- Open Access
Denitrification from nitrogen-fixing biologically crusted soils in a cool desert environment, southeast Utah, USA
© Barger et al.; licensee Springer. 2013
Received: 19 January 2013
Accepted: 23 May 2013
Published: 20 June 2013
Nitrogen fixation by microorganisms within biological soil crust (“biocrust”) communities provides an important pathway for N inputs in cool desert environments where soil nutrients are low and symbiotic N-fixing plants may be rare. Estimates of N fixation in biocrusts often greatly exceed that of N accretion rates leading to uncertainty regarding N loss pathways.
In this study we examined nitrogen fixation and denitrification rates in biocrust communities that differed in N fixation potential (low N fixation = light cyanobacterial biocrust, high N fixation = dark cyanolichen crust) at four temperature levels (10, 20, 30, 40°C) and four simulated rainfall levels (0.05, 0.2, 0.6, 1 cm rain events) under controlled laboratory conditions.
Acetylene reduction rates (AR, an index of N fixation activity) were over six-fold higher in dark crusts relative to light crusts. Dark biocrusts also exhibited eight-fold higher denitrification rates. There was no consistent effect of temperature on denitrification rates, but there was an interactive effect of water addition and crust type. In light crusts, denitrification rates increased with increasing water addition, whereas the highest denitrification rates in dark crusts were observed at the lowest level of water addition.
These results suggest that there are no clear and consistent environmental controls on short-term denitrification rates in these biologically crusted soils. Taken together, estimates of denitrification from light and dark biocrusts constituted 3 and 4% of N fixation rates, respectively suggesting that losses as denitrification are not significant relative to N inputs via fixation. This estimate is based on a previously published conversion ratio of ethylene produced to N fixed that is low (0.295), resulting in high estimates of N fixation. If future N fixation studies in biologically crusted soils show that these ratios are closer to the theoretical 3:1 ratio, denitrification may constitute a more significant loss pathway relative to N fixed.
Biological soil crusts (“biocrusts”) are diverse communities of cyanobacteria, algae, lichens, mosses, fungi, and other bacteria, which exist in open soil areas not favorable for the growth of higher autotrophs. They comprise up to 70% of the living cover at many sites in arid and semi-arid regions of the western United States (Belnap et al. 2001), contributing to a broad range of ecological functions. One such function of primary importance in dryland ecosystems is the ability of microorganisms within biocrusts to fix atmospheric nitrogen (N) (Mayland and McIntosh 1966; Zaady et al. 1998; Evans and Belnap 1999; Hartley and Schlesinger 2002; Billings et al. 2003; Johnson et al. 2007). Nitrogen fixation by microorganisms within biocrust communities provides an important pathway for N inputs in cool desert environments that are characteristically low in nutrient availability and have a paucity of symbiotic N-fixing plants.
What has been less clear is the fate of the N fixed by biocrust organisms and whether N fixed is retained within the ecosystem. Estimates of N fixation in biocrusts often greatly exceed that of N accretion rates (Peterjohn and Schlesinger 1990), leading to uncertainty regarding the fate of the fixed N by biologically crusted soils and the potentially important N loss pathways. Soils in dryland ecosystems are characterized by pulse precipitation events resulting in wet and drying cycles. These pulsed dynamics in soils may result in N “leakage” by biological soil crust organisms to the surrounding soil environment in such forms as NH4+ and other soluble organic nitrogen compounds (Mayland and McIntosh 1966; Johnson et al. 2007). Nitrogen leakage from biocrusts may not only enhance soil nutrient availability to support plant growth (Mayland and McIntosh 1966; Belnap and Harper 1995but may also be lost from the system via gaseous N loss in transformations related to nitrification and denitrification processes (Zaady 2005; Barger et al. 2005; Johnson et al. 2007; Strauss et al. 2012; Brankatschk et al. 2013).
Denitrification is the biological process that occurs under reducing conditions where NO3- is used by denitrifying bacteria (primarily heterotrophic bacteria) in the absence of O2 as an electron acceptor. NO3- is converted to NO, N2O and N2 along a reduction pathway. Factors regulating denitrification rates are low O2 partial pressure, available NO3- to serve as an oxidant, and organic C as an energy source for heterotrophic bacteria (Williams et al. 1992). Previously, it was thought that denitrification in dryland ecosystems should be low because anaerobic conditions should rarely occur in arid environments. However, the presence of anaerobic microsites within dryland soils is not as rare as previously believed with oxygen levels reaching near zero in the surface soils (Garcia-Pichel and Belnap 1996; Johnson et al. 2007). A large portion of the microbial community resides in the top few millimeters of dryland soils. Thus a pulse in microbial activity after a rain event may quickly reduce soil oxygen levels (Garcia-Pichel and Belnap 1996; Johnson et al. 2007).
Estimates of denitrification are highly variable in desert ecosystems ranging from 0.4 to 9 kg N ha-1 year-1 in hot North American deserts (e.g., Chihuahuan and Sonoran) ( Virginia et al.1982; Peterjohn and Schlesinger 1991; Guilbault and Matthias 1998; Schade et al. 2002). In soils from a cold desert site on the Colorado Plateau, denitrification was estimated as high as 19 kg N ha-1 year-1 (West and Skujins 1977). These highly variable estimates are likely driven by high spatial and temporal variability (e.g., hot spots and hot moments) in denitrification rates. Both biotic and abiotic processes drive patterns in resource distribution in dryland ecosystems resulting in accumulation of nutrients beneath shrub and tree canopies relative to interspace soils in what has been previously described as “islands of fertility” (Noy-Meir 1985; Schlesinger and Pilmanis 1998). At a Sonoran desert site, Virginia et al. (1982) reported a 58-fold increase in denitrification rates under Prosopis glandulosa, an N-fixing shrub, as compared to plant interspaces. These patterns in denitrification suggest that high N availability associated with N fixation is an important driver of this process.
Past studies of denitrification in biologically crusted soils have yielded a wide range of denitrification rates. Denitrification rates within surface soils (i.e., top 1 cm) containing biocrusts were negligible relative to other N loss pathways (Johnson et al. 2007; Strauss et al. 2012) or increased with biocrust development (Brankatschk et al. 2013). These studies, however, evaluated denitrification from biologically crusted soils at a single temperature and soil moisture level, environmental conditions that may strongly influence not only N fixation but also denitrification rates.
Following this, our objective was to examine the influence of biocrust community on denitrification rates across a range of environmental conditions in the lab to better understand the potential for denitrification from biocrust communities in dryland ecosystems. We hypothesized that denitrification rates would increase with increasing N fixation potential of the biocrust community and that environmental conditions such as temperature and soil moisture would further influence these rates. In this study, we examined nitrogen fixation and denitrification rates in two biocrust communities that differed in their N fixation potential (light cyanobacterial biocrust and dark cyanolichen crust) at four temperature levels (10, 20, 30, 40°C) and four simulated rainfall levels (0.05, 0.2, 0.6, 1 cm rain events) under controlled laboratory conditions.
In the spring of 2009, intact biocrust cores were collected to a 5 cm depth near the Island-in-the-Sky District of Canyonlands National Park, UT (38˚33'19.7" N, 109˚44'38.8" 1,883 m.a.s.l.). Mean annual precipitation in this area was 231 mm ranging from a low of 179 mm to a high of 327 mm in the 10 years prior to our study (NADP site UT09). Throughout Canyonlands, well-developed biocrust communities often occur on Rizno, dry-Rock outcrop soils, which are classified as loamy, mixed calcareous, mesic Lithic Ustic Torriorthents (Web Soil Survey, http://websoilsurvey.nrcs.usda.gov/app/HomePage.htm). High sand content and low organic C and N characterize these soils.
Visual inspection of the presence of lichen species and coloration in biocrusts is a strong indicator of biocrust community structure and function across the cool desert regions of the western U.S. (Barger et al. 2005; Belnap et al. 2008). In our study we used visual inspection of biocrust color in the field to evaluate the N fixation potential of the biocrust community. “Light” biologically crusted soils are often dominated by the free-living filamentous cyanobacteria Microcoleus vaginatus and M. steenstruppi (Gundlapally and Garcia-Pichel 2006) with little to no presence of dark pigmented cyanobacteria (Yeager et al. 2004). In contrast, “dark” biologically crusted soils contain not only Microcoleus spp. but also the darker pigmented cyanobacteria such as Scytonema myochrous and Nostoc commune (Yeager et al. 2004; Gundlapally and Garcia-Pichel 2006). In addition to these cyanobacterial organisms, the N-fixing lichens Collema tenax and C. coccophorum may also be present on dark biologically crusted soils. Coloration is not only an indicator of microorganism composition but also biocrust function. Chlorophyll a (chla), exopolysaccharide, and soil aggregate stability are strongly and positively correlated with biocrust darkness (Belnap et al. 2008).
In the field, biocrusts were gently covered with a towel and wet by a watering can with distilled water in order to minimize breaking of the crust surface during sampling. We used a 5.3 cm diameter polyvinyl chloride (PVC) cylinder to core the soil and then gently retrieved the core with a spatula and fitted the bottom with a plastic cap. Sampling was done within the soil type described above within a 30 × 30 m area. We collected 64 cores from both light and dark biocrusts for a total of 128 cores. Following collection, soils within the PVC cylinders were allowed to dry immediately in overcast/sunny conditions and transported to the laboratory.
Although we based our field collections on visual assessment of coloration, we further quantified biocrust cover in the lab. Biocrust cover was measured for each 22 cm2 core using the point-intercept method. A small wire grid with evenly spaced cells was placed on the surface of each core. Cover at each point on the grid was classified using the six different cover classes: light cyanobacteria, dark cyanobacteria, Collema lichens, all other lichens, moss, and rock.
To examine the influence of water addition and temperature on nitrogen fixation and denitrification rates, we conducted a full factorial design of biocrust color (dark, light), simulated rain event size (0.05, 0.2, 0.6, 1 cm), and temperature (10, 20, 30, 40°C) in the laboratory. Within the light and dark biocrusts, each core received water addition to simulate rain events of a specific size. The four rain event sizes were chosen to represent the amount of water these biocrust organisms may experience under field conditions. Each of these cores was then incubated at one of the four experimental temperatures. There were four replicates within each level of rain event and incubation temperature.
Acetylene reduction assay
Incubation chambers were constructed of mason jars that were pre-drilled through the glass bottom and plugged with a stopper that had a small section of glass tubing fitted with half-hole septa. When incubation chambers were assembled, crust cores were placed on the jar lid and the jar was turned upside down, allowing cores to be fully exposed to the incubation lights. Biocrusts were wetted with deionized water at the levels described above and placed in incubators in open mason jars for a period of 4 h at the desired temperature. Following the pre-incubation period, jars were plugged with rubber stoppers to form an airtight chamber and a 10% acetylene atmosphere was created in each chamber by first removing a volume of headspace and replacing that same volume with acetylene gas. Acetylene gas was made in the lab by reacting calcium carbide with water and trapping the gas generated from the reaction in an airtight gas sampling bag. After the 4 h pre-incubation, biocrust cores were immediately incubated in the presence of the acetylene atmosphere for an additional 2 h. Following the 2 h incubation, a gas sample was drawn from the chambers using an airtight syringe fitted with a needle and injected into pre-evacuated Exetainers (Labco Limited, UK). Ethylene and N2O gas were simultaneously analyzed by gas chromatography (Shimadzu, Columbia, MD) equipped with both an FID and an ECD, such that there was a front flush mechanism in order to prevent acetylene exposure to the ECD, and fitted with a 1 cm sample loop.
Following incubation, biocrust cores were cut into cross-sections of the 0–2 and 2–5 cm sections. Total soil mass of each sub-sample was recorded. Each horizon was homogenized and then split for different analyses. A subsample of each horizon was extracted immediately with 40 mL of 2M KCl for 1 h on a reciprocal shaker. Soil extracts were filtered (Whatman #1) and were immediately frozen. NH4+ concentrations were analyzed using the phenol-hypochlorite reaction described by Weatherburn (1967), and NO3- was determined using a method adapted from Doane and Horwáth (2003). Both NH4+ and NO3- were determined colorimetrically using a microplate reader (Biotek, Winooski, VT). An additional subsample of each horizon was dried at 105°C for gravimetric water content determination. Samples from each horizon were split and oven dried (60°C) for organic carbon [C] and N analysis. Total organic soil C and N measurements were made on a CHN 4010 Elemental Combustion System (Costech Analytical Technologies, Valencia, CA). All C and N analyses were calibrated with an atropine standard. Soil inorganic carbon was determined using the modified pressure transducer method (Sherrod et al. 2002). A subsample of the 0–2 cm sample was removed for chla analysis and air-dried, sieved, and ground. Chla was extracted with ethanol (Castle et al. 2011) and assessed spectrophotometrically (Beckman DU-64, Beckman Instruments Inc., Fullerton, CA). Soil texture was determined using a modified rapid method procedure described by Kettler et al. (2001), which involved removing carbonates and organic matter using sodium acetate and sodium hypochlorite, respectively.
Acetylene reduction (AR) assay data and denitrification rates were log transformed to meet the assumptions of parametric statistical tests. Denitrification rates were highly variable across samples. Thus denitrification rates that were greater than three standard deviations from the mean were removed before analysis. When this cutoff was applied, only one dark biocrust core incubated at 30°C with a 0.5 cm water addition was removed from the analysis. We conducted a three-way analysis of variance (ANOVA) of AR activity, denitrification rates, and inorganic N pools evaluating the two crust types (light, dark), four levels of temperature, and four levels of moisture (IBM SPSS Statistics 20.0).
Results and discussion
Biocrust biological, physical, and chemical characteristics
μg g soil-1
Soil texture (0–5 cm)
% by mass
% by mass
% by mass
Soil organic C 0–2 cm
% by mass
Soil organic C 2–5 cm
% by mass
Soil total N 0–2 cm
% by mass
Soil total N 2–5 cm
% by mass
The higher N fixation rates in dark crust were likely due not only to the presence of the N-fixing Collema spp. but also the higher level of N-fixing cyanobacteria as supported by the nearly two-fold greater soil chla in dark biocrust soils relative to light biocrusts (Table 1). Overall, these results are consistent with patterns and controls on N fixation in biologically crusted soils in cool desert environments, confirming that dark biologically crusted soil has higher N fixation potential than light crusts with optimal temperatures for fixation occurring around 20°C (Belnap 2002; Johnson et al. 2007).
Estimates of N gas loss from biocrusts
Nitrogen fixation and gas loss from biocrusts
μg N m-2day-1
μg N m-2day-1
Johnson et al. 2007*
Strauss et al. 2012*
Brankatschk et al. 2013†
(Germany inland dune)
Barger et al. 2005*
Evans and Johansen 1999
Although denitrification rates were higher in dark biocrusts that exhibited higher N fixation rates relative to light biocrusts, denitrification rates were much lower than those observed beneath the N-fixing shrub, P. glandulosa, in the Sonoran desert. Denitrification rates were two orders of magnitude lower in our study of N-fixing biocrusts relative to the N-fixing shrub P. glandulosa (27,840 μg N m-2 day-1; Virginia et al. 1982). Following this, we would predict that denitrification rates will be enhanced by the presence of N-fixing cyanobacteria and lichens in biocrusts, but rates are not on par with those observed in soils beneath symbiotic N-fixing plants.
There was no consistent effect of temperature on denitrification rates, but there was an interactive effect of water addition and biocrust type. In light crusts, denitrification rates increased with increasing water addition, whereas the highest denitrification rates (but also the most variable) in dark crusts were observed at the lowest level of water addition (Figure 2A, B, crust × water, F = 3.93 P = 0.001). Previous studies of denitrification enzyme activity (DEA) in desert soils showed optimal activities at 40°C (Peterjohn 1991). In contrast to these results, some the highest denitrification rates in dark biocrusts in our study occurred at 10 and 20°C after a 1 cm simulated rain event (Figure 2B). Although the amount of water added did influence denitrification rates, it did not do so in a predictable manner. Percent soil moisture ranged from less than 1% in the 0.05 cm rainfall simulation up to 11% in the 1 cm rainfall in the top 0–2 cm of soil (mean % soil moisture; 0.05 cm = 0.05%; 0.2 cm = 3%; 0.6 cm = 7%; 1.0 cm = 12%). These results are in contrast to previous studies that have shown strong differences in denitrification rates with varying soil moisture levels (Groffman and Tiedje 1988). Overall the lack of a consistent response to our temperature and water manipulations suggests that more traditional modeling approaches of denitrification dynamics, which are often based on environmental variables, would fail to adequately describe denitrification rates in biocrust soil systems.
Extractable soil NH4+ was nearly 40% higher in dark crusts relative to light crusts [Figure 3C, D; mean NO3- (mg g soil-1): light = 0.66, dark = 1.00]. There was also an interactive effect of temperature and water addition on soil NH4+, in which levels were two- to three-fold higher at the 40°C and highest levels of water additions (Figure 3C, D). High extractable NH4+ levels at 40°C may be due to increased mineralization at this temperature but also declines in NH4+ uptake by biocrusts. Although microorganisms within biocrusts fix N, biocrusts may also exhibit high uptake rates of NH4+ when active. Biocrust photosynthetic activity, however, declines dramatically at temperatures at or above 40°C (Lange et al. 1998). This pattern of NH4+ release has been observed in previous studies, in which NH4+ production in soils peaked at approximately 50–60°C (Chantigny et al. 2010). Overall the higher soil organic C in addition to NO3- levels in dark biocrusts relative to light biocrusts may support the observed higher denitrification rates in our study.
Coupling N fixation to denitrification
Our hypothesis that denitrification rates would increase with increasing N fixation potential of biologically crusted soils was supported in this study. Denitrification rates from dark cyanolichen biocrusts were eight-fold higher than light cyanobacterial crusts. In contrast to numerous studies across a broad range of ecosystems, soil moisture and temperature had inconsistent and mixed effects on denitrification rates. Taken together, estimates of denitrification from light and dark biocrusts in this lab experiment constituted 3 and 4% of N fixation rates, respectively, indicating that denitrification rates are unlikely to be significant relevant to N inputs via fixation.
We would like to thank Heidi Guenther, Matt Ross, and Conor Morrison, who all helped conduct the laboratory experiment. In addition, we would like to thank Will Wieder and the Townsend Lab at the University of Colorado for assistance analyzing gas samples and Dr. William Adams for providing use of laboratory equipment. Finally, we would like to acknowledge the two anonymous reviewers and Dr. Bettina Weber for reviewing the manuscript.
- Barger NN: Biogeochemical cycling and N dynamics of biological soil crusts in a semi-arid ecosystem. PhD Dissertation, Colorado State University, Ft. Collins; 2003.Google Scholar
- Barger NN, Belnap J, Ojima DS, Mosier A: NO gas loss from biologically crusted soils in Canyonlands National Park, Utah. Biogeochemistry 2005, 75: 373–391. 10.1007/s10533-005-1378-9View ArticleGoogle Scholar
- Belnap J: Nitrogen fixation in biological soil crusts from southeast Utah, USA. Biol Fertil Soils 2002, 35: 128–135. 10.1007/s00374-002-0452-xView ArticleGoogle Scholar
- Belnap J, Harper K: Influence of cryptobiotic soil crusts on elemental content of tissue of two desert seed plants. Arid Soil Res Rehabil 1995, 9: 107–115. 10.1080/15324989509385879View ArticleGoogle Scholar
- Belnap J, Rosentreter R, Leonard S, Kaltenecker JH, Williams J, Eldridge D: Biological soil crusts: ecology and management. US Department of the Interior Technical Reference 1730–2, US Dept of the Interior, Denver; 2001.Google Scholar
- Belnap J, Phillips SL, Witwicki DL, Miller ME: Visually assessing the level of development and soil surface stability of cyanobacterially dominated biological soil crusts. J Arid Environ 2008, 72: 1257–1264. 10.1016/j.jaridenv.2008.02.019View ArticleGoogle Scholar
- Billings SA, Schaeffer SM, Evans RD: Nitrogen fixation by biological soil crusts and heterotrophic bacteria in an intact Mojave Desert ecosystem with elevated CO2 and added soil carbon. Soil Biol Biochem 2003, 35: 643–649. 10.1016/S0038-0717(03)00011-7View ArticleGoogle Scholar
- Brankatschk R, Fischer T, Veste M, Zeyer J: Succession of N cycling processes in biological soil crusts on a Central European inland dune. FEMS Microbiol Ecol 2013, 83: 149–160. 10.1111/j.1574-6941.2012.01459.xView ArticleGoogle Scholar
- Castle SC, Morrison CD, Barger NN: Extraction of chlorophyll a from biological soil crusts: a comparison of solvents for spectrophotometric determination. Soil Biol Biochem 2011, 43: 853–856. 10.1016/j.soilbio.2010.11.025View ArticleGoogle Scholar
- Chantigny MH, Curtin D, Beare MH, Greenfield LG: Influence of temperature on water-extractable organic matter and ammonium production in mineral soils. Soil Sci Soc Am J 2010, 74: 517–524. 10.2136/sssaj2008.0347View ArticleGoogle Scholar
- Doane TA, Horwáth WR: Spectrophotometric determination of nitrate with a single reagent. Anal Lett 2003, 36: 2713–2722. 10.1081/AL-120024647View ArticleGoogle Scholar
- Evans RD, Belnap J: Long-term consequences of disturbance on nitrogen dynamics in an arid ecosystem. Ecology 1999, 80: 150–160. 10.1890/0012-9658(1999)080[0150:LTCODO]2.0.CO;2View ArticleGoogle Scholar
- Evans RD, Johansen JR: Microbiotic crusts and ecosystem processes. Crit Rev Plant Sci 1999, 18: 183–225. 10.1016/S0735-2689(99)00384-6View ArticleGoogle Scholar
- Garcia-Pichel F, Belnap J: Microenvironments and microscale productivity of cyanobacterial desert crusts. J Phycol 1996, 32: 774–782. 10.1111/j.0022-3646.1996.00774.xView ArticleGoogle Scholar
- Groffman PM, Tiedje JM: Denitrification hysteresis during wetting and drying cycles in soil. Soil Sci Soc Am J 1988, 52: 1626–1629. 10.2136/sssaj1988.03615995005200060022xView ArticleGoogle Scholar
- Guilbault MR, Matthias AD: Emissions of N2O from Sonoran Desert and effluent-irrigated grass ecosytems. J Arid Environ 1998, 38: 87–98. 10.1006/jare.1997.0300View ArticleGoogle Scholar
- Gundlapally SR, Garcia-Pichel F: The community and phylogenetic diversity of biological soil crusts in the Colorado Plateau studied by molecular fingerprinting and intensive cultivation. Microb Ecol 2006, 52: 345–357. 10.1007/s00248-006-9011-6View ArticleGoogle Scholar
- Hartley A, Schlesinger W: Potential environmental controls on nitrogenase activity in biological crusts of the northern Chihuahuan Desert. J Arid Environ 2002, 52: 293–304. 10.1006/jare.2002.1007View ArticleGoogle Scholar
- Johnson SL, Neuer S, Garcia-Pichel F: Export of nitrogenous compounds due to incomplete cycling within biological soil crusts of arid lands. Environ Microbiol 2007, 9: 680–689. 10.1111/j.1462-2920.2006.01187.xView ArticleGoogle Scholar
- Kettler TA, Doran JW, Gilbert TL: Simplified method for soil particle-size determination to accompany soil-quality analyses. Soil Sci Soc Am J 2001, 65: 849–852. 10.2136/sssaj2001.653849xView ArticleGoogle Scholar
- Lange OL, Belnap J, Reichenberger H: Photosynthesis of the cyanobacterial soil-crust lichen Collema tenax from arid lands in southern Utah, USA: role of water content on light and temperature responses of CO2 exchange. Funct Ecol 1998, 12: 195–202. 10.1046/j.1365-2435.1998.00192.xView ArticleGoogle Scholar
- Liengen T: Conversion factor between acetylene reduction and nitrogen fixation in free-living cyanobacteria from high Arctic habitats. Can J Microbiol 1999, 45: 223–229. 10.1139/w98-219View ArticleGoogle Scholar
- Mayland HF, McIntosh TH: Availability of biologically fixed atmospheric nitrogen-15 to higher plants. Nature 1966, 209: 421–422. 10.1038/209421a0View ArticleGoogle Scholar
- Montoya JP, Voss M, Kahler P, Capone DG: A simple, high-precision, high-sensitivity tracer assay for N2 fixation. Appl Environ Microbiol 1996, 62: 986–993.Google Scholar
- Nohrstedt H: Conversion factor between acetylene reduction and nitrogen fixation in soil: effect of water content and nitrogenase activity. Soil Biol Biochem 1983, 15: 275–279. 10.1016/0038-0717(83)90071-8View ArticleGoogle Scholar
- Nohrstedt H: Nonsymbiotic nitrogen fixation in the topsoil of some forest stands in central Sweden. Can J For Res 1985, 15: 715–722. 10.1139/x85-116View ArticleGoogle Scholar
- Noy-Meir I: Desert ecosystem structure and function. In Hot deserts and arid shrublands. Edited by: Evenari M. Elsevier Science, Amsterdam; 1985.Google Scholar
- Peterjohn W: Denitrification: enzyme content and activity in desert soils. Soil Biol Biochem 1991, 23: 845–855. 10.1016/0038-0717(91)90096-3View ArticleGoogle Scholar
- Peterjohn WT, Schlesinger WH: Nitrogen loss from deserts in the southwestern United States. Biogeochemistry 1990, 10: 67–79.View ArticleGoogle Scholar
- Peterjohn WT, Schlesinger WH: Factors controlling denitrification in a Chihuahuan desert ecosystem. Soil Sci Soc Am J 1991, 55: 1694–1701. 10.2136/sssaj1991.03615995005500060032xView ArticleGoogle Scholar
- Rice WA, Paul EA: The acetylene reduction assay for measuring nitrogen fixation in water-logged soil. Can J Microbiol 1971, 17: 1049–1056. 10.1139/m71-166View ArticleGoogle Scholar
- Schade JD, Marti E, Welter JR, Fisher SG, Grimm NB: Sources of nitrogen to the riparian zone of a desert stream: implications for riparian vegetation and nitrogen retention. Ecosystems 2002, 5: 68–79. 10.1007/s10021-001-0056-6View ArticleGoogle Scholar
- Schlesinger WH, Pilmanis AM: Plant-soil interactions in deserts. Biogeochemistry 1998, 42: 169–187. 10.1023/A:1005939924434View ArticleGoogle Scholar
- Sherrod LA, Dunn G, Peterson GA, Kolberg RL: Inorganic carbon analysis by modified pressure-calcimeter method. Soil Sci Soc Am J 2002, 66: 299–305. 10.2136/sssaj2002.0299View ArticleGoogle Scholar
- Strauss SL, Day TA, Garcia-Pichel F: Nitrogen cycling in desert biological soil crusts across biogeographic regions in the southwestern United States. Biogeochemistry 2012, 108: 171–182. 10.1007/s10533-011-9587-xView ArticleGoogle Scholar
- Sullivan TJ, McDonnell TC, McPherson GT, Mackey SD, Moore D: Evaluation of the sensitivity of inventory and monitoring of National Parks to nutrient enrichment effects from atmospheric nitrogen deposition. Nat Resour Rep NPS/NRPC/ARD/NRR 2011/321, US Dept of the Interior, Denver; 2011.Google Scholar
- Virginia RA, Jarrell WM, Franco-Vizcaino E: Direct measurement of denitrification in a Prosopis (Mesquite) dominated Sonoran Desert ecosystem. Oecologia 1982, 53: 120–122. 10.1007/BF00377145View ArticleGoogle Scholar
- Weatherburn MW: Phenol-hypochlorite reaction for determination of ammonia. Analytical Chem 1967, 39: 971–974. 10.1021/ac60252a045View ArticleGoogle Scholar
- West NE, Skujins JJ: The nitrogen cycle in North American cold-winter semi-desert ecosystems. Oecol Plant 1977, 12: 45–53.Google Scholar
- Williams EJ, Hutchinson GL, Fehsenfeld FC: NOx and N2O emissions from soil. Glob Biogeochem Cycles 1992, 6: 351–388. 10.1029/92GB02124View ArticleGoogle Scholar
- Yeager CM, Kornosky JL, Housman DC, Grote EE, Belnap J, Kuske CR: Diazotrophic community structure and function in two successional stages of biological soil crusts from the Colorado Plateau and Chihuahuan Desert. Appl Environ Microbiol 2004, 70: 973–983. 10.1128/AEM.70.2.973-983.2004View ArticleGoogle Scholar
- Zaady E: Seasonal change and nitrogen cycling in a patchy Negev Desert: a review. Arid Land Res Manage 2005, 19: 111–124. 10.1080/15324980590916512View ArticleGoogle Scholar
- Zaady E, Groffman PM, Shachak M: Nitrogen fixation in macro- and microphytic patches in the Negev desert. Soil Biol Biochem 1998, 30: 449–454. 10.1016/S0038-0717(97)00195-8View ArticleGoogle Scholar
This article is published under license to BioMed Central Ltd. This is an Open Access article distributed under the terms of the Creative Commons Attribution License (http://creativecommons.org/licenses/by/2.0), which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.