The specific gravity/salinity/temperature relationship in natural sea water
TL;DR: In this article, a mathematical expression for the relationship between specific gravity, salinity and temperature has been computed for natural sea waters covering the salinity range 9 − 41% at temperatures of 0 − 25°C.
About: This article is published in Deep Sea Research and Oceanographic Abstracts.The article was published on 1970-08-01. It has received 71 citations till now. The article focuses on the topics: Salinity & Seawater.
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DOI•
01 Jan 1983
TL;DR: In this article, the APSO Joint Panel on Oceanographic Tables and Standards (APSO) and SCOR Working Group (SCOR) have published a joint report on oceanographic tables and standards.
Abstract: Endorsed by
Unesco/SCOR/ICES/lAPSO Joint Panel
on Oceanographic Tables and Standards
and SCOR Working Group 51
1,534 citations
Cites methods from "The specific gravity/salinity/tempe..."
...Thi~ equation is more precise than the currently used equations (Knudsen et al., 1902; ~kman, 1908; Cox et al., 1970) and covers a wi·der range of temperature and pressure....
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TL;DR: In this article, the composition of the organic matter oxidized within the thermocline of the Atlantic and Indian oceans has been estimated from the chemical data along the σθ 27.0 and 27.2 horizons.
Abstract: The composition of the organic matter oxidized within the thermocline of the Atlantic and Indian oceans has been estimated from the chemical data along the σθ 27.0 and 27.2 horizons. These estimates are based on the differences between the preformed and observed concentrations of PO4, NO3, total inorganic CO2, alkalinity, and O2. Since these isopycnal horizons are ventilated both from the north and the south, the preformed concentration estimates take into account the relative contributions of these two end-members. The proportions of these end-members are estimated on the basis of the potential temperature of the water, assuming that no cross-isopycnal mixing occurred. Except for the northern Indian Ocean, the composition of the waters entering the isopycnal horizons is established through linear extrapolation of the property-oxygen trends to oxygen saturation. The σθ 27.0 and 27.2 waters do not outcrop in the northern Indian Ocean, and these horizons receive waters spilling into the Indian Ocean from the Red Sea. Therefore the composition of the Red Sea overflow water with these densities is taken to be the northern Indian end-member. The results of this study indicate that the accepted Redfield P:N:C: −O2 ratio of 1:16:106:138 requires revision. Our analysis yields a ratio of 1:16:103:172 if the carbon value is represented by the observed increase in the total CO2 concentration. On the other hand, if the carbon value is assumed to be represented by the oxygen utilization minus the oxygen used for oxidation of NH3 with two moles of O2 per nitrogen atom, a ratio of 1:16:140:172 is obtained. Thus the P: −O2 ratio lies between 1:103 and 1:140. This discrepancy may be accounted for by the increased CO2 concentrations in the source waters as a result of the uptake of anthropogenic CO2 or by an excess demand of oxygen for oxidation of hydrogenated organic molecules. Therefore, without a firm knowledge of either the corrections for the anthropogenic CO2 effect or the hydrogen content of the biological residues, the true P:C ratio cannot be obtained. The ratio of P:CaCO3 dissolution has been estimated to be about 1:12. This indicates that the CO2 produced by the oxidation of organic carbon to that derived from the dissolution of CaCO3 is bout 10:1 at these density horizons.
690 citations
TL;DR: The Practical Salinity Scale 1978 as mentioned in this paper is an attempt to remove the shortcomings; it has been recommended for international acceptance; the basis for this new scale is an equation relating the ratio of the electrical conductivity of the seawater sample to that of a standard potassium chloride solution (KCI) at 15\deg C atmospheric pressure.
Abstract: The history of the definition of salinity and the methods of computing It are traced from the beginning of the twentieth century until the present. Difficulties that have arisen in existing practices are discussed, in particular, the situation regarding reduction of in-situ CTD observations. The Practical Salinity Scale 1978 is an attempt to remove the shortcomings; it has been recommended for international acceptance. The basis for this new scale is an equation relating the ratio of the electrical conductivity of the seawater sample to that of a standard potassium chloride solution (KCI) at 15\deg C atmospheric pressure. The samples used were prepared from standard seawater diluted with distilled water or evaporated by weight. Finally, the set of new equations for CTD data reduction is given, based upon the work of authors whose papers are appearing elsewhere in this volume.
270 citations
TL;DR: In this paper, it has been shown that the ratio of O2 utilization to phosphate production in the sea is 175±6 (rather than 138, as proposed by Redfield et al. (1963)).
Abstract: Through the deconvolution of ocean chemical data it has been shown that the ratio of O2 utilization to phosphate production in the sea is 175±6 (rather than 138, as proposed by Redfield et al. (1963)). We find no evidence that this ratio changes significantly with location or depth in the sea. We have used this new ratio to calculate the initial phosphate concentrations for the waters sampled during the GEOSECS and TTO programs. The important application of these new results is in constraining the origin and flow patterns of deep waters in the ocean. We believe that a strong case can be made that Antarctic salinity maximum water (i.e., the common water of Montgomery (1958)) is produced by the mixing of waters entering the Antarctic from mid-depths in the Indian, Pacific, and Atlantic with Weddell Sea bottom water (southern component). Antarctic common water consists of about 45% Weddell Sea bottom water, 30% intermediate waters from the Pacific and Indian oceans, and 25% deep water originating from the northern Atlantic.
241 citations
TL;DR: The changes in distribution of sea surface temperature and salinity in the North Atlantic between 40 and 60°N were reconstructed for the time interval between 40 to 30 kyr BP, which includes the large iceberg discharge event associated with the deposition of Heinrich layer 4.
203 citations
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598 citations
TL;DR: In this article, the minimax norm is used to deal with the competing requirements of data-fitting problems, and the two norms most frequently considered are the minimization norm and the minimisation norm 11 e 11 for the vector.
Abstract: the yk(X,) f,. cannot ordinarily all be made 0 simultaneously. When they cannot, the m conditions (2) compete with one another, and the numerical analyst must somehow take account of this in order to formulate a problem of data-fitting. The m numbers e, = Yk(X,) are the m components of an error vector e. Since the x,, and f,, are regarded as fixed, the vector e depends only on the parameters t(7k), , tk. Each common method for dealing with the competing requirements (2) corresponds to the selection of a norm 11 e 11 for the vector e. The two norms most frequently considered are the minimax norm
426 citations
Book•
01 Jan 1966
TL;DR: The Journal of Marine Research (JMR) as discussed by the authors is an online peer-reviewed journal that publishes original research on a broad array of topics in physical, biological, and chemical oceanography.
Abstract: PO Box 208118, New Haven, CT 06520-8118 USA (203) 432-3154 fax (203) 432-5872 jmr@yale.edu www.journalofmarineresearch.org The Journal of Marine Research is an online peer-reviewed journal that publishes original research on a broad array of topics in physical, biological, and chemical oceanography. In publication since 1937, it is one of the oldest journals in American marine science and occupies a unique niche within the ocean sciences, with a rich tradition and distinguished history as part of the Sears Foundation for Marine Research at Yale University.
91 citations
Abstract: For a given wave length, an equation of the form B(t -20)3+ A(t-20)2+ C(t-20) n,-nzo=(t+ D)X107 ' an adaptation of the t ype of equation used by Thiesen for representing data on the density of water, has been compared with fourand six-parameter polynomials in t as a means for exprcssing th ermal variations in the r efractivity of water. All adjust ments were made by the method of least squares with a p recision of a few parts per million. This type of equation has also been fi tted to the data obtained by Chappuis on the density of water at the International Bureau of Weights anel Measures in 1891 an d 1897. It fits thcm better than do his tabula ted values. All results are examined statistically, a revised t able of the d ensity of water is given, and it is concluded that this t ype of equation is superior to a power series for representing either the refractive index or the density of distilled water. CONTENTS :Page I. Discussion of function-t equations ___ ______________________________ 205 II. T ests with refractive-index data ______ _____________________________ 207 1. Adjustment of observations_ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ 207 2. Adjusted values of function-t constants _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ 208 3. Relat ive goodness of fit and Chi-tesL ___ _______ _________________ 208 III. Tests with density data __ _______ _________________________________ 209 1. Reexamination of the Chappuis observations _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ 211 2. Results of readjustment __ ___ _____ _____________________________ _ 211 IV. Concluding discussioll ___ ______ ________ ___________________________ 213 1. DISCUSSION OF FUNCTION-t EQUATIONS For any given wave length, observed values of refractive indices may be conveniently adjusted after they have been approximately expressed as functions of the temperature, t, by what may be called function-t equations. Such functions of t are customarily polynomials in powers of t. It is well known that such equations are, in general, not desirably accurate when limited to a few terms . Moreover, Hall and Payne 1 have expressed the opinion that a single equation of this sort is not valid for a temperature range from 0 to 100° O. It seems, however, that no other type of direct 2 relationship between index and temperature has been published. 1 Phys. Rev. [2) 20, 249 (1922). 2 E. Kettler (Ann. Physik 269, 512 (1888» used an eqnation that involves density as well as temperatnre . Regardless oC its possible merit, both his sets oC computed values show systematic Cailure to represent his data. 205 206 Journal oj Research oj the National Bureau oj Standards [Vol. IS Under these circumstances, and remembering the quasi-constant relationship between refractivity and density, it seemed pertinent to consider function-t equations of other types that have been found suitable for representing the observed density of water. Only one such type of formula has been used for the range 0 to 40° C for water.3 It was published by Thiesen, Scheel, and Diesselhorst,4 who represented their data obtained at the Reichsa·lstalt in 1896, with a fourconstant equation of the form (1 _d)_(t-A)2 t+O B °t+D' (1) where A is the temperature of maximum density, and the unit of density is 1 g per milliliter. Moreover, Thiesen 5 later found this same form of equation to be approximately adequate over the larger temperature range 0 to 100° C. He also obtained somewhat better results by extending the equatipn to six parameters, of which two were arbitrarily selected. The final comparison between his formulas is conditioned, however, by the fact that in both cases his computations for determining the constants were limited to five significant figures. Preliminary computations made by the authors indicated that an equation of the same type and limited to the four-constant form (t-A)2 t+ 0 nt=nma,,B ° t+D (2) would be useful for representing refractive index, but a transformation was desirable because in this case no assumption concerning an exact value for the maximum index of water was advisable. Consequently, since index data at 20° C were more numerous and somewhat more reliably determined than those for other temperatures, eq 2 was written for a temperature of [20+ (t-20))O and for n max its value in terms of n20 was substituted. The result is O'(A' )2 [(t 20) + A')2 (t 20)+O' nt=n20+ BD' B (t20)+D\" (3) where A'=20-A, 0'=20+0, and D'=20+D. Then after combining terms, eq. 3 may be written in simpler form as Blt-203) + A(t-20)2+ C(t-20) n t-n20=(t+D) X 107 ' where the new parameters in terms of those in eq 2, are
63 citations
35 citations