Examples of radiogenic

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Chapter 3 is a short but elegant introduction to geochronology and the principle of radiogenic tracers, a topic returned to later in the book.
Stable and radiogenic isotopes are often used to refine conclusions based on elemental work, to provide age constraints and to elucidate petrogenetic processes.
All aspects are covered: mineralogy, major- and trace-element compositions, and isotope (radiogenic and stable) geochemistry.
Such thermal models are, however, highly time-dependent as radiogenic heat production and erosion are relatively slow processes.
Because of error magnification, owing to the very low proportions of radiogenic argon, the ages of such young lavas are not well constrained.
A grand weighted mean of these radiogenic ratios is then computed.
Thus, considerable loss of radiogenic argon, resulting in a younger apparent age, is clearly implicated in this case.
A third section gave aberrant ages that indicate the presence of inherited or excess radiogenic argon.
These alternatives may be distinguished by radiogenic isotope ratios.
The next two chapters deal with isotope geochemistry, first stable then radiogenic.
An important assumption in these thermal models is the level of crustal radiogenic heat production.
Radiogenic isotope compositions are compatible with a common magmatic source for the two lithologies.
A is radiogenic heat production rate.
The lower crust was divided into two sub-layers of equal thickness having different values of radiogenic heat production, to take into account differences between migmatitic paragneisses and granulites.
Radiogenic and tidal heating in the silicate core may drive metamorphic dehydration of salts in the upper few kilometers of suboceanic crust.
High sums/(n-2) on inverse-isochron regressions are due to the highly radiogenic nature of gas released (poorly constrained upper intercept) and very low analytical uncertainty on each data point.

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