As planetesimals collided, various fragments were scattered and produced meteorites.
Iron meteorites were identified as pieces of the core, while stony meteorites were segments of the mantle and crustal units of these various planetesimals.
The most accurate ages are produced by samples near the y-axis, which was achieved by step-wise leaching and analysis of the samples.
Previously, when applying the alternative Pb–Pb ischron diagram, the The result of U-corrected Pb–Pb dating has produced ages of 4567.35 ± 0.28 My for CAIs (A) and chondrules with ages between 4564.71 ± 0..32 ± 0.42 My (B and C) (see figure).
The Pb ratios of three stony and two iron meteorites were measured.
The dating of meteorites would then help Patterson in determining not only the age of these meteorites but also the age of Earth’s formation.
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However, the absence of zircon or other uranium-rich minerals in chondrites, and the presence of initial non-radiogenic Pb (common Pb), rules out direct use of the U-Pb concordia method.
This makes it difficult to determine the analytical uncertainty on the age.
To avoid this problem, researchers Pb ratio, corresponding to the slope of a normal Pb/Pb isochron, which yields the age.
If the sample behaved as a closed system then graphing the difference between the present and initial ratios of Pb should produce a straight line.
The distance the point moves along this line is dependent on the U/Pb ratio, whereas the slope of the line depends on the time since Earth's formation. The development of the Geochron was mainly attributed to Clair Cameron Patterson’s application of Pb-Pb dating on meteorites in 1956.