An observation-based assessment of the influences of air temperature and snow depth on soil temperature in Russia

Park, Hotaek; Sherstiukov, A. B.; Fedorov, A.A.; Polyakov, Igor V.; Walsh, John E.

doi:10.1088/1748-9326/9/6/064026

Cited by 89 publications

(63 citation statements)

References 19 publications

(37 reference statements)

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“…This percentage was greater than or equal to the contribution of the SAT. Our assessment is generally consistent with previous studies (Stieglitz et al 2003;Osterkamp 2007;Lawrence and Slater 2010;Park et al 2014 …”

Section: Contributions Of Sat and Snd To T Soilsupporting

confidence: 92%

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Effect of snow cover on pan-Arctic permafrost thermal regimes

et al. 2014

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in winter, due to insulation of the soil resulting from early cooling. Simulations revealed that T SOIL tended to increase over most of the pan-Arctic from 1901 to 2009, and that this increase was significant in northern regions, especially in northeastern Siberia where SND is responsible for 50 % or more of the changes in T SOIL at a depth of 3.6 m. In the same region, ALT also increased at a rate of approximately 2.3 cm per decade. The most sensitive response of ALT to changes in SND appeared in the southern boundary regions of permafrost, in contrast to permafrost temperatures within the 60°N-80°N region, which were more sensitive to changes in snow cover. Finally, our model suggests that snow cover contributes to the warming of permafrost in northern regions and could play a more important role under conditions of future Arctic warming.

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Section: Contributions Of Sat and Snd To T Soilsupporting

confidence: 92%

“…A change in an area with deeper SND in the winter could have a smaller effect than the same changes in an area with shallower SND because snow insulation varies more strongly at shallow depths (Park et al 2014). This is evident in Fig.…”

Section: Soil Temperaturementioning

confidence: 99%

Effect of snow cover on pan-Arctic permafrost thermal regimes

et al. 2014

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“…5 for each model. Based on ground soil temperature observation, annual T s at 1.6 m increased by 0.02-0.03 • C yr −1 from the 1960s to 2000s in Russia (Park et al, 2014). The simulated trends of T s at 1.6 m over BOAS in most models are within this range (Fig.…”

Section: Attenuation Of the Trend In Soil Temperature With Soil Depthmentioning

confidence: 78%

Simulated high-latitude soil thermal dynamics during the past 4 decades

et al. 2016

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Abstract. Soil temperature (T s ) change is a key indicator of the dynamics of permafrost. On seasonal and interannual timescales, the variability of T s determines the activelayer depth, which regulates hydrological soil properties and biogeochemical processes. On the multi-decadal scale, increasing T s not only drives permafrost thaw/retreat but can also trigger and accelerate the decomposition of soil organic carbon. The magnitude of permafrost carbon feedbacks is thus closely linked to the rate of change of soil thermal regimes. In this study, we used nine process-based ecosystem models with permafrost processes, all forced by different observation-based climate forcing during the period 1960-2000, to characterize the warming rate of T s in permafrost regions. There is a large spread of T s trends at 20 cm depth across the models, with trend values ranging from 0.010 ± 0.003 to 0.031 ± 0.005 • C yr −1 . Most models show smaller increase in T s with increasing depth. Air temperature (T a ) and longwave downward radiation (LWDR) are the main drivers of T s trends, but their relative contributions differ amongst the models. Different trends of LWDR used in the forcing of models can explain 61 % of their differences in T s trends, while trends of T a only explain 5 % of the differences in T s trends. Uncertain climate forcing contributes a larger uncertainty in T s trends (0.021 ± 0.008 • C yr −1 , mean ± standard deviation) than the uncertainty of model structure (0.012 ± 0.001 • C yr −1 ), diagnosed from the range Published by Copernicus Publications on behalf of the European Geosciences Union. S. Peng et al.: Simulated high-latitude soil thermal dynamics during the past 4 decadesof response between different models, normalized to the same forcing. In addition, the loss rate of near-surface permafrost area, defined as total area where the maximum seasonal active-layer thickness (ALT) is less than 3 m loss rate, is found to be significantly correlated with the magnitude of the trends of T s at 1 m depth across the models (R = −0.85, P = 0.003), but not with the initial total nearsurface permafrost area (R = −0.30, P = 0.438). The sensitivity of the total boreal near-surface permafrost area to T s at 1 m is estimated to be of −2.80 ± 0.67 million km 2 • C −1 . Finally, by using two long-term LWDR data sets and relationships between trends of LWDR and T s across models, we infer an observation-constrained total boreal near-surface permafrost area decrease comprising between 39 ± 14 × 10 3 and 75 ± 14 × 10 3 km 2 yr −1 from 1960 to 2000. This corresponds to 9-18 % degradation of the current permafrost area.

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“…Firstly, study years with 365 daily records were utilized in the annual indices. Secondly, we detect the outliers with 3 standard deviations (3σ ) from its long-term mean as described by Polyakov et al (2003) and Park et al (2014). To ensure a specific outlier which may be questionable, we check the outlier with neighboring stations within 200 km.…”

Section: Methodsmentioning

confidence: 99%

Changes in the timing and duration of the near-surface soil freeze/thaw status from 1956 to 2006 across China

2015

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Abstract. The near-surface soil freeze/thaw status is an important indicator of climate change. Using data from 636 meteorological stations across China, we investigated the changes in the first date, the last date, the duration, and the number of days of the near-surface soil freeze over the period 1956-2006. The results reveal that the first date of the near-surface soil freeze was delayed by about 5 days, or at a rate of 0.10 ± 0.03 day yr −1 , and the last date was advanced by about 7 days, or at a rate of 0.15 ± 0.02 day yr −1 . The duration of the near-surface soil freeze decreased by about 12 days or at a rate of 0.25 ± 0.04 day yr −1 , while the actual number of the near-surface soil freeze days decreased by about 10 days or at a rate of 0.20 ± 0.03 day yr −1 . The rates of changes in the near-surface soil freeze/thaw status increased dramatically from the early 1990s through the end of the study period. Regionally, the changes in western China were greater than those in eastern China. Changes in the nearsurface soil freeze/thaw status were primarily controlled by changes in air temperature, but urbanization may also play an important role.

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An observation-based assessment of the influences of air temperature and snow depth on soil temperature in Russia

Cited by 89 publications

References 19 publications

Effect of snow cover on pan-Arctic permafrost thermal regimes

Effect of snow cover on pan-Arctic permafrost thermal regimes

Simulated high-latitude soil thermal dynamics during the past 4 decades

Changes in the timing and duration of the near-surface soil freeze/thaw status from 1956 to 2006 across China

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