Nitrogen in Atmospheric Wet Depositions Over the East Indian Ocean and West Pacific Ocean: Spatial Variability, Source Identification, and Potential Influences

Atmospheric deposition is the dominant pathway for the loading of exogenous nitrogen (N) to open ocean. Here, rainwater samples were collected from 31 stations in the equatorial East Indian Ocean (EIO) and West Pacific Ocean (WPO) to explore the spatial variability of N species, potential sources, and related ecological influences. Among two oceans, nitrate (NO3–) and ammonium (NH4+) were the main components in the rainwater N inventory. NO3– concentrations varied from 0.19 to 100.5 μM, whereas NH4+ concentrations ranged from 0.54 to 110.6 μM. Among all stations, low concentrations of NO3– and NH4+ appeared in the remote ocean, whereas high concentrations were observed at the stations near the Malacca Strait and New Guinea, coupled with an enhancement of non-sea salt major ions, e.g., calcium ions (Ca2+) and sulfate (SO42–), revealing the influence from coastal human activities, such as coal and gasoline combustion. In the remote ocean, δ15N–NH4+ ranged from −5.7 to −9.3‰, whereas it dropped to -15.5‰ near coasts. A logarithmic decay between δ15N–NH4+ and NH4+ concentrations in rainwater samples was obtained, suggesting a shift from natural source (seawater emission) in oceanic precipitation events to anthropogenic source (chemical fertilizer volatilization and vehicle exhaust) in coastal rainwaters. δ15N–NO3– in the remote ocean varied between −1.7 and 0.4‰ with low levels found in the WPO, likely related to the ascending air flow driven by the Walker Circulation. In coastal oceans, δ15N–NO3– ranged from 1.5 to 3.5‰. The linkage between δ15N–NO3– and NO3– concentrations varied in two oceans, resulting from difference in biological and fossil fuel combustion contributions. Compared with ocean surface water, N in the rainwater was markedly enriched, suggesting that N from atmospheric wet depositions could rapidly enhance the dissolved N availability in ocean surface water. However, the N redundancy according to the Redfield–Brzezinski ratio (N:Si:P = 16:16:1) in the rainwater might benefit from the growth of N-preference phytoplankton species and microbes. As the first study on N concentrations, sources, and stoichiometry balance in rainwater over the equatorial WPO and EIO, the results could be a support to the global N budget estimation and oceanic primary production modeling.

Atmospheric deposition is the dominant pathway for the loading of exogenous nitrogen (N) to open ocean. Here, rainwater samples were collected from 31 stations in the equatorial East Indian Ocean (EIO) and West Pacific Ocean (WPO) to explore the spatial variability of N species, potential sources, and related ecological influences. Among two oceans, nitrate (NO 3 − ) and ammonium (NH 4 + ) were the main components in the rainwater N inventory. NO 3 − concentrations varied from 0.19 to 100.5 µM, whereas NH 4 + concentrations ranged from 0.54 to 110.6 µM. Among all stations, low concentrations of NO 3 − and NH 4 + appeared in the remote ocean, whereas high concentrations were observed at the stations near the Malacca Strait and New Guinea, coupled with an enhancement of non-sea salt major ions, e.g., calcium ions (Ca 2+ ) and sulfate (SO 4 2− ), revealing the influence from coastal human activities, such as coal and gasoline combustion. In the remote ocean, δ 15 N-NH 4 + ranged from −5.7 to −9.3 , whereas it dropped to -15.5 near coasts. A logarithmic decay between δ 15 N-NH 4 + and NH 4 + concentrations in rainwater samples was obtained, suggesting a shift from natural source (seawater emission) in oceanic precipitation events to anthropogenic source (chemical fertilizer volatilization and vehicle exhaust) in coastal rainwaters. δ 15 N-NO 3 − in the remote ocean varied between −1.7 and 0.4 with low levels found in the WPO, likely related to the ascending air flow driven by the Walker Circulation. In coastal oceans, δ 15 N-NO 3 − ranged from 1.5 to 3.5 . The linkage between δ 15 N-NO 3 − and NO 3 − concentrations varied in two oceans, resulting from difference in biological and fossil fuel combustion contributions. Compared with ocean surface water, N in the rainwater was markedly enriched, suggesting that N from atmospheric wet depositions could rapidly enhance the dissolved N availability in ocean surface water. However,

INTRODUCTION
Nitrogen (N) is essential for the biosynthesis of amino acids, phospholipid, nucleic acids, etc. Since preindustrial times, the reactive N storage in the biosphere has rapidly increased due to anthropogenic N fixation (Kuypers et al., 2018). Given the high solubility and chemical activity, reactive N intensively transports among different systems in the biosphere (Galloway et al., 2008). Though the importance in biological actives, excessive N frequently leads to negative ecological feedbacks, especially in aquatic systems, such as harmful algae blooms, benthic hypoxia, and phytoplankton community succession. Accordingly, N cycling with regard to transport and transformation receives great attention from the scientific community.
On a global scale, the magnitude of N deposition flux to terrestrial systems is relatively well gauged based on monitoring projects in continents (e.g., Loÿe-Pilot et al., 1990;Fenn et al., 2003;Duan et al., 2016). In contrast, the impacts of N deposition to oceans are less evaluated, with sporadic measurements and limited spatial coverage archived in the past several decades (e.g., the tropical Atlantic Ocean, Baker et al., 2007; Bermuda, Altieri et al., 2013;the North Pacific Jung et al., 2013). In those unexplored oceans, our knowledge of atmospheric N deposition, with regard to concentration, species, and sources, is highly scarce. This knowledge gap adds great uncertainties in global N budget estimations, such as oceanic N storages and N reaction rates. In addition, the limitation of oceanic N deposition data also produces the difficulty in ecological explanation on the variability of N-related phytoplankton community structure (Li et al., 2015). Furthermore, the lack of oceanic N deposition data also hampers the understanding of carbon cycles because of the reaction linkage of the sequestration capability of atmospheric CO 2 via primary producers (Capone, 2001).
In the present study, wet deposition (rainwater) samples from two cruises covering tropical areas in the East Indian Ocean (EIO) and West Pacific Ocean (WPO) were obtained ( Figure 1A). The sampling area in the EIO is adjacent to the Peninsular Thailand and Indonesia Archipelagoes on the east and the Indian Subcontinent and Sri Lanka on the north. In those regions, dense population (>1.5 billion) and intensive agriculture/manufacture are characterized. From May to September, the south-west monsoon introduces significant precipitation to South Asia, whereas the east wind from November to April introduces substantial land-derived matter from the Indian Subcontinent to the EIO (Sinha et al., 2019). For the sampling region in the WPO, it is surrounded by tropical islands, e.g., Guam, Borneo, and New Guinea. Walker Circulation (latitudinal) and Hadley Circulation (meridional) related east wind is prevailing at the eastern boundary of this sampling region, whereas the west wind from the Sulawesi Sea introduces terrestrial compounds derived from the Borneo and Indonesian islands (Supplementary Figure S1). The equatorial EIO and WPO have been identified as global sea ranches for tuna and squid catching more than 30 years (Takashi and Tsukada, 1988), whereas the primary productivity in seawater frequently remains a low level due to oligotrophic status (Supplementary Figure S2). During these two cruises, 31 rainwater samples ( − during these precipitation events (e.g., volatilized fertilizer, vehicle exhaust, and lighting production) according to their significant variability in isotopic fractions (e.g., Felix et al., 2015;Elliott et al., 2019;Zeng et al., 2019). Together with the backward trajectory mode from the National Oceanic and Atmospheric Administration (NOAA) (Figure 1A), we aimed to: (1) determine the spatial variability of N species in wet precipitations in the equatorial EIO and WPO and dynamic linkage with the Walker Circulation and Hadley Circulation; (2) identify potential sources of rainwater N and evaluate the influence of anthropogenic activities from adjacent coasts on rainwater N inventory; and (3) explore the potential ecology/environment impacts from wet deposition derived N on the equatorial EIO and WPO.

Sample Collection
The EIO cruise was conducted from 17th March 2018 to 12th May 2018 on the Shiyan III R/V, whereas the WPO cruise ranged from 15th November 2018 to 30th January 2019 on the Kexue R/V. Atmospheric temperature and wind speed were automatically recorded on board during both campaigns. Rainwater samples were collected with an acid-prewashed container at an open area of the top deck. The collection ranged from 2 to 6 h in each site. After rainwater gathering, the precipitation amount (unit: mm) was estimated, and then the collected rainwater was used for filtration and pH measurement (sketch in Figure 1B). The filtration was conducted at aircleaning environment, using polycarbonate membrane filter FIGURE 1 | Sampling sites in both EIO and WPO cruises (A), the dash lines indicate 72 h transport pathway of atmospheric particles at an altitude of 1,000 m (back-trajectory analysis). (B) Sketch of the sampling procedure, including atmospheric blank analysis (only WPO) and rainwater collection/filtration.
(0.4 µm pore size, Whatman R ). The filtrate was stored in acidprewashed high-density polyethylene (HDPE) bottles at −20 • C environment for major ions, nutrients, and N stable isotope fractions. Water stable isotope samples were stored in air-tight vacutainers at 4 • C environment (Jiang et al., 2017). Occasionally, the volume of collected rainwater was limited. In these cases, nutrients and major ions collection were priority targets. The pH of the rainwater (unfiltered) was measured with a calibrated WTW multi-function probe (350 type, Germany) on board. After each collection, the sampling container was cleaned using ethanol (analytical reagent purity) and deionized (DI) water (resistance: 18.2 M .cm) and then resettled on the top deck. In total, 13 rainwater samples were collected from the EIO cruise (E1-E13), and 18 rainwater samples were obtained from the WPO cruise (W1-W18; Figure 1A). In addition, during both cruises, a series of blank experiments was conducted to quantitively determine the bias introduced from the filtration system (test 1st and 2nd) and seawater spray on the collected rainwater (test 3rd-6th).
In practice, 100 ml DI water was filtered and then stored in acid-prewashed sampling bottles to determine the bias from the filtration system. For the seawater spray influence, approximately 500 ml DI water was injected into the container and received sunlight exposure at the sampling spot for 1 (3rd, 4th, 5th) and 3 days (6th). Subsequently, the water was filtered and analyzed with rainwater samples together. Notably, the filtration blank was conducted in both EIO and WPO cruises, whereas the spray effect was only determined in the WPO.

Chemical Analyses
After thawing, concentrations of NH 4 + , NO 2 − , NO 3 − , soluble reaction phosphorus (SRP), and dissolved silicate (Si) in water samples were determined on a flow injection system (SKLAR + +, the Netherlands) with the standard colorimetric approach. The method precision for all species was <5%. The concentration of total dissolved nitrogen (TDN) and total dissolved phosphorus (TDP) was quantified on the identical system after 30 min at 121 • C digestion with alkaline potassium persulfate solution. Dissolved organic nitrogen (DON) and dissolved organic phosphorus (DOP) were assumed to be the concentration difference between TDN and dissolved inorganic nitrogen (DIN), as well as TDP and SRP, respectively . Both δ 15 N-NO 3 − and δ 18 O-NO 3 − were determined via transforming NO 3 − to N 2 O using a denitrifier with the reference of USGS-32, USGS-34, and IAEA-N3 (Sigman et al., 2001) after removing NO 2 − (Weigand et al., 2016). The produced N 2 O was concentrated in a Thermo-Fisher Precon system at liquid nitrogen environment, and the signal of N 2 O was detected in a Thermo-Fisher Delta V Advantage Isotope Mass Spectrometer (Jin et al., 2020). The method detection limit was approximately 1 µM, and the method variation for δ 15 N-NO 3 − <0.2 and δ 18 O-NO 3 − <0.5 was based on the long run. The δ 15 N-NH 4 + was determined via transforming NH 4 + to N 2 O using the sodium hypobromite-sodium azide method with the reference of USGS-26, USGS-25, and IAEA-N1 (Zhang et al., 2007). The detection limit was ca. 2 µM, and the method variation was approximately 0.5 . The water stable isotope fractions ( 2 H-H 2 O) and ( 18 O-H 2 O) were analyzed on an Elementary Analyzer-Isotope Ratio Mass Spectrometer. The concentration of major ions, including sodium (Na + ), potassium (K + ), calcium (Ca 2+ ), magnesium (Mg 2+ ), chloride (Cl − ), sulfate (SO 4 2− ), and fluoride (F − ), was tested using ion chromatography (Dione ICS-2000). The eluent was potassium hydroxide solution (25 mM) for anions and methanesulfonic acid solution (20 mM) for cations, with the flow rate of 1 ml min −1 . The detection limit was approximately 0.01 mg L −1 for all species. The precision for major ions was below 4%.

Data Analyses
The linear regression, cluster analysis, and Spearman's rank correlation were conducted in the Minitab software (version 17.5). The redundancy analysis (RDA) was conducted in the Canoco 5 software. The statistical significance was assumed to be P ≤ 0.05. Chlorophyll a concentration in the sampled ocean areas was estimated from the remote sensing and downloaded from the online database 1 . The visualized atmospheric circulation (wind speed and direction) information (altitude of 850 hPa, approximately 1,500 m height; download from https://earth. nullschool.net) on two sampling regions was invoked to validate the long-range atmospheric dispersion (e.g., Yang et al., 2017). To identify the origin of aerosol particles via atmospheric transport, back-trajectory analysis has been performed (dash lines in Figure 1A). The trajectory of aerosol particles was back to 72 h at an altitude of 1,000 m (e.g., Zhang et al., 2004;Sinha et al., 2019).

Meteorology
During the EIO cruise, the atmospheric temperature was 20 • C at Guangzhou, China (Supplementary Figure S3). 1 https://giovanni.gsfc.nasa.gov Temperature ranged from 26.2 to 34.3 • C during the EIO cruise. Concurrently, the wind speed varied from 0.96 to 14.8 m s −1 (Supplementary Figure S3). The wind direction was northeast at 850 hPa with eddies (Supplementary Figure S1). Both temperature and wind speed showed insignificant variations during precipitation events. The precipitation amount ranged from approximately 0.4 to 22 mm, and pH in the EIO rainwater varied between 4.3 (Guangzhou) and 6.6 (remote ocean). Chlorophyll a concentration in surface EIO was <8 mg m −3 (Supplementary Figure S2). During the WPO cruise, the atmospheric temperature increased from 9 • C at Qingdao to approximately 29 • C at the equatorial WPO. Wind speed varied between 1.6 and 14.1 m s −1 . The east wind was prevailing, whereas several sites near the New Guinea coast were influenced by the west wind (Supplementary Figure S1). The precipitation amount varied between 0.3 and 32 mm, and the pH ranged from 5.2 to 6.4. Similar with the EIO, insignificant variations in both temperature and wind speed during precipitation events and low-level chlorophyll a concentration in the equatorial WPO were found (Supplementary Figure S2).

Blank Test
In the filter blank, nutrient concentrations were below the detection limit (Supplementary Table S1). For the 1-day exposure, concentrations of NH 4 + , NO 2 − , and NO 3 − slightly increased, reaching 0.54 µM. After the 3-day exposure, approximately 20% of DI water was evaporated. N species and dissolved Si increased, whereas the level of SRP and DOP remained low. Excluding the influence from evaporation, the addition rate for nutrient species ranged from 1.3 to 13.0 nmol L −1 h −1 . Considering that the rainwater collection only lasted 6 h (maximum) at each site, the exogenous nutrient concentration from seawater spray introduced into the sampling container should be <0.12 µM, indicating an insignificant influence.

N Concentrations and Isotope Fractions
NH 4 + concentration in rainwater samples from the EIO cruise varied between 1.8 and 110 µM, peaking at Guangzhou (Figure 2). Enrichment of NH 4 + was also found at sites near the Malacca Strait. In the WPO, the NH 4 + concentration ranged from 0.9 to 12.3 µM (Figure 2). High concentrations were observed between the W4 and W8 sites (near New Guinea). δ 15 N-NH 4 + in the EIO cruise ranged from -7.5 to 15.5 that the lowest value was still found at Guangzhou. In the WPO, δ 15 N-NH 4 + ranged from -5.4 to -14.7 (Figure 2). In both EIO and WPO, δ 15 N-NH 4 + showed a logarithmic decay with NH 4 + concentrations ( Figure 3A). For NO 3 − concentration, it varied from 0.6 to 55.6 µM in the EIO apart from the highest level at Guangzhou (100.5 µM). During the WPO cruise, NO 3 − concentration ranged from 0.5 to 66 µM. High-level NO 3 − spatially co-occurred with NH 4 + enrichments (Figure 2). In the EIO, an exponential increase was obtained between NH 4 + and NO 3 − concentrations ( Figure 3B), whereas rainwater samples in the WPO were comparatively enriched of NO 3 − than NH 4 + , suggesting a potential reduction of terrestrial NH 4 + inputs. Under the low pH condition, the NO 3 − content in wet precipitations was likely in the chemical form of HNO 3 ( Figure 3E). For δ 15 N-NO 3 − , it varied from 0.03 to 1.3 in the EIO and from -1.6 to 3.5 in the WPO (Figure 2), whereas the linkage between δ 15 N-NO 3 − and NO 3 − concentrations was variable among two oceans ( Figure 3C). An insignificant linkage was obtained between δ 18 O-NO 3 − and NO 3 − concentrations ( Figure 3D). NO 2 − was the minor portion in the rainwater DIN inventory, likely due to the rapid transformation from NO 2 − to nitric acid. The concentration of NO 2 − in both EIO and WPO was frequently < 1 µM. For DON, it varied from 1.4 to 16.9 µM during the EIO cruise and from 1.1 to 11.6 µM during the WPO cruise (Figure 2). In addition, a significantly linear correlation was identified between DON and NO 3 − concentrations in rainwaters from both oceans ( Figure 3F). Based on the N compound compositions and concentrations (Figures 4A,B), the rainwater in the EIO and WPO was assigned into three clusters (the Euclidean-distance similarity), namely, the low N (<7.8 µM in the EIO, <4.1 µM in the WPO), moderate N (11.6-17.2 µM in the EIO, 8.7-18.6 µM in the WPO), and high N groups (>17.3 µM in the EIO, >18.7 µM in the WPO). The RDA also identified the variation of N inventory among different groups during two cruises (Figures 4C,D).

P Species and Dissolved Si
For SRP and DOP, the concentration in rainwaters was frequently below 1 µM ( Table 1). Apart from NO 2 − content, positive correlations among SRP/DOP and N species were observed in both oceans (Table 2), especially for the high N groups and P species (Figures 4C,D). Dissolved Si accounted for a low level in rainwater compared with N content. The highest concentration was 2.3 µM, whereas the remaining was <1 µM (Table 1). Such low-concentration P and Si contents led to stoichiometric N-redundancy in all samples based on the Redfield-Brzezinski ratio plot (N:Si:P = 16:16:1; Figure 5A).

Water Stable Isotopes
δ 2 H-H 2 O and δ 18 O-H 2 O in oceanic rainwater were significantly linearly correlated ( Figure 5B). In the EIO, the slope (8.2) of the regression curve was similar to the global meteoric water line (GMWL, slope 8), whereas the intercept (15.8) was much higher (GMWL, intercept 10). In contrast, in the WPO, both slope (6.5) and intercept (9.7) of the curve were slightly smaller than those of the GMWL. Such difference suggests the variability of hydrologic cycle between seawater and atmospheric water vapor in the EIO and WPO. In addition, significant correlations were found between δ 15 N-NH 4 + and δ 18 O-H 2 O

Major Ions
Na + was the most abundant cation in the rainwater. The concentration in the rainwater collected from the EIO ranged from 1.2 to 123 mg L −1 ( Table 1). In the WPO, Na + concentration varied between 0.5 and 275 mg L −1 . The highest level of Na + was obtained in the moderate and high N groups, with a similar distribution pattern of K + , Ca 2+ , and Mg 2+ ( Table 1). In the WPO, the Cl − concentration in rainwater reached 460 mg L −1 , much higher than the level of SO 4 2− and F − . After removing the sea salt in rainwater based on the standard seawater composition , the concentrations of non-sea salt (nss) K + , Ca 2+ , Mg 2+ , SO 4 2− , and F − markedly  The concentration range is listed in low (L), moderate (M), and high (H) N groups. The unit for SRP, DOP, and Si is µM and major ions is mg L −1 . B.D. is below the detection limit. The unit for these major ions and nutrients is mg L −1 , and nutrient is µM, respectively. * indicates P < 0.05 and ** indicates P < 0.01.
decreased (e.g., Figures 5F,G). Several nss-cations and nss-anions were correlated, e.g., F − vs. K + and SO 4 2− vs. Ca 2+ ( Table 2). More importantly, the enrichment of nss fractions varied between the EIO and WPO. In particular, both nss-Mg 2+ and nss-F − were relatively enriched in the WPO. Significant correlations were also obtained between nss-ions and nutrient species (Table 2), such as the exponential increase between nss-SO 4 2− and NH 4 + ( Figure 5H). Notably, the mole ratio between NO 3 − and nss-SO 4 2− in the EIO and WPO frequently ranged between 1/3 and 2, whereas the ratio in three sites was >2, indicating nss-SO 4 2− as the dominant solute in acid rains ( Figure 5I).

Wet Deposition N in the EIO
In the EIO, high atmospheric temperature (>26 • C, Supplementary Figure S3) accelerated the seawater evaporation and introduced 13 precipitation events. Given the variability of rainwater N inventory, low, moderate, and high N clusters were identified (Figure 4A). The low-level N group includes three sites with the lowest content found in the remote ocean (E5 in Figure 1A), where received west-direction wind. At the E5 site, NO 3 − and NH 4 + were key species in N inventory, but their concentrations were <3 µM. The west wind also produced the remaining two low-level N sites near the coast of Sumatra Island (E2 and E3). Low concentrations of N species in these sites are comparable to observations made in other oceanic environments, such as the record made in the North Pacific Ocean and the Bermuda Island (Figure 6). In the low-level group, the concentrations of nss-cations and nss-anions were also frequently <2 mg L −1 , which was 1-2 orders of magnitude lower than the measurement at Guangzhou (E13 in Figure 1A), further suggesting a minor influence from terrestrial sources (e.g., coal combustion and agriculture emission, sketch in Figure 7). Consequently, NH 4 + in the low N group can be assumed to be the product of NH 4 + emission from the surface seawater, whereas NO 3 − mainly resulted from lighting fixation (Figure 7). The δ 15 N-NH 4 + directly supports that NH 4 + in the low N group derived from oceanic surface water emission was the main source of NH 4 + . In particular, δ 15 N-NH 4 + in the surface seawater was approximately -0.5 (Hoch et al., 1994). Accordingly, the oceanic emission of δ 15 N-NH 4 + was found to be -0.5 to -9 (Lin et al., 2016), as highlighted in Supplementary  Figure S4. Due to the positive correlation between temperature and emitted δ 15 N-NH 4 + (Elliott et al., 2019), δ 15 N-NH 4 + derived from oceanic emission in equatorial regions tended to be higher in this range, which fitted our observation in the remote ocean. Furthermore, lighting fixation may also produce a small quantity of NH 4 + via the combination between N and H molecules (NOAA site) 2 . δ 15 N-NH 4 + produced from nitrogen gas (N 2 ) via lighting fixation is still approaching 0, which could not significantly change the δ 15 N-NH 4 + in oceanic environments. By contrast, δ 15 N-NH 4 + from volatilized fertilizer [e.g., (NH 4 ) 2 SO 4 , NH 4 Cl] frequently hosts a more negative isotope value (dropping to -56 ; Pan et al., 2018). In addition, during the atmospheric transport from inland to remote oceans, terrestrial NH 4 + could be easily loosed during the long-range transport (Lin et al., 2016), and δ 15 N-NH 4 + tends to be decreasing due to the "washout" of heavy isotopes from aerosols (Agnihotri et al., 2011;Altieri et al., 2014). In the EIO low N group, δ 15 N-NH 4 + was markedly higher than δ 15 N-NH 4 + reported in terrestrial precipitation events, e.g., Toshima, Japan (mean: -25 , Uchiyama et al., 2017) and Guiyang, China (mean: -15 ; Xiao et al., 2012), also confirming its oceanic origin. In the low N group, the oceanic NO 3 − is the oxidation product of lighting-produced NO and NO 2 (NO x ; Altieri et al., 2013). These gas products host δ 15 N of 0 (Hoering, 1957), indicating that the oceanic δ 15 N-NO 3 − should be 0 with a small variation after transformation (Supplementary Figure S4).
In these samples, δ 15 N-NO 3 − was 1 , suggesting that the lighting-induced reaction was the dominant source.
When sampling sites were approaching the Indian Subcontinent and Malaysian Peninsular (Figure 1A), N concentrations in rainwater samples increased and created the moderate and high N concentration groups ( Figure 4A). The NH 4 + concentration is similar to the rainwater collected from the Bay of Bengal (Figure 6). Such high-level NH 4 + is beyond the requirement of neutralization (NH 4 + to neutralize nss-SO 4 2− and NO 3 − ; Supplementary Figure S5) when ammonium available index (AAI) is introduced (Szép et al., 2018). Large AAI indicates the excessive NH 4 + from intensive human activities (Szép et al., 2018). Concurrently, nss-ions, e.g., Ca 2+ and K + , also markedly increased, suggesting the input from terrestrial materials into the rainwaters (Martino et al., 2013). In particular, Ca 2+ was the byproduct of coal combustion in India (Singh et al., 2007), whereas K + was identified as the product of biomass burning (Srinivas et al., 2011). Accordingly,  Table S2). The majority of them are around the EIO and WPO. Notably, the NO 3 -/NH 4 + concentration range in the EIO excludes the value obtained from Guangzhou.
the increase of NH 4 + concentration in rainwater was deemed to be responsible for anthropogenic activities. Given the isotopic information, atmospheric NH 4 + likely resulted from several activities. The fertilizer volatilization is assumed to be a key factor for atmospheric NH 4 + (Xiao et al., 2020). In the Indian Subcontinent, a significant amount of chemical fertilizer, e.g., urea, NH 4 Cl, and (NH 4 ) 2 SO 4 , is intensively applied to enhance the yield. For instance, the 16.9 million tones N yr −1 fertilizer was applied to the Indian farmland in 2014 3 and the application amount kept increasing in the recent 20 years. The fertilizer application in China is also prominent. The redundant NH 3 in soils is easily volatilized into the atmosphere coupled with the high temperature and air humidity (Sommer et al., 1991). In addition, approximately 45% of fertilized urea was transformed to NH 3 and then increased atmospheric NH 3 concentration (Trierweiler and Bishop, 1983). In the atmosphere, with the combination of acid materials, such as H 2 SO 4 from petrochemical industry, steelmaking, thermo power stations, and volcanic activities (Martino et al., 2014), NH 3 is transformed to NH 4 + (Jia and Chen, 2010). The positive increase in both sulfide and NH 3 led to the accumulation of atmospheric NH 4 + (Figure 7), which, in turn, increased NH 4 + concentration in the wet deposition. Apart from agriculture, traffic (vehicle exhaust) was also a significant source of atmospheric NH 4 + , which increased δ 15 N-NH 4 + in precipitations (Chang et al., 2016) due to the significant positive values (Supplementary Figure S4). In the surrounding coasts, the 1.5 billion population in India, Bangladesh, Thailand, etc., could be a key contributor of fossil fuel NH 3 via daily transport. Notably, based on the logarithmic decay between NH 4 + concentration and δ 15 N-NH 4 + (Figure 3A), the contribution from chemical fertilizer seemed to be stronger than that of vehicle exhaust on the rainwater NH 4 + enrichment, indicating the necessity of fertilizer application regulation and management.
Different from NH 4 + , the increase of NO 3 − concentration in the moderate group did not significantly influence δ 15 N-NO 3 − and δ 18 O-NO 3 − in the EIO (Figures 3C,D), indicating multiple sources for terrestrial NO 3 − in these precipitation events (Supplementary Figure S4). Notably, human activities could not directly introduce NO 3 − but add the precursor of NO 3 − , i.e., NO x , into the atmosphere (Figure 7). NO x is rapidly transformed to NO 2 − in humid environment. Due to the instability of NO 2 − and the presence of O 3 , the majority of NO 2 − could be transformed to NO 3 − (Elliott et al., 2019), typically as the nitric acid under low pH condition (e.g., low pH conditions in Figure 3E). The combustion of fossil fuels, mainly as gasolines from vehicles, is a significant source of NO x . Anthropogenic NO x is usually positive in δ 15 N, ranging from 3.7 to 13 (Jia and Chen, 2010) and from 5 to 25 (Felix et al., 2015). In contrast, NO x from soil microbiota is usually negative in δ 15 N (-20 to -50 ; Felix et al., 2015) due to the preferential utilization of 14 N compounds in metabolism (Harrison et al., 2007). In addition, thermo power plants, especially in India, also markedly contribute to anthropogenic NO x emissions (Ghude et al., 2012). Coupled with north direction wind (Figure 1 and Supplementary Figure S1), the terrestrial NO x is transported along the meridional direction into the equatorial EIO, as evidenced by the significant correlation between δ 15 N-NO 3 − and δ 18 O-H 2 O (Figure 5D). On the other hand, the intensive chemical fertilizer triggered active nitrification and denitrification in terrestrial soils, especially in the Indo-Gangetic Plains where intensive agriculture has been conducted (Ghude et al., 2012), leading to an active production of NO x (Pathak et al., 2002). This clearly introduces biological NO 3 − in the rainwater N inventory. Accordingly, the mixing of these sources likely compensates the isotopic variation of NO 3 − , leading to the distribution pattern observed in Figures 3C,D. When the samples were collected in coastal zones (<1 km distance), such as the Malacca Strait and Guangzhou, China (Figure 1A), the influence of anthropogenic activities peaked (both soil emission and fossil fuel combustion; Supplementary  Figure S4), producing high-level N compounds, as well as nss major ions (e.g., SO 4 2− ). The increase of these compounds markedly decreased rainwater pH ( Figure 3E) and further accelerated the transformation from NH 3 to NH 4 + and from NO x to NO 3 − , eventually leading to the significant enhancement in NH 4 + and NO 3 − in precipitation.

Wet Deposition N in the WPO
Similar with the EIO, three categories in the WPO were observed ( Figure 4B). The low N group was obtained in the east boundary of the sampling area, where received east trade wind driven by the Hadley Circulation (Supplementary Figure S1). Both NH 4 + and NO 3 − concentrations in the low N group were < 2.7 µM, which was highly comparable to the record in the EIO (Figure 4A vs. Figure 4B). In addition, the nss portion of ions in the low N group between oceans was similar (cf. Figures 5F,G). Accordingly, marine sourced N should be identified as the dominance in these samples. In the low N group, δ 15 N-NH 4 + varied between -10 and -6 , which was in line with the range found in the EIO samples ( Figure 3A), as well as the range (-0.5-9 ) in the Atlantic Ocean (Lin et al., 2016), reinforcing that the seawater emission can be identified as the major source of NH 4 + in oceanic samples. For NO 3 − in the WPO low N group, both δ 15 N-NO 3 − and δ 18 O-NO 3 − were more negative (-1.5-0) compared with the EIO, indicating a potential difference during the transformation of NO x to NO 3 − in atmospheric environments. Apart from influence from "isotope washout" during longrange transport, as a reaction mainly oxidized by O 3 (Altieri et al., 2013;Elliott et al., 2019), the concentration of O 3 might be a key for the NO 3 − isotopic signature. Between two oceans, the hydrologic cycle impacted by the Walker Circulation deeply influences atmospheric O 3 . In particular, the water stable isotopes (δ 2 H-H 2 O vs δ 18 O-H 2 O) usually decrease from the equatorial ocean to high-latitude oceans (Field et al., 2010). The slope and intercept of the regression line is a mirror of hydrologic cycle on a local scale (Vallet-Coulomb et al., 2008). Compared with the EIO, small values in regression slope and intercept were found in the WPO (Figure 5B), indicating the unsteady isotopic fractionation during the precipitation (Gat, 1996). This unsteady state is linked to the environment characterized as evaporation with strong ascending air, termed as "sub-cloud secondary evaporation" (Xia et al., 2019). These sites with δ 18 O-H 2 O > 0 also appeared in the WPO (Figure 5B), adding the evidence of ascending air flow in tropical systems (e.g., Gonfiantini et al., 2001;Vallet-Coulomb et al., 2008). In the WPO, such environment settings result from the Walker Circulation, which continuously pumps moisture from the warm pool into FIGURE 7 | Sketch of N sources, atmospheric transport, and reaction pathways in oceanic precipitation events (modified from Cao et al., 2021).
the atmosphere (Stechmann and Ogrosky, 2014). This ascending flow likely dilutes the atmospheric O 3 in the turbulently mixed sublayer, as the low-level O 3 from 0 to 2 km altitude in the tropical Pacific Ocean (Singh et al., 1996). According to the dynamic balance between NO x and O 3 (Elliott et al., 2019), lowlevel O 3 likely produced a weak oxidation with the preference of 14 N compounds (Altieri et al., 2013), hence leading to a more negative value of δ 15 N-NO 3 − . In addition, δ 18 O in O 3 ranges from 90 to 122 (Johnston and Thiemens, 1997). The reduced reaction potential also decreased δ 18 O-NO 3 − , creating a drop of both δ 15 N-NO 3 − and δ 18 O-NO 3 − in the WPO low N group (Figure 3D), as well as different correlations in water stable isotopes ( Figure 5E).
In contrast, the rainwater samples collected from the west boundary of WPO hosted the high concentration of N compounds ( Figure 4B). From W1 to W4, the short distance to the Philippines/Indonesia coasts and seaward wind introduced a significant amount of terrestrial materials (Figure 1A), leading to the enrichment of land-derived NH 4 + (low-level 15 N signals) with the longitude signal ( Figure 5C). This west wind that drives the air flow toward the Pacific Ocean center also results from the Walker Circulation (Stechmann and Ogrosky, 2014) and further leads to the increase of NH 4 + concentration at sites near New Guinea. Interestingly, though the impacts of anthropogenic influence, the enrichment of NH 4 + in the WPO was relatively weak than that in the EIO (e.g., AAI in the WPO < 100%, Supplementary Figure S5). In addition, the NH 4 + concentration in aerosol PM 2 . 5 particles detected in the northwestern Philippines was approximately 0.5 µg N-NH 4 + m −3 (Bagtasa et al., 2018), which was significantly smaller than the value found in the Bay of Bengal (2.8 µg N-NH 4 + m −3 ; Srinivas et al., 2011). This likely results from variation of chemical fertilizer application during local agriculture activities in the Philippines, Malaysia, and Indonesia. Specifically, in these three countries, the agriculture activities mainly include the rubber and oil palm plantations (Sia et al., 2019), which produce a lowlevel application of N fertilizer in agriculture compared with South Asia 4 . However, the requirement on magnesium fertilizer is intensive in peatlands at tropical countries (e.g., Panhwar et al., 2014). As a response, we observed the pattern of low NH 4 + enrichment but the high-level nss-Mg 2+ in the WPO precipitation events.
Interestingly, NO 3 − concentrations in the WPO high N group were comparable to the EIO high N group, excluding the Guangzhou site (Figures 3B, 6). However, the total population in the Philippines, Malaysia, and Indonesia is much smaller than that in India, Thailand, and Bangladesh 5 , indicating a low contribution of NO x to the atmosphere on fossil fuel combustion from economic activities. Accordingly, NO 3 − concentration in the WPO samples should be significantly reduced. This contradiction might be resulted from the multiple sources of atmospheric NO x from terrestrial systems in Southeast Asia (Li et al., 2020). In particular, the Indonesian volcanic activities are an important source for NO x with δ 15 N from N gas compounds of 0.1-4.0 (Sano et al., 2001), which is similar to the range found in the WPO (Figure 2). During December 2018, the Dungusan Soputan Volcano erupted (Indonesian Geology Bureau) 6 and added a significant amount of ashes into the atmosphere (reaching 7,000 m height). The enrichment of nss-F − (easily evaporated element; Figure 5G) in the WPO samples could be a support of the volcanic activities. In addition, croplands in Indonesia are also a hotpot of NO x with a significant annual increase in NO x emission (Takakai et al., 2006). Besides, a significant fraction of peatland in Southeast Asia has been changed to oil palm plantations . The releasing rate of N 2 O from these peatlands is significantly higher (emission factors: 2.4-2.7%) than the IPCC standard on a global scale (1%; Rahman et al., 2019). Though low-level application of chemical fertilizer, the rapid and active production from peatland could contribute to atmospheric NO x . Emissions from the biomass burning, e.g., rice straw burning after harvesting (Bagtasa et al., 2018;Xiao et al., 2020) and forest/peatland fire events induced from high temperature and accidents (Kumar et al., 2019;Szép et al., 2019), are also an unneglectable source for atmospheric NO x . Coupled with west wind driven by the Walker Circulation, the terrestrial NO x is easily delivered into the equatorial WPO. In addition, the volcano activities may also introduce a significant amount of atmospheric nss-SO 4 2− (Martino et al., 2014). Such high-level nss-SO 4 2− drove the acid rain event in the WPO as the SO 4 2− -NO 3 − mixing type ( Figure 5I). In the WPO high N group, the W9 site is located in the east boundary of the sampling area ( Figure 1A). This sample was collected at Pohnpei, Micronesia, directly receiving the anthropogenic influence. However, the population in Pohnpei is only approximately 35,000. In addition, the manufacture and agriculture activities in Micronesia are less developed, and citizens are mainly dependent on imported food (Connell, 2015). Compared with NO 3 − and NH 4 + in the wet precipitation collected at Guangzhou (Figure 2) and other coastal sites with millions of population residence, e.g., Wenchang, China  and Toshima, Japan (Uchiyama et al., 2017), the N content in the Pohnpei harbor is minor, reinforcing that the major driver of wet precipitation N inventory is population-based anthropogenic activities instead of latitude effect driven by the Hardly Circulation.

Budget Estimation and Ecological Implications
Compared with the surface seawater in remote ocean, DIN concentrations in the rainwater were frequently higher, indicating a significant influence on ecological structure from precipitation (Zhang et al., 2004). The estimated precipitation amount in the equatorial EIO was approximately 1,900 mm yr −1 , whereas it increased to 2,000 mm yr −1 in the equatorial WPO (Béranger et al., 2006). By the mean precipitation rate and the lowest rainwater DIN concentration, the wet precipitation conservatively introduced 66.5 and 47.6 kg N-DIN km −2 yr −1 into the remote EIO and WPO, respectively. Such conservative contribution from wet deposition events is comparable to the WPO dry deposition (132 kg N-DIN km −2 yr −1 ; Martino et al., 2014). As aforementioned, in the remote ocean, biological fixation and atmospheric disposition are only pathway for the replenishment of N. Biological N fixation is frequently constrained by the input of P and trace elements, such as iron (Großkopf et al., 2012). In the equatorial EIO and WPO, the estimated biological fixation would be <280 kg N km −2 yr −1 (Deutsch et al., 2007), indicating wet depositions in the EIO and WPO as a key N contributor. Coupled with the surface seawater mixing, the deposited DIN could be rapidly diluted and assimilated by phytoplankton communities (Zhang et al., 2004). Excluding the influence from nutrient stoichiometric balance, the completely biological consumption of rainwater DIN could produce 378 and 270 kg C km −2 yr −1 sequestration in the EIO and WPO at the conservative scenarios, respectively. The carbon sequestration capability induced by the wet precipitation could easily go to the magnitude of 2,000 kg C km −2 yr −1 in those regions that received terrestrial materials, such as the area near the Malacca Strait and New Guinea coasts (Figure 1A), which is highly comparable to the estimated results in the continental margin of the East China Sea (1,825-3,650 kg C km −2 yr −1 , Zhang et al., 2004).
Currently, the source of DON in the atmospheric wet deposition is still under debate (reviewed by Cape et al., 2011). Terrestrial source is assumed to be significant in many investigations (e.g., Mace et al., 2003 at Cape Grim, Australia;Luo et al., 2018 at North Pacific Ocean). In the present study, based on the tight linkage between DON and NO 3 − (Figure 3F), a significant portion of DON is estimated to be terrestrial emission. Though DON compounds frequently account for a small portion in the oceanic aerosol and wet precipitation N inventory (Cornell et al., 2001;Matsumoto and Uematsu, 2005;Luo et al., 2018) and the recalcitrant nature, DON in surface oceans might also be important by primary producers after phytodegradation (Deutsch et al., 2007), enhancing the carbon sequestration capability. Apart from stimulation on the growth of primary producers (Paerl, 1985), the enrichment of DIN in the rainwater may also add negative effects to the oceanic ecological system, mainly resulting from the imbalanced stichometry ratio among DIN, P, and Si. In particular, the DIN content was constantly redundant in rainwaters from both EIO and WPO, as outlined in Figure 5A. Such significant N-redundancy might significantly benefit from the growth of N-preference species in oceanic environments (Rocha et al., 2002). In the equatorial EIO and WPO, the dominant phytoplankton species was mainly picophytoplankton, such as Synechococcus and Prochlorococcus (Li et al., 2015;Wei et al., 2019). The in situ incubation in the WPO has revealed an enhancement in the biomass of diatom and dinoflagellates with excessive N loading (Li et al., 2015). Accordingly, the long-term N excess from the wet atmospheric deposition potentially triggers the ecological succession of phytoplankton species, which should receive further attention.

CONCLUSION
The present study investigated the N inventory in rainwaters obtained from the EIO and WPO. NH 4 + and NO 3 − frequently accounted for the dominant species with highly variable concentrations. Accordingly, three clusters, namely low, moderate, and high N groups, were identified. In both oceans, the sites included in the low N group were located in the remote ocean. Main N sources were oceanic NH 4 + emission and lighting fixation (NO 3 − ). In contrast, the sites near the coastal line frequently host the higher N concentrations, especially subject to the west wind driven by the Walker Circulation in the WPO. The enhancement of NH 4 + concentration in rainwater resulted from the intensive application of chemical fertilizer and daily transport, especially in EIO surrounding countries. The enrichment of NO 3 − is deemed to be responsible for the microbial reactions in terrestrial soils and combustion of fossil fuel. Different contributions from these two sources produced variable correlation between NO 3 − concentration and δ 15 N-NO 3 − in rainwaters. Together with the precipitation, 66.5-47.6 kg N km −2 yr −1 could be introduced into the EIO and WPO, respectively, acting as an important source to support the oceanic CO 2 sequestration. Notably, compared with N content, SRP and Si in rainwater were relatively insufficient based on the Redfield-Brzezinski ratio. As the major path for the exogenous N input, the wet precipitation likely benefits from the growth of N-preference phytoplankton and eventually modifies the ecological structure in tropical oceans. This deserves further attention from the scientific community.

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 author/s.

AUTHOR CONTRIBUTIONS
ShaJ: field survey, laboratory analyses, and data analysis. JJ, YW, and SL: laboratory analysis and data analysis. ShuJ, JW, ZZ, and JZ: field survey and data analysis. JC and YC: data analysis. LW: laboratory analysis. All authors contributed significantly on this manuscript.

FUNDING
This work was supported by the National Natural Science Foundation of China (41876071, 41876074, 41476065, 41706081, and 41806096) and Scientific Research Foundation of SKLEC (2017RCDW04).