Carbon Isotopes (12C, 13C, 14C)
Background
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.
Abundance of carbon isotopes in nature
12C
|
13C
|
14C
|
98.89 %
|
1.11 %
|
~10-12
|
13C measurements are reported in the d13C
notation relative to a standard (PDB, or the newer VPDB standard,
considered identical to PDB)
Isotope ratios are typically measured by mass spectrometry
d13C values cover a wide
range in nature (Fig) influenced
by fractionation processes analogue to what we discussed in the water
isotope section
14C activities are referred to an international standard,
known as as 'modern carbon'
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
The production rate has not been constant over time, comparison with
tree ring chronologies and corals have shown variations in the
production rate which result in an offset between calendar and 14C
ages of thousands of years (Fig)
(Fig)
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). Differnt
fields tend to use different half lifes.
Natural global inventory
The global inventory of natural 14C is about 75 tons. The
specific
activity in pre-industrial times was 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). 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.
Before bomb production began, 14C (and 13C)
dropped due to anthopogenic
emisssions of fossil carbon (Suess effect, Fig)
Notation
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 –19.3‰ with respect to PDB. The factor of 0.95 adjusts the oxalic
acid
to the activity of wood from 1840 to 1860 (‘pre-industrial’). Results
are reported in pmC (% modern carbon).
A0N = 0.95 AOX [1 – 2.3(d13C
+ 19.3)/1000]
- AON: 14C activity of oxalic acid
normalized for 14C
fractionation
- AOX: 14C activity of oxalic acid
- The d13C correction of 19‰
takes
into account the fractionation of 14C during the combustion
of oxalic acid.
Generally radiocarbon concentrations of samples are normalized to a
common d13C value of -25‰. The
fractionation for 14C is 2.3 times the fractionation for 13C and
therefore the enrichment in 14C due to a factionation amounts to:
2.3(
d13C
+ 25‰)
For example if you have a sample with d13C = 1.5‰, and a 14C
activity of 65pmc, the correction amounts to: 2.3(-25-1.5)/1000=-6.1%.
The final radiocarbon value is the 65*0.939 = 61pmC.
Groundwater:
For groundwater studies, the pmc (percent modern carbon) notation is
used.
pmc = (ASN/Aabs) 100% = ASN [AON
e l(y-1950)]-1
100%
- ASN: activity of sample normalized for fractionation
using d13C
- AON: 13C normalized activity of oxalic acid
- Aabs: Absolute 14C activity of the sample
- y: year of measurement of oxalic acid
14C dating
Principle:
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 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):
- activity in soil CO2 (soil air and root respiration);
activity
» 100 pmc
- dissolution of carbonates (lime stone); activity » 0 pmc
- dissolution of carbonates can occur in the unsaturated soil zone
(open
system) or in the saturated soil zone (closed system).
- isotope exchange can lead to a decrease in 14C
activity in
addition
to radioactive decay
- a variety of models can be used to estimate the initial 14C
activity in groundwater. They include the very simple ‘Vogel’ model,
several
models that correct for carbon chemistry using chemical or 13C
balances, and the complex NETPATH model by Plummer. The latter accounts
for the chemical evolution of the groundwater along flowpaths.
14CO2 + H2O + CaCO3
--> Ca2+ + HCO3-
completely open system: 14C activity: » 100 pmc
completely closed system: 14C activity: » 50 pmc
Chemical and isotopc evolution in recharge zone: (Fig) (Fig) Open and closed system
conditions
‘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.
Measurement
- Technique: low-level b - counting using gas-filled proportional
counters
or AMS (Accelerator mass spectrometry)
- Water sample size: ca. 100 liters (low-level counting) or several
hundred
ml (AMS)
- Measurement precision: ± 0.2 to ± 1% (1-s
error) for concentrations close to 100 pmc. This corresponds to an age
resolution of about ± 16 to ± 40 years.
- Detection limit: <1% modern corresponding to ages of about
40000
years.
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.
Resources
- Fairbanks,
R. G., Mortlock, R. A., Chiu, T. C., Cao, L., Kaplan, A., Guilderson,
T. P., Fairbanks, T. W., Bloom, A. L., Grootes, P. M., and Nadeau, M.
J. (2005). Radiocarbon calibration curve spanning 0 to 50,000 years
BP based on paired Th-230/U-234/U-238 and C-14 dates on pristine
corals. Quaternary Science Reviews 24, 1781-1796.
- Reimer,
P. J., Baillie, M. G. L., Bard, E., Bayliss, A., Beck, J. W., Bertrand,
C. J. H., Blackwell, P. G., Buck, C. E., Burr, G. S., Cutler, K. B.,
Damon, P. E., Edwards, R. L., Fairbanks, R. G., Friedrich, M.,
Guilderson, T. P., Hogg, A. G., Hughen, K. A., Kromer, B., McCormac,
G., Manning, S., Ramsey, C. B., Reimer, R. W., Remmele, S., Southon, J.
R., Stuiver, M., Talamo, S., Taylor, F. W., van der Plicht, J., and
Weyhenmeyer, C. E. (2004). IntCal04 terrestrial radiocarbon age
calibration, 0-26 cal kyr BP. Radiocarbon 46, 1029-1058.
- Levin,
I. and Hesshaimer, V. (2000) Radiocarbon - a unique tracer of
global carbon cycle dynamics. Radiocarbon, 42, 1, 69-80.
- Fontes, J. C.; Garnier, J. M. (1979) Determination of the initial
14C
activity
of the total dissolved carbon; a review of the existing models and a
new approach. Water Resour. Res., 15, 399-413.
- Mook, W.G. (1980)
Carbon-14 in hydrogeological studies. In:
Handbook of
environmental isotope geochemistry (Fritz, P, and Fontes, J.C.,
editors),
Vol 1, Elsevier Sci. Publ. Co., Amsterdam, 49-74.
- Plummer, L.N., E.C. Prestemon, and D.L. Parkhurst (1991) An
interactive
code (NETPATH) for modeling net geochemical reactions along a flow
path.
USGS Water-Resources Investigations Report,} 91-4078, USGS, Reston.
- Plummer, L.N., Prestemon, E.C., and Parkhurst, D.L., 1994,
An interactive code (NETPATH) for modeling NET geochemical
reactions along a flow PATH--version 2.0: U.S.
Geological Survey Water- Resources Investigations Report 94-4169, 130 p.
- NETPATH
home page
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continental European Suess effect. Radiocarbon 31(3):431–40.