S deep water

Earlier in Ghapter 5 a map of the G age of DIG in the ocean s deep waters (Fig. 5.17) revealed that the age difference between the northern North Atlantic Deep Water and that in the Northeast Pacific is C.1700 y. This value compares the most recent and most ancient ventilation ages of the deep ocean, whereas the box model compares the mean deep water age of the entire ocean, c. - 160%o (c. 1480 y) with that of the surface ocean, c. - 50%o (400 y) (1480 - 400 = 1080 y). In some ways, the largest task of the two-layer-ocean calculation is determining representative A G values for the mean surface and deep ocean. More complicated models with more reservoirs (see, for... 

Ingrin, J., Hercule, S. Charton, T. (1995). Diffusion of hydrogen in diopside results of dehydration experiments. Journal of Geophysical Research, Vol. 100, pp. 15489-15499 Jacobsen, S.D. Van der Lee, S. (2006). Earth s Deep Water Cycle, Geophysical Monograph Series, Vol. 168, American Geophysical Union, Washington, D.C. 

The gas reservoirs located ia very deep waters, ia coal beds, and ia tight sands are now more accessible. Fifteen percent of the U.S. gas supply ia 1992 was derived from tight sand formations and 1.4 x 10 of coal-bed methane was added to the proven reserves (22). In 1992, U.S. proven reserves were placed at 4.67 x 10 ia the lower 48 states, and it was estimated that the identified gas resource ia the United States and Canada exceeds 3.4 X 10. Based on the 1992 rate of natural gas consumption, the United States has between 8 and 10 years of proven reserves and a domestic... 

A number of current coupled ocean-atmosphere climate models predict that the overturning of the North Atlantic may decrease somewhat under a future warmer climate.While this is not a feature that coupled models deal with well, its direct impact on the ocean s sequestration of carbon would be to cause a significant decline in the carbon that is stored in the deep water. This is a positive feedback, as oceanic carbon uptake would decline. Flowever, the expansion of area populated by the productive cool water plankton, and the associated decline... 

An air-lift pump raises 0.01 m3/s of water from a well 100 m deep through a 100 mm diameter pipe. The level of water is 40 m below the surface. The air flow is 0.1 m3/s of free air compressed to 800 kN/m2. Calculate the efficiency of the pump and the mean velocity of the mixture in the pipe. 

Conventional T-S diagrams for specific locations in the individual oceans are shown in Fig. 10-4. The inflections in the curves reflect the inputs of water from different sources. The linear regions represent mixing intervals between these core sources. For example, in the Atlantic Ocean the curves reflect input from Antarctic Bottom Water (AABW), North Atlantic Deep Water (NADW), Antarctic Intermediate Water (AIW), Mediterranean Water (MW), and Warm Surface Water (WSW). 

All deep waters of the ocean were once in contact with the atmosphere. Since over 95% of the total of all gases (except radon) reside in the atmosphere, the atmosphere dictates the ocean s gas contents. CO2 is also a special case because the ocean has high total CO2. As discussed in Chapter 7, the composition of the atmosphere is nearly constant horizontally. 

The solubility of calcite and aragonite increases with increasing pressure and decreasing temperature in such a way that deep waters are undersaturated with respect to calcium carbonate, while surface waters are supersaturated. The level at which the effects of dissolution are first seen on carbonate shells in the sediments is termed the lysocline and coincides fairly well with the depth of the carbonate saturation horizon. The lysocline commonly lies between 3 and 4 km depth in today s oceans. Below the lysocline is the level where no carbonate remains in the sediment this level is termed the carbonate compensation depth. 

Mangini A, Lomitschka M, Eichstadter R, Frank N, Vogler S, Bonani G, Hajdas I Patzold J (1998) Coral provides way to age deep water. Natme 392 347-348... 

Toole J, Baxter M S and Thomson J (1987) The behavior of uranium isotopes with salinity change in three U.K. Estuaries. Estuarine Coastal Shelf Sci. 25 283-297 Torgersen T, Turekian KK, Turekian VC, Tanaka N, DeAngelo E, O Donnell JO (1996) " Ra distribution in surface and deep water of Long Island Sound Sources and horizontal transport rates. Cont Shelf Res 16 1545-1559... 

Another potential source of indoor radon is from utilities including water and natural gas. As reported by Hess et al. (1987) there are wells that can have extremely high radon concentrations per unit volume of water. Thus, use of such water could be an important indoor radon source. Radon in water is typically of the order of several thousand picocuries per liter or less. Surveys of U.S. drinking water sources indicate that 74 had concentrations below 2,000 pCi/1 and only 5 had values above 10,000 pCi/1. The problem appears to exist primarily in deep drilled wells and a concentration... 

Surface Water t,/2 = 16 h (calculated for river water 1 m deep, water velocity 0.5 m/s, wind velocity 1 m/s from air-water partition coefficients (Southworth 1979 Hallett Brecher 1984)... 

The method of intercomparison of the various devices was to deploy pairs of sampler types on different hydrowires to collect water samples from a homogeneous body of deep water at Ocean Station S (Panulirus Station) near Bermuda (Fig. 1.1). The water at this depth has characteristics of 3.97 0.05 °C... 

Since detrital POM is continuously settling out of the surface waters of all the world s ocean, water masses moving laterally through the ocean basins are continuously receiving a rain of detrital POM. Aerobic respiration of this detrital POM causes the O2 concentration in a water mass to decrease as it travels through the deep sea. The amount of O2 consumed since a water mass was last at the sea surface can be... 

Nutrients are carried back to the sea surface by the return flow of deep-water circulation. The degree of horizontal segregation exhibited by a biolimiting element is thus determined by the rates of water motion to and from the deep sea, the flux of biogenic particles, and the element s recycling efficiency (/and from the Broecker Box model). If a steady state exists, the deep-water concentration gradient must be the result of a balance between the rates of nutrient supply and removal via the physical return of water to the sea surface. 

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