The field campaign was conducted at the Shouxian National Climatology Observatory (32°25^′ N, 116°47^′ E; 25 m above sea level), located 9 km south of Shouxian, Anhui (Fig. S1 in the Supplement). This location represents a typical rice–wheat rotation ecosystem in the Huang–Huai agroecological region, which serves as the primary grain production area in China, contributing to 18 % of the nation's total grain production. Additionally, it is responsible for 76.3 % of the country's total nitrogen fertilizer application (Cao et al., 2019). The site covers a 17 ha field and is dedicated to the cultivation of rice–wheat rotations. It serves as an experimental site for studying surface–atmosphere exchange. The site is situated amidst other agricultural fields, with a low-traffic road to the north (250 m). The region has a prevailing subtropical monsoon climate, characterized by distinct seasons, with high temperatures and rainfall occurring in the same season. The average annual temperature is 14.8 °C, and the average annual precipitation amount is 905 mm.

The flux measurements were conducted from 1 June to 14 July 2021, immediately following the winter wheat harvest on 31 May 2021. The tillage process took place over 11 d, from 2 to 13 June, followed by periods of flood irrigation and fertilization with a compound fertilizer (N–P₂O₅–K₂O (15 %–15 %–15 %)), applied at a rate of 67.5 kg N ha⁻¹, before 22 June 2021. Consequently, the surface was a mixture of bare soil and sparse winter wheat residues before irrigation took place (09:00 LT on 13 June; hereafter, all times are given in local time), while the soil became waterlogged after flood irrigation. The paddy seedlings were transplanted on 26 and 27 June at a density of 1.8×105 plants ha⁻¹ and grew from 0.14 m to approximately 0.22 m during the campaign. Additionally, irrigation was employed following the paddy transplantation to mitigate water deficiency during the growth phase, thereby preventing the potential mortality of paddy seedlings. The 46 % N urea solution (69 kg N ha⁻¹) was applied as a top dressing on 10 July.

Concentrations of HONO and NO₂ in the ambient air were measured using a homemade BBCEAS instrument with a time resolution of 1 min and detection limits of 54 pptv (2σ) for HONO and 98 pptv (2σ) for NO₂. The measurement uncertainties were 8.7 % for HONO and 8.1 % for NO₂. Further details regarding the BBCEAS, such as its principle, instrument parameters, and quality control, are described in detail elsewhere (Duan et al., 2018; Tang et al., 2019). NO was measured using a custom-built chemiluminescence instrument (Model 42i-TL, Thermo Fisher Scientific, USA), and O₃ was measured using Model 49i (Thermo Fisher Scientific), with detection limits of 50 pptv for NO and 500 pptv for O₃. Measurements of soil temperature and moisture, as well as meteorological and micrometeorological parameters, are presented in Sect. S1 in the Supplement.

Trace gas profiles of HONO, NO, and NO₂ were obtained using inlets positioned at heights of 0.2 and 1.6 m, which were adjusted to 0.3 and 1.6 m, respectively, on 27 June to accommodate the canopy height, ensuring they consistently exceeded the canopy height throughout the campaign (Fig. 1). Two BBCEAS instruments were used to measure HONO and NO₂ at different heights. They were intercompared several times throughout the campaign and exhibited excellent agreement (R2=0.989 for HONO and R2=0.998 for NO₂), with slopes close to 1 (Fig. S2). An NO_x analyzer for NO measurements was connected to a Teflon solenoid valve to enable sequential measurements at two different heights. All instruments were placed in a thermostated container controlled by an air conditioner, with external sampling inlets affixed to a small mast. The sampling inlets were oriented away from the mast and toward the prevailing wind direction to minimize turbulence disruption. To prevent photolysis and the condensation of water vapor, the perfluoroalkoxy (PFA) inlet lines (7.5 m in length with a 6 mm external diameter) were shielded from radiation and slightly heated using heating tape, with the heating temperature set to about 30 °C.

The HONO, NO, and NO₂ fluxes were calculated using the AG method at time intervals of 30 min, as elaborated upon in previous studies (Laufs et al., 2017; Meng et al., 2022; Stella et al., 2012) and briefly introduced here. The flux (Fχ) of trace gas is calculated from the friction velocity (u∗) and the mixing-ratio scaling parameter (χ∗) as follows: 1Fχ=-u∗χ∗, where u∗ is calculated from eddy covariance measurements and χ∗ is defined using the stability-corrected gradient of the scalar mixing ratio (χ) and height (z) as 2χ∗=κ⋅∂χ∂lnz-d-ΨHz-dL. The fluxes (FHONO,NO,andNO2) of trace gases at the geometric mean height can be expressed as 3FHONO,NO,andNO2=-κ⋅u∗⋅∂cHONO,NOandNO2∂ln⁡z-d-ΨHz-dL, where κ is the von Kármán constant (κ=0.4), z is the height above the ground, d is the zero-plane displacement (taken as 2/3⋅hc, where hc is the canopy height), L is the Obukhov length, and ΨH is the integrated stability correction function for scalars (Sutton et al., 1993).

Data from all instruments could not always be collected simultaneously for flux calculations due to various factors, such as calibration, malfunction, and disturbances from agricultural activities. Consequently, the affected data were excluded when calculating fluxes. The dataset used for the determination of HONO, NO, and NO₂ fluxes comprised 68 % of the HONO data, 81 % of the NO data, and 86 % of the NO₂ data. The total uncertainty in the flux is composed of the gradient error and the friction velocity error (Laufs et al., 2017; Meng et al., 2022). The average uncertainties for HONO, NO, and NO₂ fluxes (each calculated using the median of the 25th–75th percentile range) corresponded to 11 %, 16 %, and 20 %, respectively. Furthermore, the fluxes were discarded under very stable conditions with low wind speeds and friction velocities. It is important to note that HONO, NO, and NO₂ are subject to chemical reactions, which may lead to a vertical divergence of flux between the surface and the measurement height. The influence of chemical reactions during turbulent transport was checked utilizing the Damköhler number (DA), as detailed in Sect. S2. The divergence caused by chemical reactions of HONO could be neglected when interpreting the potential sources of HONO and the driving factors of HONO flux. DA values for the NO–O₃–NO₂ triad were generally less than 1; however, a sharp increase in flux divergence occurred when DA values became greater than 1 (Stella et al., 2012). Additionally, the upward NO₂ flux exhibited a significant correlation (R=0.82) with NO flux, suggesting that the upward NO₂ flux could be attributed to the reaction of NO and O₃. Consequently, in light of the influence of chemical reactions on the fluxes of NO and NO₂, these fluxes (5.9 % for NO flux and 10.5 % for NO₂ flux) were excluded from subsequent analysis.

Time series of meteorological parameters recorded throughout the observation period are shown in Fig. 2. The campaign weather was dominated by sunny days, with 64 % of the days having a daily maximum global radiation level above 700 W m⁻². Ambient temperature ranged from 17.0 to 36.6 °C, and soil temperature ranged from 20.0 to 34.8 °C, with average values of 26.8±3.5 and 26.5±2.7 °C, respectively. The relative humidity (RH) ranged from 22 % to 98 %, and the soil water-filled pore space (WFPS) ranged from 44 % to 88 %, with average values of 77%±17% and 69%±15%, respectively. The average wind speed was 3 m s⁻¹, with a maximum wind speed of 11.0 m s⁻¹ occurring during the rotary tillage period. The PM_2.5 concentration varied from 1 to 100 µg m⁻³, with its daily average value remaining below the Class II threshold of the Chinese National Ambient Air Quality Standard (75 µg m⁻³). Intermittent rainfall occurred from 13 June to 5 July, with a total precipitation amount of 186.1 mm. Notably, after irrigation of the agricultural field on 13 June, the WFPS increased from 45 % to 80 %.

The field campaign was conducted across various agricultural-management activities, including rotary tillage (2–13 June), flood irrigation (13–19 June), fertilization (19–21 June), paddy cultivation (26–27 June), and top dressing (10 July). Figure 3 illustrates the time series of HONO, NO, NO₂, and O₃ mixing ratios. Throughout the campaign, ambient O₃ concentrations varied from 0.54 to 131.57 ppbv, with an average of 48.44±26.29 ppbv. The peak NO mixing ratio reached 36.02 ppbv during rotary tillage, and the average mixing ratios of NO at lower (0.2–0.3 m) and upper (1.6 m) levels were 0.75±2.21 and 0.46±1.16 ppbv, respectively. Higher NO mixing ratios were measured at the lower level, likely due to soil NO emissions caused by microbiological activity (Bargsten et al., 2010; Ludwig et al., 2001). Moreover, the average NO₂ mixing ratios were 4.48±4.96 and 4.75±4.38 ppbv at the lower and upper levels, respectively. The synchronous peaks of NO and NO₂ and the decrease in O₃ (e.g., in the early hours of 7 June) indicate that NO release from soil may react rapidly with O₃ to form NO₂. Ambient HONO mixing ratios ranged from below detection limits to 3.60 ppbv at the lower level and 2.36 ppbv at the upper level, with averages of 0.46±0.59 and 0.37±0.37 ppbv, respectively. The average HONO / NO_x ratio of 0.079±0.059 was significantly higher than the values in the range for direct emissions from vehicle exhausts, as reported in previous studies (0.003–0.018) (Kirchstetter et al., 1996; Kurtenbach et al., 2001; Liang et al., 2017; Liu et al., 2017; Nakashima and Kajii, 2017; Nakashima and Kondo, 2022), and was comparable to the value observed for summer agricultural fields in the NCP (0.0929; Song et al., 2022). Notably, successive HONO peaks were measured during rotary tillage, with HONO mixing ratios reaching 3.60 ppbv at the lower level. These values exceeded those observed during the winter at the same site (Meng et al., 2022) and were comparable to observations at suburban sites in the Pearl River Delta (Li et al., 2012; Su et al., 2008) and those at rural sites in the NCP (Xue et al., 2020). However, HONO levels declined rapidly following flood irrigation (see Fig. 3 and Table 1). After fertilization and top dressing, a noticeable rise in HONO levels was observed, which can be attributed to the increase in HONO release due to fertilizer application at high levels of water content (Tang et al., 2019; Wang et al., 2021; Wu et al., 2019; Xue et al., 2019). Nevertheless, these levels were significantly lower than the mixing ratios observed during rotary tillage.

The fluxes of HONO, NO, and NO₂ determined by the AG method are illustrated in Fig. 3. Upward fluxes were commonly observed for HONO and NO, while NO₂ was deposited on the ground. The magnitude of observed HONO fluxes ranged from -0.70 to 1.86 nmol m⁻² s⁻¹, with an average of 0.07±0.22 nmol m⁻² s⁻¹, which falls within the range of HONO flux measurements for rural and suburban regions reported in the literature (see Table 2). Upward HONO fluxes were mostly observed during rotary tillage, reaching up to 1.86 nmol m⁻² s⁻¹. After irrigation, an increase in soil moisture content (∼80% WFPS) led to a significant reduction in HONO flux. Previous laboratory studies have also demonstrated that lower levels of HONO flux at high water-holding capacities, low gas diffusion rates, and high solubility levels could limit the release of HONO from soil (Ermel et al., 2018; Meusel et al., 2018; Wu et al., 2014). Observations from before and after irrigation demonstrate the regulatory role of soil moisture in the HONO exchange process, which has been systematically investigated in previous studies by examining HONO emission flux as a function of soil moisture (Mamtimin et al., 2016; Wang et al., 2021). Soil moisture determines whether nitrification or denitrification processes dominate gas emissions and strongly influences the corresponding gas emission rates and concentration compensation points (Cheng, 2013). Several laboratory findings indicate that nitrification under conditions of low soil moisture is the dominant process behind HONO emissions (Oswald et al., 2013; Scharko et al., 2015), and field observations of HONO have predominantly focused on dryland ecosystems (Ren et al., 2011). Conversely, Wu et al. (2019) demonstrated that soil with a high water content (with a 75 %–140 % water-holding capacity (WHC)) can also exhibit substantial emissions of HONO, with the average ratio of the highest HONO flux during the wet peak to that during the dry peak being approximately 30 %. However, actual field observations have revealed that HONO fluxes are very low (close to zero) under conditions of high water content, which may be attributed to the influence of soil moisture on microbial metabolic activity and gas diffusion in the soil (Hu et al., 2015; Linn and Doran, 1984). Furthermore, Wang et al. (2021) reported the promoting effect of fertilization on HONO flux under conditions of high soil moisture (75 %–95 % WHC). Nevertheless, we did not observe this phenomenon in our field experiments conducted in paddy fields. This discrepancy is probably attributed to the anaerobic or microaerobic conditions created by pre-fertilization irrigation, which exerted a greater inhibitory effect on the nitrification process than the promoting effect of fertilization. Currently, the estimation of HONO flux at the regional scale relies more on laboratory research findings (Gan et al., 2024; Wu et al., 2022). This study highlights discrepancies between laboratory and field observations corresponding to high levels of soil water content, which pose significant challenges to the uncertainty in estimation results.

The agricultural field acted as a well-known source of atmospheric NO, with an average flux of 0.19±0.53 nmol m⁻² s⁻¹ observed in this study. Similar to HONO fluxes, upward NO fluxes were mostly observed during rotary tillage, with a maximum flux of 9.12 nmol m⁻² s⁻¹ during the early morning (Table 1). This finding is consistent with previous studies that show that tillage increases NO emissions (Chatskikh and Olesen, 2007; Fang et al., 2006; Fang and Yujing, 2009; Liu et al., 2005; Pinto et al., 2004; Sehy et al., 2003; Yao et al., 2009; Yamulki and Jarvis, 2002). However, the NO fluxes were close to zero when the paddy field was waterlogged, probably because the nitrification process that dominates NO production in soil was greatly hindered in water-saturated soil and at anoxic microsites (Fang and Yujing, 2009). Similarly, we also did not observe significant emissions of HONO under sustained conditions of high moisture. The coinciding peaks in HONO flux and NO flux during rotary tillage suggest that HONO release from soil, similar to NO release, is associated with microbial activity in the soil (Bargsten et al., 2010; Skiba et al., 1993). Furthermore, notably elevated fluxes of HONO and NO were observed during rotary tillage compared to other phases of agricultural activities (Fig. S3). The higher emission rates of NO and HONO may account for the successive peaks in their concentrations and fluxes. Similar to NO emission, the emission of HONO from soil may be significantly stimulated by soil tillage. Additionally, an average NO₂ flux of -0.42±0.44 nmol m⁻² s⁻¹ (with flux values ranging from -3.50 to 0.50 nmol m⁻² s⁻¹) indicates that the agricultural field acted as a sink for atmospheric NO₂ (Fang and Yujing, 2009; Tang et al., 2020).

Diurnal variations in NO₂ photolysis frequency (J(NO₂)), air temperature, relative humidity, soil temperature, WFPS, NO flux, NO₂ flux, and HONO flux are illustrated in Fig. 4. The diurnal HONO flux exhibited no discernible diurnal pattern throughout the entire campaign, similar to the diurnal profile observed during BEARPEX 2009 in California (Ren et al., 2011). Significant HONO emissions were primarily observed during rotary tillage, and their daily pattern is depicted in Fig. 4. Upward HONO fluxes were observed throughout the day, with a maximum value of 0.55 nmol m⁻² s⁻¹ in the early morning. Distinct HONO emissions were observed in the morning after sunrise. Moreover, the magnitudes of the daytime fluxes (0.25±0.13 nmol m⁻² s⁻¹) were comparable to the nocturnal values (0.27±0.13 nmol m⁻² s⁻¹). The diurnal profile of NO flux exhibited consistent levels of NO emissions throughout the day, except during a noticeable peak in the early morning. It is worth noting that synchronous peaks in HONO flux and NO flux were observed in the morning. Unlike for the fluxes of HONO and NO, deposition was the prevailing process for NO₂ flux. A greater downward NO₂ flux of -0.85±0.27 nmol m⁻² s⁻¹ (-0.57±0.23 nmol m⁻² s⁻¹ at night) was observed during the daytime, potentially due to an increase in the dry-deposition velocity of NO₂ during the day.

Throughout the rotary tillage period, the emissions of HONO and NO were significant, with maximum fluxes reaching 1.86 nmol m⁻² s⁻¹ for HONO and 9.12 nmol m⁻² s⁻¹ for NO. The concurrent peaks in HONO and NO fluxes indicate that HONO emissions may originate from soil sources as it is well established that NO is primarily generated by and released from soil microbial processes (Feig et al., 2008; Rende et al., 1989). As shown in Fig. 5, a significant correlation (R=0.77) was observed between the fluxes of HONO and NO during the rotary tillage period, suggesting a shared source for both gases. This could be attributed to the generation and release of HONO and NO via soil microbial processes, aligning with the results reported by Tang et al. (2020). A Gaussian fitting was employed to analyze variations in HONO and NO fluxes with soil temperature (Fig. S4). It was found that both HONO and NO exhibited maximum emission fluxes at approximately 25 and 24 °C, respectively, which correspond to the optimal temperature (25 °C) for soil microbial nitrification and denitrification processes (Agehara and Warncke, 2005; Fang and Yujing, 2009). This finding further supports the hypothesis that HONO is generated by and released from soil biological processes. Additionally, there was an indication of an elevation in HONO flux during periods of intense solar radiation in the morning. Although the correlations between HONO flux and NO₂, J(NO₂), or NO₂ fluxes were found to be low (R=0.28, 0.12, and 0.25, respectively), we observed a significant correlation (R=0.60) between HONO flux and the product of J(NO₂) × NO₂ (Fig. 6), as well as a moderate correlation (R=0.41) between HONO flux and the product of J(NO₂) × NO₂ flux (Fig. S5). This indicates that light-induced NO₂ conversion serves as an important source of HONO during the day. Furthermore, another mechanism of acid displacement can be ruled out as the major strong acid, HNO₃, is primarily generated during the daytime and subsequently deposited on the ground. Consequently, the peak of the HONO source is expected to occur in the afternoon (Vandenboer et al., 2015). Finally, the results indicate that both mechanisms – release from soil biological processes and that from light-induced NO₂ conversion – are likely active, together affecting the diurnal HONO flux pattern.

In Sect. 3.3, we presented the potential sources of HONO flux during rotary tillage by conducting a correlation analysis. Here, we will further calculate the specific contributions of HONO sources through a budget analysis. The HONO budget can be derived from known HONO sources and sinks, and the potential unknown HONO source during rotary tillage was estimated. The lower-level data that better describe ground source processes were used for the budget analysis. In this study, the investigated HONO sources included the homogeneous reaction (POH+NO) and the heterogeneous reactions of NO₂ on the aerosol surface and that on the ground surface (Paerosol and Pground, respectively). The HONO sinks included the reaction of HONO with OH (LOH+HONO), the photolysis of HONO (Lphoto), and the dry-deposition loss of HONO (Ldep). The calculations of HONO sources and sinks, as well as the estimates of the mixing-layer height (MLH), are described in detail in Sect. S3. 4dHONOdt=POH+NO+Punknown+Paerosol+Pground-LOH+HONO+Lphoto+Ldep Simplifying Eq. (4), dHONO/dt is approximated by ΔHONO/Δt. Then, Eq. (4) becomes Eq. (5) as follows: 5Punknown=ΔHONOΔt+LOH+HONO+Lphoto+Ldep-POH+NO-Paerosol-Pground. The average production and loss rates for the diurnal HONO budget are shown in Fig. 7. The homogeneous reaction of NO and OH accounted for 12.8 % of HONO production, with an average POH+NO value of 0.15±0.10 ppbv h⁻¹. The heterogeneous conversion of NO₂ on the ground surface accounted for 12.4 % (0.1±0.07 ppbv h⁻¹) of HONO production at night. Paerosol (0.01±0.006 ppbv h⁻¹) was negligible compared to other HONO sources due to its relatively small aerosol surface area (Fig. S6). Photodecomposition (Lphoto) was the primary sink of HONO during the daytime, with a peak of 2.03 ppbv h⁻¹ at 11:00 and an average of 1.44±0.69 ppbv h⁻¹, while LOH+HONO was very small and accounted for less than 5 % of Lphoto. The dry deposition of HONO (Ldep) was influenced by the mixing-layer height (MLH) and dominated the loss of HONO at night, with a rate exceeding 0.6 ppbv h⁻¹. Punknown exhibited an obvious diurnal variation, with higher values during the daytime (1.31±0.54 ppbv h⁻¹) and lower values at night (0.53±0.25 ppbv h⁻¹). The peak of Punknown occurred from 07:00–12:00, with a maximum value of 2.18 ppb h⁻¹. The peak value of Punknown is comparable to the value measured in Taizhou (2.5 ppbv h⁻¹) (Ye et al., 2023) and larger than the values measured in Wangdu (0.62 ppbv h⁻¹) (Song et al., 2022) and Nanjing (1.04 ppbv h⁻¹) (Liu et al., 2019a). Similar to the observed asymmetry around noon reported in previous studies, this could be attributed to the combined effect of solar radiation and variations in precursor NO₂ (Song et al., 2022; Xue et al., 2022). Due to the significantly larger unknown source strength of HONO during the daytime, we focused on analyzing the unknown source of HONO during the day. Based on the above analysis, we evaluated the contribution of the photo-enhanced heterogeneous pathways.

The coefficients widely adopted in previous studies generally range from 10⁻⁶ to 10⁻⁴ (Chen et al., 2023; Liu et al., 2019b; Song et al., 2022; Wong et al., 2013). Here, we used 1×10-5 for the photo-enhanced uptake coefficients (γa+hv and γg+hv) to calculate Paerosol+hv and Pground+hv (Qin et al., 2023; Xue et al., 2020). As shown in Fig. 8, the average Paerosol+hv and Pground+hv values were 0.02±0.009 and 0.53±0.50 ppbv h⁻¹, respectively, during the day, accounting for 1.4 % and 40.2 % of Punknown, respectively. Moreover, Paerosol+hv was a negligible source of daytime HONO formation. The photo-enhanced NO₂ heterogeneous reaction on the surface matched the calculated Punknown value and effectively explained the HONO budget for the morning. Furthermore, a higher photo-enhanced uptake coefficient of 3.5×10-5 was adopted as the upper limit for calculating the production of the photosensitive conversion of NO₂ (Chen et al., 2023). The calculation results demonstrated that the daytime value of Punknown could be explained when the upper limit of the photo-enhanced uptake coefficient was used (Fig. S8).

However, there could be other light-driven reaction pathways for producing HONO in the afternoon, as indicated by the diurnal variation in Punknown. Previous studies have demonstrated that the photolysis of pNO₃ / HNO₃ can contribute to HONO production (Chen et al., 2023; Laufs et al., 2017). Recently, Chen et al. (2023) found that the photolysis of HNO₃ at the surface interface could effectively explain the observed Punknown value for the afternoon. However, the lack of information about HNO₃ concentration prevents us from directly estimating the contribution of HNO₃ photolysis in the present study. Future studies should include measurements of pNO₃ / HNO₃ to better characterize the contribution of this potentially important HONO formation pathway.

Based on the measured fluxes, we also estimated the HONO emission rate from soil (Psoil). The nighttime HONO fluxes ranged from 0.15 to 0.43 nmol m⁻² s⁻¹, with corresponding HONO flux rates of 0.32 to 0.79 ppbv h⁻¹; these values were sufficient for explaining Punknown (ranging from 0.012 to 0.90 ppbv h⁻¹). Therefore, light-induced HONO sources (i.e., the photosensitive conversion of NO₂ and photolysis of pNO₃ / HNO₃) and soil emissions may together serve as significant HONO sources in agricultural fields, thereby influencing the overall atmospheric HONO budget.

The significant increase in atmospheric HONO from agricultural fields can enhance the formation of OH radicals via the photolysis of HONO (see the detailed OH production rate calculation in Sect. S4). Figure 9a exhibits the OH production rates from the photolysis of HONO (P(OH)HONO) and O₃ (P(OH)O3). P(OH)HONO and P(OH)O3 were found to be 0.82 and 1.49 ppbv h⁻¹, respectively, meaning they were significantly higher than the corresponding winter levels at the same site (Fig. S9). The higher O₃ concentration in summer plays a primary role in the generation of OH radicals through daytime O₃ photolysis, accounting for 70 % of the total OH production rate. However, the contribution of P(OH)HONO, approximately 30 %, is still significant and cannot be ignored.

During the rotary tillage period, continuous peaks in HONO concentration and flux were observed, with maximum values of 3.06 ppbv and 1.86 nmol m⁻² s⁻¹, respectively. P(OH)HONO was calculated to be 1.42 ppbv h⁻¹, and P(OH)O3 was determined to be 1.35 ppbv h⁻¹, accounting for 51 % and 49 % of the total OH production rate, respectively (Fig. 9b). P(OH)HONO dominated in the early morning, with a value of 2.48 ppbv h⁻¹, while P(OH)O3 became the main source at midday, with a value of 2.74 ppbv h⁻¹. The comparable peak magnitudes of P(OH)HONO and P(OH)O3 indicate that HONO photolysis is an important source of daytime OH radicals. Furthermore, the peaks in both P(OH)HONO and HONO flux co-occur in the early morning, revealing the significant contribution of agricultural HONO emissions to the regional atmospheric oxidation capacity of the Huaihe River Basin.