Latitudinal distribution of soil CO2 efflux and temperature along the Dalton Highway, Alaska

Kim, Yongwon; Kim, Seong-Deog; Enomoto, Hiroyuki; Kushida, Keiji; Kondoh, Miyuki; Uchida, Masao

doi:10.1016/j.polar.2012.11.002

Cited by 22 publications

(40 citation statements)

References 43 publications

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“…In collapse scar sites, lower ER could be attributed to slow decomposition rates of deep organic matter, low O 2 availability in saturated soils, low temperature, and substrate recalcitrance [36,37,71]. Although winter surface CO 2 fluxes were not measured in this study, Wang et al [43] reported that in high-boreal forest, winter SR accounted for 5%-19% of the annual ER, which agrees well with the value reported in similar boreal forests [72] while Kim et al [39] observed that wintertime soil CO 2 efflux contributed 24% of the annual CO 2 efflux in Alaska.…”

Section: Quantitative Relationships Between Nce and Er And Climate Vasupporting

confidence: 85%

“…CO2 exchange from the surface of permafrost-affected areas is determined by a combination of several factors, including soil microclimate [31][32][33][34], landform features [2,[35][36][37], water table depth [38], extent of permafrost [2,39,40], and vegetation type [41,42]. There are two important contributors to the CO2 flux: soil respiration and assimilation, and respiration of the ground cover vegetation.…”

Section: Discussionmentioning

confidence: 99%

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Surface CO2 Exchange Dynamics across a Climatic Gradient in McKenzie Valley: Effect of Landforms, Climate and Permafrost

Startsev

Bhatti

Jassal

2016

Forests

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Abstract:Northern regions are experiencing considerable climate change affecting the state of permafrost, peat accumulation rates, and the large pool of carbon (C) stored in soil, thereby emphasizing the importance of monitoring surface C fluxes in different landform sites along a climate gradient. We studied surface net C exchange (NCE) and ecosystem respiration (ER) across different landforms (upland, peat plateau, collapse scar) in mid-boreal to high subarctic ecoregions in the Mackenzie Valley of northwestern Canada for three years. NCE and ER were measured using automatic CO 2 chambers (ADC, Bioscientific LTD., Herts, England), and soil respiration (SR) was measured with solid state infrared CO 2 sensors (Carbocaps, Vaisala, Vantaa, Finland) using the concentration gradient technique. Both NCE and ER were primarily controlled by soil temperature in the upper horizons. In upland forest locations, ER varied from 583 to 214 g C·m −2 ·year −1 from mid-boreal to high subarctic zones, respectively. For the bog and peat plateau areas, ER was less than half that at the upland locations. Of SR, nearly 75% was generated in the upper 5 cm layer composed of live bryophytes and actively decomposing fibric material. Our results suggest that for the upland and bog locations, ER significantly exceeded NCE. Bryophyte NCE was greatest in continuously waterlogged collapsed areas and was negligible in other locations. Overall, upland forest sites were sources of CO 2 (from 64 g·C·m −2 ·year −1 in the high subarctic to 588 g C·m −2 ·year −1 in mid-boreal zone); collapsed areas were sinks of C, especially in high subarctic (from 27 g· C· m −2 year −1 in mid-boreal to 86 g·C·m −2 ·year −1 in high subarctic) and peat plateaus were minor sources (from 153 g· C· m −2 · year −1 in mid-boreal to 6 g·C·m −2 ·year −1 in high subarctic). The results are important in understanding how different landforms are responding to climate change and would be useful in modeling the effect of future climate change on the soil C balance in the northern regions.

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Section: Quantitative Relationships Between Nce and Er And Climate Vasupporting

confidence: 85%

Section: Discussionmentioning

confidence: 99%

Surface CO2 Exchange Dynamics across a Climatic Gradient in McKenzie Valley: Effect of Landforms, Climate and Permafrost

Startsev

Bhatti

Jassal

2016

Forests

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“…Patterns in the northern foothills of the North Slope include cotton-grass tussock tundra, bryophyte, lichen, and graminoid communities (Raynolds et al, 2006). Meanwhile, the boreal forest extends across the lowlands and uplands of the Tanana-Yukon flats, comprising white and black spruce and deciduous forests (Raynolds et al, 2006;Kim et al, 2013). Continuous and discontinuous permafrost underlies the tundra and boreal forest ecosystems, respectively, while no permafrost exists throughout the white spruce forest.…”

Section: Sampling Descriptions and Methodsmentioning

confidence: 99%

“…Recently, the magnitude of soil CO 2 efflux has seemed to depend on tundra greening and boreal forest browning (Verbyla, 2008;Bhatt et al, 2010;Parent and Verbyla, 2010), as well as on the timing of both snow disappearance and the snow-covered period (Stone et al, 2002;McDonald et al, 2004;Sturm et al, 2005). During the seasonally snow-covered period, winter CO 2 efflux measurements have heretofore been gathered in tundra (Oechel et al, 1997;Fahnestock et al, 1998Fahnestock et al, , 1998Björkman et al, 2010;Kim et al, 2013), alpine and subalpine forests (Brooks et al, 1996;Mast et al, 1998;Monson et al, 2006a, b), and boreal forests Winston et al, 1995Winston et al, , 1997Kim et al, 2007, accounting for 10-30 % of the variability in annual carbon emissions. However, it is difficult to determine the timing of snow disappearance in the early spring season, due to shorter snow disappearance time spans, including changes of −0.13 day year −1 over 60 years in Barrow, Alaska, according to NOAA/CMDL historical data (Stone et al, 2002), and −0.94 day year −1 over 14 years according to microwave remote sensing (McDonald et al, 2004).…”

Section: Introductionmentioning

confidence: 99%

“…Indeed, soil temperature and moisture are important parameters in regulating soil CO 2 efflux across tundra and boreal forest ecosystems (Lloyd and Taylor, 1994;Davidson et al, 1998;Xu and Qi, 2001;Davidson and Janssens, 2006;Rayment and Jarvis, 2000;Kim et al, 2007Kim et al, , 2013, and these parameters must be validated for terrestrial ecosystem process-based models, for the assessment of carbon budgets on regional and global scales. Also noted here are snow depth and snow crust, which slightly affect winter/spring CO 2 efflux in vegetation types across the North Slope of Alaska (R 2 = 0.19; Fahnestock et al, 1998), and in subalpine soils of Rocky Mountain National Park, Colorado (Mast et al, 1998), respectively.…”

Section: Introductionmentioning

confidence: 99%

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Effect of ablation rings and soil temperature on 3-year spring CO<sub>2</sub> efflux along the Dalton Highway, Alaska

Kim

2014

Biogeosciences

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Abstract. Winter and spring soil CO 2 efflux measurements represent a significant component in the assessment of annual carbon budgets of tundra and boreal forest ecosystems, reflecting responses to climate change in the Arctic. This study was conducted in order to quantify CO 2 efflux, using a portable chamber system at representative sites along the Dalton Highway. Study sites included three tundra, two white spruce, and three black spruce forest locations during the winter and spring seasons of 2010-2012; the study of these sites promised better understanding of winter and spring carbon contributions to the annual carbon budget, as well as the respective ablation-ring effects during spring. Three-year spring CO 2 efflux depends on soil temperature at 5 cm depth on a regional scale. At their highest, Q 10 values were 4.2 × 10 6 , within the exposed tussock tundra of the upland tundra site, which tundra soils warmed from −0.9 to 0.5 • C, involving soil microbial activity. From the forest census (400 m 2 ) of the two white spruce forest sites, CO 2 emissions were estimated as 0.09-0.36 gC m −2 day −1 in winter and 0.14-4.95 gC m −2 day −1 in spring, corresponding to 1-3 % and 1-27 % of annual carbon, respectively. Contributions from spring CO 2 emissions are likely to increase as exposed soils widen in average length (major axis) from the east-, west-, south-, and north-side lengths (minor axis). Considering the periods of winter and spring seasons across tundra and boreal forests, average winter-and springseasonal CO 2 contributions to annual carbon budgets correspond roughly to 14-22 % for tundra and 9-24 % for boreal forest sites during 2011 and 2012. Spring carbon contributions, such as growing season CO 2 emissions, are sensitive to subtle changes at the onset of spring and during the snowcovered period in northern high latitudes, in response to recent Arctic climate change.

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Boreal Forest and Forest Fires

Kim

Kobayashi

Nagai

et al. 2020

Arctic Hydrology, Permafrost and Ecosystems

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Latitudinal distribution of soil CO2 efflux and temperature along the Dalton Highway, Alaska

Cited by 22 publications

References 43 publications

Surface CO2 Exchange Dynamics across a Climatic Gradient in McKenzie Valley: Effect of Landforms, Climate and Permafrost

Surface CO2 Exchange Dynamics across a Climatic Gradient in McKenzie Valley: Effect of Landforms, Climate and Permafrost

Effect of ablation rings and soil temperature on 3-year spring CO<sub>2</sub> efflux along the Dalton Highway, Alaska

Boreal Forest and Forest Fires

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Latitudinal distribution of soil CO2 efflux and temperature along the Dalton Highway, Alaska

Cited by 22 publications

References 43 publications

Surface CO2 Exchange Dynamics across a Climatic Gradient in McKenzie Valley: Effect of Landforms, Climate and Permafrost

Surface CO2 Exchange Dynamics across a Climatic Gradient in McKenzie Valley: Effect of Landforms, Climate and Permafrost

Effect of ablation rings and soil temperature on 3-year spring CO&lt;sub&gt;2&lt;/sub&gt; efflux along the Dalton Highway, Alaska

Boreal Forest and Forest Fires

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Effect of ablation rings and soil temperature on 3-year spring CO<sub>2</sub> efflux along the Dalton Highway, Alaska