One of the characteristics of global climate change is the increase in extreme climate events, e.g., droughts and floods. Forest adaptation strategies to extreme climate events are the key to predict ecosystem responses to global change. Severe floods alter the hydrological regime of an ecosystem which influences biochemical processes that control greenhouse gas fluxes. We conducted a flooding experiment in a mature grey alder (Alnus incana (L.) Moench) forest to understand flux dynamics in the soil-tree-atmosphere continuum related to ecosystem N2O and CH4 turn-over. The gas exchange was determined at adjacent soil-tree-pairs: stem fluxes were measured in vertical profiles using manual static chambers and gas chromatography; soil fluxes were measured with automated chambers connected to a gas analyser. The tree stems and soil surface were net sources of N2O and CH4 during the flooding. Contrary to N2O, the increase in CH4 fluxes delayed in response to flooding. Stem N2O fluxes were lower although stem CH4 emissions were significantly higher than from soil after the flooding. Stem fluxes decreased with stem height. Our flooding experiment indicated soil water and nitrogen content as the main controlling factors of stem and soil N2O fluxes. The stems contributed up to 88% of CH4 emissions to the stem-soil continuum during the investigated period but soil N2O fluxes dominated (up to 16 times the stem fluxes) during all periods. Conclusively, stem fluxes of CH4 and N2O are essential elements in forest carbon and nitrogen cycles and must be included in relevant models.
Greenhouse gases (GHG), in particular, methane (CH4) and nitrous oxide (N2O) contribute 16% and 6% to global warming, respectively1. In addition, N2O is a dangerous stratospheric O3 layer depleting agent2. Due to the increasing emissions, both gases have high radiative forcing potential. In principle, terrestrial biosphere may be seen as a net source of GHG to the atmosphere3. Temperate as well as tropical forest soils (in general) seem to be a central natural emitting source of N2O, on the one hand, a natural sink of CH4 on the other4,5,6,7,8,9. Flux estimations of N2O and CH4 in forest systems are mainly based on studies of forest soil measurements, usually excluding exchange potential of vegetation5,7,10. Nevertheless, investigations on GHG fluxes from plants in wetland or riparian ecosystems show that plants, especially trees, can be essential sources of CH4 and N2O9,11,12,13. However, recent studies uncover the relevance of tree stem surfaces playing an important role in understanding GHG dynamics in different forest ecosystems8,9,14.
Grey alder (Alnus incana (L.) Moench)) is a fast-growing, pioneer tree species with excellent potential for short-rotation forestry in the Northern hemisphere15,16,17,18. Due to the symbiotic Frankia bacteria which fix atmospheric nitrogen, alder forests are important nitrogen sequestering ecosystems19,20. Decomposition of nutrient-rich alder litter improves soil properties, in particular, the carbon:nitrogen (C:N) ratio21,22,23,24, which alters the microbial activity in the soil and affects the production and consumption of CH4 and N2O in the soil25.
CH4 is produced under anaerobic conditions in a water-saturated environment by methanogenic archaea and can be oxidised by aerobic or anaerobic methanotrophs. N2O, on the other hand, is a natural product of several N turnover processes (e.g. nitrification, denitrification)10,26. Even if both gases release into the atmosphere by gas diffusion at the soil surface, trees may contribute to ecosystem GHG exchange by i) gas uptake from soil via their root system, transport into the aboveground tree tissues and emission into the atmosphere; ii) uptake of CH4 and N2O from the atmosphere, or iii) alternation of gas turnover processes in adjacent soils12,27,28.
In reaction to stressing factors, for instance, a natural or even artificial creation of anaerobic soil conditions due to flooding events, biosynthetic processes like production and consumption of CH4 and N2O and their respective transportation may become modified and, thus, may lead to a change of the potential trace gas emissions29,30,31. Importantly, plant species react differently, depending on their anatomical and physiological predisposition/adaptation to stresses, soil characteristics32, seasonal effects, temperature33, and intensity of the stressing event in general26.
Nevertheless, field experiments, investigating CH4 and N2O fluxes in riparian tree communities exposed to environmental stress are scarce. Thus, a large-scale forest manipulation experiment was conducted in a grey alder forest in summer 2017. The main objective of the FluxGAF (“Biogeochemical Fluxes in Grey Alder Forest”) campaign was to investigate the response of the forest ecosystem to heavy overland flow. The objective was to understand the biochemical process and flux dynamics in the soil-tree-atmosphere continuum related to ecosystem CH4 and N2O turnover and exchange. Therefore, we quantified CH4 and N2O fluxes from stems of grey alder and adjacent soil in response to an artificial flooding event. The trace gas fluxes were measured on mature trees in an alder forest in Estonia together with forest floor CH4 and N2O fluxes, and a variety of environmental parameters (including (micro)meteorological, soil and atmospheric parameters). The study site consisted of two plots: a flooded plot (FP), where 55–70 m³ of water per day was applied for two weeks in summer 2017, and a control plot (CP). The study period was divided into three periods: pre-experimental (July 24th–August 7th), experimental (mimicking flooding; August 8th–21st) and post-experimental (August 22nd–September 4th).
We hypothesize that: (1) due to the flooding, emission of methane and nitrous oxide from both the soil and tree stems will increase while the lower parts of stems will have higher emission, (2) flooding will change the proportion of soil and stem fluxes in overall emissions while the dynamics are different for CH4 and N2O.
Soil physicochemical conditions and characteristics of the tree stand
The study period was characterised by mean air temperature (mean ± standard deviation) of 19.9 ± 2.1 °C, and soil temperature at a soil depth of 5 cm at the flooded and control plot, 15.1 ± 0.6 and 15.3 ± 0.6 °C, respectively (Fig. 1a). No significant differences were detected in Soil Water Content (SWC) between flooded and control plots in the pre-experimental period, although SWC was significantly higher in the flooded plot during the experimental (p < 0.001) and post-experimental periods (p < 0.05) (Fig. 1b and Supplementary Table S1). Single rain incidents occurred and one at the beginning of post-experimental period also increased SWC in the control plot (Fig. 1a). These trends were also reflected in the water table (Supplementary Fig. S1).
Tree stand density was approximately 1500 trees per hectare and tree height was 19.2 ± 1.4 m in both studied plots. In addition, tree diameter at 1.3 m height showed no significant difference between FP and CP and was approximately 0.17 ± 0.03 m on both sites.
Experimental (FP_Flooding) and post-experimental (FP_Post) periods of the flooded plot were clearly distinct from pre-experimental period of the flooded plot and all periods of the control plot (p < 0.05; Fig. 2). Pre-experimental period of the flooded plot (FP_Pre) was different from the experimental period of the control plot (CP_Flooding; p < 0.05). The flooded plot was characterised by higher NH4 + levels during the experimental (p < 0.001) and post-experimental period (p < 0.05), and lowered NO3 − values during the experimental period (p < 0.001, Supplementary Fig. S2). pH, phosphorous (P), nitrogen (N), organic matter and soil temperature values showed no significant differences between the two plots in different periods. Soil bulk density varied between 0.77 and 0.96 and was not significantly different between studied plots.
Fluxes of CH4 and N2O and their relation to environmental factors
Different patterns emerged for CH4 and N2O emissions in the studied plots and their periods (Fig. 2). No significant differences were detected in CH4 emissions from soil and 170 cm stem level between flooded and control plots in the pre-experimental period, although CH4 emissions were significantly higher from soil and all stem levels in the flooded plot during the experiment (p < 0.05 for soil, p < 0.001 for all stem levels) (Supplementary Table S1). Moreover, CH4 emissions were significantly higher from the soil and stems at 10, 80 and 170 cm level in the flooded plot compared to the control plot during the post-experimental period (p < 0.001 in all cases).
N2O emissions from the soil and different stem heights showed more controversial results (Supplementary Table S1). Very few significant differences in N2O emission appeared between flooded and control plots before and during the experiment. However, N2O emissions from all stem heights were significantly lower in the flooded plot compared to the control plot during the post-experimental period (p < 0.001 in all cases).
Soil NO3− was positively and NH4+ was negatively related to N2O emissions from soil and different stem heights (Fig. 2). In addition, soil moisture was negatively related to N2O emissions, whereas it showed positive relationships to CH4 emissions from both the soil and stems. Soil temperature, pH, P, N, and organic matter were almost perpendicular to the CH4 and N2O flux vectors, indicating little or no correlations.
Both soil and stem surfaces were net emitters of CH4 and N2O (Figs. 3 and 4). At the flooded plot, we observed an increase (p < 0.05) of stem CH4 fluxes at 10 cm from the pre- to the post-experimental period (Fig. 3a). A significant decline (p < 0.05) along the overall vertical stem profile was found during and after the experiment. On the control plot, there was significant difference at the 10 cm level before and after the experimental period only (Fig. 3b).
At the flooded plot, N2O fluxes from the 10 and 80 cm level of stems increased significantly with the flooding experiment and declined afterwards (p < 0.001). Fluxes from the 170 cm level decreased significantly during the post-flooding period only (p < 0.001). The N2O fluxes showed a diminishing trend with tree height (Fig. 3c).
At the 10 cm level in the control plot, we observed tendentially higher N2O fluxes without a general decrease with increasing stem height (p > 0.1). Nevertheless, the intensive rain forced occasional peaks with significant effect at the post-experimental period (Fig. 3d).
The soil CH4 fluxes increased significantly (p < 0.001) from light consumption (−0.2 ± 1.7 µg m−2 h−1, mean ± std. err.) before the experimental to 12.8 ± 2.1 µg m−2 h−1 at the post period (Fig. 4a). N2O fluxes from soil did not differ significantly (p > 0.2) either between the periods nor plots (Fig. 4b).
Cumulative values of mean flux for each sampled day (Fig. 5) clearly demonstrate the flooding-induced dominance of CH4 fluxes from tree stems over soil emissions: the difference is up to 400 times. Furthermore, the vertical decrease in both CH4 and N2O emissions along the stem profile was remarkably enhanced by the flood. Methane fluxes from the soil, on the other hand, weighed in after the experiment.
Cumulative N2O fluxes responded positively to the artificial flooding and remained almost stable afterwards. The soils showed almost linear rise in cumulative emissions.
The relative contribution of the stems and soil to the CH4 and N2O fluxes
Stem fluxes were upscaled to unit of ground area of forest and compared with related soil fluxes (Fig. 6). At the flooded plot, CH4 emissions from tree stems dominated 7 times more with up to 88% contribution but small uptake rates from soil surfaces balanced with stem emissions at the control area (Fig. 6a,b).
Stems and soils were N2O emitters while no consumption was observed. Soil dominated N2O flux ratio on both plots with up to 99%, accordingly up to 145 times more. However, stem fluxes contributed 12% at the control plot’s post-experimental period (Fig. 6c,d).
The relevance of the experimental set-up
The choice of the experimental area depended on many environmental factors. One of them was a slight slope which allowed slow movement of the added water and, most importantly, did not influence groundwater level and quality on the adjacent control plot (Supplementary Fig. S4). The impact of the slope and a 1 m high dyke, which separated the flooded and control plots, can be seen in the similar characteristics of FP and CP during the pre-experimental period (Supplementary Table S1, Figs. 4 and 5).
Main controllers of CH4 and N2O fluxes
Methane is produced in anoxic soils and sediments, while well-drained soils act as a sink for atmospheric CH4 due to methane oxidation, both processes are controlled by different microorganisms. The main environmental factors controlling the CH4 emission in soils are the availability and quality of carbon, soil temperature and water content34. Since in our study area, the carbon content of the soil is not a limiting factor (Fig. 2), soil water content (water table) and temperature determine the most variation of CH4 fluxes in soil and stems (Fig. 2, Supplementary Table S1).
N2O is produced in the soil mainly via nitrification under aerobic conditions, where ammonia is oxidised, and by denitrification, which occurs under anaerobic conditions, where nitrate is sequentially reduced to nitrite, N2O and pure molecular nitrogen (N2)35. The gaseous nitrogen losses directly depend on soil nitrate content and soil moisture which affects oxygen availability in the soil36. Soils at a water content of 0.5–0.6 m3 m–3 emit the largest amounts of N2O36. This soil water content indicates the commonly known condition where both nitrification and denitrification contribute N2O37,38.
Under laboratory conditions, Unger et al.31 showed that alternating oxic/suboxic and anaerobic conditions, which are similar to our field study soil moisture, can coherently change NH4+ and NO3– concentrations. Also, under laboratory conditions, Klemedtsson et al.39 showed the relationships between soil moisture and N2O production during nitrification and denitrification. Nevertheless, variation in N2O concentrations does not stringently correlate to variation of denitrifying activity. N2O can be produced by a range of organisms, further, denitrifiers such as bacteria or archaea may both produce and consume N2O. Nitrate may limit denitrification in forest ecosystems40. In our study, a decline of nitrate was coherent with the increase of ammonia in the soil (Supplementary Fig. S2).
In conclusion, the flash flooding significantly enhanced both nitrification and denitrification processes in the soil. N2O could be produced from both processes. Further, flooding can accelerate production of both CH4 and N2O that may lead to increased emissions from forest ecosystems.
Comparison of results with outcomes from similar studies
Although our full-size flooding experiment during a reliable timeframe is the first attempt to measure both CH4 and N2O emissions from soil and tree stems simultaneously, there are analogous experiments conducted in laboratory conditions and/or in mesocosms. Rusch and Rennenberg11 considered an increase of N2O emissions from 3 years old black alder seedlings immediately after flooding had started but no effect on CH4 emissions but vice versa results after 40 days, in particular, N2O fluxes were below the detection limit, but CH4 increased enormously. Further, they found the efflux decrease with stem height from 0 to 2 m. On the other hand, Keppler et al.41 concluded after greenhouse experiments that even plants may produce CH4 in situ, covering 10–30% of the world’s total CH4 emissions. However, Terazawa et al.,42 concluded soil temperature and water table depth as possible environmental factors controlling stem CH4 emissions”. Mander et al.43, for instance, investigated the impact of flooding, using a pulsing groundwater level on GHG fluxes from the soil and found an increase of CH4 emissions but a decrease of N2O emissions after flooding. However, our field experiment on flooding the Alnus incana forest indicated a “chimney effect” similar to Rice et al.44, i.e. soil microbes produce CH4 which is transported via roots, stems, and leaves to be released to the atmosphere. Comparing to a mesocosm experiment with Alnus glutinosa seedlings under laboratory conditions conducted by Machacova et al.12 we found an increase of flooding-induced N2O stem emissions of up to 10 times (instead of a factor of 740 by Machacova et al.) but CH4 emissions in our experiment were up to 100 times higher. To compare with other studies, our flooding-induced CH4 emissions from alder stems were significantly higher, especially when comparing them with the soil fluxes. Pitz et al.45 measured methane fluxes from tree stems and soils along a habitat gradient and found mean stem CH4 emissions of 68.8 ± 13.0 (mean ± standard error), 180.7 ± 55.2 and 567.9 ± 174.5 g CH4-C m−2 h−1 for the upland, transitional and wetland habitats, respectively. In the same time, mean soil methane fluxes in the upland, transitional and wetland were −64.8 ± 6.2, 7.4 ± 25.0 and 190.0 ± 123.0 g CH4-C m−2 h−1, respectively.
Fluxes from other tree compartments can have an effect on CH4 and N2O balances. Machacova et al.46 show that mature Scots pine trees consistently emit CH4 and N2O from both stems and shoots. The shoot fluxes of CH4 and N2O exceeded the stem flux rates by 41 and 16 times, respectively. Therefore, further investigations at canopy level are very important.
Likewise, full-year investigations of gas emissions might change the results. For instance, Machacova et al.47 found a clear N2O emission peak from stems of boreal trees during the vegetation season/summer while there was no effect of soil water content on tree N2O fluxes in the vegetation season.
In future climate, the frequency of both flash floods and drought events is expected to be increased48,49,50,51. Although trees and other plants indicate the “forest ecosystem”, their role within gas cycles is somehow underestimated12. Therefore, understanding the capacity of ecosystems to adapt to such environmental modifications is the key to predict ecosystem responses to global change52.
Our experimental flooding induced changes of water regime and consequent dynamics of CH4 and N2O pathways: emission of these gases from both soil and tree stem increased significantly. Thus, our first hypothesis has been supported. As well, the lower parts of stems showed higher emission compared with the higher positions. Likewise, the second hypothesis could be supported: we saw that flooding changed the proportion of soil and stem fluxes in overall emissions showing significantly different patterns for CH4 and N2O. Methane fluxes from tree stems were observed up to 100 times higher than related fluxes from soil chambers. In contradiction, nitrous oxide fluxes from the soil surface were up to 16 times higher than stem N2O fluxes close to the ground at the post-experimental period. Furthermore, the stems contributed up to 88% of CH4 emissions to the stem-soil continuum during the investigated period but soil fluxes dominated the N2O contribution during all periods when upscaling for forest area unit. A substantial link was shown between N2O fluxes from the stems and soil with soil water content and nitrogen availability as the main controlling factors.
Our results convince us that the N2O and CH4 exchange of riparian trees should be included in forest ecosystem GHGs budgets and forest-ecosystem process models. In addition, extreme climate events (flooding, drought) are significantly altering not only the soil fluxes, but also the stem fluxes. However, emission from tree stems of different species may vary significantly and further studies are needed for comprehensive flux estimates for different forest types.
Material and Methods
Site description and experimental design
The measurements were performed at the experimental site of Agali (58°17′N; 27°17′E) situated in eastern Estonia, 10 km west of Lake Peipus. The studied forest is a 40-year old hemiboreal Filipendula type grey alder (Alnus incana (L.) Moench) forest stand in a former agricultural Gleysol.
The artificial flooding was conducted in summer 2017 and was divided into three periods: a pre-experimental (July 24th–August 07th), experimental (August 8th–21st), and a post-experimental (August 22nd–September 4th) period. Within the forest, two experimental plots were established, a flooded plot (FP, 40 × 40 m), where water was pumped into using an irrigation pipe system mimicking the intensive-rain induced overland flow, and a control plot (CP, 20 × 20 m). The plots were separated by a 1 m high natural dyke preventing the spread of water into the control plot. Slight slope (1%) parallel to the dyke guaranteed isolated groundwater dynamics in the plots (Supplementary Fig. S4). Every experiment day, 55 to 70 m3 of pond water (pH 7.41, total C 76 mg/l, total N 1.8 mg/l, NH4+-N 0.79 mg/l, NO3−-N 32.6 µg/l) was applied to the FP by a fire truck. The total water amount of 875 m3 was distributed over 1,600 m² forest area, which is an equivalent to 547 mm precipitation. The long-term average annual precipitation of the region is 650 mm, and the average temperature is 17.0 °C in July and −6.7 °C in January. The duration of the growing season is typically 175–180 days from mid-April to October53.
Nine representative mature grey alder trees were selected for stem flux measurements at the FP, four at the CP (Supplementary Fig. S4). Soil fluxes were investigated close to each selected tree. The dominating ground vegetation at both plots was Alnus incana ((L.) Moench), Filipendula ulmaria ((L.) Maxim.), Prunus padus (L.), and Rubus idaeus (L.).
Stem flux measurements
The tree fluxes were measured manually: five measurement sets in the pre-, six in the experimental and four in the post-experimental period. The representative trees were equipped with static closed tree stem chamber systems for stem flux measurements28. The chambers were installed at the bottom part of the tree (approximately 10 cm above the soil). In addition, a vertical profile of the stem fluxes (measurements at three stem heights of approximately 10, 80 and 170 cm above the ground) was studied in 6 and 2 trees at the FP and CP, respectively. The chambers were installed in June 2017 one month prior to the campaign. The rectangular shape stem chambers were made of transparent plastic containers, including removable airtight lids (Lock & Lock, South Korea). The bottom was cut and hot-glued with a neoprene band. The chambers were sealed with non-acid silicone to the smoothed stem surface and tested for airtightness. Two chambers per profile were set randomly across 180° and interconnected with tubes into one system (total volume of 0.00119 m³) covering 0.0108 m² of stem surface. A pump (Thomas, Germany, model 1410VD, 12 V) was used to homogenize the gas concentration prior to sampling. Chamber systems remained open between each sampling campaign. During 15 measurement campaigns, four gas samples (25 ml) were collected from each chamber system via septum in a 60 min interval: 0/60/120/180 min sequence (sampling time between 12:00 and 16:00) and stored in pre-evacuated (0.3 bar) 12 ml coated gas-tight vials (LabCo International, United Kingdom). The gas samples were analysed in the laboratory at University of Tartu within 2 weeks using gas chromatography (GC-2014; Shimadzu, Japan) equipped with an electron capture detector for detection of N2O and a flame ionization detector for CH4. The gas samples were injected automatically using Loftfield autosampler (Loftfield / Germany). For gas-chromatographical settings see Soosaar et al.54.
Fluxes were quantified on a linear approach according to change of CH4 and N2O concentrations in the chamber headspace over time, using the equation according to Livingston and Hutchison55.
Soil flux measurements
Soil fluxes were measured using automatic dynamic chambers located close to each measurement tree and installed in June 2017. Nine chambers were situated at the FP, four at the CP. Every PVC made soil chamber covered a 0.16 m² soil surface, containing a volume of 0.032 m³. To avoid stratification of gas inside of the chamber, air with a constant flow rate 1.8 L/min was circulated within a closed loop between the chamber and gas analyzer unit during the measurements by a diaphragm pump. The air sample was taken from the top of the chamber headspace and pumped back by distributing it to each side of the chamber. For the measurements, the soil chambers were closed automatically for a duration of 9 minutes each. Flushing time of the whole system with ambient air between measurement periods was 1 minute. Thus, there were approximately 12 measurements per chamber per day. A Picarro G2508 (Picarro Inc., United States) gas analyzer using cavity ring-down spectroscopy (CRDS) technology was used to monitor CO2, CH4 and N2O gas concentrations in the frequency of approximately 1.17 measurements per second. The chambers were connected to the gas analyzer using a multiplexer.
The air temperature in the chamber was measured and used to convert the concentrations from ppm[v] to mg m−3 according to the ideal gas law before flux calculation56. Soil fluxes were calculated for a selected time window (150 seconds), after discarding initial 90 seconds to exclude the initial stabilisation period, using the linear model. The linear models is based on the assumption of a linear relationship between concentrations inside the chamber headspace and time. Fluxes were calculated using the equation, according to Livingston and Hutchison55.
To compare the contribution of soil and stems, the stem fluxes were up-scaled to hectare of ground area based on average tree diameter, stem surface area, tree density, and stand basal area estimated for each period and plot. A cylindric shape of tree stem was assumed. To estimate average stem emissions, fitted regression curves for different periods were made between the stem emissions and height of the measurements as previously done by Sjögersten et al.57. The regression model parameters are reported in Supplementary Table S2.
Data quality check
Fluxes were quantified on a linear approach according to change of CO2, CH4 and N2O concentrations in the chamber headspace over time. A data quality control was applied based on R2 values of linear fit for CO2 measurements. When the R2 value for CO2 efflux was above 0.9, the conditions inside the chamber were applicable, and the calculations for both CH4 and N2O gases were also accepted in spite of their R2 values. Calculations with lower R2 value (R2 < 0.9) were removed from the database.
Automatic groundwater level data loggers (Hobo U20L-04, Onset Computer Corporation, USA) were installed in groundwater wells. Soil temperature (107, CAMPBELL SCIENTIFIC. INC, USA) and soil moisture sensors (ML3 ThetaProbe, Delta-T Devices, United Kingdom) were installed at 0–10 cm soil depth close to adjacent tree spots. During five campaigns (two in the pre-experimental period, two in experimental period, and one in post-experimental period) composite topsoil samples with soil corer at depth 0–10 cm were taken for physical and chemical analysis using standard methods58.
Principal Component Analysis (PCA) was performed on real and imputed data sets of soil physicochemical and gas flux measurements using the R package ade4 v. 1.7–1359. For PCA, missing data patterns were identified and explored using the packages “naniar” v. 0.4.260 and “VIM” v. 4.8.061 (Supplementary Table S3). In addition, R package “missMDA” v. 1.1462 was applied to impute missing data values in case of PCA. Differences in PCA between the plots and periods were evaluated using PERMANOVA with 9999 permutations and pairwise comparisons were corrected with Bonferroni method, using the R package vegan v. 2.5-663. To evaluate the significance of the differences between the plots and their periods with respect to physicochemical variables values, multivariate linear models were constructed, and models were tested after 9999 permutations using the anova function in R package mvabund v. 4.0.164. Linear mixed-effects models (LMM) were applied to investigate differences in soil moisture and gas flux measurements between the control and flooded plots using the R method “lmer” incorporating both temporal (sampling days) and spatial (different trees) effects as random effects (v. 1.1–21)65, while p-values were calculated in order to confirm the significance of the relationships using the R package lmerTest v. 3.0-166. The same mixed effects method was used to test statistical significance between different periodic groups of soil and stem fluxes. LMM was also used to detect differences between stem fluxes of different stem heights in different periods. For exploring LMMs fit, inspection of residuals patterns for the model was used as diagnostic tool65,67. To meet the analysis assumptions, rank transformation of the data was performed and LMM on the rank-transformed response variables are analysed and reported68. The regression models for stem heights and stem fluxes of different periods were estimated by nonlinear least squares, using the R function “nls.” R version 3.6.1 (R Development Core Team, 2019) was used to conduct all the statistical analyses. The significance level (alpha) considered for all the tests was 0.05.
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This study was supported by the Ministry of Education and Science of Estonia (SF0180127s08 grant), the Estonian Research Council (IUT2-16, PRG-352, and MOBERC20), the Czech Science Foundation (17-18112Y), the Ministry of Education, Youth and Sports of Czech Republic within the National Sustainability Program I (NPU I), grant number LO1415, the EU through the European Regional Development Fund (ENVIRON and EcolChange Centres of Excellence, Estonia, and MOBTP101 returning researcher grant by the Mobilitas Pluss programme) and the European Social Fund (Doctoral School of Earth Sciences and Ecology).
The authors declare no competing interests.
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Schindler, T., Mander, Ü., Machacova, K. et al. Short-term flooding increases CH4 and N2O emissions from trees in a riparian forest soil-stem continuum. Sci Rep 10, 3204 (2020). https://doi.org/10.1038/s41598-020-60058-7
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