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A general trend appears in these data: peaks in the cooling age populations appear to young to the east from 25 to 20 Ma to 10 8 Ma.
The isotopic age then is called a cooling age.
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In practice, fission-track dates are regarded as cooling ages unless proved otherwise.
These apparent He ages can be interpreted as (A) cooling ages following total thermal resetting, (B) cooling ages following cooling from temperatures which only partially reset the He clocks, or (C) mixed ages of multiple populations.
The northern Gawler Craton mainly records post-Hiltaba Event (∼1590 Ma) U Pb cooling ages.
Detrital thermochronology involves sampling sedimentary materials and acquiring cooling ages from detrital components, in order to constrain the cooling history of the sediment source regions.
Because the exhumation history of different source ranges changes across the Himalaya, the cooling ages of different minerals can be used to constrain where sediment sources.
The tectonic exhumation was also recorded by several other thermochronological systems (e.g. biotite 40Ar/39Ar) with concordant middle Miocene cooling ages in different structural positions across the GHS.
Fig. 8 Comparison of Ar-Ar muscovite cooling ages and depositional ages from the Jawalamukhi section of Najman et al. (2009) and the Jogindernagar section of White et al. (2002).
Alternatively, if the slab breakoff mechanism proposed by Webb et al. (2017) is correct, then the difference in fission track cooling ages may simply reflect the propagation of the tear and uplift from west to east during the Miocene.
The THO east of the fault system records U Pb titanite and total-Pb monazite domain ages that are relatively indistinguishable from 40Ar/39Ar hornblende and mica cooling ages, indicating rapid cooling, and perhaps exhumation, following 1.77 Ga metamorphism.
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