Eight static closed no vented-chambers (similar to those of Holland et al., 1999) were used to measure soil CO₂, N₂O and CH₄ fluxes. The chambers were distributed in the field to capture the soil and crop variability. One polyvinyl chloride (PVC) collar was inserted 10 cm into the soil at each measurement point six days before the first sampling date. PVC chambers (19.7 cm height, 30 cm inner diameter; volume of 13.9 L) coated with a reflective bubble wrap material were fitted into the collars at the time of sampling. During 2016 the plants were removed, cutting periodically from the ground, but during 2017, the plants were left inside growing. Chambers were sampled every 3 to 4 weeks with 16 and 17 sampling times in 2016 and 2017, respectively. At each sampling date, 15 mL of air from inside each chamber were taken at 0, 30, and 60 min after chamber closure using a polypropylene syringe, and injected into 12-mL Exetainer® borosilicate glass vials (Labco Ltd., Lampeter, UK). Air samplings were mostly performed between 10:00 to 11:30 A.M. (Greenwich Mean Time) considering that soil temperature was the main factor driving daily changes in soil N₂O fluxes (Alves et al., 2012) and that soil temperature at that time was close to the daily average. Air samples were analyzed by gas chromatography using an Agilent 7890B chromatograph with electron-capture (ECD) and flame-ionization detector (FID). Soil fluxes of CO₂ (kg ha^-1 day^-1), N₂O (g N ha^-1 day^-1) and CH₄ (g C ha^-1 day^-1) were calculated fitting a linear regression of the gas concentration in the chamber (corrected for air temperature) versus time. No significant differences (paired t-test; p>0.05) in soil N₂O fluxes were obtained using 0-30 min and 0-60 min closure times, which indicates no significant saturation effect. There was a total of 33 sampling dates during the two growing seasons, with an average sampling interval of 21 days. Cumulative emissions were calculated with the trapezoid rule, interpolating the averaged flux between consecutive sampling dates and multiplying it by the time period between the two samplings dates. The total N-scaled emissions were calculated as the total N₂O emission divided by the total N uptake of the aboveground alfalfa crop in each year.

The topsoil (0-10 cm) was sampled to monitor SMN concentration in the upper part of the soil profile at every GHG sampling date (except in 3 dates), with a total of 29 dates. SWC was measured gravimetrically (drying at 105 ºC until constant weight) and a 10 g wet soil subsample was extracted with 30 mL of 2 N KCl after shaking on a reciprocal shaker for 30 min and filtering through cellulose filter. The soil extracts were analyzed by colorimetry using a segmented flow analyzer (AutoAnalyser3, Bran+Luebbe, Germany) to obtain nitrate (NO₃‾) and ammonium (NH₄+) concentrations (mg N kg^-1 soil). Topsoil moisture and temperature were also monitored continuously (3-min interval; averaged every 30 min) at the 5-cm depth in three locations of the field using SDI-12 Hydraprobe sensors (Stevens Water Monitoring Systems Inc., Beaverton, USA) connected to a data logger CR-200 (Campbell Scientific Ltd., Logan, USA). SWC values were calculated from the sensor readings with a calibration curve (R²=0.81; n=28) obtained from soil sampling. Soil WFPS was calculated according to Linn & Doran (1984) as the quotient between volumetric soil water content and total soil porosity. Total soil porosity (44.5%) was estimated considering a particle density of 2.65 Mg m^-3, and the soil bulk density from 0 to 5 cm determined ‘in situ’ using the cylinder method (Grossman & Reinsch, 2002) as 1.47 Mg m^-3. Daily air temperature and precipitation were registered with an automated weather station located 100 m apart from the experimental site.

A short-term experiment was carried out during the 2017 growing season to analyze the temporal variability of soil N₂O emissions during the period between the first and the second alfalfa harvest (April 26 to May 25). Two automated transient-state closed-system canopy chambers were used to continuously measure the gas exchange during the 29 days period. The chambers (Tecno El, Formello, Italy) were similar to that described by Steduto et al. (2002). It had a module that is a rectangular box with five transparent polycarbonate walls (1.5 mm thick), held together by a narrow aluminum angular frame. The chamber was open in the bottom, had a ground surface area of 0.75 m² (1.0 m × 0.75 m), and had a height of 0.5 m. It has a metal base that is inserted 5 cm into the soil. The chamber has four fans (Ebmpapst, Mulfingen, Germany) mounted in the corners which provide a total flux of 1.4 m3 min^-1. The chamber top-cover has a hinge on one side, is usually open but can be moved to close the chamber in order to measure the gas exchange.

One thermocouple (Campbell Sci., TCBR-3, Shepshed, UK) not shielded was installed inside each chamber at half of its height to measure the air temperature at a 0.5 s interval.

The chamber top-cover was kept open for 30 min and closed for 30 min. The two chambers were synchronized so during the time that one was open the other was closed. During the time that the chamber was closed the four fans were stirring the air. A miniature diaphragm pump (model 15D1150, GAST, Benton Harbor, MI, USA) was used to continuously extract the air from inside of the chambers and to conduct it to a portable photoacoustic equipment (Innova 1412i Photoacustic Multigas Monitor) that analysed and stored temperature-corrected (25ºC) N₂O and CH₄ concentration. A flowmeter (Dwyer, model VFB-66-SSV-BFP, Michigan City, IN, USA) was used to get a constant flow of 5 L min^-1 up to the Innova. The air was recirculated to the chamber. Gas samples were analyzed by the Innova every 2-min, so 15 gas samples were taken and analysed at each 30-min period. Gas was sampled alternatively from each closed chamber by means of a switch device that allowed to sample the gas from the chamber that was closed. Thus, a continuous gas exchange data set with a 30 min interval could be obtained during 29 days.

Although the photoacustic equipment (PA) was calibrated by the manufacturer company immediately prior to this study, we performed an empirical calibration versus the gas chromatograph equipment (GC) to ensure the comparability of the data obtained with the two analytical procedures. We observed a very good relationship [Eq. 1] between photoacoustic N₂O concentrations (N₂OPA) and gas chromatography concentration (N₂O_GC), although the photoacoustic equipment was not enough sensitive to measure low concentrations (<1 mg N₂O m^-3; equivalent to fluxes of 10 g N-N₂O ha^-1 day^-1). N₂O concentrations measured with the PA were adjusted to GC using Eq. [1].

The N₂O fluxes were estimated as the slope of the linear regression of gas concentration versus time after closure. The N₂O fluxes were expressed as g N ha^-1 day^-1. The cumulative fluxes (g N ha^-1) over the whole 29-days period were obtained similarly to the static chambers experiment, through integration fluxes between two sampling dates. Methane (CH₄) measurements from photoacoustic equipment did not provide enough accuracy and were not considered.

The SWC and soil temperature at 5 cm depth were monitored every 3 min in both chambers using field calibrated (R²=0.97) SDI-12 Hydraprobe sensors (Stevens Water Monitoring Systems Inc., Beaverton, USA), similarly as described in the static chambers experiment.

The soil within each chamber was sampled 4 times along the experiment to determine the NO₃‾ and NH₄+ concentration (mg N kg^-1) in the topsoil (0-10 cm). The samples were analyzed using the same procedure already described.

During that period of 29 days, the average of daily mean, minimum, and maximum air temperature were 16.7, 8.52, and 24.5 ºC, respectively. A total of nine events of rain and two of irrigation occurred, with a total precipitation of 89.6 mm. The two irrigation events were on May 2 (39.5 mm) and May 17 (23.7 mm).

The alfalfa field was ploughed with a disk harrow and chisel on February 6, 2018, simultaneously with an adjacent field that had been cropped with maize during the previous 2016 and 2017 seasons. The maize field had been managed according to standard practices in the area with a N-fertilizer rate of 250 kg N ha^-1 distributed in 50 kg N ha^-1 at preplanting and two 100 kg N ha^-1 side-dress applications at V6 and V14 maize growth stages. The maize development was correct with a grain yield of 13.5 Mg ha^-1 (14% of humidity). The residues of alfalfa and maize in both fields were incorporated into the soil with the plough. Two days later, ten static closed no vented-chambers (similar to that described before) were installed in the two fields previously cropped with alfalfa (5 chambers) and maize (5 chambers). From February 14 to April 12 (57 days) the chambers were sampled 9 times to obtain soil GHG fluxes following the same method already described.

Previously to plough the fields, the total aboveground maize residue (stubble) was measured in one area of 5 m². In addition, the total alfalfa roots and crown residues in the topsoil (25 cm depth) were sampled in 8 locations of 0.46 m² each. The material was washed with distilled water to remove soil particles and dried to estimate the biomass of alfalfa residue. The total C and N of maize and alfalfa residues were analyzed by dry combustion (TruSpec CN, LECO, St. Joseph, MI, USA).

Analysis of variance was performed to evaluate the effect of the alfalfa vs maize crop residues on the analyzed variables. Comparisons among treatments were performed with Tukey’s test. Repeated measure analysis along time, according to a first-order autoregressive structure model AR(1), was performed to compare SMN and N₂O fluxes between alfalfa and maize fields after residue incorporation. A t-test was used to check if cumulative CH₄ fluxes were different from zero and to compare different variables between maize and alfalfa fields. In all tests, the level of significance considered by default was 95%. Soil GHG fluxes were transformed using the logarithm function when necessary to normalize their distributions and to homogenize the variances. Pearson correlation analysis was used to determine the relationship between the different variables included in the study such as N₂O fluxes and soil NO₃‾ and NH₄+ concentrations, soil temperature, and WFPS. Statistical analyses were performed using the STATGRAPHICS Centurion v.18.1.10.

A great temporal variability was observed in the daily topsoil WFPS (Fig. 2), that was mainly associated to the high number of irrigation events (36 and 33 in 2016 and 2017, respectively), very typical in sprinkler irrigated alfalfa. Thus, the daily average WFPS ranged from 24 to 80% with an average value of 54% (mode=59%), indicating that most of the time the soil was below field capacity (WFPS=67.7%), but during each irrigation event (or after a significant precipitation) the topsoil reached WFPS values above 70%. Considering the two growing seasons, about 10% of the time, the topsoil WFPS was higher than 70% (Fig. 3). The topsoil temperature ranged from 0.5 to 28.3ºC, with an average value of 14.9ºC.

The SMN in the topsoil (Fig. 4) was dominated by the NO₃‾ form. Thus, the average NO₃‾ content was 8.3 mg N kg^-1 while the average NH₄+ content was 1.5 mg N kg^-1 (comprising less than 20% of the total SMN). Only at one sampling date (April 21, 2017), the soil NH₄+ content was similar to the soil NO₃‾ content. No relationship was observed between topsoil NO₃‾ or NH₄+ content with alfalfa phenology. Averaging over chambers and sampling dates, the soil NO₃‾ content in 2017 (7.1 mg N kg^-1) was lower (p<0.01) than during 2016 (9.8 mg N kg^-1), and the opposite occurred for NH₄+ content (2016: 1.13 mg N kg^-1; 2017: 1.9 mg N kg^-1). The relationship between soil NO₃‾ content and soil temperature was not significant in both years but soil NO₃‾ content was inversely related to WFPS (r=-0.40, p<0.01).

Year-averaged soil CO₂ fluxes were higher in 2017 (74.9 kg C ha^-1 day^-1; SE=3.9) than in 2016 (23.0 kg C ha^-1 day^-1; SE=1.4). Soil CO₂ fluxes were significantly related to air temperature (r=0.76, p<0.01; data not shown). The cumulative fluxes of CO₂ during the 2016 season (no plants inside the chamber) were 7851 kg C year^-1 (SE=453, n=8), very close to the estimated C removed with the alfalfa hay in the same period (7402 kg C year^-1), and lower than the cumulative fluxes in 2017 (plants inside the chamber; Fig. S1 [suppl]).

CH₄ fluxes were low, ranging between -7.20 to 6.22 g C ha^-1 day^-1, with an average value of -0.88 and -0.54 g C ha^-1 day^-1 in 2016 and 2017, respectively (Fig. 5). In 2016, only in 4 out of 16 sampling dates the flux was significantly (p<0.05) different from zero. In these cases, the flux was negative (average flux of -4.7 g C ha^-1 day^-1). In 2017, only in 3 out of 17 samplings dates, the flux was significantly (p<0.05) different from zero, and similarly to 2016, in these two dates, the flux was negative (-1.39 g C ha^-1 day^-1). The cumulative fluxes of CH₄ in 2016 and 2017 (Figs. 5a and 5c) were not significantly different from zero (p<0.05).

In the case of N₂O, in 28 out of 33 sampling dates, the N₂O flux was significantly (p<0.05) different from zero. No significant correlation was found (p>0.05) between N₂O fluxes and air temperature (data not shown). The year-averaged fluxes were 2.26 and 5.67 g N ha day^-1 for 2016 and 2017, respectively. The higher average flux in 2017 was mainly due to a flux event recorded in one sampling date (April 21, 61.7 g N ha^-1 day^-1; SE=8) that occurred 13 days after the first alfalfa harvest. This remarkable flux was consistent among the eight replicated chambers with values ranging from 42.4 to 83.9 g N ha^-1 day^-1. That flux concurred with a high soil NH₄+ content (12.2 mg N kg^-1; ranging between 6.1 and 22 mg N kg^-1) and a relatively high daily soil WFPS (average of 72%, ranging from 64 to 85% along the day) due to the 3-hour irrigation (24 mm) event applied the previous day of the measurements. However, the soil temperature during the mentioned event was only 16.7ºC. The four chambers located in places with soil NH₄+ content greater than 10 mg N kg^-1 presented an average N₂O flux of 82.8 g N ha^-1 day^-1. The combined effect of WFPS and soil NH₄+ content on N₂O fluxes is presented in Fig. S2 [suppl]. When the soil NH₄+ content was higher than 5 mg N kg^-1 and the WFPS was higher than 65%, the N₂O fluxes were greater than 50 g N ha^-1 day^-1.

A differential relationship was found between N₂O and CO₂ fluxes depending on the top-soil water content (Fig. 6). Thus, when soil WFPS was lower than 60%, a linear relationship was observed, but the relationship became logarithmic when soil WFPS was higher than 60%.

The cumulative N₂O fluxes were 839 and 2226 g N ha^-1 year^-1 for 2016 and 2017, respectively (Fig. 5; Table 2). However, according to the results obtained from the automatic chambers experiment presented later in the document, the duration of N₂O peaks is usually very short (about 24 h). Therefore, considering the hypothesis that the duration of the high flux event was only of one day (instead of the effect on 47 days due to the low frequency GHG measurement), the corrected estimated cumulative N₂O emissions would be 890 g N ha^-1 year^-1 for the 2017 growing season.

The total production of alfalfa hay is presented in Table 2, with an accumulated two-year value of about 28 Mg ha^-1. The aboveground dry matter of alfalfa contained 387 and 501 kg N ha^-1 in 2016 and 2017, respectively. Overall, the total N-scaled nitrous oxide emissions were 2.17 y 1.78 g N kg^-1 N for the two growing seasons.

Similarly to that observed in the static chambers experiment, the topsoil (0-10 cm) NH₄+ content was lower than NO₃‾ during the experiment, ranging from 0.82 to 3.21 mg N kg^-1 with an average value of 1.5 mg N kg^-1. Soil NO₃‾ content was significantly greater than NH₄+, ranging from 8.3 to 18.3 mg N kg^-1 and with an average value of 13.2 mg N kg^-1, with a significant increase (p<0.05) during the alfalfa growing period.

The evolution of topsoil (0-10 cm) WFPS was related to rainfall and irrigation events (Fig. 7). Thus, the two-chambers average WFPS ranged from 36 to 95% with a mean value of 51.7% (53.8 and 49.7% for chambers C1 and C2, respectively). Four peaks of topsoil WFPS were observed associated to events of irrigation or rain greater than 10 mm. In three of these events the WFPS reached values close to saturation.

The N₂O fluxes in the two chambers were very similar and thereby the hourly values were averaged (Fig. 7). The average hourly N₂O flux during the period of 29 days (26 April to 25 May) was 12.6 g N ha^-1 day^-1 (SE=0.67; n=653). Some negative N₂O fluxes (14% of the total measurements) were found at some specific days, but due to the low sensitivity of photoacoustic equipment at low N₂O concentrations, the accuracy and confidence of fluxes below 10 g ha^-1 day^-1 is low. However, the two N₂O peaks observed on May 2 (maximum 160 g N ha^-1 day^-1; averaged over the two chambers) and May 17 (maximum 136 g N ha^-1 day^-1; averaged over the two chambers) in both chambers had a short but significant duration, ranging from 6 to 24 hours. Averaging over the two chambers these peaks accounted for a total N₂O emission of 47.2 and 22.6 g N ha^-1 associated to two irrigation events that increased the WFPS above 80%. It was noteworthy that another WFPS peak was measured after a rainfall occurred on May 18^th (Fig. 7) but no peak of N₂O flux was observed.

The amount of residues (roots and crowns) in the alfalfa field was 4808 kg DM ha^-1 (SE=623) with an average N content of 2.63% (SE=0.06). Thus, the total N incorporated into the topsoil with the alfalfa residues was 185 kg N ha^-1 (SE=14.9). In the adjacent field, cropped the previous year with maize, a total of 10003 kg DM ha^-1 of stubble with a N content of 0.55% was incorporated into the soil (55 kg N ha^-1). The C/N ratios of maize and alfalfa residues were 81.6 and 17.8, respectively.

A total of 144 mm of rain fell during the 57-day period (Febr. 14 to Apr. 12) included in the study (Fig. 8a). The topsoil (0-10 cm) WFPS ranged from 36 to 82% with an average of 62%, close to the 67% value corresponding to field capacity. WFPS changed over time according to rainfall events and there was a tendency of higher WFPS in the maize field (63.2%) compared to the alfalfa field (60.5%), although only in 2 out of 9 dates the difference was significant. The soil temperature at 5-cm depth ranged from 8 to 21ºC with an average value of 13.2ºC. No consistent significant differences in soil temperature were observed between maize and alfalfa fields along the whole period, but small (<1ºC) differences were found in three sampling dates.

Very low topsoil NH₄+ content was found in the two fields (Fig. 8b) with values ranging from 0.4 to 2.7 mg N kg^-1 and an average of 1.2 mg N kg^-1. No significant differences in soil NH₄+ content were found between alfalfa and maize fields. However, the topsoil NO₃‾ content in 5 out of 9 sampling dates was higher in the alfalfa field (average of 18.7 mg N kg^-1) than in the maize field (average of 10.2 mg N kg^-1).

Daily fluxes of CO₂ were significantly higher after alfalfa than after maize (Fig. 9); with a cumulative flux also significantly higher (510 kg C ha^-1 for alfalfa vs 240 kg C ha^-1 for maize) after 57 days of plow down the crop residues. The soil CH₄ flux was not significantly different from zero in 17 of the 18 samplings (9 dates × 2 plots). No significant differences of cumulative CH₄ fluxes between alfalfa and maize fields were found, with a tendency to CH₄ consumption (-3.1 g C-CH₄ ha^-1 day^-1) by the soils during the measurement period. Soil N₂O fluxes ranged from 0 to 5 g N ha^-1 day^-1 except the last sampling date in the maize field (April 12) that showed a noticeable peak of 18.5 g N ha^-1 day^-1 (SE=8.21), that occurred after two consecutive days with significant irrigation (April 10th: 14.5 mm; April 11th: 30.6 mm). A great variability in N₂O flux was observed in the last sampling date at the maize field. Thereby, the N₂O flux ranged from 6.11 to 42.3 g N ha^-1 day^-1 among the five maize chambers. Only in one sampling date (February 21) the alfalfa field had a higher N₂O flux than the maize field. However, no significant differences were observed in the cumulative N₂O fluxes between the two fields either including or excluding the last sampling date.

Greenhouse gas fluxes are closely linked to soil microbial activity and root-soil turnover, and therefore related to alfalfa yield. The alfalfa yields and crop N content were typical for the region (Cavero et al., 2017) and very similar to the values presented in the mentioned study performed close to our experimental site. At the conditions of the study, sprinkler irrigated alfalfa was not a significant source of CH₄ emissions. When fluxes were significantly different from zero they were mostly negative, suggesting a slight tendency to act as a CH₄ sink, probably due to the action of methanotrophic microbes under aerobic conditions. The seasonal average of CH₄ fluxes (-0.71 g C ha^-1 day^-1; SE=0.55) was similar to the reported value of -1.08 g C ha^-1 day^-1 by Ellert & Janzen (2008). The predominant aerobic conditions under sprinkler irrigated, that usually applies low rates of water to crops, precludes significant CH₄ emissions as it has been reported under similar soil and irrigation management conditions in other crops such as maize (Alvaro-Fuentes et al., 2016) and wheat (Mateo-Marín et al., 2020). According to Walkiewicz et al. (2018), low soil NH₄+ content increases CH₄ oxidation under aerated conditions, although the effect is very influenced by soil properties. Therefore, the low soil NH₄+ content found in our study could partially explain the slight tendency to methanotrophic activity observed in the alfalfa crop in some specific days when the negative CH₄ flux was significant.

N₂O fluxes tended to be lower during winter (i.e., from November to March), as found in other studies with other irrigated crops under similar climate conditions (Franco-Luesma et al., 2020), where besides low soil temperature, irrigation is usually not applied during the winter. N₂O emissions in sprinkler-irrigated alfalfa under our Mediterranean conditions (865 g N ha^-1 year^-1) were slightly lower than the reported under Midwestern US non-irrigated conditions (Goodroad et al., 1984; Osterholz et al., 2014) and similar to those obtained by Ellert & Janzen (2008) for sprinkler-irrigated alfalfa in Alberta (Canada) with similar soil texture, although with lower seasonal air temperature (6.2ºC). However, the N₂O emissions found in our study were clearly smaller than those reported by Burger et al. (2016) in a 5^th year alfalfa stand (5.26 kg N ha^-1 year^-1) and a 2th year alfalfa stand (2.26 kg N ha^-1 year^-1) under similar climatic conditions but under flood irrigation. The shorter period of time where the SWC is above field capacity under sprinkler irrigation as compared to flood irrigation could be the reason of the lower N₂O emissions found in our experiment, as found in maize in a nearby experiment (Franco-Luesma et al., 2020). Mateo-Marin (2020) reported 35% lower N₂O fluxes when wheat plants were included inside the chambers compared to trimmed plants. However, no significant effect was found in our study with alfalfa, with similar cumulative fluxes in 2016 and 2017, may be due to the deeper root system of alfalfa compared to wheat.

Although the daily average of WFPS in the topsoil during the two years was 54%, indicating the predominance of aerobic conditions in sprinkler-irrigated alfalfa, there were short periods of anaerobic conditions. Thus, over the two-year period of sprinkler irrigated alfalfa, during 1669 hours (79 days) the upper 10 cm of the soil presented WFPS values higher than 70%, and during a total of 187 hours (8 days) the topsoil presented a WFPS higher than 80%. A rapid response of N₂O fluxes to topsoil saturated conditions, due to irrigation or rainfall events, were observed in the automatic chambers experiment. There were also irrigation events that increased soil water content near to saturation but with no significant peaks of N₂O, indicating that availability of NO₃‾ or labile carbon can be limiting N₂O losses by denitrification, or promoting complete denitrification, i.e., N₂O reduction to N₂. However, Burger et al. (2016) did not find a relationship between dissolved organic carbon (DOC) concentration and N₂O fluxes in flooded-irrigated alfalfa, which suggest a complex interaction remaining to be clarified to fully understand the complex denitrification processes. Anyhow, only continuous or very frequent measurements can consistently detect these high peaks of N₂O flux, that are difficult to foresee in alfalfa because N fertilizer is not applied.

In agreement with the results reported by Beauchamp et al. (1996) and Burger et al. (2016), the largest N₂O fluxes observed in alfalfa (up to 263 g N ha^-1 day^-1) were related to significant irrigation or rainfall events (>20 mm). These large fluxes had a very short duration since they dropped to one third after three hours, and are difficult to observe, unless continuous measurement is made. That short-time large fluxes, in absence of N fertilizer applications and high soil NH₄+ content, can be associated to the N turnover from alfalfa roots and exudates, inducing both nitrification and denitrification and opportunity to N₂O emissions, depending on the SWC.

In both growing seasons, a large N₂O peak was observed at April-May, between the first and the second alfalfa harvest in the static chambers experiment. However, this early season peak of N₂O was much higher in 2017. A relatively long time period (28 days) without rain or irrigation, due to a problem with the pumping station, preceded this unique remarkable N₂O flux event. During this period, the soil experienced a sharp decrease in the WFPS (average of 29.7% from 13 to 19 April) and a sudden soil rewetting associated to irrigation the day before to the observed peak. Recent studies (Szukics et al., 2010; Bergstermann et al., 2011; Barrat et al., 2021), described very rapid responses of nitrifiers and denitrifiers to changes in soil moisture, that can partly explain the unique high-emission event detected during our experiment. Main findings from these studies are that the N₂O pulses after rewetting are mainly related to the drought intensity before the rewetting event. As demonstrated by Zhu et al. (2013), the coincidence of low oxygen availability with large soil NH₄+ concentration suggests that, the different ammonia oxidation pathways (nitrifier nitrification, nitrifier denitrification, and nitrification-coupled denitrification) can play a significant role in the observed N₂O peak. The observed peak in soil NH₄+ could also be explained by an event happened at the end of 2016 growing season. Thus, in November 22 (2016) a significant regrowth of alfalfa was chopped and left into the soil surface due to impossibility to get natural hay process. The decomposition of a relatively large amount of plant residues with low C/N composition and high WFPS could trigger a raising in soil NH₄+ as was described by López-Bellido et al. (2014) in Mediterranean conditions.

Our results also showed that the N₂O fluxes were significantly linked to CO₂ fluxes (C-mineralization) but the relationship differed according to the soil aeration status, as found by Samad et al. (2016). The observed year-averaged fluxes measured in the static chambers experiment were similar or lower than the basal fluxes from non N fertilized fields observed in other crops such as maize (mean=4.05 g N ha^-1 day^-1; Alvaro-Fuentes et al., 2016) and wheat (mean=2.80 g N ha^-1 day^-1; Mateo-Marín et al., 2020) under similar agroecological conditions.

In the static chambers experiment and manual air sampling, as probably happen in other similar studies, we were not able to sample during the hours immediately following irrigation or rainfall events due to the difficulty to move on saturated soils and to prevent human trampling on experimental areas near the chambers. This methodology can leave unnoticed short-duration N₂O peaks emissions that can be relatively frequent under sprinkler irrigated alfalfa (on average 34 irrigation events every year), leading to an underestimation of the cumulative N₂O emissions. However, as was showed in the 2017 alfalfa experiment, the static chamber methodology can also overestimate N₂O fluxes, attributing longer peak duration due to the large sampling interval. Therefore, the overall effect on cumulative emissions quite is unpredictable. However, the observed absence of N₂O peaks after some irrigation (or rainfall) events in which the WFPS surpassed 80-90% together with a significant lack of knowledge about denitrification kinetics (Samad et al., 2016) maintain considerable uncertainty about the overall contribution of these short-lived emission peaks in the whole growing season.

The spring incorporation of a large amount of low C/N residue after alfalfa termination induced a higher microbiological activity (higher soil respiration rate) compared to the incorporation of a higher C/N residue observed in an adjacent maize cropped field. Pascault et al. (2013) demonstrated that the biochemical composition of the fresh residue added to the soil has a significant impact on the type of microbial communities that are stimulated to degrade the fresh organic matter with greater respiration rate after incorporating alfalfa residues compared to wheat residues with higher C/N ratio. In our experiment this effect was also observed with higher CO₂ emissions after incorporating alfalfa (613 kg C ha^-1; SE=47) than after incorporating maize (296 kg C ha^-1; SE=35) in the 57-days period after residue incorporation.

According to a recent meta-analysis (Charles et al., 2017) the C/N ratio of crop residues has a significant impact on N₂O emissions. A lower C/N ratio results in a higher N₂O emission. However, contrary to the mentioned study and our initial hypothesis, N₂O emissions were not significantly affected by the type of residue, even when in the maize-stubble field the soil NO₃‾ concentration was significantly lower than in the alfalfa-residue field. Although the N₂O fluxes were relatively low (< 5 g N-N₂O ha^-1 day^-1), we cannot discard larger fluxes of other N gases such as N₂, specially at higher WFPS conditions and for high soil pH soils, as found by Pu et al. (1999). Large N₂ losses are unimportant from a GHG contribution perspective but are of interest if considered as N lost from the soil-crop system.