Experimental study on soil respiration of temperate grassland in China

Wang, Gengchen; Du, Rui; Kong, Qinxin; Lü, Daren

doi:10.1360/03wd0241

Cited by 17 publications

(8 citation statements)

References 3 publications

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“…Hence, the CO 2 emissions during midsummer as determined in this study (mean: 37.4 mg C m -2 h -1 ) are within the range of the published values. Likewise, the mean soil CO 2 emission (34.7±33.8 mg C m -2 h -1 ) for cores taken from typical steppes was in agreement with findings from previous studies conducted in the typical steppe of Inner Mongolia (ranging from 5.9-44.5 mg C m -2 h -1 ; Li et al 2000;Cui et al 2000;Zhang et al 2003;Wang et al 2004;Qi et al 2007;Zou et al 2007). Temperature and precipitation are considered to be the most important environmental factors in determining spatial variations of soil CO 2 emission (Xu and Qi 2001;Wang and Fang 2009).…”

Section: Patterns Magnitudes and Environmental Controls Of Ghg Fluxessupporting

confidence: 90%

Spatial variability of N2O, CH4 and CO2 fluxes within the Xilin River catchment of Inner Mongolia, China: a soil core study

Yao

Wolf²,

Chen

et al. 2009

Plant Soil

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In order to identify the effects of land-use/ cover types, soil types and soil properties on the soilatmosphere exchange of greenhouse gases (GHG) in semiarid grasslands as well as provide a reliable estimate of the midsummer GHG budget, nitrous oxide (N 2 O), methane (CH 4 ) and carbon dioxide (CO 2 ) fluxes of soil cores from 30 representative sites were determined in the upper Xilin River catchment in Inner Mongolia. The soil N 2 O emissions across all of the investigated sites ranged from 0.18 to 21.8 μg N m -2 h -1 , with a mean of 3.4 μg N m -2 h -1 and a coefficient of variation (CV, which is given as a percentage ratio of one standard deviation to the mean) as large as 130%. CH 4 fluxes ranged from -88.6 to 2,782.8 μg C m -2 h -1 (with a CV of 849%). Net CH 4 emissions were only observed from cores taken from a marshland site, whereas all of the other 29 investigated sites showed net CH 4 uptake (mean: -33.3 μg C m -2 h -1 ). CO 2 emissions from all sites ranged from 3.6 to 109.3 mg C m -2 h -1 , with a mean value of 37.4 mg C m -2 h -1 and a CV of 66%. Soil moisture primarily and positively regulated the spatial variability in N 2 O and CO 2 emissions (R 2 =0.15-0.28, P<0.05). The spatial variation of N 2 O emissions was also influenced by soil inorganic N contents (P< 0.05). By simply up-scaling the site measurements by the various land-use/cover types to the entire catchment area (3,900 km 2 ), the fluxes of N 2 O, CH 4 and CO 2 at the time of sampling (mid-summer 2007) were estimated at 29 t CO 2 -C-eq d -1 , -26 t CO 2 -C-eq d -1 and 3,223 t C d -1 , respectively. This suggests that, in terms of assessing the spatial variability of total GHG fluxes from the soils at a semiarid catchment/region, intensive studies may focus on CO 2 exchange, which is dominating the global warming potential of midsummer soil-atmosphere GHG fluxes. In addition, average GHG fluxes in midsummer, weighted by the areal extent of these land-use/cover types in the region, were approximately -30.0 μg C m -2 h -1 for CH 4 , 2.4 μg N m -2 h -1 for N 2 O and 34.5 mg C m -2 h -1 for CO 2 .

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Section: Patterns Magnitudes and Environmental Controls Of Ghg Fluxessupporting

confidence: 90%

Spatial variability of N2O, CH4 and CO2 fluxes within the Xilin River catchment of Inner Mongolia, China: a soil core study

Yao

Wolf²,

Chen

et al. 2009

Plant Soil

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“…The patchy vegetative cover of sparse U. pumila woodland is similar with the woody plant encroached grassland (such as shrublands), and the spatial variation of soil respiration within the site of U. pumila woodland is revelatory to other heterogeneous sites. The monthly mean of soil respiration in the canopy field of U. pumila trees, i.e., 305.5-730.8 mg CO 2 m À2 h À1 in our study, were much higher than the semi-arid temperature grasslands of China (i.e., 297-331 CO 2 m À2 h À1 ; Wang et al 2004) under the same climate and the world's major temperate grasslands (55.3-347 mg CO 2 m À2 h À1 ; Raich and Schlesinger 1992). Soil respiration in the canopy field of the U. pumila trees was similar with that in forest ecosystems (Buchmann 2000;Borken et al 2006).…”

Section: Discussioncontrasting

confidence: 51%

Dynamics of soil respiration in sparse Ulmus pumila woodland under semi‐arid climate

Jin

Sun

Luo

et al. 2008

Ecological Research

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Sparse Ulmus pumila woodlands play an important role in contributing to ecosystem function in semi-arid grassland of northern China. To understand the key attributes of soil carbon cycling in U. pumila woodland, we studied dynamics of soil respiration in the canopy field (i.e., the projected crown cover area) and the open field at locations differing in distance (i.e., at 1-1.5, 3-4, 10, and >15 m) to tree stems from July through September of 2005, and measured soil biotic factors (e.g., fine root mass, soil microbial biomass, and activity) and abiotic factors [e.g., soil water content (SWC) and organic carbon] in mid-August. Soil respiration was further separated into root component and microbial component at the end of the field measurement in September. Results showed that soil respiration had a significant exponent relationship with soil temperature at 10-cm depth. The temperature sensitivity index of soil respiration, Q 10 , was lower than the global average of 2.0, and declined significantly (P < 0.05) with distance. The rate of soil respiration was generally greater in the canopy field than in the open field; monthly mean of soil respiration was 305.5-730.8 mg CO 2 m À2 h À1 in the canopy field and 299.6-443.1 mg CO 2 m À2 h À1 in the open field from July through September; basal soil respiration at 10°C declined with distance, and varied from $250 mg CO 2 m À2 h À1 near tree stems to <200 mg CO 2 m À2 h À1 in the open field. Variations in soil respiration with distance were consistent with patterns of SWC, fine root mass, microbial biomass and activities. Regression analysis indicated that soil respiration was tightly coupled with microbial respiration and only weakly related to root respiration. Overall, variations in SWC, soil nutrients, microbial biomass, and microbial activity are largely responsible for the spatial heterogeneity of soil respiration in this semi-arid U. pumila woodland.

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“…The soil CO 2 flux in the Kobresia humilis meadow is larger than that in the Dasiphora fruticosa shrub meadow, consistent with other studies [10,17] , but this result is less than that from Cao (663 g C m −2 a −1 and 661 g C m −2 a −1 respectively) [10] . By comparison, the soil CO 2 flux in the Tibetan Plateau is significantly higher than that in Tundra (60 g C m −2 a −1 ), and evidently less than that (457-488 g C m −2 a −1 ) in adjacent latitude, low altitude North American great plain (38°50′N, 92°02′W) [43] and that (390-866 g C m −2 a −1 ) in Inner Mongolia grassland [46] . This phenomenon results from the alpine environment on the Tibetan Plateau.…”

Section: Soil Co 2 Flux Released From Decomposition Of Organic Mattermentioning

confidence: 77%

Soil organic carbon storage and soil CO2 flux in the alpine meadow ecosystem

et al. 2007

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High-resolution sampling, measurements of organic carbon contents and 14 C signatures of selected four soil profiles in the Haibei Station situated on the northeast Tibetan Plateau, and application of 14 C tracing technology were conducted in an attempt to investigate the turnover times of soil organic carbon and the soil-CO 2 flux in the alpine meadow ecosystem. The results show that the organic carbon stored in the soils varies from 22.12×10 4 kg C hm −2 to 30.75×10 4 kg C hm −2 in the alpine meadow ecosystems, with an average of 26.86×10 4 kg C hm −2 . Turnover times of organic carbon pools increase with depth from 45 a to 73 a in the surface soil horizon to hundreds of years or millennia or even longer at the deep soil horizons in the alpine meadow ecosystems. The soil-CO 2 flux ranges from 103.24 g C m −2 a −1 to 254.93 gC m −2 a −1 , with an average of 191.23 g C m −2 a −1 . The CO 2 efflux produced from microbial decomposition of organic matter varies from 73.3 g C m −2 a −1 to 181 g C m −2 a −1 . More than 30% of total soil organic carbon resides in the active carbon pool and 72.8%-81.23% of total CO 2 emitted from organic matter decomposition results from the topsoil horizon (from 0 cm to 10 cm) for the Kobresia meadow. Responding to global warming, the storage, volume of flow and fate of the soil organic carbon in the alpine meadow ecosystem of the Tibetan Plateau will be changed, which needs further research.

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Experimental study on soil respiration of temperate grassland in China

Cited by 17 publications

References 3 publications

Spatial variability of N2O, CH4 and CO2 fluxes within the Xilin River catchment of Inner Mongolia, China: a soil core study

Spatial variability of N2O, CH4 and CO2 fluxes within the Xilin River catchment of Inner Mongolia, China: a soil core study

Dynamics of soil respiration in sparse Ulmus pumila woodland under semi‐arid climate

Soil organic carbon storage and soil CO2 flux in the alpine meadow ecosystem

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