Salinity measurements and definitions throughout history
Since as far as Ancient Greece times, attempts have been made to try to measure the "saltiness" of seawater. However, methods' efficiency was very incipient and their sensitivity and repeatability was very limited. During the Modern History more precise methodologies were developed: weighing after evaporation (Boyle,1693; Birch, 1965), solvent extraction (Lavoisier, 1772) and precipitation (Bergman, 1784). In 1865, Forchhammer introduced the term salinity and dedicated himself to measure individual components of seasalt rather than the total salinity. He found that the ratio of major salts in samples of seawater from various locations was constant. This constant ratio is known as Forchhammer's Principle, or the Principle of Constant Proportions. Towards the end of the nineteenth century, William Dittmar, following the work of Forchhammer, tested several methods to analyse the salinity and the chemical composition of seawater. The Dittmar methods for chemical analysis of the seawater were extremely precise. Dittmar analysed the chlorine content in seawater using silver nitrate precipitation of the chloride, and compared it with synthetically prepared seawater samples to vouch for the method's accuracy. He later analysed 77 samples from around the world, taken during the Challenger Expedition and noticed the same constancy of composition observed by Forchhammer: "although the concentration of the waters is very different, the percentage composition of the dissolved material is almost the same in all cases". 
ICES - 1902
With more accurate techniques to measure salinity, there was a need to have the same definition of salinity and measuring methods across the scientific community. In 1889, Martin Knudsen was named by ICES to preside a commission to address the salinity issues.
"Salinity is the total amount of solid materials, in grams, dissolved in one kilogram of sea water when all the carbonate has been converted to oxide, the bromine and iodine replaced by chlorine and all organic matter completely oxidized  .Definition of Salinity, ICES, 1902
Although this definition is correct and served oceanographers for the next 65 years, the methodology is impractical and difficult to carryout with precision. Knowing that the seawater composition was constant and chlorine could be accurately measured by silver volumetric titration, the commission defined "chlorinity" as a measure of salinity. After analyzing several samples from nine locations, Knudsen and his colleagues developed an equation to calculate salinity based on chlorine content:
where chlorinity is defined as the mass of silver required to precipitate completely the halogens in 0.3285234kg of the sea-water sample:
JPOTS - 1966
As seen from the formula above, this method has its limitations and is not entirely correct: when chlorinity is 0, salinity is 0.03. Furthermore, Carritt and Carpenter (1959) have estimated that the uncertainty of a computed value of salinity from a measured value of chlorinity using this relation can be as much as 0.04‰. This is due to variations in the chemical composition in some seawater samples (Baltic) and the fact that only 9 different locations were sampled to define chlorinity.
In the beginning of the 60's, with the development of conductivity bridges, it became possible to measure salinity with great precision (± 0.003‰) . Bridges gave conductivity ratios between the sample and standard seawater used to calibrate the bridges. However the standard seawater had been developed for chlorinity measurements and not for conductivity, so a new conductivity standard was commissioned to the Joint Panel for Oceanographic Tables and Standards (JPOTS) and based on new measurements of salinity, temperature and conductivity from samples around the world, the standing formula of chlorinity was revised to:
Practical Salinity Scale-1978 / EOS-80
The relation between salinity and conductivity ratio was based on precise determinations of chlorinity and R15 on 135 natural seawater samples, all collected within 100 m of the surface, and including samples from all oceans and the Baltic, Black, Mediterranean, and Red Seas. After chlorinity was converted to salinity, using the formula shown previously, the following polynomial was computed by least squares:
where C (S, T, 0) is the conductivity of the sea-water sample at temperature T and standard atmospheric pressure, and C (KCl, T, 0) is the conductivity of the standard potassium chloride (KCl) solution at temperature T and standard atmospheric pressure. The standard KCl solution contains a mass of 32.4356 grams of KCl in a mass of 1 kg of solution, and the conductivity of this solution at 15°C and 1 atmosphere is exactly 35.
The present equation of seawater for seawater in use as the international standard for oceanography, is the 1980 International Equation of State of Seawater (EOS-80, released by the Joint Panel on Oceanographic Tables and Standards (JPOTS), and published by Millero et al. (1980). It is based on the temperature scale IPTS-68 and on the Practical Salinity Scale 1978, PSS-78 (Lewis and Perkin, 1981)
Quite recently adopted by UNESCO's IOC and still under scrutiny by both sensor manufacturers and oceanographers, the new thermodynamic equation of state was based on the fact that seawater composition changes with depth (see box bellow). The points that motivated an updated thermodynamic description of seawater are shown bellow as stated by Mcdougall et. al, 2009 .
- Several of the polynomial expressions of the International Equation of State of Seawater (EOS-80) are not totally consistent with each other as they do not exactly obey the thermodynamic Maxwell cross-differentiation relations. The new approach eliminates this problem.
- Since the late 1970s a more accurate thermodynamic description of pure water has appeared (IAPWS-95). Also more and rather accurate measurements of the properties of seawater (such as for (i) heat capacity, (ii) sound speed and (iii) the temperature of maximum density) have been made and can be incorporated into a new thermodynamic description of seawater.
- The impact on seawater density of the variation of the composition of seawater in the different ocean basins has become better understood.
- The increasing emphasis on the ocean as being an integral part of the global heat engine points to the need for accurate expressions for the enthalpy and internal energy of seawater so that heat fluxes can be more accurately determined in the ocean (enthalpy and internal energy were not available from EOS-80).
- The temperature scale has been revised from ITS-68 to ITS-90 and the atomic weights of the elements have been revised (IUPAC, 2005).
Platinum Electrode Conductivity Sensor
Salinity is a ratio and not a physical parameter that can be measured(under PSS-78, see box). Thus, “Salinity sensors” do not exist. What is commonly referred to as a salinity sensor is in fact a conductivity sensor.
This Conductivity Sensor measures the ability of a solution to conduct an electric current between two electrodes. In solution, the current flows by ion transport; therefore, an increasing concentration of ions in the solution will result in higher conductivity values. Conductance is defined as the reciprocal of resistance. When resistance is measured in ohms, conductance is measured using the SI unit, siemens (formerly known as a mho). Since the siemens is a very large unit, aqueous samples are commonly measured in microsiemens, or µS. Conductivity, C, is found using the following formula:
is the conductance, and kc is the cell constant. The cell constant is determined for a probe using the following formula:
where is the distance between the two electrodes, and is the area of the electrode surface. For example, the Conductivity Sensor has a cell constant, for instance:
The conductivity value is found by multiplying conductance and the cell constant. A potential difference is applied to the two probe electrodes in the Salinity Sensor. The resulting current is proportional to the conductivity of the solution. This current is converted into a voltage.
Electrodeless Conductivity Sensor (Inductive)
Electrodeless conductivity sensors use inductive coils. The inductive conductivity sensor consists of two coils which are incorporated next to one another in a polymer or ceramic body. These coils form current transformers. The sensor is designed so part of the liquid media forms a closed conductive current path passing through the coils. Current is applied to the primary coil (generating coil), which induces an alternating voltage in the liquid loop. In liquids which conduct electricity, this causes a current flow captured by the second coil (receiving coil), which is proportional to the conductivity of the sample solution.
Comparing the sensors
- The main advantages of electrode sensors are:
- there is no proximity effect, the sensor can be mounted next to other sensors without interference
- easily calibrated in small baths
- The main disadvantages are:
- any changes in the cell constant will be reflected in the conductivity, and the cell cannot be cleaned in the field
- electrodes are subject to corrosion or damage (thought, most sensors used in oceanography are inside a cell that prevents this, as shown in the image above)
- electrodes inside a cell need seawater pumping which limits the measuring rate
- The main advantages of inductive sensors are:
- robust construction
- they can be cleaned with soap or solvents and a brush.
- there are no electrodes, so there is no possibility of their damage.
- The main disadvantages are:
- a significant part of the measurement is external leading to major consequences result from this external field. The inductive sensors require a 3 inches radius from any other surface, from adjacent sensors. It is particularly difficult to address this problem in companion mounts such as ARGO floats or biological fouling.
- mounting and calibration of the sensor to companion packages (Argo floats, current meters, AUVs, etc.) must be undertaken to avoid intrusion into the external area. Because final package geometry influences the results, the calibration must be performed on the fully assembled package.
- Zero Calibration Point: Simply perform this calibration point with the probe out of any liquid or solution (e.g., in the air). A very small voltage reading will be read. Call this value 0 ppt.
- Standard Solution Calibration Point: Place the Salinity Sensor into a standard solution (solution of known concentration). Wait for the displayed voltage to stabilize. Enter the value of the standard solution (e.g., 35 ppt).
Historical overview of salinity measurements and definitions
- ↑ William J. Wallace (1974). The Development of the Chlorinity/Salinity Concept in Oceanography. Amsterdam: Elsevier. 239.
- ↑ UNESCO (1985) The international system of units (SI) in oceanography. UNESCO Technical Papers No.45, IAPSO Pub. Sci. No. 32, Paris, France.
- ↑ http://www.aslo.org/lo/toc/vol_14/issue_3/0437.pdf
- ↑ KNUDSEN, M. 1901. Hydrographical tables. G.E.C. Gad, Copenhagen, 63p
- ↑ McDougall, T.J., R. Feistel, F. J. Millero, D. R. Jackett, D. G. Wright, B. A. King, G. M. Marion, C. T. A. Chen and P. Spitzer, 2009: Calculation of the Thermophysical Properties of Seawater, Global Shipbased Repeat Hydrography Manual, IOCCP Report No. 14, ICPO Publication Series no. 134
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