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|Name, symbol||Oxygen-18,18O, Ω|
|Isotope mass||17.9991610 u|
|Complete table of nuclides|
O is an important precursor for the production of fluorodeoxyglucose (FDG) used in positron emission tomography (PET). Generally, in the radiopharmaceutical industry, enriched water (H
O) is bombarded with hydrogen ions in either a cyclotron or linear accelerator, creating fluorine-18. This is then synthesized into FDG and injected into a patient. It can also be used to make an extremely heavy version of water when combined with tritium (hydrogen-3): 3
O or T
O. This compound has a density almost 30% greater than that of natural water
In ice cores, mainly Arctic and Antarctic, the ratio of 18
O to 16
O (known as δ18
O) can be used to determine the temperature of precipitation through time. Assuming that atmospheric circulation and elevation has not changed significantly over the poles, the temperature of ice formation can be calculated as equilibrium fractionation between phases of water that is known for different temperatures. Water molecules are also subject to Rayleigh fractionation as atmospheric water moves from the equator poleward which results in progressive depletion of O-18, or lower δ18
O values. In the 1950s, Harold Urey performed an experiment in which he mixed both normal water and water with oxygen-18 in a barrel, and then partially froze the barrel's contents.
The ratio O-18/O-16 (δ18
O) can also be used to determine paleothermometry in certain types of fossils. The fossils in question have to show progressive growth in the animal or plant that the fossil represents. The fossil material used is generally calcite or aragonite, however oxygen isotope paleothermometry has also been done of phosphatic fossils using SHRIMP. For example, seasonal temperature variations may be determined from a single sea shell from a scallop. As the scallop grows, an extension is seen on the surface of the shell. Each growth band can be measured, and a calculation is used to determine the probable sea water temperature in comparison to each growth. The equation for this is:
Where T is temperature in Celsius and A and B are constants.
For determination of ocean temperatures over geologic time, multiple fossils of the same species in different stratigraphic layers would be measured, and the difference between them would indicate long term changes.
In the study of plants' photorespiration, the labeling of atmosphere by oxygen-18 allows us to measure the oxygen uptake by the photorespiration pathway. Labeling by 18
2 gives the unidirectional flux of O
2 uptake, while there is a net photosynthetic 16
2 evolution. It was demonstrated that, under preindustrial atmosphere, most plants reabsorb, by photorespiration, half of the oxygen produced by photosynthesis. Then, the yield of photosynthesis was halved by the presence of oxygen in atmosphere.
Fluorine-18 is usually produced by irradiation of 18O-enriched water (H218O) with high-energy (about 18 MeV) protons prepared in a cyclotron or a linear accelerator, yielding an aqueous solution of 18F fluoride. This solution is then used for rapid synthesis of a labeled molecule, often with the fluorine atom replacing a hydroxyl group. The labeled molecules or radiopharmaceuticals have to be synthetized after the radiofluorine is prepared, as the high energy proton radiation would destroy the molecules.
An example of the production cycle is an irradiation of 2 milliliters of 18O-enriched water in a titanium cell, through a 25 µm thick window made of Havar (a cobalt alloy) foil. A proton beam with energy of 17.5 MeV and beam current of 30 microamperes for 90 minutes.
The irradiated water has to be purified before another irradiation, to remove organic contaminants, traces of tritium produced by a 18O(p,t)16O reaction, and ions leached from the target cell and sputtered from the Havar foil.
- http://www.cedex.es/NR/rdonlyres/B8A9522A-5D6F-4675-921A- 24BB8458187B/124720/Capilla_et_al_geoENV_2012_Valencia_Espa%C3%B1a_Extended.pdf
- Pauling, Linus (1988). "12-7. Heavy Water". General Chemistry (3rd ed.). Dover. p. 438. ISBN 978-0-486-65622-9.
- Kendall, C.; Caldwell, E.A. (1998). "Chapter 2: Fundamentals in Isotope Geochemistry". Isotope Tracers in Catchment Hydrology. Elsevier Science B.V., Amsterdam.
- Trotter, J.A.; Williams, I.S.; Barnes, C.R.; Lécuyer, C.; Nicoll, R.S. (2008). "Did Cooling Oceans Trigger Ordovician Biodiversification? Evidence from Conodont Thermometry". Science. 321 (5888): 550–4. Bibcode:2008Sci...321..550T. doi:10.1126/science.1155814. PMID 18653889.
- Kendall, C.; McDonnell, J.J. (1998). Isotope Tracers in Catchment Hydrology. Elsevier Science B.V., Amsterdam.
- Gerbaud A, André M (November 1979). "Photosynthesis and photorespiration in whole plants of wheat". Plant Physiol. 64 (5): 735–8. doi:10.1104/pp.64.5.735. PMC 543347. PMID 16661044.
- Canvin DT, Berry JA, Badger MR, Fock H, Osmond CB (August 1980). "Oxygen exchange in leaves in the light". Plant Physiol. 66 (2): 302–7. doi:10.1104/pp.66.2.302. PMC 440587. PMID 16661426.
|Oxygen-18 is an
isotope of oxygen
|Decay product of:
nitrogen-18, nitrogen-19, fluorine-18
|Decays to: |