Nitrous oxide (N2O) is a powerful greenhouse gas and the main driver of stratospheric ozone depletion. Since soils are the largest source of N2O, predicting soil response to changes in climate or land use is central to understanding and managing N2O. Here we find that N2O flux can be predicted by models incorporating soil nitrate concentration (NO3−), water content and temperature using a global field survey of N2O emissions and potential driving factors across a wide range of organic soils. N2O emissions increase with NO3− and follow a bell-shaped distribution with water content. Combining the two functions explains 72% of N2O emission from all organic soils. Above 5 mg NO3−-N kg−1, either draining wet soils or irrigating well-drained soils increases N2O emission by orders of magnitude. As soil temperature together with NO3− explains 69% of N2O emission, tropical wetlands should be a priority for N2O management.
Organic soils make up more than one-tenth of the world’s soil nitrogen (N) pool1 and are a significant global source of the greenhouse gas nitrous oxide (N2O). We do not fully understand the underlying microbial production and consumption processes and how these interact with environmental drivers such as the microclimate, physics, and chemistry of the soil2. N2O can be emitted as a by-produce of both incomplete nitrification and incomplete denitrification. Under anaerobic conditions, N is primarily conserved in organic compounds, and nitrification (the conversion of ammonium (NH4+) to NO3−) is limited to the rooting zone or is absent. The normally low availability of NO3− also restricts rates of denitrification (the conversion of NO3− to N2) in anaerobic soil; if sufficient NO3− is present but oxygen remains restricted, denitrification may go to completion, producing atmospheric N23,4,5,6. Reduction of soil moisture promotes mineralisation of organic N to NH4+, which can be nitrified to NO3−7,8, and produces the partially-oxidised conditions that are conducive to incomplete denitrification, a major source of N2O9. N2O emission has been both positively and negatively correlated with soil moisture, as water-filled pore space (WFPS) or volumetric water content (VWC)10,11,12,13,14,15,16,17,18,19,20,21,22,23,24,25,26 depending upon water status: intermediate levels of around 50–80% WFPS or VWC appear to be optimal for N2O production26,27,28,29,30,31,32,33,34,35,36.
Increases in soil temperature normally enhance N2O production37 up to about 24 °C, where bacterial denitrification reaches an optimum38,39, above which N2O efflux drops. However, denitrifier communities may adapt to higher temperatures, leading to further increases in N2O emissions40. A review of laboratory and field studies shows inconsistent relationships between temperature and N2O emissions13,21,41 from strongly positive to negative, illustrating that temperature alone cannot explain N2O fluxes but must be considered in the context of other drivers, especially soil moisture. At near-zero soil temperatures, the freeze-thaw effect may produce significant amounts of N2O42,43,44,45.
As growing population pressure has increased the extent of fertilised and drained organic soil, nitrogen-rich organic soils will become increasingly important global N2O sources2,46. Currently N2O contributes 12% of CO2-equivalent GHG emissions from land use in tropics47. Quantifying the influence of both increasing rates of land drainage and climate change on organic soil N2O fluxes is thus critically important2. However, emission factors used to assess N2O fluxes from different land uses and ecosystems are usually simple proportions of the application rate of fertiliser (or atmospheric reactive N deposition for non-cultivated soils) and broad land-use categories; these models also do not take into account climate-related changes48. Thus we lack an inclusive model to quantify the potential of organic soils to be a globally important source of N2O2,49. To address this challenge we undertook a standardised global survey of in situ N2O fluxes from organic soils, together with ancillary measurements of key drivers, to derive a model of N2O emissions that would be applicable to a wide range of biomes and environmental conditions. We find that N2O emission from organic soils increases with rising soil NO3−, follows a bell-shaped distribution with soil moisture, and increases with rising soil temperature. This emphasises the importance of warm drained fertile soils to climate change.
Principal component analysis
Site-mean N2O fluxes by study region superimposed on a global organic-soil map are shown in Fig. 1. The principal component analysis (PCA) differentiated tropical sites from temperate and boreal ones, and low agricultural-intensity sites (index 0 and 1) from arable sites (index 3) (p < 0.05; Fig. 2a, b). Soil NO3− was positively related to N2O emission; VWC and water table were strongly negatively correlated with N2O emissions, and C/N, C, and organic matter were less strongly negatively correlated with N2O emissions, and soil temperature was positively related to N2O emissions (Fig. 2c). Soil-available P was orthogonal to the N2O-flux vectors, indicating no correlation. The difference between N2O emissions from drained and natural sites was clear in all three major climate types (Supplementary Table 1).
Of the 18 parameters assessed (Supplementary Data 1), soil NO3− was the strongest predictor of site-mean N2O, explaining 60% of the variation in log N2O flux (Fig. 3a). The generalised additive model (GAM) trend was similar to concave log-log quadratic. Inclusion of site-mean VWC (Fig. 3b) raised the explanatory power of the multiple-regression GAM to 72% (n = 58; R2 = 0.72; p < 0.001; Eq. (1); Fig. 4a). The regression surface was similar to a convex paraboloid with an apex at approximately 50% VWC:
In an independent comparison of the model with published data, relative N2O emissions were represented well. The relationship between the mean N2O fluxes (relative to the maximum value in the respective external data set) and VWC was best described by a bell-shaped GAM regression curve (R2 = 0.78; p < 0.001; Fig. 5) similar to the VWC component of our global model (Fig. 3b). Both curves peaked at around 50% soil moisture.
Both our model and the literature support the idea that fluctuation around the intermediate VWC (~0.5 m3 m−3) creates variability in the oxygen content within the soil profile. That, in turn, stimulates mineralisation and nitrification which contribute to higher NO3− content895051. Intermediate VWC also promotes incomplete denitrification, in agreement with early conceptualisations25,40, previous regional-scale studies28,33,34,35 and experiments9,51,52. The maximum N2O emission at the intermediate VWC means that both wetting from lower moisture values and drying from higher moisture will increase N2O emissions. At a VWC of ~0.8 m3 m−3, oxygen concentration in the pore water is 5–9% of saturation, which is low enough to trigger N2O production but insufficient for complete denitrification9,51,52.
There was no significant relationship between N2O flux and NH4-N among our observations (p = 0.79), suggesting that denitrification was probably the main source of N2O emissions rather than nitrification. Only one site (Tasmania drained fen 2) directly received mineral fertiliser, whereas the nitrate in the other 57 sites originated from livestock and natural sources such as nitrification, atmospheric deposition, runoff and groundwater. Thus our global model describes N2O emission due to grazing and naturally transported nitrate.
We found only a weak relationship between N2O fluxes and soil temperature (40cm-depth temperature log GAM R2 = 0.21, p < 0.001; Fig. 3c). The soil temperatures normalised to local annual air-temperature maxima gave even lower correlation values (e.g. with temperature at 40 cm-depth log GAM R2 = 0.09, p = 0.018). This may have been partially due to the short time span of our measurements per site. However, that is consistent with the meta-analysis of published data in eleven papers showing no correlation between long-term N2O fluxes and soil temperature17,24,31,32,34,53,54,55,56,57,58. The test for an upper boundary59 in our temperature data was negative (p > 0.05). Therefore we accepted the H0 hypothesis that our data are from a bivariate normal process and so the envelope of the data points does not represent a boundary. This also suggests that the high N2O fluxes were measured in soils where temperature was not the limiting factor. A multiple-regression GAM model containing soil temperature at 40 cm depth and log NO3− explained 69% of log N2O fluxes (n = 58; R2 = 0.69; p < 0.001; Eq. (2); Fig. 4b):
Within our drained sites (Supplementary Data 1; n = 27) the temperature relationship was somewhat stronger (R2 = 0.27; p < 0.0078; Fig. 3c). This shows that organic soils exposed to warmer conditions, such as in the tropics, can act as N2O-emission hotspots where soil moisture is optimal (Fig. 3b) and NO3− is above a threshold of 5 mg N kg−1 (Fig. 3a).
Because we sampled each site for only a few days and that we visited temperate and boreal sites during the growing seasons this study was not designed to detect the effect of seasonal or synoptic-scale variation of temperature, soil nitrate, and other factors within each site. Thus our global models are only applicable to estimate daily N2O emissions based on instantaneous environmental conditions at organic-soil sites. Annual-average N2O emissions at sites under a seasonal climate may be more difficult to draw from our model. Yet the model could be useful to estimate N2O emissions at sites under a lack of seasonal variation in environmental conditions such as the humid tropical climate. Upscaling our three tropical sites with intensive land use (the Malaysian oil palm plantation, and the Myanmar and Uganda arable sites; Supplementary Data 1) to a year’s duration and comparing them with the special default emission values (EF2) in IPCC Guidelines 2006 for tropical organic soils60 (16 kg N2O-N ha−1 y−1, range 5–48 kg ha−1 y−1) gave us the following results. For the Malaysian site, soil temperature was 27–30 °C, the mean emission rate was 294.3 μg N2O-N m−2 h−1 = 25.8 kg N2O-N ha−1 y−1. For Myanmar, 14–19 °C (upland), the figures were 125.5 μg N2O-N m−2 h−1 = 11.0 kg N2O-N ha−1 y−1. For Uganda, 17–20 °C (upland), the figures were 507.3 μg N2O-N m−2 h−1 = 44.5 kg ha−1 y−1. Thus the annual fluxes obtained by this simple upscaling all fell within the IPCC tropical default range.
Other potential drivers
The logarithm of C:N ratio, a common scalar explanatory variable used to predict N2O emissions61, was correlated with N2O emissions (R2 = 0.16; p = 0.001; Supplementary Fig. 1) but was not significant in a model that contained NO3−. Agricultural intensity explained 25% of the variability in N2O fluxes (log GAM R2 = 0.25; p < 0.001), but again was not significant in a model containing NO3− and VWC as proximal controllers of N2O emission. The effect of agriculture on N2O emissions was mainly related to cultivation (Fig. 2b). We could detect no significant difference between N2O emissions from agriculturally unused sites and pastures or hay fields. Thus non-agricultural sources of elevated N (e.g. from chronically elevated atmospheric N deposition), and lower soil water content (e.g. reductions in precipitation) would likely have a similar impact on N2O emissions as agricultural fertilisation and drainage.
This is the first time that simple, robust global models of N2O emissions driven by nitrate, moisture and temperature of organic soils have been identified. It is notable that the models encompass temperate, continental, and tropical biomes. Our findings provide more accurate models of the drivers of N2O emissions from organic soils across a wide range of biomes and management regimes than heretofore developed. This highlights the importance of soil nitrate, moisture, and temperature in organic soils as significant global contributors to climate change and stratospheric ozone depletion. Our global-scale models show that constantly high soil moisture results in low N2O emissions, whereas drainage creates fluctuation around the intermediate soil moisture and thus increases N2O emissions from organic soils. The temperature effect on N2O emissions emphasises the importance of considering the warm fertile soils in the global N2O budget. The implication of this work is that wetland conservation should be a priority for climate change mitigation, particularly given the evidence for future increases in the magnitude and frequency of summer droughts60. The anticipated large N2O emissions from N-rich drained organic soils can be mitigated through wetland conservation and restoration, and through appropriate soil management, such as reduced tillage, nutrient management and improved crop rotations46. These have been implemented to some extent in developed countries but need to be further expanded and extended, as a matter of urgency, to tropical and sub-tropical regions.
Our global soil- and gas-sampling campaign was conducted during the vegetation periods between August 2011 and March 2017, following a standard protocol. We sampled 58 organic-soil sites using criteria for organic soils (>12% soil carbon content in the upper 0.1 m) adapted from the FAO World Reference Base for Soils62 in 23 regions throughout the A (rainy tropical), C (temperate), and D (boreal) climates of the Köppen classification (Fig. 1; Supplementary Data 1). Both natural and artificially drained sites were identified, based on the proximity of drainage ditches, water table height, and characteristic vegetation. The hydrology and trophic status of the natural sites ranged from groundwater-fed swamps and fens to ombrotrophic peat bogs. We measured the most important environmental drivers that were possible.
Field and laboratory measurements
Within each region, we established sites to capture the full range of environmental conditions as described above. The depth of the topsoil organic horizon ranged from 0.1 to 6 m across the sites. Land use ranged from natural mire and swamp forest to managed grassland and arable land. A four-grade agricultural-intensity index was used to quantify the effect of land conversion: 0—no agricultural land use (natural mire, swamp, or bog forest), 1—moderate grazing or mowing (once a year or less), 2—intensive grazing or mowing (more than once a year), and 3—arable land (directly fertilised or unfertilised). The agricultural intensity index was estimated based on observation and contacts with site managers and local researchers.
At each site, 1 to 4 stations were established 15–500 m apart to maximise the environmental variance. Each station was instrumented with 3–5 white opaque PVC 65 L truncated conical chambers 1.5–5 m apart and a 1-m-deep observation well (a 50-mm-diametre perforated PP-HT pipe wrapped in geotextile). The total number of chambers was 444. N2O fluxes were measured using the static chamber method63 using PVC collars of 0.5 m diameter and 0.1 m depth installed in the soil. A stabilisation period of 3–12 h was allowed before gas sampling to reduce the disturbance effect on fluxes from inserting the collars. The chambers were placed into water-filled rings on top of the collars. Gas was sampled from the chamber headspace into a 50 mL glass vial every 20 min during a 1-h session. The vials had been evacuated in the laboratory 2–6 days before the sampling. At least three sampling sessions per location were conducted over 3 days. The gas samples were brought to the University of Tartu and analysed for N2O concentration within 2 weeks using two Shimadzu GC-2014 gas chromatographs equipped with ECD, TCD, and Loftfield-type autosamplers63. N2O fluxes were determined on the basis of linear regressions obtained from consecutive N2O concentrations in three to five samples taken when the chamber was closed, resulting in 61 negative and 502 positive N2O fluxes (p < 0.05 for the goodness of fit to linear regression). There were 982 additional insignificant fluxes (p > 0.05) below the gas-chromatography measuring accuracy (regression change of N2O concentration, δv, <10 ppb) reported as zero in the database and included in the analyses.
Water-table height was recorded daily from the observation wells during the gas sampling at least 8 h after placement. Soil temperature was measured at 10, 20, 30, and 40 cm depth. Soil samples of 150–200 g were collected from the chambers at 0–10 cm depth after the final gas sampling. Humification was rated on the von Post scale, 1 to 10 grades from completely undecomposed to completely decomposed peat64. The soil samples were brought to Estonian University of Life Sciences for chemical and physical analyses. During transport, the samples were kept below the ambient soil temperature at which they were collected.
In the laboratory, plant-available phosphorus (P) was determined on a FiaStar5000 flow-injection analyser (KCl extractable). Plant-available potassium (K) was determined from the same solution by the flame-photometric method, and plant-available magnesium (Mg) was determined from a 100-mL NH4-acetate solution with a titanium-yellow reagent on the flow-injection analyser. Available calcium (Ca) was analysed using the same solution by the flame-photometrical method. Soil pH was determined on a 1 N KCl solution65. Soil NH4-N and NO3-N were determined on a 2 M KCl extract of soil by flow-injection analysis65. Total nitrogen and carbon contents of oven-dry samples were determined using a dry-combustion method on a varioMAX CNS elemental analyser. The organic-matter content of oven-dry soil (SOM) was determined by loss on ignition at 360 °C. We determined gravimetric water content (GWC) as the difference between the fresh and oven-dry weight divided by the oven-dry weight66. Bulk density was determined as follows67:
BD is bulk density, g cm−3,
Dbm is the empirically determined bulk density of the mineral fraction (2.65 g cm−3)66,
Dbo is the empirically determined bulk density of the organic fraction (0.035–0.23 g cm−3 according to the von Post humification scale68), and
SOM is the organic content of the oven-dry soil, g g−1.
We determined VWC as66:
VWC is volumetric water content, m3 m−3,
GWC is gravimetric water content, Mg Mg−1, and
BD is bulk density, Mg m−3.
For normalising the soil temperature to possible local optima we divided our soil-temperature measurements with the mean air temperature at the nearest weather station in the warmest month of the year69 (KNMI Climate Explorer http://climexp.knmi.nl; Supplementary Data 1).
Principal component analysis (PCA), Spearman’s rank correlation and stepwise multiple regression of site-mean efflux vs. the environmental parameters were used. The tests were run using both untransformed and log-transformed N2O fluxes. Before the log-transformation, a constant value was added to all fluxes to account for negative values. Normality of the variables and the residuals was checked by the Shapiro–Wilk test. Neither the N2O fluxes nor their logarithms were normally distributed (p < 0.05); this is a commonly reported issue with N2O. Therefore only a nonparametric test such as Spearman’s rank correlation and generalised additive models (GAM) could be applied. We used the mgcv package of the R Project to calculate the GAM regressions using minimal smoothness (k = 3). We reported p-values (significance level p < 0.05) from the summaries of the GAM regressions produced by the summary.gam package of the R Project. We only reported GAM regressions when the residuals were normally distributed. As a presumption for the stepwise multiple regression, the independent variables were checked for GAM concurvity—we only reported multiple relationships with a variance inflation factor <10 between the independent variables. We tested the presence of a boundary in our data59. The test compared the density of points in the region of the data set’s upper envelope to the expected density of the upper envelope of a bivariate normally distributed data set of the same size59.
In order to compare our model with independent external data, we surveyed literature referenced in the Thomson Reuters Web of Science. The search terms were: N2O and organic soil and nitrous oxide and organic soil. We only included publications that reported time series of at least a year’s duration that reported N2O fluxes and simultaneous soil temperature and soil moisture observations (either VWC or WFPS). Eleven papers17,24,31,32,34,53,54,55,56,57,58 qualified under these criteria. The study sites were fairly evenly distributed throughout major organic soil regions of the world. Only three of these papers reported soil NO3− concentrations17,24,58. We converted the WFPS values to VWC as follows66:
VWC is volumetric water content, m3 water m−3 fresh soil,
WFPS is water-filled porosity, m3 water m−3 pore space, and
TP is total porosity, m3 pore space m−3 soil.
To standardise the highly different absolute N2O values among data sets we normalised them by scaling to the maximum value measured at each site70. We calculated average relative N2O fluxes in 15 soil temperature classes: 0 °C to 2 °C, 2 °C to 4 °C, … and 28 °C to 30 °C, and 10 soil moisture classes: 0% to 10%, 10% to 20%,… and 90% to 100%. Linear and GAM regressions with minimal smoothness (k = 3) were determined between soil temperature, soil moisture and both the individual and average relative N2O fluxes.
The data reported in this paper are deposited in the PANGAEA repository https://doi.pangaea.de/10.1594/PANGAEA.885897.
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This study was supported by the Ministry of Education and Science of Estonia (the SF0180127s08 grant), the Estonian Research Council (the IUT2-16, IUT2-17 and PUTJD619 grants); and the EU through the European Regional Development Fund (ENVIRON and EcolChange Centres of Excellence, Estonia), the 7th Framework People programme (the PIRSES-GA-2009-269227 grant), the European Social Fund (Doctoral School of Earth Sciences and Ecology, Estonia), the IAEA’s Coordinated Research Project D12010, and Labex VOLTAIRE (ANR-10-LABX-100-01). We are sincerely grateful to the assistance of Dr. I. Filippov, G. Gabiri, Dr. J. B. Gallagher, I. Gheorghe, Dr. W. Hartman, Dr. R. Iturraspe, C.K. Luswata, S. Mander, Dr. M. Metspalu, R. Moreton, Dr. H. Óskarsson, Dr. J. Paal, Dr. E.S.-O. Parrodi, Dr. S. Pellerin, Dr. S. Pihu, K. Raudsepp, Dr. F. Sabater, D. Silveira Batista, and Dr. E. Uuemaa in study-site selection and field investigation. Our work benefitted from technical assistance from Dr. C. Vohla, discussions with Dr. T. Leppelt and Dr. A. Kanal, and a pre-review by Prof. U. Skiba. Dr. T. Ligi, Dr. M. Metspalu, K. Oopkaup and Dr. M. Truu contributed to the perspective microbiological study.
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