Isotopes of carbon

"Carbon-15" redirects here. For the firearm, see Carbon 15.

Isotopes of carbon (₆C)

Main isotopes Decay abun­dance half-life (t1/2) mode pro­duct 11C synth 20.34 min β+ 11B 12C 98.9% stable 13C 1.06% stable 14C 1 ppt (1⁄1012) 5.70×103 y β− 14N
Standard atomic weight Ar°(C)
	[12.0096, 12.0116] 12.011±0.002 (abridged)

Carbon (₆C) has 15 known isotopes, from ⁸C to ²²C, of which ¹²C and ¹³C are stable. The longest-lived radioisotope is ¹⁴C, with a half-life of 5,700 years. This is also the only carbon radioisotope found in nature—trace quantities are formed cosmogenically by the reaction ¹⁴N + ¹n → ¹⁴C + ¹H. The most stable artificial radioisotope is ¹¹C, which has a half-life of 20.334 minutes. All other radioisotopes have half-lives under 20 seconds, most less than 200 milliseconds. The least stable isotope is ⁸C, with a half-life of 2.0 x 10⁻²¹ s.

Carbon-11

Carbon-11 or ¹¹C is a radioactive isotope of carbon that decays to boron-11. This decay mainly occurs due to positron emission; however, around 0.19–0.23% of the time, it is a result of electron capture. It has a half-life of 20.334 minutes.

¹¹
C
→ +
e⁺
+
ν
_e + 0.96 MeV

¹¹
C
+
e⁻
→ + Electron neutrino + 1.98 MeV

It is produced from nitrogen in a cyclotron by the reaction

¹⁴
N
+
p
→ ¹¹
C
+ ⁴
He

Carbon-11 is commonly used as a radioisotope for the radioactive labeling of molecules in positron emission tomography. Among the many molecules used in this context is the radioligand [¹¹
C
]DASB.

Natural isotopes

Main articles: Carbon-12, Carbon-13, and Carbon-14

There are three naturally occurring isotopes of carbon: 12, 13, and 14. ¹²C and ¹³C are stable, occurring in a natural proportion of approximately 99:1. ¹⁴C is produced by thermal neutrons from cosmic radiation in the upper atmosphere, and is transported down to earth to be absorbed by living biological material. Isotopically, ¹⁴C constitutes a negligible part; but, since it is radioactive with a half-life of 5,700 years, it is radiometrically detectable. Since dead tissue doesn't absorb ¹⁴C, the amount of ¹⁴C is one of the methods used within the field of archeology for radiometric dating of biological material.

Paleoclimate

¹²C and ¹³C are measured as the isotope ratio δ¹³C in benthic foraminifera and used as a proxy for nutrient cycling and the temperature dependent air-sea exchange of CO₂ (ventilation) (Lynch-Stieglitz et al., 1995). Plants find it easier to use the lighter isotopes (¹²C) when they convert sunlight and carbon dioxide into food. So, for example, large blooms of plankton (free-floating organisms) absorb large amounts of ¹²C from the oceans. Originally, the ¹²C was mostly incorporated into the seawater from the atmosphere. If the oceans that the plankton live in are stratified (meaning that there are layers of warm water near the top, and colder water deeper down), then the surface water does not mix very much with the deeper waters, so that when the plankton dies, it sinks and takes away ¹²C from the surface, leaving the surface layers relatively rich in ¹³C. Where cold waters well up from the depths (such as in the North Atlantic), the water carries ¹²C back up with it. So, when the ocean was less stratified than today, there was much more ¹²C in the skeletons of surface-dwelling species. Other indicators of past climate include the presence of tropical species, coral growths rings, etc.

Tracing food sources and diets

The quantities of the different isotopes can be measured by mass spectrometry and compared to a standard; the result (e.g. the delta of the ¹³C = δ¹³C) is expressed as parts per thousand (‰):

$\delta ^{13}C=\left({\frac {\left({\frac {^{13}C}{^{12}C}}\right)_{\text{sample}}}{\left({\frac {^{13}C}{^{12}C}}\right)_{\text{standard}}}}-1\right)\times 1000\ ^{\text{o}}\!\!/\!_{\text{oo}}.$

Stable carbon isotopes in carbon dioxide are utilized differentially by plants during photosynthesis. Grasses in temperate climates (barley, rice, wheat, rye and oats, plus sunflower, potato, tomatoes, peanuts, cotton, sugar beet, and most trees and their nuts/fruits, roses and Kentucky bluegrass) follow a C3 photosynthetic pathway that will yield δ¹³C values averaging about −26.5‰. Grasses in hot arid climates (maize in particular, but also millet, sorghum, sugar cane and crabgrass) follow a C4 photosynthetic pathway that produces δ¹³C values averaging about −12.5‰.

It follows that eating these different plants will affect the δ¹³C values in the consumer's body tissues. If an animal (or human) eats only C3 plants, their δ¹³C values will be from −18.5 to −22.0‰ in their bone collagen and −14.5‰ in the hydroxylapatite of their teeth and bones.

In contrast, C4 feeders will have bone collagen with a value of −7.5‰ and hydroxylapatite value of −0.5‰.

In actual case studies, millet and maize eaters can easily be distinguished from rice and wheat eaters. Studying how these dietary preferences are distributed geographically through time can illuminate migration paths of people and dispersal paths of different agricultural crops. However, human groups have often mixed C3 and C4 plants (northern Chinese historically subsisted on wheat and millet), or mixed plant and animal groups together (for example, southeastern Chinese subsisting on rice and fish).

List of isotopes

nuclide symbol	Z(p)	N(n)	isotopic mass (u)	half-life	decay mode(s)	daughter isotope(s)	nuclear spin	representative isotopic composition (mole fraction)	range of natural variation (mole fraction)
8C	6	2	8.037675(25)	2.0(4) × 10−21 s [230(50) keV]	2p	6 Be	0+
9C	6	3	9.0310367(23)	126.5(9) ms	β+ (60%)	9 B	(3/2−)
					β+, p (23%)	8 Be
					β+, α (17%)	5 Li
10C	6	4	10.0168532(4)	19.290(12) s	β+	10 B	0+
11C	6	5	11.0114336(10)	20.334(24) min	β+ (99.79%)	11 B	3/2−
					EC (.21%)	11 B
12C	6	6	12 exactly	Stable			0+	0.9893(8)	0.98853–0.99037
13C	6	7	13.0033548378(10)	Stable			1/2−	0.0107(8)	0.00963–0.01147
14C	6	8	14.003241989(4)	5,730 years	β−	14 N	0+	Trace	<10−12
15C	6	9	15.0105993(9)	2.449(5) s	β−	15 N	1/2+
16C	6	10	16.014701(4)	0.747(8) s	β−, n (97.9%)	15 N	0+
					β− (2.1%)	16 N
17C	6	11	17.022586(19)	193(5) ms	β− (71.59%)	17 N	(3/2+)
					β−, n (28.41%)	16 N
18C	6	12	18.02676(3)	92(2) ms	β− (68.5%)	18 N	0+
					β−, n (31.5%)	17 N
19C	6	13	19.03481(11)	46.2(23) ms	β−, n (47.0%)	18 N	(1/2+)
					β− (46.0%)	19 N
					β−, 2n (7%)	17 N
20C	6	14	20.04032(26)	16(3) ms [14(+6-5) ms]	β−, n (72.0%)	19 N	0+
					β− (28.0%)	20 N
21C	6	15	21.04934(54)#	<30 ns	n	20 C	(1/2+)#
22C	6	16	22.05720(97)#	6.2(13) ms [6.1(+14-12) ms]	β−	22 N	0+

Notes

• The precision of the isotope abundances and atomic mass is limited through variations. The given ranges should be applicable to any normal terrestrial material.
• Values marked # are not purely derived from experimental data, but at least partly from systematic trends. Spins with weak assignment arguments are enclosed in parentheses.
• Uncertainties are given in concise form in parentheses after the corresponding last digits. Uncertainty values denote one standard deviation, except isotopic composition and standard atomic mass from IUPAC, which use expanded uncertainties.
• Carbon-12 nuclide is of particular importance as it is used as the standard from which atomic masses of all nuclides are expressed: its atomic mass is by definition 12 Da.
• Nuclide masses are given by IUPAP Commission on Symbols, Units, Nomenclature, Atomic Masses and Fundamental Constants (SUNAMCO).
• Isotope abundances are given by IUPAC Commission on Isotopic Abundances and Atomic Weights (CIAAW).

See also

• Radiocarbon dating
• Cosmogenic isotopes
• Environmental isotopes
• Isotopic signature

References

• Isotope masses from:
  • G. Audi; A. H. Wapstra; C. Thibault; J. Blachot; O. Bersillon (2003). "The NUBASE evaluation of nuclear and decay properties" (PDF). Nuclear Physics A. 729: 3–128. Bibcode:2003NuPhA.729....3A. doi:10.1016/j.nuclphysa.2003.11.001. Archived from the original (PDF) on 2008-09-23. {{cite journal}}: Unknown parameter |deadurl= ignored (|url-status= suggested) (help)
• Isotopic compositions and standard atomic masses from:
  • J. R. de Laeter; J. K. Böhlke; P. De Bièvre; H. Hidaka; H. S. Peiser; K. J. R. Rosman; P. D. P. Taylor (2003). "Atomic weights of the elements. Review 2000 (IUPAC Technical Report)". Pure and Applied Chemistry. 75 (6): 683–800. doi:10.1351/pac200375060683.
  • M. E. Wieser (2006). "Atomic weights of the elements 2005 (IUPAC Technical Report)". Pure and Applied Chemistry. 78 (11): 2051–2066. doi:10.1351/pac200678112051. {{cite journal}}: Unknown parameter |laysummary= ignored (help)
• Half-life, spin, and isomer data selected from the following sources. See editing notes on this article's talk page.
  • G. Audi; A. H. Wapstra; C. Thibault; J. Blachot; O. Bersillon (2003). "The NUBASE evaluation of nuclear and decay properties" (PDF). Nuclear Physics A. 729: 3–128. Bibcode:2003NuPhA.729....3A. doi:10.1016/j.nuclphysa.2003.11.001. Archived from the original (PDF) on 2008-09-23. {{cite journal}}: Unknown parameter |deadurl= ignored (|url-status= suggested) (help)
  • National Nuclear Data Center. "NuDat 2.1 database". Brookhaven National Laboratory. Retrieved 23 February 2017.
  • N. E. Holden (2004). "Table of the Isotopes". In D. R. Lide (ed.). CRC Handbook of Chemistry and Physics (85th ed.). CRC Press. Section 11. ISBN 978-0-8493-0485-9. {{cite book}}: Unknown parameter |nopp= ignored (|no-pp= suggested) (help)