Oceans modeling

Research should be conducted to understand how the oceans have operated under past climates. This would involve paleoclimatic studies including analysis of sediment and ice core records coupled with tracer-style ocean models or box models. 

Sillen constructed his models in a stepwise fashion starting with a simplified ocean model of five components (HCl, H2O, KOH, Al(OH)3,... 

Simple three-box models with the atmosphere assumed to be one well-mixed reservoir and the oceans described by a surface layer and a deep-sea reservoir have been used extensively. Keeling (1973) has discussed this type of model in detail. The two-box ocean model is refined by including a second surface box, simulating an "outcropping" (deep-water forming) polar sea (e.g.. Keeling and Bolin, 1967, 1968), and to include a better resolution of the main thermo-cline (e.g., Bjorkstrom, 1979). The terrestrial biota are included in a simple manner (e.g., Bolin and Eriksson, 1959) in some studies Fig. 11-18 shows a model used by Machta (1972) where the role of biota is simulated by one reservoir connected to the atmosphere with a time lag of 20 years. 

Bacastow, R. B. and Bjdrkstrom, A. (1981). Comparison of ocean models for the carbon cycle. In "Carbon Cycle Modeling" (B. Bolin, ed.), pp. 29-79. Wiley, New York. 

The ice-ocean model Europa s core consists of dehydrated silicates, since heat production made dehydration possible. Around the core, there is a thick layer of liquid water (about 100 km), and above that a thin layer (about 10 km) of water ice. 

Updated model versions The atmosphere and ocean models were updated to the recent model releases ECHAM5.3.02 and MPIOM-1.2.2. The update of the biogeo-chemistiy model from the beta version of HAMOCC5 used by Guglielmo (2008) to HAMOCC5.1 [Maier-Reimer et al (2005)] introduced major changes in the model. 

As the volatilisation flux strongly depends on the absolute contaminant mass, the volatilisation mass flux divided by the total amount of DDT in the first level of the ocean model is examined instead. This parameter is called volatilisation rate. It reflects the proportion of the mass abundant in the oceanic surface layer that was volatilised within one model time step. It depends upon how much of the DDT is dissolved in water and upon wind speed and sea surface temperature. The volatilisation on the other hand would mainly mirror the deposition and emission pattern, because those are supersposed onto the volatilisation defining patterns and dominating because of the stationary application in the scenario. 

Program 0GC03 solves the steady state ocean model using Gaussian elimination and back substitution. 

Toggweiler, J.R., K. Dixon, and K. Bryan. 1989. Simulations of radiocarbon in a coarse-resolution world ocean model 1. Steady state prebomb distributions. Journal of Geophysical Research 94(C6) 8217-8242. 

Table 21.10 Results and Components in Kramer s Ocean Model. ...

We shall now consider the system HC1—H20—Al(OH) —Si02— KOH where C = 5. This system might be called an ocean model since the first two components may represent the volatile substances used to form the ocean and the three last may represent oxides in the igneous rock. It is simplified since all minor components ( and even some of the main components) are missing—i.e., CO > and sulfur compounds among the volatiles, Na, Mg, Ca, and Fe among the rock components. 

We may now pass from the simplified ocean model to the complete equilibrium model by adding one component after another—for each addition obtaining either a new concentration variable or a new phase. We shall concentrate on one intermediate model—namely, the system with eight components (C = 8) HC1—H20—Si02—Al(OH)3—NaOH— KOH—MgO—CaO. Of the major components we have still excluded iron and C02. The latter have been withheld in the form of solid CaCO ... 

Let us assume for the moment that our working hypothesis is true. We may then add one component after another to construct our complete ocean model (equilibrium model). If we add C02 and two new phases... 

Follows M.J. Ito T. and Dutkiewicz S. (2006). On the solution of the carbonate chemistry system in ocean biogeochemistry models. Ocean Modelling, 12(3-4), 290-301. 

Kemball-Cook S., Wang B. and Fu X. (2002). Simulation of the intraseasonal oscillation in the ECHAM-4 model The impact of coupling with an ocean model. Journal of the Atmospheric Sciences, 59(9), 1433-1453. 

Pa PACE PAGES PAHO PALE PAR PARCS PBL PCM PDV PhA PIK PIRA PIRATA POC POLDER Partial pressure in the atmosphere Permafrost And Climate in Europe Pilot Analysis of Global EcoSystems Pan American Health Organization Paleoclimates of Arctic Lakes and Estuaries Photosynthetic Active Radiation Paleoenvironmental ARCtic Science Planetary Boundary Layer Parallel Climate Model Pacific Decadal Variability Phytogenic Aerosol Potsdam-Institut fur Klimafolgenforschung Petroleum Industry Research Associates Pilot Research moored Array in the Tropical Atlantic Permanganate Oxidizable Carbon POLarization and Directionality of the Earth s Reflectances Princeton Ocean Model... 

Alexander, S.E. and Roughgarden, J., Larval transport and population dynamics of intertidal barnacles a coupled benthic/oceanic model, Ecol. Monogr., 66, 259, 1996. 

GATOR/MMTD (or Mesoscale, Ocean Model The gas, aerosol, transport, and radiation air quality model/a mesoscale... 

McGregor JL (1997) Semi-Lagrangian advection on a cubic gnomonic projection of the sphere. In Lin C, Laprise R, Ritchie H (eds) Numerical methods in atmospheric and oceanic modelling the Andre J. Robert Memorial (Companion volume to atmosphere-ocean). Canadian Meteorological and Oceanographic Society, Ottawa, Canada, pp 153-169... 

Caldeira, K., and Wickett, M. E. (2005). Ocean model predictions of chemistry changes from caron dioxide emisions to the atmosphere and ocean. J. Geophys. Res. 110, C09604, doi 10.1029/ 2004JC002671. 

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