Alkalinity
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Sea surface alkalinity (from the GLODAP climatology)

Alkalinity or A_T is a measure of the ability of a solution to neutralize acids to the equivalence point of carbonate or bicarbonate. Alkalinity is closely related to the acid neutralizing capacity (ANC) of a solution and ANC is often incorrectly used to refer to alkalinity. However, the acid neutralizing capacity refers to the combination of the solution and solids present (e.g., suspended matter, or aquifer solids), and the contribution of solids can dominate the ANC (see carbonate minerals below).

The alkalinity is equal to the stoichiometric sum of the bases in solution. In the natural environment carbonate alkalinity tends to make up most of the total alkalinity due to the common occurrence and dissolution of carbonate rocks and presence of carbon dioxide in the atmosphere. Other common natural components that can contribute to alkalinity include borate, hydroxide, phosphate, silicate, nitrate, dissolved ammonia, the conjugate bases of some organic acids and sulfide. Solutions produced in a laboratory may contain a virtually limitless number of bases that contribute to alkalinity. Alkalinity is usually given in the unit mEq/L (milliequivalent per liter). Commercially, as in the pool industry, alkalinity might also be given in the unit ppm or parts per million.

Alkalinity is sometimes incorrectly used interchangeably with basicity. For example, the pH of a solution can be lowered by the addition of CO₂. This will reduce the basicity; however, the alkalinity will remain unchanged (see example below).

Theoretical treatment of alkalinity

In typical groundwater or seawater the measured alkalinity is set equal to:

A_T = [HCO₃⁻_T + 2[CO₃⁻²_T + [B(OH)₄⁻_T + [OH⁻_T + 2[PO₄⁻³_T + [HPO₄⁻²_T + [SiO(OH)₃⁻_T − [H⁺_sws − [HSO₄⁻

(Subscript T indicates the total concentration of the species in the solution as measured. This is opposed to the free concentration, which takes into account the significant amount of ion pair interactions that occur in seawater.)

Alkalinity can be measured by titrating a sample with a strong acid until all the buffering capacity of the aforementioned ions above the pH of bicarbonate or carbonate is consumed. This point is functionally set to pH 4.5. At this point, all the bases of interest have been protonated to the zero level species, hence they no longer cause alkalinity. For example, the following reactions take place during the addition of acid to a typical seawater solution:

HCO₃⁻ + H⁺ → CO₂ + H₂O

CO₃⁻² + 2H⁺ → CO₂ + H₂O

B(OH)₄⁻ + H⁺ → B(OH)₃ + H₂O

OH⁻ + H⁺ → H₂O

PO₄⁻³ + 2H⁺ → H₂PO₄⁻

HPO₄⁻² + H⁺ → H₂PO₄⁻

[SiO(OH)₃⁻ + H⁺ → [Si(OH)₄⁰

It can be seen from the above protonation reactions that most bases consume one proton (H⁺) to become a neutral species, thus increasing alkalinity by one per equivalent. CO₃⁻² however, will consume two protons before becoming a zero level species (CO₂), thus it increases alkalinity by two per mole of CO₃⁻². [H⁺ and [HSO₄⁻ decrease alkalintiy, as they act as sources of protons. They are often represented collectively as [H⁺_T.

Alkalinity is typically reported as mg/L as CaCO₃. This can be converted into milliEquivalents per Liter (mEq/L) by dividing by 50 (the approximate MW of CaCO₃/2).

Example problems

Sum of contributing species

The following equations demonstrate the relative contributions of each component to the alkalinity of a typical seawater sample. Contributions are in μmol/kg-H₂O and are obtained from A Handbook of Methods for the analysis of carbon dioxide parameters in seawater "[1],"(Salinity = 35, pH = 8.1, Temperature = 25°C).

A_T = [HCO₃⁻_T + 2[CO₃⁻²_T + [B(OH)₄⁻_T + [OH⁻_T + 3[PO₄⁻³_T + [HPO₄⁻²_T + [SiO(OH)₃⁻_T − [H⁺ − [HSO₄⁻ − [HF]

Phosphates and silicate, being nutrients, are typically negligible. At pH = 8.1 [HSO₄⁻ and [HF] are also negligible. So,

A_T = [HCO₃^-_T + 2[CO₃⁻²_T + [B(OH)₄⁻_T + [OH⁻_T − [H⁺

A_T = 1830 + 2*270 + 100 + 10 − 0.01

A_T = 2480 μmol/kg−H₂O

Addition of CO₂

The addition (or removal) of CO₂ to a solution does not change the alkalinity. This is because the net reaction produces the same number of equivalents of positively contributing species (H+) as negative contributing species (HCO3- and/or CO3--).

At neutral pH's:

CO₂ + H₂O → HCO₃⁻ + H⁺

At high pH's:

CO₂ + H₂O → CO₃⁻² + 2H⁺

Dissolution of carbonate rock

Addition of CO₂ to a solution in contact with a solid can affect the alkalinity, especially for carbonate minerals in contact with groundwater or seawater . The dissolution (or precipitation) of carbonate rock has a strong influence on the alkalinity. This is because carbonate rock is composed of CaCO₃ and its dissociation will add Ca⁺² and CO₃⁻² into solution. Ca⁺² will not influence alkalinity, but CO₃⁻² will increase alkalinity by 2 units.

See also

• Alkali soils
• Biological pump
• Global Ocean Data Analysis Project
• Ocean acidification
• Base (chemistry)

Carbonate system calculators

The following packages calculate the state of the carbonate system in seawater (including pH):

• CO2SYS, a stand-alone executable (also available in a version for Microsoft Excel/VBA)
• seacarb, a R package for Windows, Mac OS X and Linux (also available here)
• CSYS, a Matlab script

External links

• Holmes-Farley, Randy. "Chemistry and the Aquarium," Advanced Aquarist's Online Magazine. Alkalinity as it pertains to salt-water aquariums.
• DOE (1994) "[2],"Handbook of methods for the analysis of the various parameters of the carbon dioxide system in sea water. Version 2, A. G. Dickson & C. Goyet, eds. ORNL/CDIAC-74. Pheobe and Brock are the coolest people who everhad to study alkalinity we rock your socks off.