Sentence examples for closure temperature from inspiring English sources

These four samples are thought to reflect a simple rapid cooling history around the closure temperature of the ZHe system.

This observation suggests that these samples experienced a relatively complicated thermal history around the closure temperature of the ZHe system.

For apatite samples, grain ages generally reproduced reasonably well (Fig. 3), suggesting a simple and relatively rapid cooling history around the closure temperature of the AHe system.

Thus, we did not calculate the weighted mean ages of the four samples since closure temperature of the zircon He system may vary with eU (Guenthner et al. 2013).

AHe T c is the closure temperature of the AHe system considering the cooling rate of each sample; detailed calculations are shown in the body text AbM Abukuma Mountains, OBR Ou Backbone Range, AsM Asahi Mountains, CrGr Cretaceous granitoid.

Since the definition of closure temperature in the 1960s, mineral ages of low-temperature geochronometers are traditionally interpreted as the result of cooling induced by erosion, whose rate is a simple, unique function of age patterns.

Because closure temperatures vary widely from, say, 300 °C for titanite and zircon to less than 100 °C for biotite and apatite, valuable information can be obtained regarding the uplift and cooling rates of crustal rocks.

The Ar isotope system, whose closure temperatures range from ca. 130 to 690°C (e.g., Faure and Mensing 2005), can provide good clue to solve it.

ZHe ages are older than or equal to the corresponding AHe ages, which is consistent with the predicted difference in closure temperatures (160 200 °C for ZHe system; Guenthner et al. 2013).

Differences in the trace element chemistry, in the structural parameters and in the intracrystalline closure temperatures suggest that a different history should be considered for Cameroon, Morocco and LB I and LB II spinels.

(U Th)/He thermochronometers have relatively low closure temperatures, ~55 to 80 °C for apatite (Flowers et al. 2009; Gautheron et al. 2009) and ~160 to 200 °C for zircon (Guenthner et al. 2013), compared to the other major thermochronometers (see Table 1 of Reiners et al. 2005).