Uranium–lead dating, abbreviated U–Pb dating, is one of the oldest and most refined of the radiometric dating schemes. It can be used to date rocks that formed and crystallised from about 1 million years to over 4.5 billion years ago with routine precisions in the 0.1–1 percent range. The method is usually applied to zircon. This mineral incorporates uranium and thorium atoms into its crystal structure, but strongly rejects lead when forming. As a result, newly-formed zircon crystals will contain no lead, meaning that any lead found in the mineral is radiogenic. Since the exact rate at which uranium decays into lead is known, the current ratio of lead to uranium in a sample of the mineral can be used to reliably determine its age. The method relies on two separate decay chains, the uranium series from 238U to 206Pb, with a half-life of 4.47 billion years and the actinium series from 235U to 207Pb, with a half-life of 710 million years.
Decay routes Uranium decays to lead via a series of alpha and beta decays, in which 238U and its daughter nuclides undergo a total of eight alpha and six beta decays, whereas 235U and its daughters only experience seven alpha and four beta decays. The existence of two 'parallel' uranium–lead decay routes (238U to 206Pb and 235U to 207Pb) leads to multiple feasible dating techniques within the overall U–Pb system. The term U–Pb dating normally implies the coupled use of both decay schemes in the 'concordia diagram' (see below). However, use of a single decay scheme (usually 238U to 206Pb) leads to the U–Pb isochron dating method, analogous to the rubidium–strontium dating method. Finally, ages can also be determined from the U–Pb system by analysis of Pb isotope ratios alone. This is termed the lead–lead dating method. Clair Cameron Patterson, an American geochemist who pioneered studies of uranium–lead radiometric dating methods, used it to obtain one of the earliest estimates of the age of the Earth in 1956 to be 4.550Gy ± 70My; a figure that has remained largely unchallenged since.
Mineralogy Although zircon (ZrSiO4) is most commonly used, other minerals such as monazite (see: monazite geochronology), titanite, and baddeleyite can also be used. Where crystals such as zircon with uranium and thorium inclusions cannot be obtained, uranium–lead dating techniques have also been applied to other minerals such as calcite / aragonite and other carbonate minerals. These types of minerals often produce lower-precision ages than igneous and metamorphic minerals traditionally used for age dating, but are more commonly available in the geologic record.
Mechanism During the alpha decay steps, the zircon crystal experiences radiation damage, associated with each alpha decay. This damage is most concentrated around the parent isotope (U and Th), expelling the daughter isotope (Pb) from its original position in the zircon lattice. In areas with a high concentration of the parent isotope, damage to the crystal lattice is quite extensive, and will often interconnect to form a network of radiation damaged areas. Fission tracks and micro-cracks within the crystal will further extend this radiation damage network. These fission tracks act as conduits deep within the crystal, providing a method of transport to facilitate the leaching of lead isotopes from the zircon crystal.
Computation Under conditions where no lead loss or gain from the outside environment has occurred, the age of the zircon can be calculated by assuming exponential decay of uranium. That is
N n = N o e − λ t {\displaystyle N_{\mathrm {n} }=N_{\mathrm {o} }e^{-\lambda t}\,}
where
N n = U {\displaystyle N_{\mathrm {n} }=\mathrm {U} } is the number of uranium atoms measured now.
N o {\displaystyle N_{\mathrm {o} }} is the number of uranium atoms originally - equal to the sum of uranium and lead atoms U + P b {\displaystyle \mathrm {U} +\mathrm {Pb} } measured now.
λ = λ U {\displaystyle \lambda =\lambda _{\mathrm {U} }} is the decay rate of Uranium.
t {\displaystyle t} is the age of the zircon, which one wants to determine. This gives
U = ( U + P b ) e − λ U t , {\displaystyle \mathrm {U} =\left(\mathrm {U} +\mathrm {Pb} \right)e^{-\lambda _{\mathrm {U} }t},}
which can be written as
P b U = e λ U t − 1. {\displaystyle {{\mathrm {Pb} } \over {\mathrm {U} }}=e^{\lambda _{\mathrm {U} }t}-1.}
The more commonly used decay chains of Uranium and Lead gives the following equations:
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