OS13B Modeling the Distribution and  15 N of Nitrogen Gas and Nitrogen Species in the Black Sea S. K. Konovalov 1, C. A. Fuchsman 2 and J.W. Murray 2 1. Marine Hydrophysical Institute, Kapitanskaya St. 2a, Sevastopol Ukraine; and 2. School of Oceanography, University of Washington, Box Seattle WA OS13B Modeling the Distribution and  15 N of Nitrogen Gas and Nitrogen Species in the Black Sea S. K. Konovalov 1, C. A. Fuchsman 2 and J.W. Murray 2 1. Marine Hydrophysical Institute, Kapitanskaya St. 2a, Sevastopol Ukraine; and 2. School of Oceanography, University of Washington, Box Seattle WA Abstract Distributions of NO 3 -, NO 2 -, NH 4 +, N 2 and PON and their  15 N values in the Black Sea were measured in order to unravel the cycling of nitrogen, especially the role of anammox (NO NH 4 + = N 2 ). We have constructed a steady state coupled physical-biogeochemical model of the water column. The physical model is a vertical transport model that includes simulation of entrainment and intrusions from the Bosporus Plume. The biogeochemical model includes mass balance equations for 14 N and 15 N. Comparison of observations and model results show: 1. The chemical distributions can be fit by adjusting the respective reaction rate constants 2. This steady state model can not simultaneously fit the concentrations and stable isotope data without including some process that removes heavy nitrogen 1. Cruises and Samples Data for this study was collected during recent cruises in the Black Sea: R/V Bilim September 2000 R/V Knorr May 2001 R/V Knorr April 2003 (Track and Station Locations shown in Fig. 1) The cruise web sites with data are located at: Fig Model #2 – Vertical Zonation of Processes: Reactions with S , HS - We allowed the reaction between NO 3 - and NH 4 + to occur in the region of the NO 3 - gradient (Fig. 11). The origin of the NH 4 + is from regenerated PON and its concentration remains low because it is rapidly utilized. Light 14 N-NO 3 - would be preferentially used to make light N 2. The heavy 15 N-NO 3 - that remains diffuses downward to be reduced by S  to NH 4 + in the lower layer (thus making heavy NH 4 + ). Fig. 11 Fig. 12 Conclusions: This model correctly simulates  15 N-N 2 and  15 N-NO 3 - but not  15 N-NH 4 + and  15 N-PON which are too heavy (Fig. 12). The  15 N-NH 4 + maximum is too shallow. 11. Model #3 – Vertical Zonation of Processes: Scavenging by MnO 2 Heavy NH 4 + is removed, possibly by preferential adsorption of NH 4 + by MnO 2. Light NH 4 + is left to react with NO 2 - to make light N 2. The adsorbed (and heavy NH 4 + ) is released back to the water when the MnO 2 is reduced in the anoxic layer (Fig. 13). 15% of the upward flux of NH 4 + is removed to the anoxic zone and the isotopic fractionation (  ) required is -20‰. Fig. 13 Fig. 14 Conclusion: The simulation results in distributions close to those observed (Fig. 14). Light N 2 is made.  15 N-NH 4 + reaches a maximum at the right depth, then decreases to minimum values that help to produce light N 2 The  15N-PON is similar to those observed. 2. Nitrogen Species Fig. 2 shows an example of distributions of NO 3 -, NO 2 - and NH 4 + NO 3 - increases to a maximum at  t = 15.6 then decreases to 0 at  t = NO 2 - has a small maximum centered at  t = 15.8 NH 4 + starts to increase at  t = The N 2 /Ar data from 2000, 2001 and 2003 are plotted as the ratio of sample/saturation versus density in Fig. 3. The water column is usually supersaturated with N2 with a maximum centered at  t ≈ Supersaturation in the shallow layers results from upward flux of N 2 from the suboxic zone. There is significant interannual variability. The concentrations can be reset to atmospheric saturation after intense storms. 4. Nitrogen Isotope Distributions (Fig. 5)  15 N-NO 3 - increases to a maximum of ≈ 18‰ in the suboxic zone then decreases with depth. Above the suboxic zone values are about 8‰ which is higher than average NO 3 - in seawater (  15 N-NO 3 - ≈ 4.5 to 6‰) (Fig. 6)  15 N-NH 4 + is very low in the deepwater (≈ 2‰) and increase to a maximum of 7‰ at the base of the suboxic zone, then decrease slightly. (Fig. 7)  15 N-N 2 in the suboxic zone maximum is extremely light (  15 N- N 2 ≈0.0‰) compared to SW in equilibrium with the atmosphere (  15 N-N 2 ≈ 0.7‰) and to the other forms of N that are sources for N 2 (  15 N-NO 3 - ≥ 8‰;  15 N-NH 4 + ≥ 8‰;  1 5N -PON = 2.7 to 9.0‰). 5. Physical Biogeochemical Model We utilized a 1.5-D physical transport model (Fig. 8) that includes simulation of the Bosporus Plume and assumes isopycnal distribution of all properties (Samodurov and Ivanov, 1998; Ivanov and Samodurov, 2001). The resulting 1-D vertical balance equations can be written as: k = vertical diffusion coefficient; = diffusive flux, w = vertical velocity and wC = the advective flux occurring due to displacement of the Black Sea deep waters with the waters from the Bosporus plume, R = rate of biogeochemical production-consumption, Cb = concentration in the “Bosporus plume” C = concentration in the ambient water. The model has been verified using 137 Cs data from 1986 to Biogeochemical Transformations Transformations of O 2, PON, DON, NO 3 -, NO 2 -, N 2, NH 4 +, H 2 S, S 0 and dissolved and particulate Mn(II) and Mn(IV) and Fe(II) and Fe(III) are included in the model. Dissolved organic N is split into labile (DON(L)) and refractory (DON(R) fractions. Particulate organic nitrogen is split into the fraction sinking from the euphotic zone (PON) and the fraction that is bacterially produced (PON(B)). Equations that parameterize biogeochemical transformations are written to follow either “chemical” or Michaelis-Menten kinetics. Thus, oxidation of sulfide by oxygen is parameterized as a chemical process. Microbiologically mediated processes, like oxidation of PON by oxygen are parameterized by Michaelis-Menten kinetics. The specific (k) and maximum (  ) rates were taken from publications, when available, and adjusted to fit the data. All values of k and  were assumed constant. 8. Simulation of  15 N distributions To simulate 14 N/ 15 N fractionation, all reactions were written in terms of both 14 N and 15 N. The rate of 15 N transformations is proportional to the rate of 14 N transformations, to the ratio of [ 15 N]/[ 14 N], and fractionation factors  , where  is the isotopic enrichment factor. Thus, the rate of oxidation of 15 N-PON is Published data on fractionation (  ) or isotopic enrichment (  ) factors are limited. It is often difficult to identify, if the published values are specific for individual reactions or processes that may involve a number of reactions. Still, the published values for the isotopic enrichment factors (  ) generally vary from 0 to 40‰. The enrichment factors (  ) required to fit the data are given below: nitrate (NO 3 - ) reduction, for all reductants (e.g. CH 2 O, S  )  = ‰ nitrite (NO 2 - ) reduction and oxidation  = ‰ reactions of particulate organic nitrogen to NH 4 +  = 2 -5‰ ammonium (NH 4 + ) consumption or oxidation (e.g. Anammox)  = 0 to a few ‰ 9. Model #1 Simulation The model was tuned to simulate  15 N profiles in the oxic and anoxic layers (Fig. 10). The initial conditions derived from the real observations are shown as dashed lines. Simulations are shown for 90 days, 1 year and 13 years. Variations in  (  ) for denitrification and anammox did not change the final result. Complete consumption of NO 3 - (NO 2 - ) and NH 4 + does not result in any fractionation. Steady State profiles are easily obtained for  15 N-NO 3 - and  15 N-NH 4 + but  15 N-N 2 decreases initially then increases rapidly. At steady state (after several decades?) the  15 N-N 2 must equal 8‰, much higher than the observed values of 0.0‰. Conclusions (Doesn’t explain all data): Can’t simultaneously model  15 N of N 2, NO 3 - and NH 4 +. Can’t make light  15 N-N 2 by total consumption of NO 3 - and NH 4 +. Conclusion Steady State model runs are not successful at simulating the observed  15 N distributions in the suboxic zone of the Black Sea unless we assume a process to remove heavy  15 N-NH 4 +. Comparison of model and data suggest three possibilities: 1. The  15 N data we are using are not representative. 2. There is a process to transport heavy NH 4 + from the suboxic zone to the anoxic zone. 3. The  15 N profiles are not at steady state. Acknowledgement This work is a part of the next projects: NSF MCB ; NSF OCE # ; NATO CLG #