Radiocarbon 14C

14C is a radioactive isotope of carbon. It was discovered in 1934 by Grosse as an unknown activity in the mineral endialyte. In the same year, Kurie (Yale) exposed nitrogen to fast neutrons and observed long tracks in a bubble chamber. He had produced 14C. It was in atmospheric CO2 by Libby in 1946. He determined the half life to be 5568 years. This half life has later been re-determined by Godwin. The new half life is 5730 years. Libby recognized that due to its occurrence in natural materials, 14C can be used as a dating tool for materials that contain carbon compounds derived from atmospheric CO2 either by simple mixing processes or by carbon exchange. The mean life time of roughly 8000 years is ideal for dating of reservoirs that are a few decades to a few ten thousand yeas old. For groundwater, this means that 14C dating can be applied to aquifers that contain water formed during periods that reach well into the past glacial time. 14C is a widely used tool to establish chronologies for groundwater flow systems and climate records for the Holocene and Pleistocene. It is considered to be the most important tool for age dating of ‘old’ groundwater.

The challenge in 14C dating of groundwater is the determination of the initial 14C content of groundwater at the time of recharge, i.e., at the time when groundwater is isolated from exchange with the soil air and moves away from the water table.

There is also a stable isotope of carbon, 13C. This isotope is important in that it allows us to correct for carbon isotope fractionation in nature and during analytical procedures.

Natural 14C production

14C is mainly produced by interaction of cosmic ray derived secondary neutrons with 14N in the atmosphere.
14N (n,p) 14C
14C can also be produced by the following reaction:
13C(d,p)14C d: deuterium or 2H
the production rate is 2.4 ± 0.2 atoms (cm2 sec)-1

Radioactive decay

14C decays by b- decay with a maximum energy of 0.158 MeV.

146C -> 147N+ e- + anti-neutrino+ Q

Its half life t is 5730 years, i.e., somewhat larger than the half life determined by Libby (5568 ys).

Natural global inventory

The global inventory of natural 14C is about 75 tons. The specific activity is » 13.56 dpm (gC)-1. dpm stands for decay per minute.

Anthropogenic 14C production

The main source of anthropogenic 14C is so-called ‘bomb’ 14C, i.e., 14C produced during atmospheric testing of nuclear weapons. At the peak of surface testing of nuclear devices in 1963, the atmospheric 14C activity had reached about twice that of natural 14C (Fig. 8.5 in Clark/Fritz). The bomb 14C has been produced by interaction of atmospheric nitrogen with the high neutron flux from the explosion of nuclear devices (mainly thermonuclear devices). Local increases in atmospheric 14C have been observed in the vicinity of nuclear power plants.


The notation of 14C activities is discussed in detail in Stuiver and Pollach (Radiocarbon, 19, 355-365, 1977). In short, 14C is calibrated against an NBS (National Bureau of Standards) oxalic acid standard. The internationally accepted radiocarbon dating reference is 95% of the activity, in 1950 AD, of the NBS oxalic acid normalized to d13C of –13‰ with respect to PDB. The factor of 0.95 adjusts the oxalic acid to the activity of wood from 1840 to 1860 (‘pre-industrial’).

A0N = 0.95 AOX [1 – 2(d13C + 19)/1000]

For groundwater studies, the pmc (percent modern carbon) notation is used.

pmc = (ASN/Aabs) 100% = ASN [AON e l(y-1950)]-1 100%

14C dating


In the atmosphere, 14C is incorporated into 14CO2 and takes part in the global carbon cycle. It is assimilated by plants. Except for isotope fractionation, 14C in living organic matter is the same as that in atmospheric CO2. After organic matter dies, the 14C concentration decreases due to radioactive decay. If there is no isotope exchange, radioactive decay is the only 14C sink and if the initial 14C activity is known, an age can be calculated from the measured 14C activity of a sample.
In groundwater applications typically DIC (dissolved inorganic carbon; DIC = CO2(aqueous) + HCO3- + CO32-) is extracted from the water a and its measured 14C activity is compared to the initial 14C activity. Determination of the initial 14C activity can be challenging and typically requires correction models that account for the carbon chemistry in the unsaturated and saturated soil zones.

14C(t) = 14C(t0) e-l (t-t0)

ln 14C(t) = ln 14C(t0) (-l (t-t0))

ln [14C(t)/14C(t0)] = -l (t-t0)

D t = (t - t0) = -l-1 ln [14C(t)/14C(t0)] = T1/2 / ln2 {ln [+C(t0)/14C(t)]}

l: radioactive decay constant of 14C: l = t-1; t : mean life time: t = T1/2/ln2

Initial 14C activity

The age equation derived above assumes a known initial 14C activity of the sample. For natural atmospheric 14C, variability in the 14C production has to be reconstructed from calibrated tree ring chronologies or from coral records dated by U/Th. (Fig. 8.4; Clark and Fritz).

Initial 14C activity in groundwater

See summary in Clark and Fritz (chapter 8) for details

In short, the 14C activity of DIC (dissolved inorganic carbon) in groundwater is determined by the following factors: (Fig. 8.6 in Clark and Fritz):

14CO2 + H2O + CaCO3 --> Ca2+ + HCO3-

completely open system: 14C activity: » 100 pmc

completely closed system: 14C activity: » 50 pmc

‘real world’ systems are somewhere in between open and closed and the correction models mentioned above and described in Clark and Fritz (chapter 8) have to be applied.

Atmospheric concentrations

Determined by

Determined by measurements Measurement There are many laboratories worldwide that can measure 14C routinely. However, only few 14C laboratories have the capability to measure 14C at precisions of ± 0.2%. In groundwater studies the overall error is dominated by systematic errors and the analytical precision is not as critical as in oceanographic studies.