Rapid and transient response of soil respiration to rain

Lee, Xuhui; Wu, Hui-Ju; Sigler, J. M.; Oishi, A. Christopher; Siccama, Thomas G.

doi:10.1111/j.1529-8817.2003.00787.x

Cited by 248 publications

(212 citation statements)

References 38 publications

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“…The strong dependence of FLD on moisture conditions was evidenced by the marked difference between sites in July 2002 and September 2003. The link between leaf litter decomposition and moisture has been documented by Lee et al (2004) who found a linear decrease in the relative contribution of the litter layer with lower litter water contents in a manipulated study in a mixed forest. In a tropical forest, an indication of the dependence of FLD on litter moisture content was observed by Goulden et al (2004) when patterns of soil respiration rates varied in concert with the moisture content of the surface leaf litter.…”

Section: Leaf Litter Decompositionmentioning

confidence: 99%

Partitioning sources of soil‐respired CO₂ and their seasonal variation using a unique radiocarbon tracer

Cisneros-Dozal

Trumbore

Hanson

2005

Global Change Biology

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Soil respiration is derived from heterotrophic (decomposition of soil organic matter) and autotrophic (root/rhizosphere respiration) sources, but there is considerable uncertainty about what factors control variations in their relative contributions in space and time. We took advantage of a unique whole-ecosystem radiocarbon label in a temperate forest to partition soil respiration into three sources: (1) recently photosynthesized carbon (C), which dominates root and rhizosphere respiration; (2) leaf litter decomposition and (3) decomposition of root litter and soil organic matter 41-2 years old.Heterotrophic sources and specifically leaf litter decomposition were large contributors to total soil respiration during the growing season. Relative contributions from leaf litter decomposition ranged from a low of $ 1 AE 3% of total soil respiration (6 AE 3 mg C m À2 h À1 ) when leaf litter was extremely dry, to a high of 42 AE 16% (96 AE 38 mg C m À2 h À1 ). Total soil respiration fluxes varied with the strength of the leaf litter decomposition source, indicating that moisture-dependent changes in litter decomposition drive variability in total soil respiration fluxes. In the surface mineral soil layer, decomposition of C fixed in the original labeling event (3-5 years earlier) dominated the isotopic signature of heterotrophic respiration.Root/rhizosphere respiration accounted for 16 AE 10% to 64 AE 22% of total soil respiration, with highest relative contributions coinciding with low overall soil respiration fluxes. In contrast to leaf litter decomposition, root respiration fluxes did not exhibit marked temporal variation ranging from 34 AE 14 to 40 AE 16 mg C m À2 h À1 at different times in the growing season with a single exception (88 AE 35 mg C m À2 h À1 ). Radiocarbon signatures of root respired CO 2 changed markedly between early and late spring (March vs. May), suggesting a switch from stored nonstructural carbohydrate sources to more recent photosynthetic products.

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Section: Leaf Litter Decompositionmentioning

confidence: 99%

Partitioning sources of soil‐respired CO₂ and their seasonal variation using a unique radiocarbon tracer

Cisneros-Dozal

Trumbore

Hanson

2005

Global Change Biology

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“…The Mediterranean climate is characterized by summer droughts that particularly affect the top soil layers; therefore, rainfall events during these dry periods can trigger abrupt increases in SR that last for days (Bowling et al, 2011;Cisneros-Dozal et al, 2007;Lee et al, 2004;Unger et al, 2010). Lee et al (2004) simulated precipitation and found that hardwood forest floors were very sensitive to changes in moisture in the upper soil layers.…”

Section: Rain Pulse and Drought Effects On Srmentioning

confidence: 99%

Does soil moisture overrule temperature dependence of soil respiration in Mediterranean riparian forests?

et al. 2014

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Abstract. Soil respiration (SR) is a major component of ecosystems' carbon cycles and represents the second largest CO 2 flux in the terrestrial biosphere. Soil temperature is considered to be the primary abiotic control on SR, whereas soil moisture is the secondary control factor. However, soil moisture can become the dominant control on SR in very wet or dry conditions. Determining the trigger that makes soil moisture as the primary control factor of SR will provide a deeper understanding on how SR changes under the projected future increase in droughts. Specific objectives of this study were (1) to investigate the seasonal variations and the relationship between SR and both soil temperature and moisture in a Mediterranean riparian forest along a groundwater level gradient; (2) to determine soil moisture thresholds at which SR is controlled by soil moisture rather than by temperature; (3) to compare SR responses under different tree species present in a Mediterranean riparian forest (Alnus glutinosa, Populus nigra and Fraxinus excelsior). Results showed that the heterotrophic soil respiration rate, groundwater level and 30 cm integral soil moisture (SM 30 ) decreased significantly from the riverside moving uphill and showed a pronounced seasonality. SR rates showed significant differences between tree species, with higher SR for P. nigra and lower SR for A. glutinosa. The lower threshold of soil moisture was 20 and 17 % for heterotrophic and total SR, respectively. Daily mean SR rate was positively correlated with soil temperature when soil moisture exceeded the threshold, with Q 10 values ranging from 1.19 to 2.14; nevertheless, SR became decoupled from soil temperature when soil moisture dropped below these thresholds.

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Section: Time Series Of Nce and Ermentioning

confidence: 99%

“…In peat plateau, the lower layer (21 to 40 cm) contributed about only 5% of SR, which could be due to the presence of the water table. Peat plateau areas exhibited greater variability in the flux with a pronounced increase in the CO2 emissions after rain events, which can be attributed to increased decomposition [26] or displacement of soil-stored CO2 [30]. Calculated flux contributions from different soil layers using the CO 2 gradient technique showed that in both peat plateau (PP) and upland (UL) areas, the greatest contribution (about 75%) of soil respiration (SR) originated in the upper 5 cm layer (Figure 7).…”

Section: Time Series Of Nce and Ermentioning

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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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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Rapid and transient response of soil respiration to rain

Cited by 248 publications

References 38 publications

Partitioning sources of soil‐respired CO₂ and their seasonal variation using a unique radiocarbon tracer

Partitioning sources of soil‐respired CO₂ and their seasonal variation using a unique radiocarbon tracer

Does soil moisture overrule temperature dependence of soil respiration in Mediterranean riparian forests?

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

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Rapid and transient response of soil respiration to rain

Cited by 248 publications

References 38 publications

Partitioning sources of soil‐respired CO2 and their seasonal variation using a unique radiocarbon tracer

Partitioning sources of soil‐respired CO2 and their seasonal variation using a unique radiocarbon tracer

Does soil moisture overrule temperature dependence of soil respiration in Mediterranean riparian forests?

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

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Partitioning sources of soil‐respired CO₂ and their seasonal variation using a unique radiocarbon tracer

Partitioning sources of soil‐respired CO₂ and their seasonal variation using a unique radiocarbon tracer