Argon–argon dating

Age equation

The age of a sample is given by the age equation:

${\displaystyle t=\frac{1}{\lambda }\ln (J\times R+1)}$

where λ is the radioactive decay constant of ⁴⁰K (approximately 5.5 × 10⁻¹⁰ year⁻¹, corresponding to a half-life of approximately 1.25 billion years), J is the J-factor (parameter associated with the irradiation process), and R is the ⁴⁰Ar*/³⁹Ar ratio. The J factor relates to the fluence of the neutron bombardment during the irradiation process; a denser flow of neutron particles will convert more atoms of ³⁹K to ³⁹Ar than a less dense one.

Relative dating only

The ⁴⁰Ar/³⁹Ar method only measures relative dates. In order for an age to be calculated by the ⁴⁰Ar/³⁹Ar technique, the J parameter must be determined by irradiating the unknown sample along with a sample of known age for a standard. Because this (primary) standard ultimately cannot be determined by ⁴⁰Ar/³⁹Ar, it must be first determined by another dating method. The method most commonly used to date the primary standard is the conventional K/Ar technique. An alternative method of calibrating the used standard is astronomical tuning (also known as orbital tuning), which arrives at a slightly different age.

Applications

The primary use for ⁴⁰Ar/³⁹Ar geochronology is dating metamorphic and igneous minerals. ⁴⁰Ar/³⁹Ar is unlikely to provide the age of intrusions of granite as the age typically reflects the time when a mineral cooled through its closure temperature. However, in a metamorphic rock that has not exceeded its closure temperature the age likely dates the crystallization of the mineral. Dating of movement on fault systems is also possible with the ⁴⁰Ar/³⁹Ar method. Different minerals have different closure temperatures; biotite is ∼300°C, muscovite is about 400°C and hornblende has a closure temperature of ∼550°C. Thus, a granite containing all three minerals will record three different "ages" of emplacement as it cools down through these closure temperatures. Thus, although a crystallization age is not recorded, the information is still useful in constructing the thermal history of the rock.

Dating minerals may provide age information on a rock, but assumptions must be made. Minerals usually only record the last time they cooled down below the closure temperature, and this may not represent all of the events which the rock has undergone, and may not match the age of intrusion. Thus, discretion and interpretation of age dating is essential. ⁴⁰Ar/³⁹Ar geochronology assumes that a rock retains all of its ⁴⁰Ar after cooling past the closing temperature and that this was properly sampled during analysis.

This technique allows the errors involved in K–Ar dating to be checked. Argon–argon dating has the advantage of not requiring determinations of potassium. Modern methods of analysis allow individual regions of crystals to be investigated. This method is important as it allows crystals forming and cooling during different events to be identified.

Recalibration

One problem with argon–argon dating has been a slight discrepancy with other methods of dating. Work by Kuiper et al. reports that a correction of 0.65% is needed. Thus the Cretaceous–Paleogene extinction (when the dinosaurs died out)—previously dated at 65.0 or 65.5 million years ago—is more accurately dated to 66.0–66.1 Ma.