Anthrax is an archetypal zoonosis that manifests its most significant burden on vulnerable pastoralist communities. Ezhova et al. (2021) investigated the dynamics of environmental factors that led to an anthrax outbreak in the Yomal Peninsula, Siberia, during 2016. They found that the local permafrost was thawing rapidly for the last 6 years before the outbreak, supporting the hypothesized role of permafrost thaw in triggering this outbreak, and concluded further that the spread of anthrax was likely intensified by the extremely dry summer of 2016 in the region. Overall, the recent findings highlight the significance of warming temperatures for anthrax ecology at northern latitudes and suggest potential mitigating effects of interventions targeting megafauna biodiversity conservation in grassland ecosystems and animal health promotion among small to midsize livestock herds

(Walsh et al., 2018). Equally important is the monitoring of climatic factors, such as warming and precipitation extremes, in Arctic regions previously contaminated by anthrax (Ezhova et al., 2021).

#### UV variations

Different geophysical parameters affecting the UV molecular number density show that, especially at high altitudes, the increased surface albedo has a significant effect on the UV growth. The new parameterization of the online UV tool (http://www.momsu.ru/uv/, last access: 18 January 2022) for northern Eurasia allows us to determine the altitude dependence of UV and to estimate the possible effects of UV on human health considering different skin types and various open body fractions for January and April conditions in the Alpine region (N. Chubarova et al., 2016). Using UV satellite retrievals, ERA-Interim data and the INM-RSHU chemistry-climate model, the changes in the UV irradiance and UV resources were estimated over northern Eurasia for the 1979–2015 period, demonstrating significant UV increases over vast areas (Chubarova et al., 2020). Referring to long-term UV measurements and model simulations in Moscow, a statistically significant positive trend of more than 5% per decade since 1979 was evaluated (Chubarova et al., 2018). Related to the connection between UV variation and stratospheric O₃, see also Sect. 2.2.1, Atmospheric composition and chemistry.

#### Examples of air pollution episodes

Street level urban air pollution is one of the key topics in urban environments. For example, in Bergen, Norway, the most extreme cases of repetitive wintertime air pollution episodes, followed by increased large-scale wind speeds above the valley, were transported by the local re-circulations to other less polluted areas with only slow dilution. This result underlines the need for better-described assumptions about transport paths and weak dispersion in classical air pollution models in order to improve the current air quality forecasts in urban areas (Wolf-Grosse et al., 2017b). A link between the persistence of the flow above the Bergen valley and the occurrence and severity of the local air pollution episodes was found. Analysis of the large-scale circulation over the North Atlantic-European region, with respect to air pollution in Bergen, revealed that the persistence in meteorological conditions connected to air pollution episodes is not necessarily caused by large-scale anomalies of the atmospheric circulation over the Norwegian western coast but is rather connected to anomalies as far away as Greenland (Wolf-Grosse et al., 2017a).

In Russia, especially intensive atmospheric pollution episodes have severe impacts on the environment and human health. O. B. Popovicheva et al. (2019) analysed the Tver region, north of Moscow, which was considerably affected by
the secondary organic aerosol (SOA) formation originating from long-lasting peat bog fires. Spectral absorbance characteristics were similar to peat burning and traffic source emissions during fire- and non-fire-related days and confirmed the effect of transported peat smoke on air quality in a megacity environment (O. B. Popovicheva et al., 2019). O. B. Popovicheva et al. (2019) also showed that long-term transport from north-western Russia and Scandinavia influences the local population.

Local Arctic air pollution alone can seriously affect public health and ecosystems locally, especially in wintertime, when the pollution can accumulate under inversion layers (Schmale et al., 2018a). We need more research on the contributing emission sources and the relevant atmospheric pollution mechanisms and more detailed epidemiological or toxicological health impact studies in the Arctic. Socio-economic changes (shipping, tourism, natural resource extraction, increasing number of population) are already taking place in the Arctic, and they will increase in the future. It is also expected that the emission types and magnitudes will increase the number of exposed individuals (Arnold et al., 2016). There is still a large variation in the number of locations as a source of emissions. Future predictions are even more difficult due to the as yet unknown development of the Arctic economic activities and their emissions (Arnold et al., 2016; Schmale et al., 2018a, b).

# 3 Synthesis and future prospects

## 3.1 Future research needs from the system perspectives

For the land ecosystem, the recent progress towards understanding of the northern Eurasian Arctic-boreal land ecosystems (Sect. 3.1) deals with improved methodologies relevant to land processes (Q1), observations of permafrost thawing (Q2), and observed changes in the northern ecosystems, especially soil conditions (Q3).

Improved satellite-based methods and (validation) data together with better quantification and, especially, the scaling of the GPP are enabling better identification and quantification of Earth surface characteristics and ecosystem carbon balance compared with the earlier capacity (Gurchenkov et al., 2017; Rautiainen et al., 2016; Nitzbon et al., 2019; Boike et al., 2019; Terentieva et al., 2016; S. Zhang et al., 2018; Pulliainen et al., 2017; Matkala et al., 2020; Bondur et al., 2008a, b). Intensive research has been carried out on the quantification of the GPP, a key variable for biological activity, in different conditions and at different scales (Pulliainen et al., 2017; Kulmala et al., 2019; Matkala et al., 2020). Further investigations are called for, for a more detailed understanding of the seasonal dynamics of the biological activity.

The northern Eurasian ecosystems' tipping points are related to multiple simultaneous stress factors. The key stress factors here are the permafrost thawing and factors impor-

tant for ecosystems, such as the prolongation of the growing season, increase in the mean temperature of the growing season and forest fires (Kukkonen et al., 2020; Biskaborn et al., 2019; Payne et al., 2016; K. Köster et al., 2016; Miles and Esau, 2016; Miles et al., 2019). New evidence of the progress of permafrost thawing in Siberia has been introduced by Kukkonen et al. (2020) and Biskaborn et al. (2019). The permafrost thawing is also triggering as yet not clearly known processes related to changing fluxes, ecosystem processes and dynamics of greenhouse gas sinks and sources (Schuur et al., 2008; Thompson et al., 2017; Commane et al., 2017; Euskirchen et al., 2017; Dean et al., 2018; Thonat et al., 2017). The progress affecting permafrost thawing has not yet been analysed in detail. For example, we need more information on the dynamics of how the thawing processes vary between soil types due to differences in water movement and, in the wintertime, how the snow cover affects ground surface temperatures (Bartsch et al., 2010). In addition to permafrost processes, the recent advances in observed changes in the northern ecosystem reveal a significant role of soil processes in biogeochemical cycles, especially the nitrogen cycle (Voigt et al., 2016; Pärn et al., 2018). Knowledge of the soil microbiological composition and the effect of forest fires has been improved (K. Köster et al., 2015, 2016; Zhang-Turpeinen et al., 2020), but further research is needed for vegetation changes influencing the below-ground microbiology, its composition and enzymatic activity (Payne et al., 2016; K. Köster et al., 2016). The NDVI methods have made it possible to detect vegetation changes (Miles and Esau, 2016). A range of vegetation cover changes in Siberia have been reported, such as the Arctic greening and browning processes, but e.g. the greening of Siberian cities will also remain an issue of intensive research in the future (Miles and Esau, 2016; Miles et al., 2019).

For the atmospheric system, the recent progress in understanding the northern Eurasian Arctic-boreal land-atmosphere system and the aspects of the megacity air quality (Sect. 3.2) are dealing with atmospheric composition changes (Q4), key feedbacks between climate and air quality (Q5), and synoptic-scale weather (Q6). Recent results demonstrate improved quantification of the carbon balance and CO₂ fluxes and concentrations due to land use change, forest fires in Siberia, and new understanding of aerosol sources and properties in the Arctic environment and across northern Eurasia (Pulliainen et al., 2017; Karelin et al., 2017; Rakitin et al., 2018; Skorokhod et al., 2017; Alekseychik et al., 2017). However, most of the results deal with atmospheric aerosol chemistry and physics in boreal and Arctic environments originating from measurements in the few flagship stations in Finland and Russia (Kerminen et al., 2018; Wiedensohler et al., 2019; Freud et al., 2017; Paasonen et al., 2018; Östrom et al., 2017; Kalogridis et al., 2018; Bondur et al., 2016; Bondur and Ginzburg, 2016; Bondur et al., 2019c, d; Bondur and Gordo, 2018; Mikhailov et al., 2017; Breider et al., 2017), indicating the need for a comprehen-
sive station network in the PEEX region. Black carbon emit-
ted by the Siberian forest fires and some other sources and
its long-range transport to the Arctic are also widely dis-
cussed (Kalogridis et al., 2018; Bondur et al., 2016; Bon-
dur and Ginzburg, 2016; Mikhailov et al., 2017; Breider et
al., 2017; Shevchenko et al., 2015; Konovalov et al., 2018;
Marelle et al., 2018). In addition, measurements of ozone
in the troposphere and stratosphere provide insight into at-
mospheric chemistry in urban environments (Skorokhod et
al., 2017), UV radiation and human health (Chubarova et al.,
2019b). Environmental health, including the impacts of air
quality and UV radiation, is foreseen as a high-momentum
research topic in the PEEX domain, and further research is
called for in this area.

Related to air pollution, we reported several new results on
the dynamics between the haze pollution and boundary-layer
meteorology in enhancing air pollution in megacity environ-
ments (Zhao et al., 2017; Ding et al., 2016a; Wang et al.,
2018b; Y. Bai et al., 2018; Ye et al., 2017). The long-term
and comprehensive measurements carried out especially at
the SORPES station in Nanjing provide valuable data pools
for such studies (Ding et al., 2016a). However, the backbone
of the recent progress has been the improved online atmo-
spheric measurements and the use of machine learning meth-
ods combined with different methodologies, such as back tra-
jectories together with the lidar and radiosonde data. In addi-
tion, improved models of emission inventories together with
the ECHAM-HAM and GAINS models have led to a better
quantification of aerosol number emissions. New knowledge
has enabled the introduction of new theoretical arguments
on the feedbacks between high aerosol concentrations and
the urban boundary layer (Petäjä et al., 2016). New measure-
ments have also been obtained from Siberian cities (Elan-
sky et al., 2016; N. Y. Chubarova et al., 2016; Mahura et al.,
2018). However, we are still in the early phase of having a
holistic picture of large-scale feedbacks due to the lack of
long-term, comprehensive measurements in these regions.

Changes in the atmospheric dynamics in the north have po-
tential impacts on short-term local/regional and sub-seasonal
to seasonal large-scale weather predictions and on long-term
projections on biogeochemical systems. It is therefore cru-
cial to understand changes in boundary-layer processes as
well as synoptic- and large-scale circulation in the Arctic and
northern Eurasia. Recent results show potential, but causally
arguable, connections between the alarming sea ice decline,
evaporation, cloudiness, atmospheric circulation and moist-
ture transport as well as Arctic and European winter temper-
ature (Nygård et al., 2019; Rinke et al., 2019; McCusker et
al., 2016; Mori et al., 2014; Blackport et al., 2019; Cohen et
al., 2020). Further investigations are needed for atmosphere-
ice-ocean interactions, coupling between small-scale pro-
cesses (such as clouds and turbulence) and synoptic-scale
weather, as well as polar prediction and extreme events. Fur-
thermore, more quantitative knowledge is needed on pan-
Arctic energy budgets (Spengler et al., 2016). The UHI phe-

nomena taking place in Arctic cities have received increasing
attention, and there is a special need for improved forecasting
services for Arctic cities (Miles and Esau, 2017; Konstanti-
nov et al., 2018; Varentsov et al., 2018b).

For the water system, we discussed the Arctic sea ice dy-
namics and thermodynamics, snow depth and sea ice thick-
ness, sea ice research supporting navigation, and rare el-
ements in the snow and ocean sediments, especially from
the perspective of improvements in the observation and
modelling methods (Q7, Sect. 3.3.1). New evidence of
atmosphere–Arctic sea ice interactions has been provided by
Lei et al. (2018) and Jakobson et al. (2019). Lei at al. (2018)
analysed how the climate warming would affect the winter
growth rate of thin and thick ice, and Jakobson et al. (2019)
gave new insight into the relation between sea ice concentra-
tion and wind speed. Furthermore, advances have been made
in understanding the thermodynamics and metamorphosis of
the snowpack on sea ice and their interactions with surface
albedo changes (Dou et al., 2019). Operational sea ice analy-
sis is increasingly important for Arctic shipping and naviga-
tion (Lei et al., 2015; Karvonen et al., 2017). New results on
rare elements, mineral composition and CO₂ and methane
fluxes associated with ocean sediments have been attained
(Maslov et al., 2018b; Yasunaka et al., 2018). This serves as
important information for mitigation plans as well as for new
estimates of the river runoff and discharge in Russian rivers
into the Arctic seas (Grigoriev and Frolova, 2018; Agafonova
et al., 2017).

The marine Arctic ecosystems are under a progressive
increase in anthropogenic impacts, the main issues calling
for better understanding being the integrated effect of Arc-
tic warming, ice melt and snowmelt, ocean freshening, air
quality and acidification of the Arctic marine ecosystems,
primary production and the carbon cycle (Q8, Sect. 3.3.2).
Quantitative information about the CO₂ accumulation into
the ocean has high momentum. Marine organisms, such as
coccolithophorid algae, are influencing the CO₂ flux ex-
change (Kondrik et al., 2018b; Pozdnyakov et al., 2017). In
addition to changing marine environments, the Arctic-boreal
lakes and rivers may undergo changes in flooding, increas-
ing the amount of freshwater and allochthonous materials
(Q9, Sect. 3.3.3). In addition to the Arctic Ocean, the ice and
snow conditions of northern lakes are under pressure. Lake
Kilpisjärvi (Finland) (Arvola et al., 2017; Leppäranta et al.,
2017) and Lake Ladoga (Russia) (Karetnikov et al., 2017)
have been subject to intensive research, and the recent results
demonstrate changes in heat fluxes, ice cover periods and
stratification. The browning of lakes and lake sediments was
discussed, and new results were attained from the Selenga
River of Lake Baikal. Dramatic changes will be expected in
the water runoff and in the number of dissolved modes of
metals, also having a serious impact on environmental health
(S. R. Chalov et al., 2015, 2016, 2017; S. Chalov et al., 2017;
Karthe et al., 2017a, b). As a comparison with the north-
ern high latitudes, we also discussed freezing lakes in cen-
tral Asia, where the climate is cold and arid. There the ice is typically snow-free or possesses only a thin snow cover, allowing penetration of sunlight into the water body (Huang et al., 2019b).

For the societal system, the anthropogenic impact has been addressed as one of the main themes (Q10). The discussion on the mitigation and adaptation, including the urban infrastructure design (Juhola, 2018) and risk assessment, was addressed in this context (Sect. 3.4.1). In social transformations, special attention was given to one of the most important local livelihoods in Lapland: reindeer grazing and how it interacts with the environment (Q11 Sect. 3.4.2). The adaptive capacity of the northern societies rests on their environment, demographic structure and economic activities (Q12). Referring to the earlier statement about future research needs for the atmospheric system with respect to environmental health, here again we would like to pay increasing attention to environmental health under a changing climate, including the spread of diseases and air pollution and their combined effects (Sect. 3.4.3).

## 3.2 Feedback mechanisms under changing climate, cryosphere conditions and urbanization

During recent years, Kulmala et al. (2004, 2021) focused on the quantification of the Continental Biosphere-Aerosol-Cloud-Climate (COBACC) feedback loop relevant to the boreal region in northern Eurasia. Previous results on the COBACC feedback loop addressed the role of BVOC emission dynamics (Arneth et al., 2016). Both higher temperatures and increased CO₂ concentrations are (separately) expected to increase emissions of BVOCs into the atmosphere. It also seems that the GPP is controlled by the BVOC effects on the clouds. Sporre et al. (2019) used an Earth system model to estimate aerosol scattering due to enhanced BVOC emissions and estimated the associated negative direct radiative effect (−0.06 W m⁻²). The total global radiative effect associated with this feedback was estimated to be −0.49 W m⁻² (Sporre et al., 2019), indicating that it has the potential to offset about 13% of the forcing associated with a doubling of CO₂. The direct effect of aerosol on GPP due to an increase in the fraction of diffuse radiation was estimated at between 6% and 14% increase in GPP at maximum observed aerosol loading compared to low aerosol loading in northern Eurasian forests (Ezhova et al., 2018b).

The results from the Tibetan Plateau demonstrate notable feedbacks between vegetation, BVOC emissions and aerosol particles. The historical wetting of the TP region has increased the vegetation cover, allowing for feedback processes via biogenic aerosol formation and aerosol–cloud–precipitation interactions. A significant wetting trend since the early 1980s in the Tibetan Plateau is most conspicuous in central and eastern Asia. Fang et al. (2015) hypothesized that the current warming may enhance emissions of BVOCs, which can increase secondary organic aerosol con-

centrations, contributing to the precipitation increase. The wetting trend can increase the vegetation cover and has a positive feedback on the BVOC emissions. The simulations suggest a significant contribution of increased BVOC emissions to the regional organic aerosol mass, and the simulated increase in BVOC emissions is significantly correlated with the wetting trend in the Tibetan Plateau.

To estimate the net effects of various feedback mechanisms on land cover changes, photosynthetic activity, GHG exchange, BVOC emissions, formation of aerosols and clouds, and radiative forcing (Q14) call for intensive collaboration and integration between the Arctic Ocean sciences and terrestrial sciences across the pan-Arctic domain and across the Arctic and high-latitude domain. The Arctic greening and browning (Sect. 3.1.3) call for a multi-disciplinary scientific approach, improved modelling tools and new data to deeply understand the biosphere–atmosphere–anthroposphere interactions and feedbacks. Petäjä et al. (2020a, b) discussed the complexity of feedbacks, especially in the Arctic context, and the interplay between the temperature, GHG, permafrost, land cover and water bodies and between photosynthetic activity, aerosols, clouds and radiation budget. The current downturn of the Arctic cryosphere (Sect. 3.1.2) together with the changes in sea ice dynamics and glaciers and the permafrost thawing affect both marine and terrestrial carbon cycles in interconnected ways (Sect. 3.3.1). Parmentier et al. (2017) discussed the changing Arctic cryosphere and how the processes in the ocean and on land are too often studied as separate systems, although the sea ice decline connects the rapid warming of the Arctic, Arctic Ocean marine processes and air–sea exchange of CO₂. Thus, future priorities would be on the development of our modelling tools towards an all-scale modelling approach to cover the feedbacks, processes and interactions at the land–ocean interface and also in urban environments in the Arctic region. We also need to support the further development of ground-based observation networks.

## 3.3 Climate scenarios for the Arctic-boreal region

Climate scenarios set the urgency for the mitigation and adaptation actions for the northern Eurasian region. The Arctic-boreal region combines an area of both amplified climate change (Arctic amplification) and large diversity in the model predictions (Collins et al., 2013; Hoegh-Guldberg et al., 2018). Under the “low-to-medium” RCP4.5 forcing scenario (van Vuuren et al., 2011), the CMIP5 multi-model mean temperature changes during the 21st century indicate the strongest wintertime warming of > 5°C in the Arctic Ocean, whereas the majority of the terrestrial region will warm by 2–4°C (Fig. 9). Even during summertime, the continental warming over the region will generally exceed 2°C. It is important to note that the diversity of model projections is accentuated over the Arctic and northern Eurasian domain: the mechanisms behind the Arctic amplification are imple-
<figure><img src="image_14.png" /><figcaption>**Figure 9.** Changes in 2 m temperature (°C, upper panels) and precipitation (%, lower panels) during the 21st century. Present-day climatology is averaged over the years 1981–2010 and end-of-century climatology over 2070–2099. Winter (left) and summer (right) are shown separately. Dotted areas indicate high variability in the model ensemble (for temperature: standard deviation of 21st century change exceeds 1°C; for precipitation: standard deviation of 21st century change exceeds 100% or present-day precipitation). The model results are from IPCC AR5, based on 42 individual models in CMIP5 experiments under the RCP4.5 scenario.</figcaption></figure>

mented in varying details in the distinct models, and the asso-
ciated interactions and feedback processes provide a diverse
picture of the future in the Arctic-boreal regions.

In addition to considerable trends in atmospheric temper-
ature, the models further indicate prominent changes in pre-
cipitation (Collins et al., 2013; Hoegh-Guldberg et al., 2018).
For the Arctic-boreal region, this is largely depicted as in-
creasing rainfall during both winter and summer, extending
to 15%–25% over most of the terrestrial domain over the
winter and somewhat less during summer (Fig. 9). Contem-
porary warm Arctic temperatures and large sea ice deficits
(75% volume loss) demonstrate climate states outside our
previous experience. The modelled changes in the Arctic
cryosphere demonstrate that even limiting the global temper-
ature increase to 2°C will leave the Arctic a much differ-
ent environment by mid-century, with less snow and sea ice,
melted permafrost, altered ecosystems, and a projected an-
nual mean Arctic temperature increase of +4°C. Even under
ambitious emission reduction scenarios, high-latitude land
ice melt, including Greenland, is foreseen to continue due
to internal lags, leading to accelerating global sea level rise
throughout the century (Overland et al., 2019).

4 Concluding remarks

Only the integration of different observing networks and pro-
grammes into an inter-operable and integrated observation
system can provide data needed for understanding the mech-
anisms of the Arctic-boreal system. There is a fundamental
need for an integrated, comprehensive network of state-of-
the-art in situ stations measuring Earth surface-atmosphere
interactions (Kulmala et al., 2016a, 2018; Uttal et al., 2016;
Hari et al., 2016; Alekseychik et al., 2016; Vihma et al.,
2019). The results obtained in the Pan-Eurasian Experiment
(PEEX) programme in Russian and China introduced in this
paper are based on a combination of long-term observations
and campaign data. In addition, the Arctic marine regions re-
quire comprehensive observations and subsequent synthesis,
as these regions are under a lot of environmental stresses.
Therefore, we need more in situ observations of the Arctic
system covering the marine atmosphere, sea ice and ocean.
However, there are pronounced technological and logistical
challenges to set up such continuous, marine in situ observa-
tions (e.g. Vihma et al., 2019). Furthermore, improved mon-
itoring is needed for river discharge and associated fluxes
of greenhouse gases and other key compounds and more re-
search on the understanding of coastal processes and atmo-
spheric transport and specific regional socio-economic issues