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Uranium–lead dating, abbreviated U–Pb dating, is one of the oldest^[1] and most refined of the radiometric dating schemes. It can be used to date rocks that formed and crystallised ^[2] from about 1 million years to over 4.5 billion years ago with routine precisions in the 0.1–1 percent range.^[3]

The dating method is usually performed on the mineral zircon. The mineral incorporates uranium and thorium atoms into its crystal structure, but strongly rejects lead. Therefore, one can assume that the entire lead content of the zircon is radiogenic, i.e. it is produced solely by a process of radioactive decay after the formation of the mineral. Thus the current ratio of lead to uranium in the mineral can be used to determine its age^{[citation needed]}.

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

The above uranium to lead decay routes occur via a series of alpha (and beta) decays, in which ²³⁸U with daughter nuclides undergo total eight alpha and six beta decays whereas ²³⁵U with daughters only experience seven alpha and four beta decays.^[4]

The existence of two 'parallel' uranium–lead decay routes (²³⁸U to ²⁰⁶Pb and ²³⁵U to ²⁰⁷Pb) leads to multiple 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, is famous for having used it to obtain one of the earliest estimates of the age of the Earth.

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 do not occur, a better, more inclusive, model of the data must be applied. 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 common in the geologic record.

Interaction between mineralogy and radioactive breakdown

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.^[4]Fission tracks and micro-cracks within the crystal will further extend this radiation damage network.

These fission tracks inevitably act as conduits deep within the crystal, thereby providing a method of transport to facilitate the leaching of lead isotopes from the zircon crystal.^[5]

Details

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

NNow=NOrige−λtdisplaystyle N_mathrm Now =N_mathrm Orig e^-lambda t,

where

• 
  NNow=Udisplaystyle N_mathrm Now =mathrm U is the number of uranium atoms measured now.


• 
  NOrigdisplaystyle N_mathrm Orig is the number of uranium atoms originally - equal to the sum of uranium and lead atoms U+Pbdisplaystyle mathrm U +mathrm Pb measured now.


• 
  λ=λUdisplaystyle lambda =lambda _mathrm U is the decay rate of Uranium.


• 
  tdisplaystyle t is the age of the zircon, which one wants to determine.

This gives

U=(U+Pb)e−λUt,displaystyle mathrm U =left(mathrm U +mathrm Pb right)e^-lambda _mathrm U t,

which can be written as

PbU=eλUt−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:

206Pb∗238U=eλ238t−1,displaystyle ^text206,!textPb^* over ^text238,!textU=e^lambda _238t-1,

(1)

207Pb∗235U=eλ235t−1.displaystyle ^text207,!textPb^* over ^text235,!textU=e^lambda _235t-1.

(2)

These are said to yield concordant ages.^{[clarification needed]} It is these concordant ages, plotted over a series of time intervals, that result in the concordant line.^[6]

Loss (leakage) of lead from the sample will result in a discrepancy in the ages determined by each decay scheme. This effect is referred to as discordance and is demonstrated in Figure 1. If a series of zircon samples has lost different amounts of lead, the samples generate a discordant line. The upper intercept of the concordia and the discordia line will reflect the original age of formation, while the lower intercept will reflect the age of the event that led to open system behavior and therefore the lead loss; although there has been some disagreement regarding the meaning of the lower intercept ages.^[6]

Figure 1: Concordia diagram for data published by Mattinson^[5] for zircon samples from Klamath Mountains in Northern California. Ages for the concordia increase in increments of 100 million years.

Undamaged zircon retains the lead generated by radioactive decay of uranium and thorium until very high temperatures (about 900 °C), though accumulated radiation damage within zones of very high uranium can lower this temperature substantially. Zircon is very chemically inert and resistant to mechanical weathering—a mixed blessing for geochronologists, as zones or even whole crystals can survive melting of their parent rock with their original uranium-lead age intact. Zircon crystals with prolonged and complex histories can thus contain zones of dramatically different ages (usually, with the oldest and youngest zones forming the core and rim, respectively, of the crystal), and thus are said to demonstrate inherited characteristics. Unraveling such complications (which, depending on their maximum lead-retention temperature, can also exist within other minerals) generally requires in situ micro-beam analysis via, say, ion microprobe (SIMS) or laser ICP-MS.

See also

• 
  Lead–lead dating (Pb–Pb dating)

References

The Wikibook Historical Geology has a page on the topic of: Other isochron methods

The Wikibook Historical Geology has a page on the topic of: U-Pb, Pb-Pb, and fission track dating