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The contents and properties of soil organic phosphorus (Po) largely drive ecosystem productivity with increasing development of natural soil. We hypothesized that soil Po would initially increase with paddy management and then would persist under steady-state conditions. We analyzed soils from a 2000-year chronosequence of a rice-wheat rotation and an adjacent non-paddy 700-year chronosequence in Bay of Hangzhou (China) for their Po composition using solution 31P-NMR after NaOH-EDTA extraction. Land reclamation promoted Po accumulation in both paddy and non-paddy topsoils (depths≤18cm) until steady-state equilibria were reached within 200 years of land use. Greater Po concentrations were found, however, in the non-paddy subsoils than in those under paddy management. Apparently, the formation of a dense paddy plough pan hindered long-term Po accumulation in the paddy subsoil. The surface soils showed higher proportions of orthophosphate diesters under paddy than under non-paddy management, likely reflecting suppressed decomposition of crop residues despite elevated microbial P compounds stocks under anaerobic paddy-rice management. Intriguingly, the composition of Po was remarkably stable after 194-years of paddy management and 144-years of non-paddy management, suggesting novel steady-state equilibria of P dynamics had been reached in these man-made ecosystems after less than two centuries.
Phosphorus is an essential macronutrient for all life on earth. In soil, there is increasing evidence that the P pool changes its composition, abundance, and bioavailability during soil development in natural and agricultural ecosystems1–5. In undisturbed terrestrial ecosystems, organic P (Po) accumulates under nitrogen (N) limitation in the early stage of ecosystem development, while at advanced stages of ecosystem development Po concentrations decline under conditions of P limitation2, 6, 7. Much less is known, however, about human impacts on temporal soil P dynamics. These impacts might be particularly large in anthropogenically-modified soils such as paddy soils. More than 50% of the world’s population relies on rice as a dietary staple and about 163 million ha of land is used as flooded lowland rice fields8. These paddy systems are known to accumulate organic matter and microbial N residues9–14, and thus may potentially accumulate Po 3.
Paddy soils environments likely behave differently from natural wetlands, because of the addition of chemical and organic (manure, residues) N and P fertilizers, removal of nutrients during harvest, intensive puddling, and alternating flooding and draining regimes3, 15. These processes result in accelerated soil weathering15 so that after only 700- to 1000- years, the soils are decalcified and have significant iron (Fe) oxide transformations, which can alter the sorption of specific Po forms14, 16.
Soil Po is comprised of a variety of compounds that differ in their stability and biological availability in environment17. The variation of P composition over pedogenic time scales has ecological significance5, as it may alter species composition of the seedling community, change the competitive ability of adult plant species18, and modulate soil microbial P cycling19, 20. To reveal changes in Po composition, solution31P-nuclear magnetic resonance (31P-NMR) spectroscopy after NaOH-Na2EDTA extraction has been the method of choice21–23. This allows the identification of specific Po species, such as deoxyribonucleic acid (DNA), α- and β-glycerophosphate, mononucleotides, phosphonates, and even inorganic long-chain polyphosphate and pyrophosphate structures, including compounds originating from living microbial cells and fungal tissue5, 24–26. However, little information is available on the degree and rates at which different Po species reflect impacts of prolonged paddy or non-paddy management on the overall Po status of the soils.
The objective of this study was to evaluate how prolonged paddy management influenced the degree and rates at which various Po compounds accumulated in soil. For this purpose, we extracted Po with NaOH-Na2EDTA and characterized compounds by solution 31P-NMR spectroscopy. Samples originated from a unique 2000-year-old chronosequence of paddy soil management; adjacent sites under non-paddy management for 700 years served as a reference. All soils had developed from tidal wetland sediments in the Yangtze River delta, China. We hypothesized that paddy management accelerated the accumulation of Po compounds in soil, which may then persist for several hundred years under steady-state conditions.
During paddy soil management, the puddling of surface soil accompanies the formation of a dense plough (Ardp) horizon, which potentially restricts root growth into the deeper subsoil27. With increasing time of paddy soil development, as these Ardp horizons mature, topsoil surfaces may become increasingly decoupled from subsoil biogeochemistry13, 14. In order to understand the role of paddy management in the biological cycling of P, particularly when compared to native ecosystems, we thus have to understand both the transformation of P with increasing soil depth as well as with time of management.
Total P concentrations decreased with increasing depth from ~800mgP kg−1 in the 100-year-old paddy topsoils and from ~1100mgP kg−1 in the respective non- paddy topsoils down to 40–50cm soil depth (600–690mgP kg−1) and then remained relatively constant in the subsoil (Table 1). The concentrations of NaOH-Na2EDTA extractable total P (EP) and inorganic P (EP-Pi) in these soils showed a similar trend (Table 1). The contributions of extracted Po (Ep-Po) to total P in the topsoil of the paddy soil were almost double those under non-paddy management, whereas those in paddy subsoil were reduced compared with subsoil under non-paddy management (Table 1). The contribution of Ep-Po declined with depth while that of Ep-Pi increased (Table 1). As a result, all Po species in the paddy subsoil (from 30 to 100cm) showed very low 31P-NMR signal intensities, and the spectra were dominated by orthophosphate P (Table 2). The non-paddy site showed a greater proportion of total P as orthophosphate monoesters below 30cm soil depth than the paddy site, but the lowest subsoil was again dominated by Pi (Table 2).
Above 30cm depth, orthophosphate diesters and myo-IHP were much higher proportions of EP in the paddy soils than in the non-paddy soils. There was a substantial increase in phosphonates at the 30–50cm depth in the paddy soils. Overall, the effects of paddy management on Po dynamics were thus mainly detectable for the surface soils. Hence, we hereafter concentrated on topsoil samples (~0–15cm) in our study of P transformations along the chronosequence.
The tidal wetland (TW) sediment, i.e. the parent material of soil formation for paddy and non-paddy soils, had a total P concentration of 760mgP kg−1 in surface soil (Table 3). After land embankment, soil formation started with the salt marsh (SM) having a comparable P concentration (730mgP kg−1) in the surface horizon. With prolonged arable management, total P concentrations increased, reaching on average significantly greater concentrations in the non-paddy topsoils (average of 1128±198mgP kg−1) than in those under paddy management (average of 890±149mgP kg−1; Table 3; p<0.001).
The total P recoveries in NaOH-Na2EDTA extracts of the youngest soil were extremely low (4.2–5.2% of total P in TW and SM respectively, Table 3). With prolonged management, the EP concentrations from paddy topsoil increased during pedogenesis to 12.0–31.4% of total P (Table 3). This gain in both absolute concentrations and relative proportions of EP occurred for both Pi and Po species, although with different curve progression (Table 3, Fig. 1). Notably, Po concentrations increased only during early stages of soil formation and then remained relatively constant in older soils, both under paddy and non-paddy management (Table 3, Fig. 1b). Kinetic modeling revealed that accumulation of Po in paddy topsoils needed about 50 years more time to reach steady-state (Xe=178 years) than in non-paddy topsoils, but differences in rate constants (k) were not significant when including the uncertainty of k into the assessment of Xe (Table 4 and Fig. S1).
Multiplying the 31P-NMR results (in percent) by those for EP and factoring in changes in bulk density gave results in kg P ha−1 (Table 5), which showed that concentrations of extracted orthophosphate in paddy soil significantly increased (p<0.001) with increasing duration of paddy rice cultivation. The concentrations of all other P compounds followed a similar trend through early stage of pedogenesis, i.e. being low or undetectable at the onset of soil development in TW and SM, but increasing thereafter in the paddy soils rapidly to a maximum that was obtained after no more than 300 years (Table 5). At the latter stage of the chronosequence, the concentrations of some P compounds like pyrophosphate, polyphosphate, orthophosphate monoesters, myo-IHP, other orthophosphate monoesters (calculated as total P in the orthophosphate monoester region after subtracting myo-IHP, scyllo-IHP, α- and β-glycerophosphate and the mononucleotides) or glycerophosphates+mononucleotides even tended to decline, whereas those of other compounds could be sustained even after prolonged land use (e.g., scyllo-IHP, orthophosphate diesters, phosphonates; Table 5). In the non-paddy topsoils, the concentrations of all P compounds increased rapidly after 50 years of management, and then continued to increase slowly (except for orthophosphate and DNA) with subsequent management (up to 700 years; Table 5).
To better understand changes in P dynamics, we normalized the respective concentrations to the total amount of Pi or Po extracted, i.e., we evaluated to which degree a given Pi or Po compound contributed to overall Pi or Po from 31P NMR spectra. The results showed that paddy topsoils showed increasing proportions of total Pi for orthophosphate and declining ones for pyrophosphate during soil development, whereas non-paddy topsoils showed the opposite tendency (Fig. S1a and b). The contributions of polyphosphates to extractable Pi did not exhibit a clear temporal trend in both land-use systems, though proportions were larger in the paddy soils (Fig. S1c).
In contrast to the Pi forms, changes in Po composition were more consistent: the proportions of orthophosphate monoesters to extracted Po increased until a steady-state maximum was reached after 113 years of paddy and 91 years of non-paddy management (Table 4, Fig. 2a). Moreover, orthophosphate monoesters constituted the highest proportion of total Po in both paddy and non-paddy topsoils at steady-state, though with higher proportions in the non-paddy soils (Fig. 2a). The myo-IHP and scyllo-IHP as typical orthophosphate monoesters showed similar accumulation patterns to total orthophosphate monoester, but they constituted only a small proportion of total Po in both paddy and non-paddy topsoils (Fig. 2b and c, Table 5). The orthophosphate monoesters, myo-IHP, and scyllo-IHP were found to need a longer time to reach steady-state in paddy topsoils than in non-paddy topsoils (Table 4).
Although orthophosphate diesters may have a different origin than orthophosphate monoesters, the contribution of orthophosphate diesters to total Po also increased rapidly at early stages of pedogenesis until a steady-state plateau was reached in the paddy soils; no such trend was observed for the non-paddy topsoils (Fig. 2d). The sum of the diester degradation products (α/β-glycerophosphates from phospholipids and mononucleotides from RNA) also showed this curve progression to a plateau with higher proportions in the paddy topsoils (Fig. 2e). The DNA content was larger in the paddy topsoils than the non-paddy ones, and tended to increase with the increasing duration of management and related pedogenesis in the paddy soils (Fig. 2f). Only the phosphonates did not confirm a P accrual with time – their proportions declined with time in both paddy and non-paddy soils (Fig. 2g). To determine if the modelling results were affected by the longer time scale for the paddy soils, we redid our analyses using 700 years as the oldest date for both soil types. The trends observed when the 1000 and 2000 year old sites were included for the paddy soils were also observed with the analyzes up to 700 years only (Fig. S2 and Table S2). The overall changes in organic P compounds with time are shown in Fig. 3.
We did not analyze any physical properties for these samples, nor any chemical properties beyond P forms by P-NMR, because this information is available in other studies13, 15, 28. We have summarized the information here that is expected to be relevant for understanding P cycling in these soils. The pH values were 8.2 and 7.8 in the youngest soil (TW and SM; Table 6). With prolonged soil development, the pH values declined to 5.1 after 2000 years of paddy-rice management. This increasing acidification was related to the loss of carbonates (Table 6)14. In this regard, long-term paddy cultivation with submergence and drainage, as well as ploughing and puddling, resulted in faster decalcification than in non-paddy soils14, and thus in accelerated loss of related primary materials (e.g. CaCO3), clays, and P-sorbing Fe oxides3. These processes likely led to the increase in P in non-paddy soils compared with soils under paddy management (Table 3), despite greater SOM accrual in the latter13, 14. Higher yields of paddy rice than non-paddy crops also contributed to lower P storage in paddy soils.
Concentrations of calcium (Ca), magnesium (Mg), Fe, manganese (Mn), and aluminum (Al) decreased with cultivation time in the paddy topsoils, so that the greatest concentrations of these elements were found mainly in the younger surface soils15. The dithionite-citrate-bicarbonate- (DCB-) extractable Fe in paddy and non-paddy chronosequences did not show large differences. However, greater concentrations of oxalate-extractable Fe (i.e. poorly crystalline Fe) in the paddy topsoils than in the non-paddy soils supported previous findings of enhanced redox cycling and accelerated weathering (Table 6). The greater proportion of poorly crystalline Fe oxides was probably also responsible for the large proportion of mineral-associated soil organic matter in paddy soils29. The N and microbial residue accumulation were limited to initial stages of paddy soil development and restricted to the surface horizons13. Consequently, we assumed similar impacts on related P forms.
Overall, NaOH-Na2EDTA extracted 12–31% of P-total in the paddy and non-paddy soils. We tested extraction methods to try to improve P recovery for these soils (see supplemental information); however, we found that a sequential repeated extraction did not increase the proportion of extracted Po and caused hydrolysis for some orthophosphate diesters (data not shown). The low P extraction yield in these soils may be related to the marine sediment parent materials and inputs of riverine sediments; most labile P was probably removed by sea water, leaving the majority of P occluded within Ca minerals. Low P recoveries (16–29% of total P) have been reported for NaOH-EDTA extracts of Ca-rich sea sediments30, 31, and similar low recoveries of P from Ca-rich soils have been reported for NaOH-Na2EDTA extracts32, 33 and for NaOH-NaF extracts34. The total P recoveries in NaOH-Na2EDTA extracts of the youngest soils without pronounced pedogenesis were extremely low (4.2–5.2% of total P in TW and SM respectively, Table 3). Turner et al.22 suggested that low proportions of extracted P indicate that the majority of phosphate is present in primary minerals. The low TP and Po concentrations of the tidal wetland and salt marsh samples are consistent with other reports of P concentrations in the sediments of this region35. It is important to note, however, that inputs of riverine sediments to coastal areas in this region have been significantly altered by upstream water diversion over time36. As such, current nutrient concentrations in the tidal wetland and salt marsh may not fully reflect concentrations 700 or 2000 years ago, but should reflect conditions for the more recent soils in these chronosequence.
The paddy and non-paddy soils of the chronosequence were formed from marine sediment with an extremely low Po concentration, as indicated by the TW EP-Po concentrations (Table 3). This suggests that the majority of Po in the older paddy and non-paddy soils did not originate from marine P. After land embankment, soil formation led to an initial accumulation of Po from the few grasses and shrub vegetation growing in the topsoils37. With the start of cultivation, the Po stocks continued to increase exponentially (Fig. 1b), probably due to increased biomass inputs from the crops and manure applications13 and from decreasing pH and changes in mineralogy17.
The decomposition of organic matter is less efficient under anaerobic conditions during anthropogenic submergence of paddy topsoils. This results in a larger accumulation of organic matter relative to the non-paddy topsoils14, 27. The gains in organic matter and the use of organic fertilizers such as manures likely promoted Po accrual in the surface soils15. Dense plough pans, developed from anthropogenic ploughing and puddling in the paddy soils13, reduced infiltration rates and thus blocked the vertical transport of organic matter into paddy subsoil38, 39. As a result, the concentrations of all Po species generally declined more strongly with depth in the paddy soil profile than in the adjacent non-paddy counterpart (calculated by using Tables 1 and and2).2). We believe that this tendency is consistent with soil profiles of other ages, given that the 100-year-old paddy topsoil had some of the largest Po concentrations among the soils samples along the chronosequence (Table 3). Thus, the increase in paddy Po stocks over time with cultivation seems to be mainly driven by the accumulation of P in the topsoil but not by processes storing P in the subsoils. In addition, advanced Fe reduction in the paddy subsoil15 likely hindered the effective binding of P in that part of the soil.
The accumulation of Po in both land-use systems followed exponential growth curves to a maximum, indicating a saturation of Po concentrations and stocks in both systems over time. Such saturation implies both limited sorption capacity and steady-state conditions, i.e., at given amounts of Po stored, Po input and output rates must be similar. The findings are consistent with patterns of organic N accumulation in topsoils of both land-use systems, which reached plateaus within a similar time scales [78–193 years for N stock13 and 144–194 years for Po stock].
Phosphorus speciation along a chronosequence is mainly regulated by changes in soil mineralogy for P stabilization, P inputs and biological production and utilization of various P compounds2. Alkali-extractable Pi was classified as phosphate that is mainly associated with Fe and Al in soil40, 41. It is a dynamic P pool and may act as an important P source for rice growth42. As Pi concentrations continuously increased with increasing duration of paddy management (Table 5), our results implied a sustained change in soil nutrient composition for at least 2000 years. The results are different from native ecosystems where fertilization is lacking: results from a coastal dune chronosequence and nearby Franz Josef glacial chronosequence in New Zealand indicated that the concentrations of alkali-extractable phosphate increased only in the early stages of pedogenesis and then declined due to depletion of total P2, 5.
The concentrations of pyrophosphate and polyphosphate were so small that they hardly contributed to the overall contents of total Pi. The proportions of pyrophosphate even decreased with time in paddy soil, suggesting that it is not a stable P form in these environments. Low pyrophosphate proportions were also found in humic acid extracts of paddy soils in Philippines43. We conclude that pyrophosphate is easily decomposed, even when microbial activity may be reduced during the wet season under submerged anaerobic conditions in paddy soil43. Certainly, these changes in redox conditions promoted greater steady-state percentages of orthophosphate diesters in paddy than in the non-paddy soils (Fig. 2d). Orthophosphate diesters may accumulate due to reduced decomposition or increased microbial synthesis. The exact source assignment of orthophosphate diesters to plants and microbes is frequently ambiguous. However, paddy soils also contained larger contents of microbial N residues than their non-paddy counterparts13; Therefore, it seems reasonable to assume co-accumulation of some microbial P forms that were rich in orthophosphate diesters5.
Intriguingly, and unlike other Po species, the portions of DNA continued to increase in paddy soils with time (Fig. 2f). The DNA extracted for 31P-NMR may be present in the soil in microorganisms or plant residues, or may be stabilized on soil minerals, and stabilization in soil or in soil organic matter may be favored at lower soil pH2, 17. Similarly, proportions of DNA increased with time in the 120,000 year Franz Josef post-glacial chronosequence, New Zealand, correlating significantly and positively with soil total organic carbon and N and negatively with soil pH2. Thus, with respect to accumulation of DNA with time, both the anthropogenically-modified ecosystems of this study and the native ecosystems in the New Zealand showed similar stabilization patterns of DNA with time.
The proportion of the sum of α/β-glycerophosphate and mononucleotides to total Po increased in the first 50 years and then slightly declined with prolonged cropping (Fig. 2e), which caused a similar tendency for total orthophosphate diesters. However, the tendency is equivocal because the highest proportion at 50 years is only sustained by one data point and may thus also be an outlier in our chronosequence; additionally, no other P species showed a similar tendency. Therefore, we ignored the highest point and considered the α/β-glycerophosphate and mononucleotides to have reached a plateau after steady-state conditions. Soil phospholipids and RNA are associated with living soil microbial biomass2, 44–46. In this line, a higher proportion of α/β-glycerophosphate and mononucleotides is consistent with increased microbial residues in the paddy soils compared with non-paddy soils that were observed in previous studies from these sites13, 15.
Unlike the forest/shrub soil chronosequences in New Zealand with abundant inositol hexakisphosphate1, 2, 5, myo-IHP and scyllo-IHP constituted only a small proportion of orthophosphate monoesters in our study. In general, inositol phosphates may be stabilized by amorphous Fe oxides2, and close relationships between the contents of inositol phosphates and amorphous metal oxides have been found in a range of ecosystems2, 47–50. However, the submergence during paddy cultivation induced anaerobic conditions, under which amorphous Fe oxides are easily dissolved. Hence, associated inositol phosphates may be released or even lost with subsequent drainage or surface runoff. Additionally, there could be potentially larger inputs of inositol hexakisphosphate from plant materials (e.g. seeds) into the forest/shrub soil chronosequences in New Zealand than into the studied paddy soils2.
The Walker & Syers model51 of P transformation predicts that with increasing time of pedogenesis there will be a loss in total P, a depletion of primary mineral P pools, but an accumulation of Po stocks in early stage of soil development followed by a slow, subsequent decline with time. Our sites are different to those studies by Walker and Syers51 in that our soils are fertilized to supplement P losses; besides, our land-use sequence covers a much shorter time scale to the chronosequence of Walker and Syers51. Our detailed assessment of Po species using31P NMR, including individual Po compounds and functional groups along 2000 years of rice paddy and non-paddy soil development demonstrated that: (i) the chemical nature of Po changes during pedogenesis, and (ii) soil paddy management strongly influences Po composition. All Po species accumulated rapidly in the early stages of pedogenesis. Thereafter, a plateau that is typical for steady-state conditions was reached. Studies in natural ecosystems2, 6, 7 noted that Po stocks that accumulated during early soil development stages would decline gradually in later stages of the ecosystem, as a response to nutrient limitation. For example, soil Po accumulated under N limitation but declined under P limitation in natural ecosystems2. In our arable study sites, concentrations of available N were low in the young paddy systems13, so the initial gain in Po may be explained by similar processes as described by Turner et al.2; in addition, the mere accrual of organic matter14 co-accumulated Po. In older systems, however, nutrient limitations have been counterbalanced by fertilization, so Po losses in response to P limitation do not occur because these ‘old’ systems do not become P limited.
The studied soils are located in the Bay of Hangzhou near the city of Cixi (30°10′N, 121°14′E), Zhejiang Province. Dike building over last 2000 years for land reclamation resulted in a chronosequence containing paddy and non-paddy soils. More details about the sites are available in other publications14, 15, 52. A sample of the marine Yangtze River sediment in a tidal wetland (TW, 2–30cm) was taken in the Bay of Hangzhou as substrate reference. After 30 years of land embankment behind the youngest dike, built in 1977, an initial surface soil was considered as the starting point (0 years of cropping) for our land use with the growth of salt-tolerant shrubs on an initial salt marsh (SW, 0–13cm). The soil chronosequence contained replicated sites under paddy cultivation for 50, 100, 300, 700, 1000, and 2000 years (PR50–2000), as well as adjacent replicated sites under non-paddy cultivation for 50, 100, 300, and 700 years (NPR50–700). Additionally, the soils with 100 years paddy and non-paddy managements (i.e. PR100 and NPR100) were sampled by soil horizon to around 100cm for elucidating changes in Po composition with soil depth; for the other soils we only analyzed the top A horizons (~0–15cm depth). More details about these soil samples are shown in Table 6 and may also be obtained from Roth et al.13 and Lehndorff et al.28. It should be noted that the traditional paddy management practice in this region in China is a crop rotation of rice in the wet season followed by wheat or other upland crops in the dry season53. Total soil P concentrations were determined by melting a mixture of soils and lithium borate at 1000°C for 30min, followed by inductively coupled plasma optical emission spectrometry (ICP-OES)54.
Solution 31P-NMR spectroscopy of alkaline extracts is commonly considered to be a reliable method for the quantification of Po 40. Soil samples from each of the replicated plots at each location were extracted by shaking 4g of air-dried soil with 40mL of a solution containing 0.25M NaOH and 0.05M Na2EDTA for 4h, followed by centrifugation at 10,000×g for 30min23, 55. A 2-mL aliquot of each supernatant was used to determine total extracted P by ICP-mass spectrometer (MS); the remaining solutions were frozen at −80°C, lyophilized, and ground. Each freeze-dried extract (~100mg) was re-dissolved in 0.1mL of deuterium oxide and 0.9mL of a solution containing 1.0M NaOH and 0.1M Na2EDTA, and then immediately transferred to a 5-mm NMR tube.
Solution 31P-NMR spectra were obtained using a Bruker 600-MHz spectrometer equipped with a prodigy-probe (a broadband CryoProbe that uses N-cooled RF coils and preamplifiers to deliver a sensitivity enhancement over room temperature probes by a factor of 2 to 3 for nuclei from 15N to 31P). Extracts were measured with a D2O-field lock at room temperature, and chemical shifts were referenced to 85% orthophosphoric acid (0 ppm). The NMR parameters generally used were: 32K data points, 2.6s repetition delay, 0.7s acquisition time, 30° pulse width and 10,000 scans. The delay time used here allows sufficient spin-lattice relaxation between scans for P compounds in NaOH-Na2EDTA (see supplemental information Fig. S3). Peak areas were calculated by integration on spectra processed with 7 and 2Hz line-broadening, using NUTS software (2000 edition; Acorn NMR, Livermore, CA) and manual calculation. Individual P compounds were identified by manual inspection and the peak-picking subroutine in the NUTS software, based on their chemical shifts from reports in the literature56 and by spiking selected samples with myo-inositol hexakisphosphate (myo-IHP)1. The orthophosphate peak in each spectrum was standardized to 6.0ppm during processing57, 58. Identified compounds and compound classes include orthophosphate (6 ppm), pyrophosphate (~−5 ppm), polyphosphate (−4 to −5, −5 to −50 ppm), orthophosphate monoesters (3 to 6, 6 to 7 ppm), orthophosphate diesters (3 to −4 ppm), and phosphonates (7 to 50 ppm). Because α- and β-glycerophosphates and mononucleotides, which result from degradation of orthophosphate diesters during 31P-NMR analysis59, were detected in orthophosphate monoester region, we assigned these compounds to orthophosphate diesters rather than to monoesters58, 60. The concentrations of individual P species were calculated by multiplying 31P-NMR proportions by the total NaOH-Na2EDTA extractable P concentration. The percentage of each P compound or compound class was calculated manually by integration across the entire spectrum and also by integrating smaller regions within each spectrum. The high-molecular weight (HMW) Po recently identified by McLaren et al.61 is included with the unknown peaks in the P-mono-other category (Table S3). In our experience (B. Cade-Menun, unpublished data), peaks for these unknown HMW compounds are better resolved when lyophilized samples are prepared for NMR with NaOH-EDTA than with only water and D2O61, which is also reflected in the clear separation of all the myo-IHP peaks from the orthophosphate peak (Fig. S4).
The total P concentrations between paddy and non-paddy soils were tested for significant differences (set to p<0.05) by t test, one-way ANOVA was used to test significant differences of P compound concentrations among soil chronosequences, and regression functions of concentrations and distributions of various Pi and Po during pedogenesis were calculated. All statistical analyses were conducted using Sigmaplot 12.5 for Windows. To estimate accumulation rates, a mono exponential regression model was used:
where X t is the parameter of issue at cultivation time t (years), X e is the parameter stock at absolute equilibrium, X 0 is the initial parameter concentration in the tidal wetland (t=0), and k is a rate constant13.
All data generated or analysed during this study are included in this published article (and its Supplementary Information files).
X. Jiang thanks the China Scholarship Council (CSC) for financial support and acknowledges C. Walraf for technical assistance as well as Elisha Willaschek and Eva Lehndorff for help in taking sampling aliquots from the soils archive in Bonn. We thank the Chinese Academy of Sciences, Department of Soil Sciences, Nanjing, for organizing the sampling campaign, and the German Science Foundation (DFG FOR995; Am 134/9-1,2) for its funding.
X. Jiang contributed to project design, perform experiment and write the main manuscript. W. Amelung contributed to project design and initiation, field sampling and writing the paper. B. J. Cade-Menun assisted with the interpretation of NMR data and writing the paper. E. Klumpp and R. Bol contributed to project design and initiation, and writing the paper. S. Willbold conducted the NMR analyses and reviewed the manuscript. Z. Cao assisted with soil sampling and reviewing the manuscript.
The authors declare that they have no competing interests.
Electronic supplementary material
Supplementary information accompanies this paper at doi:10.1038/s41598-017-10071-0
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