Inference of a detailed P– T path from P– T pseudosections using metapelitic rocks of variable composition from a single outcrop, Shackleton Range, Antarctica

• Published in: Journal of Metamorphic Geology
• Main Author: Zeh, A.
• Format: Article in Journal/Newspaper
• Language: English
• Published: Wiley 2001
• Subjects: Antarc*; Antarctica
• Online Access: http://dx.doi.org/10.1046/j.0263-4929.2000.00314.x; https://api.wiley.com/onlinelibrary/tdm/v1/articles/10.1046%2Fj.0263-4929.2000.00314.x; https://onlinelibrary.wiley.com/doi/pdf/10.1046/j.0263-4929.2000.00314.x

Abstract Generally, P – T pseudosections for reduced compositional systems, such as K 2 O–FeO–MgO–Al 2 O 3 –SiO 2 –H 2 O, Na 2 O–K 2 O–FeO–MgO–Al 2 O 3 –SiO 2 –H 2 O and MnO–K 2 O–FeO–MgO–Al 2 O 3 –SiO 2 –H 2 O, are well suited for inferring detailed P – T paths, comparing mineral assemblages observed in natural rocks with those calculated. Examples are provided by P – T paths inferred for four metapelitic samples from a 1 m 2 wide outcrop of the Herbert Mountains in the Shackleton Range, Antarctica. The method works well if the bulk composition used is reconstituted from average mineral modes and mineral compositions (AMC) or when X‐ray fluorescence (XRF) data are corrected for Al 2 O 3 and FeO. A plagioclase correction is suitable for Al 2 O 3 . Correction for FeO is dependent on additional microscopic observations, e.g. the kind and amount of opaque minerals. In some cases, all iron can be treated as FeO tot , whereas in others a magnetite or hematite correction yields much better results. Comparison between calculated and observed mineral modes and mineral compositions shows that the AMC bulk composition is best suited to the interpretation of rock textures using P – T pseudosections, whereas corrected XRF data yield good results only when the investigated sample has few opaque minerals. The results indicate that metapelitic rocks from the Herbert Mountains of the Northern Shackleton Range underwent a prograde P – T evolution from about 600 °C/5.5 kbar to 660 °C/7 kbar, followed by nearly adiabatic cooling to about 600 °C at 4.5 kbar.