PubMed · 10348034
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P Kandela. 1999-05-22. The Thames.. https://doi.org/10.1016/s0140-6736(05)75922-5
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Sulfoquinovose (SQ), a sulfonated sugar produced on a gigaton scale each year, contributes to global sulfur cycling, yet the microbes and pathways mediating its turnover in the environment have been inferred largely from genomic potential rather than direct activity. Here, we coupled incubations of environmental samples with 13C-labeled SQ to DNA-stable isotope probing to identify active SQ carbon assimilators across estuary, mangrove, and lake ecosystems. In estuarine communities, Vibrio and Cognatishimia incorporated SQ-derived 13C; Novosphingobium dominated in the mangrove, and Agrobacterium in the lake. Pure-culture experiments, coupled with comparative proteomics and gene knockout validation, demonstrated that Vibrio strains degrade SQ via modified sulfoglycolytic Embden-Meyerhof-Parnas and Entner-Doudoroff pathways to produce the environmentally significant organosulfur 2,3-dihydroxypropanesulfonate. Comparative genomic analyses suggested that closely related genome representatives of Novosphingobium, Cognatishimia, and Agrobacterium encode the sulfolytic SQ monooxygenase pathway. A global survey of aquatic microbial genomes indicated that over 9% harbor SQ degradation clusters, supporting a widespread distribution of bacterial SQ catabolic potential in aquatic environments.
A method has been developed for the speciation of trace dissolved Fe(II) and Fe(II) in water by on-line coupling of flow injection separation and preconcentration with inductively coupled plasma mass spectrometry (ICPMS). Selective determination of Fe(III) in the presence of Fe(II) was made possible by on-line formation and sorption of the Fe(III)-pyrrolidinecarbodithioate (PDC) complex in a PTFE knotted reactor over a sample acidity range of 0.07-0.4 mol L(-1) HCl, elution with 1 mol L(-1) HNO3, and detection by ICPMS. Over a sample acidity range of 0.001-0.004 mol L(-1) HCl, the sum of Fe(III) and Fe(II), i.e., Fe(III + II), could be determined without the need for preoxidation of Fe(II) to Fe(III). The concentration of Fe(II) was obtained as the difference between those of Fe(III + II) and Fe(III). With a sample flow rate of 5 mL min(-1) and a 30-s preconcentration time, an enhancement factor of 12, a retention efficiency of 80%, and a detection limit (3s) of 0.08 microg L(-1) were obtained at a sampling frequency of 21 samples h(-1). The relative standard deviation (n = 11) was 2.9% at the 10 microg L(-1) Fe(III) level. Recoveries of spiked Fe(III) and Fe(II) in local tap water, river water, and groundwater samples ranged from 95% to 103%. The concentrations of Fe(III) and Fe(II) in synthetic aqueous mixtures obtained by the proposed method were in good agreement with the spiked values. The result for total iron concentration in the river water reference material SLRS-3 was in good agreement with the certified value. The method was successfully applied to the determination of trace dissolved Fe(III) and Fe(II) in local tap water, river water, and groundwater samples.
Nitrogen from the Mississippi River Basin is believed to be at least partly responsible for the large zone of oxygen-depleted water that develops in the Gulf of Mexico each summer. Historical data show that concentrations of nitrate in the Mississippi River and some of its tributaries have increased by factors of 2 to more than 5 since the early 1900s. We have used the historical streamflow and concentration data in regression models to estimate the annual flux of nitrogen (N) to the Gulf of Mexico and to determine where the nitrogen originates within the Mississippi Basin. Results show that for 1980-1996 the mean annual total N flux to the Gulf of Mexico was 1,568,000 t/year. The flux was approximately 61% nitrate as N, 37% organic N, and 2% ammonium as N. The flux of nitrate to the Gulf has approximately tripled in the last 30 years with most of the increase occurring between 1970 and 1983. The mean annual N flux has changed little since the early 1980s, but large year-to-year variations in N flux occur because of variations in precipitation. During wet years the N flux can increase by 50% or more due to flushing of nitrate that has accumulated in the soils and unsaturated zones in the basin. The principal source areas of N are basins in southern Minnesota, Iowa, Illinois, Indiana, and Ohio that drain agricultural land. Basins in this region yield 800 to more than 3100 kg total N/km2 per year to streams, several times the N yield of basins outside this region. Assuming conservative transport of N in the Mississippi River, streams draining Iowa and Illinois contribute on average approximately 35% of the total N discharged by the Mississippi River to the Gulf of Mexico. In years with high precipitation they can contribute a larger percentage.