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37 results for “soil fractions”
Data for a leaf litter decomposition study and soil density fractionation analysis at a whole-watershed fertilization experiment in a temperate forest
To assess how elevated N deposition influences leaf litter decomposition dynamics and soil organic matter formation in a temperate deciduous forest, we coupled a reciprocal transplant leaf litter decomposition study with an analysis of the distribution of soil organic matter in mineral associated and particulate organic matter fractions at a long-term, whole-watershed, N fertilization experiment. We found that nearly 30 years of N additions slowed decay rates by about 11% for leaf litter decomposed in the fertilized watershed, regardless of the watershed from which the initial litter was collected. An apparent consequence of the altered rates of decomposition was that the soil in the fertilized watershed had about a 40% greater fraction of SOM in light particulate organic matter compared to the reference watershed, which was positively correlated with the bulk soil carbon to nitrogen ratio. Collectively, our results suggest that under conditions of N saturation, the physical transfer pathway of SOM formation is favored, which can have important implications for the future of the soil organic matter stock and nutrient cycling.
Data to support the publication "Impact of agricultural management on soil aggregates and associated organic carbon fractions: Analysis of long-term experiments in Europe"
<p><strong>Raw data:</strong> Experimental plot ids and information, mass distribution of all aggregate fractions after wet sieving, Sand content of each fraction to conduct the sand correction, mass distribution of all fractions after isolating the micro-aggregates held within the macroaggregates, yields per treatment, carbon content per fraction (raw data)</p> <p><strong>All data per plot: </strong>SOC content, MAOM and POM content of each fraction presented in the fractionation scheme included in the manuscript, together with the mass of the relative fractions. </p> <p> </p>
Global bare soil, photosynthetic and non-photosynthetic vegetation fraction annual at 500 m resolution
<p>Annual mean and std for (1) bare soil fraction, and (2) photosynthetic and (3) non-photosynthetic vegetation annual at 500 m resolution for 2001–2023. The dataset was obtained from: <a href="https://thredds.nci.org.au/thredds/catalog/tc43/modis-fc/v310/tiles/monthly/cover/catalog.html">https://thredds.nci.org.au/thredds/catalog/tc43/modis-fc/v310/tiles/monthly/cover/catalog.html</a> (monthly values; 320GB in total). Mean and std was derived using terra package in R using functions "mean" and "std" from 12 monthly values; missing values were ignored during derivation.</p> <p>Note: the Global Vegetation Fractional Cover Product (GVFCP) v3.1 (<a href="https://doi.org/10.1016/j.agee.2021.107719">Hill and Guerschman, 2022</a>) is derived from spectral unmixing of all seven optical bands from the 500 m MODIS (Moderate Resolution Imaging Spectroradiometer) Nadir BRDF (Bidirectional Reflectance Distribution Function)-adjusted Reflectance Product (NBAR, MCD43A4 Collection 6). A similar dataset has been produced by <a href="https://doi.org/10.5194/essd-16-1333-2024">Sun et al., (2024)</a>, covering period 2001–2022. Below is the sample code explaining how were the mean, max and std derived.</p> <pre><code>## Download from: https://thredds.nci.org.au/thredds/catalog/tc43/modis-fc/v310/tiles/monthly/cover/catalog.html ## wget -e robots=off -nH --cut-dirs 4 -nc -r -l5 -A '*.nc' -R 'catalog*' -I /thredds/fileServer/,/thredds/catalog/ 'https://thredds.nci.org.au/thredds/catalog/tc43/modis-fc/v310/tiles/monthly/cover/catalog.html' ## 6857 tiles library(terra) modis.tiles = list.files("/mnt/lacus/raw/modis-fc/v310/tiles/monthly/cover/", pattern = glob2rx("*.nc")) mod.lst = unique(sapply(modis.tiles, function(i){strsplit(i, "\\.")[[1]][4]})) str(mod.lst) ## 272 ## aggregate per year per tile nc_tile <- function(i, year, dir.x="/mnt/lacus/raw/modis-fc/v310/tiles/monthly/cover/", mc.cores=parallel::detectCores()){ require(terra) if(year == 2023 | year == 2024){ in.filename = paste0(dir.x, "FC_Monthly_Medoid.v310.MCD43A4.", i, ".", year, ".061.nc") } else { in.filename = paste0(dir.x, "FC_Monthly_Medoid.v310.MCD43A4.", i, ".", year, ".006.nc") } bs.filenames = paste0("./modis-fc/bs_", c("mean", "max", "std"), "/FC_Monthly_Medoid.v310.MCD43A4.", i, ".", year, ".006.tif") dg = terra::rast(in.filename) if(any(!file.exists(bs.filenames))){ bs = dg["bare_soil"] ## 12 months dg.m = app(bs, fun=mean, na.rm=TRUE, filename=bs.filenames[1], wopt=list(gdal=c("COMPRESS=DEFLATE"), datatype='INT1S'), overwrite=TRUE, cores = mc.cores) dg.x = app(bs, fun=max, na.rm=TRUE, filename=bs.filenames[2], wopt=list(gdal=c("COMPRESS=DEFLATE"), datatype='INT1S'), overwrite=TRUE, cores = mc.cores) dg.s = app(bs, fun=sd, na.rm=TRUE, filename=bs.filenames[3], wopt=list(gdal=c("COMPRESS=DEFLATE"), datatype='INT1S'), overwrite=TRUE, cores = mc.cores) } } ## run in parallel for(year in 2001:2024){ x = parallel::mclapply(sample(mod.lst), function(i){try( nc_tile(i, year=year, mc.cores = 2) )}, mc.cores = 40) tmpFiles(remove=TRUE) }</code></pre>
Modeling dust mineralogical composition: sensitivity to soil mineralogy atlases and their expected climate impacts. Soil and airborne mineral fraction datasets.
<p>These datasets correspond to soil and airbone mass mineral fractions as described and generated for "Modeling dust mineralogical composition: sensitivity to soil mineralogy" by Gonçalves Ageitos, M., Obiso, V., Miller, R.L., Jorba, O., Klose, M., Dawson, M., Balkanski, Y., Perlwitz, J., Basart, S., Di Tomaso, E., Escribano, J., Macchia, F., Montané, G., Mahowald, M.M., Green, R.O., Thompson, D.R. and Pérez García-Pando, C., ACP, 2023. </p> <p>There are 4 netCDF files that include the soil mass mineralogical fractions (0-1) in the clay (0-2 <span class="math-tex">\(\mu\)</span>m in diameter) and silt (2-63 <span class="math-tex">\(\mu\)</span>m in diameter) size classes as derived from the works of Claquin et al., (1999), and updated by Nickovic et al. (2012): <strong>C1999-SMA</strong>, and Journet et al. (2014): <strong>J2014-SMA</strong>. The data is mapped in a regular global grid with a horizontal resolution of 0.083º. Additional information on the FAO soil units, and soil texture data from HWSDv1.2 is provided in the J2014-SMA files. </p> <p>File details: </p> <ul> <li>C1999-SMA_CLAY_minfrac_0.083deg.nc - Claquin et al. (1999), Nickovic et al. (2012) soil mineralogy data for the clay fraction.</li> <li>C1999-SMA_SILT_minfrac_0.083deg.nc - Claquin et al. (1999), Nickovic et al. (2012) soil mineralogy data for the clay fraction.</li> <li>J2014-C2-SMA_CLAY_minfrac_0.083deg.nc - Journet et al. (2014) case 2 with the changes reported in Gonçalves Ageitos et al. (2023) soil mineralogy data for the clay fraction.</li> <li>J2014-C2-SMA_SILT_minfrac_0.083deg.nc - Journet et al. (2014) case 2 with the changes reported in Gonçalves Ageitos et al. (2023) soil mineralogy data for the clay fraction.</li> </ul> <p>There are 2 additional files that report the multiannual (2006-2010 period) monthly mean of the <strong>aerosol mass mineral fractions</strong> as obtained from the <strong>MONARCH model</strong> simulations described in Gonçalves Ageitos et al. (2023). The mass fractions are provided in each of the 8 size bins used in the model (ranging from 0.2 to 20 <span class="math-tex">\(\mu\)</span>m in diameter), and normalized so as to sum 1 (i.e., the sum of all minerals in all bins equals 1). Note that in order to reduce the size of these files, the variables have been compressed to short format and include an offset and scale factor as attributes. </p> <p>File details: </p> <ul> <li>20062010_monarch_minfrac_C1999.nc - climatology (2006-2010 multiannual monthly mean) of size distributed mass mineral fractions as derived from the MONARCH C1999 experiment. </li> <li>20062010_monarch_minfrac_J2014.nc - climatology (2006-2010 multiannual monthly mean) of size distributed mass mineral fractions as derived from the MONARCH J2014 experiment. </li> </ul> <p> </p> <p><em>Legend for the minerals:</em></p> <p>quar: quartz, feld: feldspars, calc: calcite, gyps: gypsum, illi: illite, mont: montmorillonite/smectite, kaol: kaolinite, verm:vermiculite, chlo: chlorite, mica: mica, hema: hematite, goet: goethite, irox:iron oxides (hematite and goethite). </p> <p>References:</p> <p>Claquin, T., Schulz, M., and Balkanski, Y. J.: Modeling the mineralogy of atmospheric dust sources, Journal of Geophysical Research<br> Atmospheres, https://doi.org/10.1029/1999JD900416, 1999.</p> <p>FAO-UNESCO: Soil Map of the World- Volume I Legend, Food and Agriculture Organization - United Nations Educational Scientific and Cultural Organization, Paris, http://www.fao.org/3/as360e/as360e.pdf, 1974.</p> <p>FAO-UNESCO: Food and Agriculture Organization - United Nations Educational Scientific and Cultural Organization. Digital Soil Map of the World and Derived Soil Properties, Food and Agriculture Organization - United Nations Educational Scientific and Cultural Organization, Rome, 1995.</p> <p>FAO/IIASA/ISRIC/ISSCAS/JRC: Harmonized World Soil Database (version 1.2), Food and Agriculture Organization, FAO, Rome, Italy and IIASA, Laxenburg, Austria, 2012.</p> <p>Journet, E., Balkanski, Y., and Harrison, S. P.: A new data set of soil mineralogy for dust-cycle modeling, Atmospheric Chemistry and<br> Physics, 14, 3801–3816, https://doi.org/10.5194/acp-14-3801-2014, 2014.</p> <p>Nickovic, S., Vukovic, A., Vujadinovic, M., Djurdjevic, V., and Pejanovic, G.: Technical Note: High-resolution mineralogical database of dust-productive soils for atmospheric dust modeling, Atmospheric Chemistry and Physics, 12, 845–855, https://doi.org/10.5194/acp-12-845-2012, 2012.</p> <p> </p>
CTE Soil Density Fractionation 2014
Climate change is increasing the intensity of severe tropical storms and cyclones (also referred to as hurricanes or typhoons), with major implications for tropical Forest structure and function. These changes in disturbance regime are likely to play an important role in regulating ecosystem carbon (C) and nutrient dynamics in tropical and subtropical forests. Canopy opening and debris deposition resulting from severe storms have complex and interacting effects on ecosystem biogeochemistry. Disentangling these complex effects will be critical to better understand the long-term implications of climate change on ecosystem C and nutrient dynamics. In this study, we used a well-replicated, long-term (10 years) canopy and debris manipulation experiment in a wet tropical forest to determine the separate and combined effects of canopy opening and debris deposition on soil C and nutrients throughout the soil profile (1 m). Debris deposition alone resulted in higher soil C and N concentrations, both at the surface (0–10 cm) and at depth (50–80 cm). Concentrations of NaOHorganic P also increased significantly in the debris deposition only treatment (20–90 cm depth), as did NaOH-total P (20–50 cm depth). Canopy opening, both with and without debris deposition, significantly increased NaOH-inorganic P concentrations from 70 to 90 cm depth. Soil iron concentrations were a strong predictor of both C and P patterns throughout the soil profile. Our results demonstrate that both surface- and subsoils have the potential to significantly increase C and nutrient storage a decade after the sudden deposition of disturbance-related organic debris. Our results also show that these effects may be partially offset by rapid decomposition and decreases in litterfall associated with canopy opening. The significant effects of debris deposition on soil C and nutrient concentrations at depth (>50 cm), suggest that deep soils are more dynamic than previously believed, and can serve as sinks of C
Phosphorus fractions and related properties in soils under Pinus sylvestris L. plantations in Spain
<p>This database presents information about the P fractions in soils determined following the method developed by Hedley et al. (1982) and modified by Tiessen and Moir (1993) and other soil chemical properties of soils under <em>Pinus sylvestris </em>L. plantations in Spain.</p> <p>Abbreviations of variables names and units are described below:</p> <p>pH: soil pH; EOC: easily oxidizable C (%); EA: exchangeable acidity (cmol<sub>(+)</sub>·kg<sup>-1</sup>); Ca: exchangeable Ca (cmol<sub>(+)</sub>·kg<sup>-1</sup>); Sat: base saturation of the exchangeable complex (%); Al<sub>A</sub>, Fe<sub>A</sub>: amorphous Al and Fe (mg kg<sup>-1</sup>); Al<sub>E</sub>: exchangeable Al (cmol<sub>(+)</sub>·kg<sup>-1</sup>); Al<sub>M</sub>, Fe<sub>M</sub>: organically bound Al and Fe (mg kg<sup>-1</sup>); SI: forest site index (m); Cmic: microbial biomass C (mg kg<sup>-1</sup>); Pmic: microbial biomass P (mg kg<sup>-1</sup>); Cmin: mineralizable C (mg·kg<sup>-1</sup>·week<sup>-1</sup>) ; AcPhos: acid phosphatase activity (µg·g<sup>-1</sup>·h<sup>-1</sup>); PAEM: available P (mg kg<sup>-1</sup>); PiNaHCO3, PoNaHCO3: inorganic and organic highly labile P (mg kg<sup>-1</sup>); PoNaOH; PiNaOH: inorganic and organic moderately labile P (mg kg<sup>-1</sup>); PHCl1M: primary P (mg kg<sup>-1</sup>); PHClconc: stable P (mg kg<sup>-1</sup>); PHClO4: residual P (mg kg<sup>-1</sup>); PTotal: addition of all previous P fractions analysed (mg kg<sup>-1</sup>).</p>
Data from: Long-term changes in soil carbon and nitrogen fractions in switchgrass, native grasses, and no-till corn bioenergy production systems
<p>Cellulosic bioenergy is a primary land-based climate mitigation strategy, with soil carbon (C) storage and nitrogen (N) conservation as important mitigation elements. Here, we present 13 years of soil C and N change under three cellulosic cropping systems: monoculture switchgrass (<em>Panicum virgatum</em> L.), a five native grasses polyculture, and no-till corn (<em>Zea mays</em> L.). Soil C and N fractions were measured four times over 12 years. Bulk soil C in the 0–25 cm depth at the end of the study period ranged from 28.4 (± 1.4 se) Mg C ha<sup>−1</sup> in no-till corn, to 30.8 (± 1.4) Mg C ha<sup>−1</sup> in switchgrass, and to 34.8 (± 1.4) Mg C ha<sup>−1</sup> in native grasses. Mineral-associated organic matter (MAOM) ranged from 60% to 90% and particulate organic matter (POM) from 10% to 40% of total soil C. Over 12 years, total C as well as both C fractions persisted under no-till corn and switchgrass and increased under native grasses. In contrast, POM N stocks decreased 33% to 45% across systems, whereas MAOM N decreased by less than 13% and only in no-till corn. Declining POM N stocks likely reflect pre-establishment land use, which included alfalfa and manure in earlier rotations. Root production and large soil aggregate formation explained 69% (p < 0.001) and 36% (p = 0.024) of total soil C change, respectively, and 60% (p = 0.020) and 41% (p = 0.023) of soil N change, demonstrating the importance of belowground productivity and soil aggregates for producing and protecting soil C and conserving soil N. Differences between switchgrass and native grasses also indicate a dependence on plant diversity. Soil C and N benefits of bioenergy crops depend strongly on root productivity and pre-establishment land use.</p>
Data from: Long-term changes in soil carbon and nitrogen fractions in switchgrass, native grasses, and no-till corn bioenergy production systems
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Density fractionation of soils from the Nevada Desert FACE Facility
These data are the result of a soil density fractionation experiment conducted on soils from the Nevada Desert FACE (Free Air Carbon Dioxide Enrichment) Facility located in Mars, NV. This study was a 10 year experiment where an undisturbed arid ecosystem was exposed to elevated atmospheric CO2 (550 ppm). The experiment had three control plots and three elevated CO2 plots. At the end of the experiment, soils were harvested from beneath five major vegetation cover types and unvegetated interspace. These species included A. dumosa, L. tridentata, L. Pallidum, L. Andersonii, and P. rigida. Bulk soils were collected in 20 cm increments from 0-100 cm. Bulk density was measured as kg soil per m2 in 20 cm increments from each plot in the experiment. The bulk density used for stock calculations here was an average of the values taken at each depth across all 6 plots. The density fractionation was conducted using sodium polytungstate at 1.85 g cm^-3. A separate set of soils from the top 0-20 cm of the soil profile were also isolated into a < 20 um fraction for analysis by pyrolysis GC/MS. Heavy and light fraction were treated with HCl fumigation to remove inorganic carbon prior to analysis for organic C and 13C and non acidified samples were analyzed for total N and 15N at the Cornell Stable Isotope Lab. Pyrolysis GC/MS samples were analyzed at Dr. Grandy's lab at UNH.
δ15N of nitric oxide produced under aerobic or anaerobic conditions from seven soils and their associated N isotope fractionations
<p>Measuring the nitrogen isotope compositions (δ<sup>15</sup>N) of nitric oxide (NO) from different sources helps to quantify the relative contributions of atmospheric NO<sub>x</sub>. Soil is one of the most important sources of atmospheric NO<sub>x</sub>, but only limited measurements on the δ<sup>15</sup>N of soil emitted NO exist, hampering our ability to partition sources to air pollution. Here we conducted soil incubations to measure the δ<sup>15</sup>N-NO under defined aerobic or anaerobic conditions, favoring either nitrification or denitrification. Soils were collected from seven sites spanning three ecosystems in northern China (two agricultural, two forest, and three grassland sites). We found that the δ<sup>15</sup>N-NO and their associated N isotope fractionations were significant different between anaerobic and aerobic conditions in seven soils. Under aerobic condition, the δ<sup>15</sup>N-NO ranged from -62‰ to -50‰ (averaged -56 ± 4‰), being significantly more negative (by 23‰) than those under anaerobic condition (-45‰ to -23‰, averaged -33 ± 7‰). The apparent N isotope fractionation for NO production under aerobic condition (<sup>15</sup><em>ε</em><sub>aerobic</sub> = 61 ± 3‰) was significantly higher (by 26‰) than under anaerobic condition (<sup>15</sup><em>ε</em><sub>anaerobic</sub> = 35 ± 6‰), with a small variability among ecosystem types. Our study demonstrates that the δ<sup>15</sup>N-NO from different soils are very different from fuel combustions (mainly from 0 to +20‰), supporting that measuring <sup>15</sup>N is a useful tool to partition the contributions of soil NO to atmospheric NO<sub>x</sub>. Our results also imply δ<sup>15</sup>N-NO produced by nitrification and denitrification distinctly different, as these two processes are dominant processes producing NO under aerobic and anaerobic conditions, respectively.</p>
Cover crops improve soil structure and change OC distribution in aggregate fractions
<p>Data set and R script on the statistic evaluation of soil data. The data derived from a long-term field trial at the Asendorf field station 70 km north of Hanover, Germany (49 m above sea level, 52°45′48.4′′N 9°01′24.3′′E). Data include soil data (OC, TN, bulk density, texture) as well as data from soil aggregate fractionation and evaluation of their aggregate stability. All methods and data will be described in an upcoming journal article (DOI will be provided soon).</p>
Contents of soil organic matter fractions as affected by warming and rain exclusion at a semiarid Mediterranean site
<p>Data and metadata of total, free, intra-aggregate, and mineral-associated organic C and N contents of soils from a dryland ecosystem warming experiment established in Aranjuez, Central Spain.</p>
Ericaceous dwarf shrubs contribute a significant but drought-sensitive fraction of soil respiration in a boreal pine forest
<p><span>Boreal forests often have a dense understory of ericaceous dwarf shrubs with ecological adaptations that contrast those of the canopy-forming trees. It is therefore important to quantify contributions by understory shrubs to ecosystem processes and disentangle shrub- and tree-driven responses, and their interactions, to climatic factors. </span><span>We quantified soil respiration driven by the pine canopy and the ericaceous shrub understory over three years, using a factorial pine root-exclusion and shrub-removal experiment in a mature <em>Pinus sylvestris</em> forest. Soil temperature and moisture-related responses of respiration attributed to autotrophic (shrubs, pine roots) and heterotrophs were compared. Additionally, we assessed effects of interactions between these functional groups on soil nitrogen availability and respiration. </span><span>Understory shrubs accounted for </span><span>22 ± 10% of total autotrophic respiration, reflecting the ericaceous proportion of fine root production in the ecosystem. Heterotrophic respiration constituted about half of total soil respiration. Shrub-driven respiration was more susceptible to drought than heterotrophic- and pine-driven autotrophic respiration. While the respiration attributed to canopy and understory remained additive, indicating no competitive release, </span><span>the plant guilds competed for inorganic N. </span><span>Ericaceous understory shrubs accounted for a small, yet significant, share of total growing season soil respiration. Overlooking understory respiration may lead to erroneous partitioning and modelling of soil respiration mediated by functional guilds with contrasting responses to soil temperature and moisture. A higher share of activity of both heterotrophs and pine roots, under drought conditions, could have important implications for soil organic matter accumulation and decomposition as the climate changes.</span></p>
Soil C saturation in tropical agricultural systems: soil fertility, climate, texture and N controls on SOM fractions
<p><span>Nature-based solutions for C sequestration in tropical croplands are paramount strategies in a changing climate. Soybean-maize-forage intercropped systems associated with soil acidity alleviation and nitrogen (N) fertilization effectively accumulate carbon (C) in weathered soils. However, the soil saturation status and the controls of C stabilization up to 40 cm soil depth into particulate (POM) and mineral-associated organic matter (MAOM) fractions are poorly understood in tropical croplands. This study tested the hypothesis of C saturation in the MAOM fraction by comparing field and published data focused on Brazilian tropical soils. We assessed the N fertilization effect on C stabilization in POM and MAOM pools, and climate, soil texture, and chemical attributes controls on POM and MAOM formation in tropical croplands using a machine-learning Random Forest (RF) modeling approach. Our findings do not support C saturation in the MAOM regardless of contrasting soil contents of silt plus clay and depths. C in the MAOM and POM fractions were not affected by N fertilizer. However, legume inclusion in the system resulted in higher total soil C and lower soil C:N ratio compared with N fertilization, which indicates that C dynamics differ whether synthetic or organic-N forms are applied to tropical croplands. Our RF model showed robust predictive performance for the MAOM but poorer for the POM fraction. Total organic carbon (TOC), total N, silt plus clay, phosphorus (P) and soil depth, zinc (Zn), cation exchange capacity, and TOC covariates were the most important variables for predicting MAOM and POM fractions, respectively. Our findings show, besides the well-known effect of calcium, that other nutrients such as P, Zn, manganese and copper play a key role in either MAOM or POM formation. Our work provides key insights on C saturation status in tropical croplands and land-management C sequestering potential, and N, climate, soil chemical attributes and texture controls on C distribution into MAOM and POM fractions up to 40 cm soil depth in tropical conservation agricultural systems. We advocate for upscaling C saturation concept nationally and further research investigating the role of climate and micronutrients contribution on MAOM and POM formation in broad scenarios and N fertilizer responsiveness for C stabilization in tropical croplands.</span></p>
Quality of free soil organic matter fraction as affected by warming and rain exclusion at a semiarid Mediterranean site
<p>Data and metadata of nuclear magnetic resonance (NMR) of free organic matter fraction of soils from a dryland ecosystem warming experiment established in Aranjuez, Central Spain.</p>
Contents of soil organic matter fractions as affected by warming and rain exclusion at a semiarid Mediterranean site
<p>Data and metadata of total, free, intra-aggregate, and mineral-associated organic C and N contents of soils from a dryland ecosystem warming experiment established in Aranjuez, Central Spain.</p>
Clay minerals control rare earth elements (REE) fractionation in Brazilian mangrove soils
<p>XRD data from different size fractions of Brazilian mangrove soils, supporting the manuscript entitled <strong><em>Clay minerals control rare earth elements (REE) fractionation in Brazilian mangrove soils, </em></strong>submitted to the journal <strong><em>Catena</em>.</strong></p>
δ15N of nitric oxide produced under aerobic or anaerobic conditions from seven soils and their associated N isotope fractionations
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Fractions of soil phosphorus mediated by rhizospheric phoD-harboring bacteria of deep-rooted desert species are determined by fine-root traits
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Ericaceous dwarf shrubs contribute a significant but drought-sensitive fraction of soil respiration in a boreal pine forest
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