Pacific Ocean temperature

Variability of Seawater Vertical sections through seawater showing the distribution of temperature, salinity, and oxygen for the Pacific Ocean and Western Atlantic Ocean are shown in Figures 21.3 and 21.4. The global variability of natural seawater and its effects on corrosion have been reviewed in particular with respect to seasonal variation of temperature, salinity, oxygen and pH in the Pacific surface water. Data is also given on... 

Fig. 21.3 Vertical sections showing distribution of temperature, salinity, and oxygen in the Pacific Ocean, approximately along the meridian of I70°W. (After Sverdrup, H. U., Oceanography for Meteorologists, Allen and Unwin (1945))...

Fig. 10-4 Average temperature/salinity diagrams for Pacific Oceans. (Reproduced with permission from G. L. Oceanography," pp. 138-139, Pergamon Press.)...

Fig. 14-6 Profiles of potential temperature and phosphate at 21 29 N, 122 15 W in the Pacific Ocean and a schematic representation of the oceanic processes controlling the P distribution. The dominant processes shown are (1) upwelling of nutrient-rich waters, (2) biological productivity and the sinking of biogenic particles, (3) regeneration of P by the decomposition of organic matter within the water column and surface sediments, (4) decomposition of particles below the main thermocline, (5) slow exchange between surface and deep waters, and (6) incorporation of P into the bottom sediments.

Soo [96] determined picogram amounts of bismuth in seawater by flameless atomic absorption spectrometry with hydride generation. The bismuth is reduced in solution by sodium borohydride to bismuthine, stripped with helium gas, and collected in situ in a modified carbon rod atomiser. The collected bismuth is subsequently atomised by increasing the atomiser temperature and detected by an atomic absorption spectrophotometer. The absolute detection limit is 3pg of bismuth. The precision of the method is 2.2% for 150 pg and 6.7% for 25 pg of bismuth. Concentrations of bismuth found in the Pacific Ocean ranged from < 0.003-0.085 (dissolved) and 0.13-0.2 ng/1 (total). 

Vertical concentration profiles of (a) temperature, (b) potential density, (c) salinity, (d) O2, (e) % saturation of O2, (f) bicarbonate and TDIC, (g) carbonate alkalinity and total alkalinity, (h) pH, (i) carbonate, ( ) carbon dioxide and carbonic acid concentrations, and (k) carbonate-to-bicarbonate ion concentration ratio. Curves labeled f,p have been corrected for the effects of in-situ temperature and pressure on equilibrium speciation. Curves labeled t, 1 atm have been corrected for the in-situ temperature effect, but not for that caused by pressure. Data from 50°27.5 N, 176°13.8 W in the North Pacific Ocean on June 1966. Source From Culberson, C., and R. M. Pytkowicz (1968). Limnology and Oceanography, 13, 403-417. 

Temperatures in the range of 20 to 100 million degrees Celsius are required for fusion reactions. For this reason, a hydrogen bomb is triggered by a conventional fission atomic bomb. The atomic bomb produces the tremendous heat necessary to fuse hydrogen nuclei therefore, fusion bombs are often referred to as thermonuclear. The United States exploded the first hydrogen bomb on Eniwetok Atoll in the Pacific Ocean on November 1, 1952. This bomb was based on the fusion of deuterium ... 

Interestingly, the vertical distribution of photochemical oxidant may not be such that it falls off rapidly at the inversion layer. In fact, in a classic series of experiments, Edinger and co-workers (1972, 1973) showed that oxidant concentrations in the Los Angeles air basin could be higher within the inversion layer than at ground level. Thus, Fig. 2.19, for example, shows one temperature and oxidant profile for June 20, 1970, over Santa Monica, California, a city adjacent to the Pacific Ocean. Several layers of oxidant (mainly O-,) exist... 

In addition, there is an obseived correlation between total column ozone and the El Nino Southern Oscillation (ENSO) in the tropical troposphere, with decreases in total ozone in middle and sometimes polar latitudes following the ENSO by several months the period associated with the ENSO is 43 months (Zerefos et al., 1992). While the association between the ENSO and ozone is not well understood, it has been proposed that the warming of the troposphere in the tropics over the Pacific Ocean causes increases in the upper troposphere air temperatures and tropopause height and an upwelling in the lower stratosphere. If sufficiently large, this could have more widespread impact than just in the tropics (e.g., see Zerefos et al., 1992 and Kalicharran et al., 1993). 

The winds in the latitudes of North America are westerly. On the western coast of the continent, therefore, air moves from the Pacific Ocean to the land. Because of water s high specific heat, ocean temperatures do not vary much... 

Kirchman, D. L., and J. H. Rich. 1997. Regulation of bacterial growth rates by dissolved organic carbon and temperature in the equatorial Pacific Ocean. Microbial Ecology 33 22-30. 

Climate researchers Palutikof and Holt (2004) say that droughts appear to be linked to the formation of blocking zones of intense high pressure over the Atlantic Ocean that divert rain-bearing wind depressions away from the Mediterranean. This blocking may be related to the cycles of El Nino, the periodic reversal of winds and waves in the tropical Pacific Ocean. Due to the effects of toxic gases, it is assumed that year-round average temperature in southern Europe will reach 18°C by the year 2030 and rainfall will diminish by 19% to 20%. 

Water exchange through the southern boundary of the Norwegian Sea is V3. The water temperature T k in Eijk (block MWT) is a function of evaporation, precipitation, river flows, and inflows of water from the Atlantic and Pacific Oceans. Its change with time in Etjk is described by the equation of heat balance ... 

In 1999 a band of maximum annual mean positive SAT anomalies stretched from the North American continent eastward across the Atlantic Ocean and the Eurasian continent toward the equatorial western sector of the Pacific Ocean. Minimum SAT anomalies were observed in a broad band of the central and northeastern region of the Pacific Ocean (including a decrease of SAT). Analysis of the observational data revealed the prevalence of positive temperature anomalies in many regions of the globe. The most vivid anomalous situations include both warming and cooling events (Scafetta et al., 2004). Here are some aspects of temperature variations in 1999 ... 

Ten-day isobaric back-trajectories were calculated for each day of the cruise (Harris, J., personal communication, 1986) indicating that air masses were predominantly advected from the open South Pacific Ocean. Wind velocities over the Drake Passage ranged between 3-30 m s 1, whereas in the inshore areas they never exceeded 10 m s 1. During about 70% of the cruise period the weather was characterized by overcast conditions with occasional snowfall and fog episodes. A high pressure weather situation occurred between April 8-14 which was responsible for sustained cloud-free conditions with intense daylight during this short period. Surface seawater temperatures were typically around 8°C in the Subantarctic and 2°C in the Antarctic and inshore waters, whereas air temperatures were around -0.S°C and showed much less latitudinal difference. 

Figure 9.3. Emission spectra from the infrared interferometer spectrometer on board the Nimbus 3 satellite for the tropical Pacific Ocean under clear-day conditions. The dashed lines represent outgoing long-wave, blackbody radiation at the temperature indicated. CO2 absorbs in the spectral window of 13-17 pm, O3 between 9-10 pm, and H2O in the entire spectral domain. Emission is measured in arbitrary units. (After Ramanathan, 1988.)...

Below the thermocline, the temperature changes only little with depth. The temperature is a non-conservative property of seawater because adiabatic compression causes a slight increase in the in situ temperature measured at depth. For instance in the Mindanao Trench in the Pacific Ocean, the temperature at 8500 and 10,000 m is 2.23 and 2.48 °C, respectively. The term potential temperature is defined to be the temperature that the water parcel would have if raised adiabatically to the ocean surface. For the examples above, the potential temperatures are 1.22 and 1.16 °C, respectively. Potential temperature of seawater is a conservative index. 

For example, a 3 per cent, solution of common salt at 10° C. is much more corrosive than tap water at the same temperature but as the temperature rises the relative corrosivity falls, so much so that at 21° C. the salt solution is the 1 ess corrosive of the two. Since sea water contains some 3 per cent, of sodium chloride, it is of interest to inquire into the effect of temperature upon its corrosive powers. The few laboratory tests that have been carried out on the subject2 indicate that at temperatures below 13° C. sea water is more corrosive than tap water, whilst at all higher temperatures it is less so. Now, in the western part of the tropical Pacific Ocean a temperature of 32° C. is sometimes attained, and in the Red Sea and Persian Gulf temperatures of 34 4° C. and 35 5° C. respectively have been registered. Such waters should therefore prove less corrosive than river waters at the same temperatures. 

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