Repeated applications of tannins and related phenolic compounds are retained by soil and affect cation exchange capacity

Retention of tannins, produced by plants, could be important for managing soil organic matter and nutrient cycling. However, we know little about the comparative retention of different classes of tannins and related compounds or if soils have a maximum storage capacity for them. To address these questions, forest, and pasture loam soils, collected at 0-5 cm (surface) and 10-20 cm (subsurface), were repeatedly treated with water (Control) or solutions containing condensed and hydrolyzable tannins or related phenolic subunits (10 mg g⁻¹ soil). Treatments included a polymeric flavonoid-based procyanidin from sorghum, catechin, tannic acid, β-1,2,3,4,6-penta-O-galloyl-d-glucose (PGG), gallic acid, and methyl gallate. After each application, soluble-C in supernatants was determined by oxidative-combustion infrared analysis and retention of treatment-carbon by soil was calculated as the difference between added and recovered soluble-C. An interaction between soil depth and treatment was evident through all applications with highest retention of both hydrophobic (PGG) and hydrophilic (procyanidin) tannins, compared to other phenolic compounds. For all treatments except gallic acid and methyl gallate, higher sorption occurred in surface soil, which contained more organic matter than subsurface soil. With each successive application, less additional treatment-C was retained by soil and the amount of C remaining in supernatants was correlated with the presence of phenolic substances. Cumulative retention by surface soil was more than 10.3, 8.5 and 6.4 mg C g⁻¹ soil for PGG, tannic acid, and procyanidin, several times higher than the other compounds. Soluble-C extracted from treated soil, with cool water (23 °C), was 1-2 orders of magnitude greater than Control samples and highly correlated with Prussian Blue (PB) phenolics, indicating some retained treatment-C was only weakly held on the soil. The final extraction, with hot water (80 °C), removed more soluble-C, particularly from surface samples, that contained fewer PB phenolics per unit soluble-C than cool water extracts. After all extractions more than 85% of sorbed procyanidin-C was retained by samples compared to 81% of methyl gallate, 79% of PGG, 74% of tannic acid, 50% of catechin, and 40% of the gallic acid. Total C, measured in soil after all extractions, was close to expected values, confirming tannins and phenolic compounds had remained in soil and were not otherwise lost. Cation exchange capacity was increased about 30% in subsurface and forest samples by PGG, a hydrolyzable tannin, but decreased by 30% and 35% in surface and pasture soil, respectively, by its monomer, gallic acid.     

Tannic acid reduces recovery of water-soluble carbon and nitrogen from soil and affects the composition of Bradford-reactive soil protein

Tannins are plant-derived polyphenolic compounds that precipitate proteins, bind to metals and complex with other compounds. Solutions of tannic acid, or other phenolic compounds, were added to soil samples to determine if they would affect recovery of soluble soil carbon (WSC) or –nitrogen (WSN) or influence the extraction and composition of Bradford-reactive soil protein (BRSP), associated with glomalin. Tannic acid-C added with water was not completely recovered from samples and the amount of total net WSC and WSN recovered was reduced, suggesting formation of insoluble complexes. By comparison, non-tannin phenolics like gallic acid, or methyl gallate, had little effect on extraction of WSC or WSN while a simple gallotannin derived from tannic acid, 1,2,3,4,6-penta-O-galloyl-d-glucose (PGG), inhibited extraction most. The C and N concentrations in BRSP increased when soil samples were treated with tannic acid or PGG before extraction, a procedure that includes autoclaving. Increases were greatest in the 10–20 cm compared to 0–5 cm depth. Accompanying these were declines in the ratio of absorbance at 465 and 665 nm (E4/E6 ratio) of BRSP extracts suggesting formation of larger or heavier molecules. In contrast, C and N composition in lyophilized BRSP was unaffected or even slightly reduced when tannic acid or PGG were added to the BRSP extract solution after the extraction process. We conclude that some tannins can reduce the solubility of labile soil C and N, at least temporarily and given unpredictability of response associated with phenolic substances, the Bradford assay should not be relied on to quantify pools or composition of soil proteins like glomalin.     

Mineralization of soil organic nitrogen solubilized by aqua ammonia fertilizer

Organic N solubilized by NH_3(aq) was extracted from ¹⁵N-labelled or unlabelled soil, concentrated and added to non-extracted soil, which was incubated under aerobic conditions at 27±1°C. Gross N mineralization, gross N immobilization, and nitrification in soils with or without addition of unlabelled soluble organic N were estimated by models based on the dilution of the NH ₄ ⁺ or NO _inf3 ^sup- pools, which were labelled with ¹⁵N at the beginning of incubation. Mineralization of labelled organic N was measured by the appearance of label in the mineral N pool. Although gross N mineralization and gross N immobilization were increased in two soils between day 0 and day 7 following addition of unlabelled organic N solubilized by NH_3(aq), there was no increase in net N mineralization. Solubilization of ¹⁵N-labelled organic N increased and the ¹⁵N enrichment of the soluble organic N decereased as the concentration of NH_3(aq) added increased. A constant proportion of approximately one-quarter of the labelled organic N added at different rates to non-extracted soil was recovered in the mineral N pool after an incubation period of 14 days, and the availability ratios calculated from net N mineralization data were 1.1:1 and 2.1:1 for 111 and 186 mg added organic-N kg^-1 soil, respectively, indicating that the mineralization of organic N was increased by solubilization.     

Extractability of 15N-labeled corn-shoot tissue in a sandy and a clay soil by 0.01 MCaCl2 method in laboratory incubation experiments

Management of N fertilization depends not only on the mineral N measured at the beginning of the growing season but also on the status of the low-molecular-weight organic-N fraction. Our study was conducted to analyze how much of the ¹⁵N applied in labeled cornshoot tissue would be recovered in 0.01 M CaCl₂-extractable ¹⁵N fractions and wheter a decrease in the CaCl₂-extractable ¹⁵N fraction quantitatively followed the trend in net mineralization of the ¹⁵N applied in corn-shoot tissue during an incubation period. The effects of adding ¹⁵N-labeled young corn-shoot tissue to a sandy soil and a clay soil were investigated for 46 days in an aerobic incubation experiment at 25°C. The application of 80 mg N kg^-1 soil in the form of labeled corn-shoot tissue (24.62 mg ¹⁵N kg^-1 soil) resulted in a significant initial increase, followed by a decrease the labeled organic-N fraction in comparison with the untreated soils during the incubation. The labeled organic-N fraction was significantly higher in the sandy soil than in the clay soil until the 4th day of incubation. The decrease in labeled organic N in the sandy soil resulted in a subsequent increase in ¹⁵NO _inf3 ^sup- during the incubation. Ammonification of applied plant N resulted in a significant increase in the 1 M HCl-extractable non-exchangeable ¹⁵NH _inf4 ^sup+ fraction in the clay soik, owing to the vermiculite content. The ¹⁵N recovery was analyzed by the 0.01 M CaCl₂ extraction method; at the beginning of the incubation experiment, recovery was 37.0% in the sandy soil and 36.7% in the clay soil. After 46 days of incubation, recovery increased to 47.2 and 43.8% in the sandy and clay soils, respectively. Net mineralization of the ¹⁵N applied in corn-shoot tissue determined after the 46-day incubation was 6.60 mg ¹⁵N kg^-1 soil (=34.9% of the applied organic ¹⁵N) and 4.37 mg ¹⁵N kg^-1 soil (=23.1% of the applied organic ¹⁵N) in the sandy and the clay soils, respectively. The decrease in the labeled organic-N fraction extracted by 0.01 M CaCl₂ over the whole incubation period was 3.14 and 2.33 mg ¹⁵N kg^-1 soil in the sandy and clay soil, respectively. These results indicate that net mineralization of ¹⁵N was not consistent with the decrease in the labeled organic-N fraction. This may have been due to the inability of 0.01 M CaCl₂ to extract or desorb all of the applied organic ¹⁵N that was mineralized during the incubation period.     

The distribution of volatile isoprenoids in the soil horizons around Pinus halepensis trees

We measured the terpene concentration in pentane and water extracts from soil horizons (litter, organic, top and low mineral) and from roots growing in top and low mineral horizons on a distance gradient from Pinus halepensis L. trees growing alone on a grassland. Terpene concentrations in pentane were higher than in water extracts, although β-caryophyllene showed relatively high solubility in water. The litter and roots were important sources of terpenes in soil. Alpha-pinene dominated in roots growing in both “top” (A1) and “low” (B) mineral horizons (123 ± 36 μg g⁻¹ or 14 ± 5 mg m⁻²) and roots in low mineral horizon (270 ± 91 μg g⁻¹ or 7 ± 2 mg m⁻²). Beta-caryophyllene dominated in litter (1469 ± 331 μg g⁻¹ or 2004 ± 481 mg m⁻²). Terpene concentration in soil decreased with increasing distance to the trunk. This is likely to be related to changes in litter and roots type on the distance gradient from pine to grass and herbs. The relative contributions of all compounds, except α-pinene, were similar in the mineral soils and litter. This suggests that litter of P. halepensis is probably the main source of major terpene compounds. However, long-term emissions of α-pinene from P. halepensis roots might also contribute to α-pinene concentrations in rhizosphere soils.     

Effects of repeated fertilizer and cattle slurry applications over 38 years on N dynamics in a temperate grassland soil

The effects of repeated synthetic fertilizer or cattle slurry applications at annual rates of 50, 100 or 200 m³ ha⁻¹ yr⁻¹ over a 38 year period were investigated with respect to herbage yield, N uptake and gross soil N dynamics at a permanent grassland site. While synthetic fertilizer had a sustained and constant effect on herbage yield and N uptake, increasing cattle slurry application rates increased the herbage yield and N uptake linearly over the entire observation period. Cattle slurry applications, two and four times the recommended rate (50 m³ ha⁻¹ yr⁻¹, 170 kg N ha⁻¹), increased N uptake by 46 and 78%, respectively after 38 years. To explain the long-term effect, a ¹⁵N tracing study was carried out to identify the potential change in N dynamics under the various treatments. The analysis model evaluated process-specific rates, such as mineralization, from two organic-N pools, as well as nitrification from NH₄⁺ and organic-N oxidation. Total mineralization was similar in all treatments. However, while in an unfertilized control treatment more than 90% of NH₄⁺ production was related to mineralization of recalcitrant organic-N, a shift occurred toward a predominance of mineralization from labile organic-N in the cattle slurry treatments and this proportion increased with the increase in slurry application rate. Furthermore, the oxidation of recalcitrant organic-N shifted from a predominant NH₄⁺ production in the control treatment, toward a predominant NO₃⁻ production (heterotrophic nitrification) in the cattle slurry treatments. The concomitant increase in heterotrophic nitrification and NH₄⁺ oxidation with increasing cattle slurry application rate was mainly responsible for the increase in net NO₃⁻ production rate. Thus the increase in N uptake and herbage yield on the cattle slurry treatments could be related to NO₃⁻ rather than NH₄⁺ production. The ¹⁵N tracing study was successful in revealing process-specific changes in the N cycle in relationship to long-term repeated amendments.     

Some factors influencing denitrification and nitrogen immobilization in a clay soil

Nitrate-N, enriched with ¹⁵N, was added to small cores of the 0–10 cm layer of a clay soil. The base of each core was sealed, then water, equivalent to 0, 10, 20 or 30mm of rain, was added to the soil surface. The cores were incubated for 1 week at 10, 20, or 30°C in the presence or absence of wheat straw. The recovery of ¹⁵N in the soil mineral-N and organic-N fractions was then measured.No significant losses of ¹⁵N were detected in the cores which received 0–10 mm of added water, and in which the soil water content was close to 0.56 g g^?1 (?10 kPa). However, ¹⁵N losses, assumed due to denitrification, were rapid from cores receiving 20 or 30 mm of water and incubated at 20–30°C. The onset of denitrification was quite sudden as the amount of added water increased from 10 to 20 mm. In this range, a small increment of added water apparently sealed a relatively large volume of soil from atmospheric O₂ diffusion. This phenomenon was strongly temperature-dependent since no losses were detected from any cores at 10°C even though the 30mm addition of water produced a thin layer of free water across the soil surface.The addition of straw did not promote denitrification in soil at water contents close to 0.56 g g^?1. At high soil water contents, adcling straw increased immobilization of labelled NO₃^? and so reduced denitrification losses. The response of immobilization to changing soil water and temperature conditions was very different from that of denitrification.     

Estimating N2 fixation by field-grown lupins (Lupinus angustifolius L.) using soil and plant 15N enrichment

Summary Biological N₂ fixation was estimated in a field experiment following the addition of NH₄Cl or KNO₃ to unconfined microplots (1.5 m²) at 2.5 g N m^-2 (10 atom% ¹⁵N). A model of total N and ¹⁵N accumulation in lupins and decreasing ¹⁵N enrichment in the KCl-extractable soil-N pool (0–0.15 m depth) was used to estimate the proportion of N in lupins derived from biological N₂ fixation. Estimates of N₂ fixation derived from the model were compared with ¹⁵N isotope-dilution estimates obtained using canola, annual ryegrass, and wheat as nonfixing reference plants. Biomass, total N accumulation, or ¹⁵N enrichment in the lupin and reference crops did not differ whether NH _inf4 ^sup+ or NO _inf3 ^sup- was added as the labelled inorganic-N source. The decrease in soil ¹⁵N enrichment was described by first-order kinetics, whereas total N and ¹⁵N accumulation in the lupins were described by logistical equations. Using these equations, the uptake of soil N by lupins was estimated and was then used to calculate fixed N₂. Estimates of N₂ fixation derived from the model increased from 0 at 50 days after sowing to a maximum of 0.79 at 190 days after sowing. Those based on the ¹⁵N enrichment of the NO _inf3 ^sup- pool were 10% higher than those based on the mineral-N pool. ¹⁵N isotope-dilution estimates of N₂ fixation ranged from 0.37 to 0.55 at 68 days after sowing and from 0.71 to 0.77 at 190 days after sowing. Reference plant-derived values of N₂ fixation were all higher than modelled estimates during the early states of growth, but were similar to modelled estimates at physiological maturity. The use of the model to estimate N₂ derived from the atmosphere has the intrinsic advantage that the need for a non-fixing reference plant is avoided.     

Shrub-interspace dynamics alter relationships between microbial community composition and belowground ecosystem characteristics

In desert ecosystems, belowground characteristics are influenced chiefly by the formation and persistence of “shrub-islands of fertility” in contrast to barren plant interspaces. If soil microbial communities are exclusively compared between these two biogeochemically distinct soil types, the impact of characteristics altered by shrub species, especially soil C and N, are likely to be overemphasized and overshadow the role of other characteristics in structuring microbial composition. To determine how belowground characteristics influence microbial community composition, and if the relative importance of these characteristics shifts across the landscape (i.e., between and within shrub and interspace soils), changes in microbial communities across a 3000-year cold desert chronosequence were related to 27 belowground characteristics in surface and subsurface soils. When shrub and interspace communities in surface and subsurface soils were combined across the entire chronosequence, communities differed and were primarily influenced by soil C, NO₃⁻ concentrations, bulk density, pH, and root presence. Within shrub soils, microbial communities were shrub species-specific, especially in surface soils, highlighting differences in soil characteristics created by specific shrub species and/or similarity in stresses structuring shrub species and microbial communities alike. Microbial communities in shrub soils were not influenced by soil C, but by NO₃⁻ and NH₄⁺ concentrations, pH, and silt in surface soils; and Cl, P, soil N, and NO₃⁻ concentrations in subsurface soils. Interspace soil communities were distinct across the chronosequence at both depths and were strongly influenced by dune development. Interspace communities were primarily associated with soil stresses (i.e., high B and Cl concentrations), which decreased with dune development. The distribution of Gram-positive bacteria, Actinobacteria, and fungi highlighted community differences between and within shrub and interspace soils, while Gram-negative bacteria were common in all soils across the chronosequence. Of the 27 belowground characteristics investigated, 13 separated shrub from interspace communities, and of those, only five emerged as factors influencing community composition within shrub and interspace soils. As dunes develop across this cold desert chronosequence, microbial community composition was not regulated primarily by soil C, but by N and P availability and soil stresses in shrub soils, and exclusively by soil stresses in interspace soils.     

Macronutrients and metals released from soils by solutions of naturally occurring phenols

Phenolic compounds produced by plants enter the soil by leaching and litter decomposition. The goal of this work is to determine the effect of phenolic compounds on solubility of plant macronutrients and metals in agroforestry systems. Soils from forest and pasture systems were repeatedly extracted with water (control) or phenolic solutions and then compared to a Mehlich 3 reference. The phenolics were aqueous solutions of tannic acid or β –1,2,3,4,6‐penta‐O‐galloyl‐D‐glucose (PGG) (hydrolyzable tannins), procyanidin (condensed tannin), or small phenolics catechin, gallic acid, or methyl gallate. The concentration of the macronutrients Ca, Mg, K, P, and S, and the metals Fe, Al, Mn, and Zn in the supernatants was determined by inductively‐coupled plasma spectroscopy. Cumulative extraction of macronutrients was generally similar to or less than the amount obtained by the Mehlich 3 extraction with the lowest recoveries obtained with the water control, PGG, and procyanidin. Metals tended to be somewhat more extractable from forest soil, especially with gallic acid, tannic acid or PGG treatments. Three mechanisms affected extraction of analytes by phenol‐containing solutions: (1) pH‐driven dissolution (Ca and Mg), (2) chelation of the metal (Al) by the polyphenol, or (3) reduction of the metal (Fe and Mn). Relatively low extraction of nutrients by some polyphenols is attributed to the tendency of some phenols to sorb to soil. This study demonstrates that tannins and related compounds change the solubility of macronutrients and metals in soils by a complex process that is not easily predictable from simple chemical properties of the phenolics.     

Patterns of natural N in soils and plants from chemically and organically fertilized uplands

Diagnostic tests for organic production of crops would be useful. In this study, the difference in natural ¹⁵N abundances (δ¹⁵N) of soils and plants between fertilizer-applied upland (FU) and compost-applied upland (CU) fields was investigated to study using δ¹⁵N as a marker of organic produce. Twenty samples each of soils and plants were collected from each field in early summer after applying fertilizer or compost. The δ¹⁵N of fertilizers and composts was −1.6±1.5‰ (n=8) and 17.4±1.2‰ (n=10), respectively. The δ¹⁵N of total soil-N was significantly (P<0.05) higher in CU fields (8.8±2.0‰) than in FU fields (5.9±0.7‰) due to long-term continuous application of ¹⁵N-enriched compost, as indicated by a positive correlation (r=0.62) between N content and δ¹⁵N of total soil-N. The NO₃⁻ pool of CU soils (11.6±4.5‰) was also significantly (P<0.05) enriched in ¹⁵N compared to FU soils (4.7±1.1‰), while the ¹⁵N contents of NH₄⁺ pool were not different between both soils. Compost application resulted in ¹⁵N enrichment of plants; the δ¹⁵N values were 14.6±3.3‰ for CU and 4.1±1.7‰ for FU fields. These results showed that long-term application of compost resulted in a significant ¹⁵N-enrichment of soils and plants relative to fertilizer. Therefore, this study suggested that δ¹⁵N could serve as promising indicators of organic fertilizers application when used with other independent evidence. However, further studies under many conditions should be conducted to prepare reliable δ¹⁵N guidelines for organic produce, since the δ¹⁵N of inorganic soil-N and plant-N are influenced by various factors such as soil type, plant species, the rate of N application, and processes such as mineralization, nitrification, and denitrifcation.     

Effects of the addition of forest floor extracts on soil carbon dioxide efflux

Composition and effects of additions of fibric (Oi) and hemic/sapric (Oe + Oa) layer extracts collected from a 20-year-old stand of radiata pine (Pinus radiata) on soil carbon dioxide (CO₂) evolution were investigated in a 94-day aerobic incubation. The ¹³C nuclear magnetic resonance spectroscopy indicated that Oi layer extract contained greater concentrations of alkyl C while Oe + Oa layer extract was rich in carboxyl C. Extracts from Oi and Oe + Oa layers were added to a forest soil at two different polyphenol concentrations (43 and 85 μg g⁻¹ soil) along with tannic acid (TA) and glucose solutions to evaluate effects on soil CO₂ efflux. CO₂ evolution was greater in amended soils than control (deionized water) indicating that water-soluble organic carbon (WSOC) was readily available to microbial degradation. However, addition of WSOC extracted from both Oi and Oe + Oa layers containing 85 μg polyphenols g⁻¹ soil severely inhibited microbial activity. Soils amended with extracts containing lower concentrations of polyphenols (43 μg polyphenols g⁻¹ soil), TA solutions, and glucose solutions released 2 to 22 times more CO₂-C than added WSOC, indicating a strong positive priming effect. The differences in CO₂ evolution rates were attributed to chemical composition of the forest floor extracts.     

Burning effects on the distribution of organic N compounds in a 15N labelled forest soil

Nitrogen distribution was studied, by successive 1 M (H1) and 3 M HCl (H2) hydrolyses, on a natural soil before (NS) and after ¹⁵N labelling (LS) in an incubation chamber and burning (BLS) in a furnace simulating an intense fire (385 °C, 10 min). The labelling increased the organic-N of H1 (H1-N) by 4.7%, due to the increase in hydrolyzable unidentified-N (HU-N, 66.3%) and amino acids (AA-N, 11.2%), which counterbalanced the reduction of amides (AM-N, 33.2%) and amino sugars (AS-N, 68.0%). After labelling, H2-N decreased by 7.5%, mainly due to the reduction of AA-N (12.2%) and AS-N (14.9%); conversely, ammonium-N (A-N) and non-hydrolyzable-N (NH-N) did not vary and total organic-N increased slightly (2.4%). In LS, the ¹⁵N labelling decreases as follows: H1-N (with AM-N>AS-N>AA-N≈HU-N)>H2-N (with HU-N>AA-N≈A-N>AS-N)>NH-N. The added ¹⁵N was mainly incorporated in organic forms (92.2%), following the distribution of the endogenous organic-N; nevertheless, the higher proportion of recently incorporated ¹⁵N in hydrolyzable fractions, and lower in NH-N, showed that it is more labile than endogenous N. The added ¹⁵N undergoes similar, but stronger, transformations and losses due to burning than the native N: (1) 18.1% of endogenous-N and 22.4% of exogenous-N were lost; (2) H1-N, H1-¹⁵N, H2-N, H2-¹⁵N, AA-N, AA-¹⁵N, HU-N and HU-¹⁵N decreased by 69.7%, 74.1%, 76.6%, 82.9%, 96.5%, 96.8%, 92.1% and 98.3%, respectively; (3) NH-N, NH-¹⁵N, A-N and A-¹⁵N increased by 81.0%, 314%, 81.3% and 78.2%, respectively; (4) AM-N increased (51.2%) whereas AM-¹⁵N decreased (1.7%). Therefore, soil burning reduces the soil organic N reserves, through N volatilization (especially of labile N), and decreases N bio-availability, through an important net transfer of N from the labile to the recalcitrant pool; jointly, both processes will increase the negative effects of wildfires on the N cycle. In spite of the previous ¹⁵N labelling process, LS could be considered as a representative forest soil, which undergoes similar changes during burning than unlabelled soils, leading to a representative burnt labelled soil. Neither in LS nor in BLS the distribution of the added ¹⁵N was uniform among the N fractions; nevertheless, as the reference levels of ¹⁵N enrichment in the organic N fractions are accurately known, both LS (as control treatment) and BLS will be useful for further studies on the efficiency of several techniques on the post-fire restoration of the soil N distribution.     

Forms of nitrogen in cultivated soil profiles in Tanzania

In cultivated soils, total soil N, organic C and C-to-N ratios were in the range of 0.24–0.49%, 3.1–5.8% and 10.7–15.0, respectively in the surface horizons and decreased with depth. Native fixed NH⁺₄-N accounted for 2.3–3.0% of total soil N in surface horizons but while the quantities of fixed NH⁺₄-N decreased with depth, the proportion to total soil N increased. Exchangeable NH⁺₄-N ranged from 15 to 32 and NO^?₃-N from 26 to 73 μg g^?1 soil in surface horizons, and both decreased with depth. Exchangeable-N accounted for 1.1–2.4% of total soil N. Over 97% of total soil N was organically bound.Of the total soil N in the surface horizons, 29.0–79.0% was acid hydrolysable and 21.0–71.0% was nonhydrolysable. The range of proportions of each of hydrolysable NH⁺₄-N, hexosamine-N, serine plus threonine α-amino acid-N, identified-N, and unidentified-N to total soil N in the surface horizons were 14.5–22.4, 4.8–9.2, 0.2–5.8, 4.0–16.7, 23.3–48.8, and 0.3–41.5%, respectively. Hydrolysable NH⁺₄-N constituted the largest proportion of the identified-N fraction. Distribution patterns of the organic-N fractions in the profiles varied from soil to soil. Sixteen amino acids were identified which accounted for 82–100% of the α-amino acid-N fraction in the soils; glycine and alanine alone accounted for 35–40%. All the organic-N fractions were transformed to varying degree during aerobic incubation.     

Nitrogen and carbon mineralization of semi-arid shrubland soil exposed to long-term atmospheric nitrogen deposition

Anthropogenic N-deposition represents a significant input of N into semi-arid chaparral and coastal sage scrub (CSS) shrublands of southern California. High levels of atmospheric N deposition have the potential to increase soil C and N mineralization, and we hypothesize that semi-arid shrubland soil exposed to long-term (decades) high N deposition will have significantly higher C and N mineralization potentials. This hypothesis was tested in a laboratory incubation where the inorganic N (NH₄+NO₃) and CO₂ production of soils maintained at a constant temperature of 25°C and a soil moisture of 0.25 g H₂O/g (65% water-filled pore space) were sampled sequentially over a 50-week period. The temporal trend in cumulative C and N mineralization was well described by a first- and zero-order model, respectively. Long-term atmospheric N deposition significantly increased potential N mineralization but not C mineralization, and both the rate and total N mineralization were significantly positively correlated with the surface (0–10 cm) soil δ ¹⁵N natural abundance and negatively correlated with the surface soil C:N ratio. While the incubation techniques used here do not provide realistic estimates of in situ C or N mineralization, these assays indicate that atmospheric N deposition has significantly altered ecosystem N storage and cycling.     

Studies of nitrogen immobilization and mineralization in calcareous soils—IV. Changes in the organic nitrogen of light and heavy subfractions of silt- and fine clay-size particles during nitrogen turnover

A calcareous clay nd a calcareous sand, were fractionated densimetrically by dispersion in organic liquids of sp. gr. 1.59–2.06. The N contents of the light fractions decreased with increasing densities of the suspending liquids and were up to 18–23 times higher than those of the whole soils. Light fraction organic-N of both the sandy and clay soils was obtained mainly from silt-size components. However, the efficiency, with which light fraction material was obtained from the two whole soils, varied. With the clay soil, the total yield of light fraction organic-N was increased markedly by applying the densimetric technique to particle size components, rather than to the whole soil.Silt-size and fine clay-size particles from soils, sampled during rapid metabolism of microbial organic-[¹⁵N], were further fractionated densimetrically in “Nemagon”, sp. gr. 2.06. The organic-[¹⁵N] of the light and heavy subtractions changed markedly (P < 0.05) during periods of net ¹⁵N immobilization and mineralization, including a period after soil fumigation when extensive decomposition of [¹⁵N]-labelled microbial biomass occurred. Changes in the ¹⁵N of complementary light and heavy subfractions followed similar trends. Light subtraction organic-[¹⁵N] usually showed the greater relative change but the differences between the subtractions were not statistically significant. It is concluded that when small proportions only of soil organic-N are associated with macroorganic debris, as in these two soils amended wth glucose and ¹⁵NO^?₃, densimetric fractionation at a sp. gr. as high as 2.06 will yield light and heavy fractions, whose nitrogenous components are similarly available to biological attack. Enhanced metabolism of light fraction material is more likely to be demonstrated when such material consists mainly of obvious plant residues, and this may be more easily achieved by fractionation in liquids of sp. gr. <2.     

Nitrogen contribution by leucaena (Leucaena leucocephala) prunings to maize in an alley cropping system

Summary The N uptake of maize was assessed on an Alfisol in a sole crop and in an alley cropping system in southwestern Nigeria. Although the application of prunings increased the maize N content in both sole and alley-cropped maize, the N contributed to the maize by the prunings was low, ranging between 4.4 and 23.8 kg ha^–1. This was equivalent to 3.2% and 9.407% of the N released during decomposition of the prunings. Application of the prunings increased the grain yields of the sole maize by 38% and the maize yield in the alley-cropped plots by 104%, compared with yields in the corresponding plots where prunings were not applied. The results indicate that part of the N from the prunings was retained in the soil organic-N pool. Maize N, dry weights and grain yields were lowest in the alley-cropped plots where prunings were removed, probably because of competition between the maize and the hedgerow trees.     

Sorption of benzoic acid onto soil colloids and its implications for allelopathy studies

The fate of allelochemicals in the soil environment largely determines the expression of allelopathy in the natural environment. In allelopathy research, the sorption of allelochemicals onto soil particles has been less well studied than their degradation. A study was carried out to evaluate the growth of cucumber (Cucumis sativus var Marketmore 76) and radish (Raphanus sativus var Crimson giant) in soil amended with 1, 5, 10 and 20 mg l^–1 benzoic acid as model allelopathic substance. Growth of both cucumber and radish was not inhibited in soil amended with benzoic acid. A labeled study indicates that sorption of benzoic acid onto soil particles increases with concentration. Benzoic acid isotherms of both soils were non-linear, with an N value of 0.875 for a garden soil and 0.891 for a garden soil + sand, and they may explain the reason for the limited allelopathic effect of benzoic acid at concentrations often recorded in natural soil.     

Effects of 15N-labelled ammonium nitrate and urea on soil nitrogen during growth of wheat (Triticum aestivum L.) under field conditions

We studied the effects of ¹⁵N-labelled ammonium nitrate and urea on the yield and uptake of labelled and unlabelled N by wheat (Triticum aestivum L., cv. Mexi-Pak-65) in a field experiment. The dry matter and N yields were significantly increased with fertilizer N application compared to those from unfertilized soil. The wheat crop used 33.6–51.5 and 30.5–40.9% of the N from ammonium nitrate and urea, respectively. Splitting the fertilizer N application had a significant effect on the uptake of fertilizer N by the wheat. The fertilizer N uptake showed that ammonium nitrate was a more available source of N for wheat than urea. The effective use of fertilizer N (ratio of fertilizer N in grain to fertilizer N in whole plant) was statistically similar for the two N fertilizers. The application of fertilizer N increased the uptake of unlabelled soil N by wheat, a result attributed to a positive added N interaction, which varied according to the fertilizer N split; six split applications gave the highest added N interaction compared to a single application or two split applications for both fertilizers. Ammonium nitrate gave 90.5, 33.5, and 48.5% more added N interaction than urea with one, two, and six split N applications. A values were not significantly correlated with the added N interaction (r=0.557). The observed added N interaction may have been the result of pool substitution, whereby added labelled fertilizer N replaced unlabelled soil N.     

Sorptive interaction between goethite and strongly reducing organic substances from anaerobic decomposition of green manures

Strongly reducing organic substances (SROS) and iron oxides exist widely in soils and sediments and have been implicated in many soil and sediment processes. In the present work, the sorptive interaction between goethite and SROS derived from anaerobic decomposition of green manures was investigated by differential pulse voltammetry (DPV). Both green manures, Astragalus sinicus (Astragalus) and Vicia varia (Vicia) were chosen to be anaerobically decomposed by the mixed microorganisms isolated from paddy soils for 30 d to prepare different SROS. Goethite used in experiments was synthesized in laboratory. The anaerobic incubation solutions from green manures at different incubation time were arranged to react with goethite, in which SROS concentration and Fe(II) species were analyzed. The anaerobic decomposition of Astragalus generally produced SROS more in amount but weaker in reducibility than that of Vicia in the same incubation time. The available SROS from Astragalus that could interact with goethite was 0.69 ± 0.04, 0.84 ± 0.04 and 1.09 ± 0.03 cmol kg⁻¹ as incubated for 10, 15 and 30 d, respectively, for Vicia, it was 0.12 ± 0.03, 0.46 ± 0.02 and 0.70 ± 0.02 cmol kg⁻¹. One of the fates of SROS as they interacted with goethite was oxidation. The amounts of oxidizable SROS from Astragalus decreased over increasing incubation time from 0.51 ± 0.05 cmol kg⁻¹ at day 10 to 0.39 ± 0.04 cmol kg⁻¹ at day 30, but for Vicia, it increased with the highest reaching to 0.58 ± 0.04 cmol kg⁻¹ at day 30. Another fate of these substances was sorption by goethite. The SROS from Astragalus were sorbed more readily than those from Vicia, and closely depended upon the incubation time, whereas for those from Vicia, the corresponding values were remarkably less and apparently unchangeable with incubation time. The extent of goethite dissolution induced by the anaerobic solution from Vicia was greater than that from Astragalus, showing its higher reactivity.