Spring Freeze–Thaw Stimulates Greenhouse Gas Emissions From Agricultural Soil

GRAPHICAL ABSTRACT

GRAPHICAL ABSTRACT

Introduction

In temperate cold regions, spring freeze-thaw events contribute to the production of greenhouse gases, which further exacerbates climate change (Pelster et al., 2013; Natali et al., 2019). Greenhouse gas production during spring freeze-thaw account for 29–73% of the annual N₂O (Hung et al., 2021), 5–50% of the annual CO₂ (Kurganova et al., 2007), and ∼80% of the annual CH₄ (Song et al., 2012). In temperate agroecosystems, greenhouse gas fluxes peak during spring freeze-thaw events due to carbon (C) and reactive nitrogen (N) remaining in the soil from the previous crop season (i.e., legacy C and N) (Wagner-Riddle et al., 2017). Accordingly, amending the soil with organic residues, high in C and N, increases the production and fluxes of greenhouse gases considerably during spring freeze-thaw events (Kariyapperuma et al., 2012; Chantigny et al., 2016). Furthermore, intermittent greenhouse gas fluxes during freeze-thaw events are also related to temporal changes in soil biophysical conditions influenced by snow melting, waterlogging, and gradual warming and drying (Congreves et al., 2018).

Biobased residues are biological wastes that include, but are not limited to, compost (e.g., food waste), biosolids, and anaerobic digestate. Biobased residues are comprised of readily accessible organic C and N, thereby enhancing soil microbial activity and greenhouse gas productions (Thangarajan et al., 2013). Furthermore, organic matter, nutrient concentration, as well as physical characteristics (e.g., composts are solid, biosolids are semi-liquid and anaerobic digestates are liquid) can vary substantially among biobased residue types (Bertora et al., 2008; Grave et al., 2018; Badewa and Oelbermann, 2020). Differences in biobased residue composition also influence the soil C and N dynamics and microbial activity, which regulates greenhouse gas production (Miura et al., 2019; Rosinger et al., 2022).

Since spring freeze-thaw influences the soil’s biophysical conditions, the presence of readily available C and N substrates to the microbial community from biobased residues can cause nitrification, incomplete denitrification or methanogenesis, resulting in the generation of greenhouse gases (Zhu-Barker et al., 2015; Brenzinger et al., 2018). Additionally, temperature fluctuation and moisture variation (waterlogged, wet, and dry) during spring freeze-thaw, where the soil has minimal or no snow cover, causes frequent and intense episodes of freezing and thawing coupled with physical deformation of soil aggregates (Miao et al., 2014; Wu et al., 2017; Wu et al., 2021). Furthermore, substantial soil warming during the thaw phase increases the microbial activity and triggers greenhouse gas emissions (Henry, 2008; Henry, 2013; Chantigny et al., 2019).

Although multiple studies determined the impact of biobased residues on greenhouse gas productions (Thangarajan et al., 2013; Insam et al., 2015; Roman-Perez et al., 2021), our knowledge on the impact of biobased residues on spring freeze-thaw events and resultant greenhouse gas fluxes remains limited. However, knowing the contribution of biobased residues to greenhouse gas fluxes is critical since biological and physicochemical properties, in addition to soil management (e.g., the rate and timing of biobased residue application, soil cultivation) and environmental characteristics (e.g., soil type, weather), vary at the local and regional scale (Dambreville et al., 2008; Eckard et al., 2010; Grave et al., 2018). Although some studies found that freeze-thaw events can cause a shift in soil physical conditions and how biobased residues influence this shift and respond to greenhouse gas production, but they have only been evaluated under laboratory conditions and with inconsistent results (Sahin et al., 2008; Liu et al., 2016; Fu et al., 2019; Pupko, 2019; Hou et al., 2020). Under field conditions, Roman-Perez et al. (2021) found that soil amended with contrasting biosolids types (composted, anaerobic digested, alkaline stabilized) varied in their production of N₂O. Roman-Perez et al. (2021) also found that N₂O fluxes from biobased residues were higher compared to those from urea. Consequently, knowledge on the impact of biobased residues on greenhouse gas production during spring freeze-thaw events in a field setting is warranted (Hung et al., 2021).

The objectives of our study were to quantify and compare greenhouse gas fluxes from soil amended with biobased residues and N fertilizer during the spring freeze-thaw events. We hypothesized that N₂O, CO₂ and CH₄ fluxes from soil amended with biobased residues will be greater compared to soil amended with N fertilizer (urea) during spring freeze-thaw since a greater quantity of C and N are available from the biobased residues than from urea. We also hypothesized that N₂O and CH₄ fluxes will be greater during the waterlogged and wet phase due to denitrification and methanogenesis caused by anaerobioses, whereas the CO₂ flux will be greater during the drying phase due to enhanced microbial activity caused by a rising soil temperature. We also assumed that the CO₂ flux is strongly related to soil temperature throughout the spring freeze-thaw.

Materials and Methods

Site Description and Field Experiment

The field site was located at Elora Research Station (43^o45′N, 80^o21′W), Elora, Ontario, Canada. The mean annual temperature at this site is 6.8°C, with mean annual precipitation of 989 mm and 6 cm snow depth, based on a 16-year data (2004–2019) from the Environment and Climate Change Canada (2021). At this field site, soils undergo spring freeze-thaw from March to April when snow begins to melt. This creates an environment with transitory waterlogging, a partial ice layer, and wet and drying conditions (Supplementary Table S1). Daily ambient temperature fluctuations during the spring cause repeated freeze thaw cycles, and the daily average maximum and minimum temperatures in this site were 6.9 to −3.2°C between March 1 and April 30 from 2004 to 2020 (Environment and Climate Change Canada, 2021). Soil at the site is classified as a grey brown Luvisol, with a silt loam approximately 29% sand, 52% silt and 19% clay. The soil (0–20 cm depth) has 25 g soil organic C kg⁻¹, 2.4 g total N kg⁻¹, and pH of 7.9.

The field experiment was established with four different treatments including urea, compost, biosolid, and digestate and applied in a completely randomized block design. Urea was a commercial granular urea fertilizer that contained 46% N applied at a rate of 170 kg N ha⁻¹. Compost was composted food waste applied at 12 t ha⁻¹ (240 kg N ha⁻¹) (Table 1). Biosolid (LysteGro^®) was hydrolyzed biosolid slurry applied at 28,000 L ha⁻¹ (215 kg N ha⁻¹). Digestate was liquid anaerobic digestate of farm green plant applied at 42,000 L ha⁻¹ (231 kg N ha⁻¹). Biobased residues and urea were applied in May of each cropping season. All the treatment plots received 27 kg P₂O₅ ha⁻¹ using triple superphosphate (0-46-0) and 55 kg K₂O ha⁻¹ potassium chloride (0-0-60) according to the local agronomic requirement (Table 1). The site was under a maize (Zea mays L.)—soybean (Glycine max) rotation, where maize was seeded in 2018 and 2020 and soybean in 2019. Crop grain was removed and the remaining aboveground biomass (stalks and leaves) and belowground residues (roots) were incorporated to a 15 cm with an offset disc harrow. However, for this study, we focused on the impact of spring thaw event on the greenhouse gas emission of the four different treatments applied in May 2020 during the spring of 2021 (March specifically). The effects of biobased residues on greenhouse gas emissions during growing and non-growing seasons is explored further in a related manuscript (Badewa et al., unpublished).

TABLE 1

TABLE 1. Chemical properties of the biobased residues used in the experiment.

The effect of ambient temperature, snow depth, and precipitation were obtained from a weather station located at the research station. Soil temperature at ∼10 cm depth was measured by temperature sensors buried in one replicate of each treatment (n = 4). Air and soil temperature followed a similar pattern from October to mid-November but were distinctly different from the end of November to mid-March when the soil was covered with snow for 95 days (Supplementary Figure S1). During this period, the snow cover (∼49 cm) and crop residues left on the soil insulated and regulated the soil temperature (0–10 cm depth) to ∼0°C with precipitation ranging from ∼29 mm (Supplementary Figure S1).

Greenhouse Gas Fluxes

Greenhouse gas fluxes were measured from 11 March to 24 March 2021 using closed static chambers. The static chamber bottom (15 cm long and 56 cm diameter) was constructed of a light grey colored polyvinyl chloride pipe and inserted into the soil depth of 10 cm, leaving 5 cm headspace above the soil surface. Chamber caps consisted of a 1 cm diameter opening fitted with rubber septa for gas sampling and a 10 cm long vent tube (9 mm inner diameter) to account for pressure differences during sample collection (Parkin and Venterea, 2010). After fitting the bottom and top cap, chamber volume was 30.2 L, with a 0.08 m² cross-sectional area. One permanent base was placed randomly in soil for each treatment replicate in October 2020 before soil freezing. The first measurement occurred on 11 March 2021, when the chamber bottom in the treatment plots were visible—not covered with snow and had <5 cm of snow. The final measurement occurred on 24 March 2021, 7 days after the snow and ice melted disappears. We were not able to record moisture due to freezing soil state and data logger issues, but we categorized our measurement days into three freeze-thaw phases using the visual moisture state observed during greenhouse gas measurement (Supplementary Table S1). First freeze-thaw phase (waterlogged) occurred when the soil was covered with melting snow and saturated. The second freeze-thaw phase (wet) occurred immediately after the snow and ice melted and when mostly wet, followed by third freeze-thaw phase (dry) that was mostly dry with wet patches (Supplementary Table S1).

Gas samples were extracted daily from each treatment replicate. To control for sinusoidal diurnal temperature variations, sampling was conducted between 10:00-h and 16:00-h (Smith et al., 2003). Gas sampling (30 ml) was carried out at 0, 10, 20 and 30 min after placing the chamber cap and transferred into pre-evacuated 12 ml glass Exetainers (LabCorp Ltd., Lampeter, Wales, United Kingdom). The collected gas samples were analyzed on a Bruker 450 gas chromatograph (Bruker Corporation, Billerica, MA, United States) fitted with a thermal conductivity detector for CO₂, a flame ionization detector for CH₄, and an electron capture detector for N₂O analysis. The gas concentration (ppm) measured by gas chromatograph was converted to mass-based concentration with the Ideal Gas Law using the relative molecular mass of C (12 g mol⁻¹) or N (28 g mol⁻¹) (Pedersen, 2017). The fluxes (µg m⁻² min⁻¹) were then estimated using the HMR package in R (version 4.1.2). Cumulative emission of the gases and the global warming potential over 100 years (GWP) during the spring freeze-thaw events (11 March to 24 March 2021) were calculated using Eqs. 1, 2.

$CE={\displaystyle \sum F_i\times 24}(1)$

Where CE is the cumulative emission of soil greenhouse gas (µg m⁻²/mg m⁻²) and Fi is the greenhouse gas flux of the ith sampling time (µg m⁻² h⁻¹). The GWP (kg CO_{2 eq} ha⁻¹) was calculated using:

$GWP=C{E}_{C{O}_2}+C{E}_{C{H}_4}\times 27.9+C{E}_{N_{2}O}\times 273(2)$

Where $C{E}_{C{O}_2}$, $C{E}_{C{H}_4}$, and $C{E}_{N_{2}O}$ represent the cumulative emissions of CO₂, CH₄, and N₂O, respectively.

Statistical Analysis

All data processing and analysis were carried out in R v.4.2.1 (R Core Team, 2020). Data did not meet assumption of normality, so data were analyzed by non-parametric statistics. The effect of treatment and the freeze thaw phases on greenhouse gas flux and emission was determined with a Kruskal wallis test and the treatment comparison was done with a Dunn test (p < 0.05). The relationship between greenhouse gas emission and soil or air temperature was determined using Pearson correlation coefficients (r). The relationship between greenhouse gas fluxes and soil temperature was evaluated using Pearson correlation coefficients (r) and exponential model.

Results

Temperature Conditions and Greenhouse Gas Fluxes

Soil temperature among treatments was identical (p > 0.05) during the spring freeze-thaw (Figure 1). Soil and air temperature varied among the freeze thaw phases (p < 0.05) with average soil temperature during greenhouse gas sampling highest for dry (7°C), followed by wet (2°C) and lowest for waterlogged (0°C) (Figure 1). Cumulative N₂O emission were different among treatments (p = 0.020) while cumulative CO₂ and CH₄ emissions were not different among treatments (p > 0.05) (Table 2). When comparing N₂O emission among treatments, the average loss was highest in compost (669 µg N₂O-N m²), followed by urea (419 µg N₂O-N m²), biosolids (259 µg N₂O-N m²), and digestate (105 µg N₂O-N m²) (p < 0.05). The global warming potential varied among treatments but was not significantly different (p > 0.05), where urea had the highest (127 kg CO₂ ha⁻¹) and digestate the lowest (55 kg CO₂ ha⁻¹) warming potential (Table 2). The greenhouse gas emission varied significantly among the freeze thaw phases (p < 0.05) with peak N₂O and CO₂ fluxes during the wet, and peak CH₄ flux during the dry (Figure 2). N₂O flux ranged from −388 to 454 µg N₂O-N m⁻² h⁻¹, CO₂ flux from −211 to 565 mg CO₂-C m⁻² h⁻¹, and CH₄ flux −1285–216 µg CH₄-C m⁻² h⁻¹. However, mean N₂O flux was highest during the wet (31 µg N₂O m⁻² h⁻¹) and lowest during waterlogged (−2 µg N₂O-N m⁻² h⁻¹), mean CO₂ flux was highest flux during the dry (34 mg CO₂ -C m⁻² h⁻¹) and lowest during waterlogged (5 mg CO₂ -C m⁻² h⁻¹) while mean CH₄ flux was highest during the wet (−11 µg CH₄-C m⁻² h⁻¹) and lowest during waterlogged (−24 µg CH₄-C m⁻² h⁻¹).

FIGURE 1

FIGURE 1. Hourly soil temperature from the four treatment plots (∼10 cm) and air temperature during the experiment period (from 11 March 2020 to 24 March 2021).

TABLE 2

TABLE 2. Cumulative greenhouse gas emission and global warming potential from soils amended with urea and biobased residues during the 2021 spring freeze-thaw event.

FIGURE 2

FIGURE 2. Greenhouse gas fluxes of N₂O, CO₂, and CH₄ during the spring freeze-thaw event of 11 March to 24 March 2021.

Relationship Between Greenhouse Gas Emissions, Air, and Soil Temperature

N₂O emission had a moderate positive correlation with CO₂ emission (p = 0.000), weak positive correlation with CH₄ emission (p = 0.006) but weak non-significant correlation with soil, or air temperature (p > 0.05) (Table 3). CO₂ emission had a weak positive correlation with soil temperature (p = 0.032), weak positive correlation with air temperature (p = 0.042) but was not significantly correlated with CH₄ emission (p > 0.05) (Table 3). CH₄ emission was not significantly correlated to CO₂ emission, and soil and air temperature (p > 0.05) except CH₄ emission (p = 0.006) (Table 3). Relationship between greenhouse gas fluxes and soil temperature were estimated using exponential model (Figure 3; Table 4) (Luo et al., 2013; Natali et al., 2019). The CO₂ flux was positively correlated with soil temperature for compost, biosolid, and digestate and when averaging all four treatments (p < 0.05) (Figure 3A). However, N₂O and CH₄ fluxes were generally not significantly correlated with soil temperature (p > 0.05) (Figures 3B,C).

TABLE 3

TABLE 3. Correlation values for the greenhouse gas fluxes and emissions and soil and ambient temperature during the spring freeze-thaw events (n = 224).

FIGURE 3

FIGURE 3. The effect of soil temperature (∼10 cm) on (A) CO₂ (B) N₂O (C) CH₄ fluxes release from the soil amended with urea and biobased residues during the spring freeze thaw event on 11 March to 24 March 2021. The graph presented the exponential model fitted (solid gray line) and the standard deviation of an exponential model fitted (gray shading) between greenhouse gas flux per treatment and soil temperature during the spring freeze thaw event (note: CH₄ flux standard deviation was not achieved due to iterative error caused by the many negative integers). The Pearson correlation coefficients (r) and the significant level (p) are shown for the treatments. SFT1 is the first spring freeze-thaw phase (waterlogged), SFT2 is the second spring freeze-thaw phase (wet) and SFT3 is the third spring freeze-thaw phase (dry). * Shows p-value < 0.05.

TABLE 4

TABLE 4. Relationship between greenhouse gas fluxes and soil temperature (∼10 cm) using exponential model during the 2021 spring freeze-thaw events.

Discussion

Influence of Soil Amendments on Greenhouse Gas Fluxes During Spring Freeze-Thaw

Nitrous oxide emission from compost amended soil was notably different from that of biosolid and digestate. This was likely due to the variation in C and N availability (Table 1), and therefore microbial activity among the different biobased residues evaluated in our study. We found that compost had a high N₂O flux compared to the other treatments, although this biobased residue has the lowest N mineralization potential (Table 1). This possibly occurred because compost has the highest application rate that supplied more C and N for N₂O production, and highest organic C and lowest N composition which takes the longest to fully mineralized. Thus, compost-treated plot has the highest residual C and N in the next year spring when the experiment was carried out. Similarly, Kariyapperuma et al. (2012) found also that the variable composition of composted swine influenced N₂O emissions during non-growing season that undergoes spring freeze thaw. Generally, composts with higher organic C and available N content cause greater N₂O fluxes and as the compost C:N ratio increases, N₂O fluxes decreases (Santos et al., 2021) suggesting chemical composition of compost could regulate soil N₂O fluxes.

The lower than expected N₂O flux for anaerobic digestate in our study (Table 2) was due to the presence of readily degradable C and the physical quality (i.e., liquid state of this residue type). Our findings were also consistent with other studies that found lower N₂O fluxes with digested materials that were in a liquid state compared to either undigested materials (e.g., solid state) or mineral fertilizer (Petersen 1999; Börjesson and Berglund, 2007; Chantigny et al., 2007; Collins et al., 2011; Rodhe et al., 2015; Baral et al., 2017). It has been shown that the low soluble organic C in anaerobic digestate leads to a lower source of energy for denitrifiers causing a reduction in the production of N₂O (Vallejo et al., 2006; Nkoa, 2014). Furthermore, digestates contain high soluble N that is readily available for plant uptake (De Vries et al., 2012; Baral et al., 2017). In our study, we found that ∼98% of the anaerobic digestate was in the mineralized form and was probably taken-up by the maize crop planted in the 2020 growing season (data not shown).

Some previous studies showed that during biosolid production and throughout the first month of its application to agricultural soil, volatile N (e.g., ammonia) is lost from the soil (e.g., Yoshida et al., 2015; Roman-Perez et al., 2021). In our study, lower N₂O flux observed was likely caused by volatilization of ammonia from the biosolid treatment. Furthermore, the biosolid used in our study was obtained from Lystek that uses a thermal hydrolysis process that disintegrates the cell walls of microbes and hydrolyses complex macromolecules into simpler compounds (Lystek, 2021). The use of heat, shearing, and alkalinity during thermal hydrolysis can cause the cell walls to lyse and it reduces the abundance of denitrifying bacteria, while C substrates persist and contribute to CO₂ and/or CH₄ emissions (Knowles, 1982; Murray et al., 2019). Results from our study also show that the N mineralization rate of the Lystek biosolid was ∼50% and indicate that most of the available N was taken-up by the maize during growing season (data not shown).

We also found a positive relationship between N₂O versus CO₂ and CH₄ emission among treatments which indicated that C input from biobased residues and urea stimulated the production of N₂O (Table. 3). Faubert et al. (2019) also found a positive relationship between N₂O and CO₂ emission and suggested that C input stimulated N₂O emission either by reducing soil oxygen availability through increased soil respiration, or by the direct use of C from biobased residues as a source of energy for hetrotophic denitrifiers (Wrage-Mönnig et al., 2018). Since biobased residues can be distinctly different due to variation in their feedstock and/or production process, the quality of C (e.g., lignin content) and its N mineralization rate also varies (Ejack and Whalen, 2021). However, Roman-Perez et al. (2021) found that regardless of biobased residue type, the processes of C mineralization is similar, whereby increased C availability enhances microbial respiration and raises CO₂ and CH₄ fluxes (Roman-Perez et al., 2021). Furthermore, in our study N mineralization likely increased available N which was transformed to N₂O via nitrification and complete denitrification (Grant et al., 2020).

Although the cumulative CO₂ and CH₄ emissions, and the global warming potential did not differ among treatments (p > 0.05), we observed a wide range in their values among treatments (Table 2). This was due to differences in nutrient availability, especially the availability of C during the spring freeze-thaw, among treatments (Adviento-Borbe et al., 2007; Brenzinger et al., 2018). Our results also supported the growing view among researchers that treatment comparisons should be explained using variability and magnitude effects and not only be limited to statistical significances (Wasserstein et al., 2019; King et al., 2021). Furthermore, results from our study that showed variation in greenhouse gas fluxes among treatments during the spring freeze-thaw, also highlights the importance of incorporating negative greenhouse gas fluxes. Since most studies in temperate environments do not account for greenhouse gas fluxes during winter and early spring (Yan et al., 2016; Kim et al., 2019; Natali et al., 2019), our study showed the importance of accounting for negative fluxes, especially in fertilized agroecosystems, since soil produces and consumes greenhouse gases (Hung et al., 2021).

Freeze Thaw Phases and Temperature Influence on Greenhouse Gas Fluxes

We found that soil freezing, and thawing combined with changes in air and soil temperature caused a high degree of variability in CO₂ fluxes in all treatments. This indicated that soil warming regulated and enhanced microbial respiration during the spring freeze-thaw (Byun et al., 2021; King et al., 2021; Rafat et al., 2021). We found that CO₂ fluxes were different among freeze-thaw phases where the dry phase had highest flux compared to the wet and waterlogged phases. This was due to the variation in soil microbial respiration, which was enhanced when the soil became warmer (Ganjurjav et al., 2016; Gao et al., 2020). Furthermore, we found that soil temperature was lowest during the waterlogged phase (∼−0°C) compared to the wet (∼2°C) and dry (∼7°C) phases. Natali et al. (2019) also found that warming during freeze-thaw allowed for the short-term mineralization of organic residues which caused the release of CO_2.

In addition, the intensity of soil respiration during freeze-thaw is positively dependent on soil temperature and moisture (Schipper et al., 2014; Byun et al., 2021). Since no crops or plants were present over the winter, the CO₂ flux quantified in our study was a direct measurement of soil microbial activity (Hung et al., 2021). Although we were not able to measure moisture in our study, we found that the significant relationship between temperature and CO₂ flux was a measure of the intensity of microbial metabolism even when temperature drop close to zero (−1–2°C) during the waterlogged and wet phase (Schaefer and Jafarov, 2016). This is because temperature controls a range of biogeochemical processes that regulate soil C cycling (Flanagan et al., 2013). In a temperate forest ecosystem, Yan et al. (2016) found a significant and positive relationship between soil CO₂ flux and soil temperature during the spring freeze-thaw.Furthermore, Zou et al. (2018) summarized that multiple field studies found a significant and positive relationship between soil respiration intensity and soil temperature and soil moisture. However, to our knowledge, our study is the first to quantify the relationship between CO₂ flux and soil temperature from various biobased residues during the spring freeze-thaw under field conditions.

We also found that soil freezing, and thawing caused a high degree of variability in N₂O and CH₄ fluxes indicating anaerobiosis caused by soil moisture state of the phases contributed to the variability of the fluxes. The freeze thaw phases in our study were determined with the visual moisture state and the N₂O flux during the wet phase was significantly highest compared to the waterlogged and dry phase. This was likely due to the release of trapped N₂O in soil pores during the wet phase. The waterlogged phase causes soil pores with transient liquid water and ice to enable microbes to undergo denitrification that produces N₂O (Kim et al., 2012; Congreves et al., 2018). The N₂O produced could however be trapped because of high tortuosity created by water and ice in the pores (Hung et al., 2021; King et al., 2021) and gradually release when the waterlogged phase transitioned to the wet phase where ice seal was removed. In addition, CH₄ flux during the wet phase was different and higher compared to dry but not the waterlogged phase. This suggests that the anaerobic and wet condition encourage microbial production of CH₄ through methanogenesis (Luo et al., 2013). Further research should consider in-depth evaluation of the simultaneous contribution of spatial and temporal soil temperature and soil moisture measurements on NO₂ and CH₄ fluxes during spring freeze thaw in temperate agricultural land.

Conclusion

We evaluated the impact of biobased residues on greenhouse gas fluxes during the spring freeze-thaw. Greenhouse gas fluxes from biobased residues is not different compared to urea except for N₂O emission from compost. There was a significant relationship between soil temperature and CO₂ flux but no relationship with N₂O and CH₄ fluxes during the spring freeze thaw. Among the freeze thaw phases, the greenhouse gas fluxes were different. We found that the dry phase during freeze-thaw caused intensified CO₂ fluxes compared to the wet and waterlogged freeze-thaw phase due to enhanced warming. We found that greenhouse gas fluxes from treatments with biobased residues and urea were controlled by the availability of C and N that regulated microbial processes of C mineralization and nitrification/denitrification. We propose that future studies should incorporate molecular techniques to elucidate the specific organisms responsible for C and N transformations during spring freeze-thaw events especially in the waterlogged and drying phases. This information will help to further understand the role of biobased residues versus N fertilizers in greenhouse gas fluxes and aid with management decisions with respect to the type and timing of biobased residue application.

Data Availability Statement

The original contributions presented in the study are included in the article/Supplementary Material, further inquiries can be directed to the corresponding authors.

Author Contributions

EB: design of experiment, data acquisition, data analysis, data interpretation, and drafting of manuscript. CY: data interpretation and revision of draft. FR: data interpretation and revision of draft. JW: design of experiment, data interpretation, and revision of draft. MO: design of experiment, data interpretation, and revision of draft.

Funding

Funding was provided by the Quebec-Ontario Cooperation for Agri-Food Research (project SR9323) supported by the Quebec Ministry of Agriculture, Fisheries and Food and the Ontario Ministry of Agriculture, Food and Rural Affairs.

Conflict of Interest

The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

Publisher’s Note

All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.

Acknowledgments

We thank Lystek International for providing Lystegro biosolid, AIM Environmental for providing the composted food waste, and BioEn for providing the anaerobic digestate. We also thank the Canadian Foundation for Innovation (CFI), the University of Waterloo and McGill University for providing research infrastructure. We thank Hicham Benslim (McGill University) for greenhouse gas sample analysis.

Supplementary Material

The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/fenvs.2022.909683/full#supplementary-material

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