The dexamethasone suppression test (DST) is used to determine the sensitivity of the hypothalamic-pituitary-adrenal axis (HPA-axis) to negative feedback. Dexamethasone is usually administered at 23:00 h or at midnight but this is often not convenient. The aim of this study was to determine whether the administration of dexamethasone at 21:00 h as compared to 23:00 h would alter the degree to which 08:00 h plasma cortisol was suppressed the following morning. Three healthy males (mean+/-SE: 32+/-7 yr) and 3 healthy females (mean+/-SE: 35+/-7 yr) took part in the study. Each subject was orally administered 1 of 3 doses of dexamethasone (0.25 mg, 0.5 mg, or 1.0 mg) on 3 separate occasions in random order at least a week apart. Each dose of dexamethasone was taken at either 21:00 h or 23:00 h so that each subject underwent 6 tests. The differences in cortisol suppression between times and doses of dexamethasone were assessed using Analysis of Variance. Plasma cortisol was suppressed less in response to 0.25 mg dexamethasone at both 21:00 h and 23:00 h as compared with doses of dexamethasone of 0.5 mg or 1.0 mg (p=0.004). Suppression of plasma cortisol in response to each dose of dexamethasone was similar regardless of the timing of dexamethasone administration (p=0.5). We conclude that in healthy subjects 0.25 mg dexamethasone suppresses plasma cortisol less than either 0.5 mg or 1.0 mg and that 0.5 mg dexamethasone suppresses plasma cortisol to a similar extent as 1.0 mg dexamethasone. Moreover, changing the administration time of dexamethasone from 23:00 h to 21:00 h does not effect the degree to which cortisol is suppressed in healthy subjects.

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In this study, data from garnet‐kyanite metapelites in ultrahigh‐pressure (UHP) domains of the Western Gneiss Region (WGR), Norway, are presented. U–Pb geochronology and trace element compositions in zircon, monazite, apatite, rutile and garnet were acquired, and pressure–temperature (P–T) conditions were calculated using mineral equilibria forward modelling and Zr‐in‐rutile thermometry. Garnet‐kyanite gneiss from Ulsteinvik record a prograde evolution passing through ~690–710°C and ~9–11 kbar. Zircon and rutile age and thermometry data indicate these prograde conditions significantly pre‐date Silurian UHP subduction in the WGR and are interpreted to record early Caledonian subduction of continental‐derived allochthons. Minimum peak conditions in the Ulsteinvik metapelite occur at ~28 kbar, constrained by an inferred garnet+kyanite+omphacite+muscovite+rutile+coesite+H2O assemblage. The retrograde evolution passed through ~740°C and ~7 kbar, first recorded by the destruction of omphacite and followed by the partial replacement of kyanite and garnet by cordierite and spinel. Garnet‐kyanite metapelite from the diamond‐bearing Fjørtoft outcrop documents a polymetamorphic history, with garnet forming during the late Mesoproterozoic and limited preservation of high‐pressure Caledonian assemblages. Similar to the Ulsteinvik metapelite, zircon and rutile age data from the Fjørtoft metapelite also record pre‐Scandian Caledonian ages. Two potential tectonic scenarios are possible: (1) The samples were exhumed at different times during pre‐Scandian subduction of the Blåhø nappe, or (2) the samples do not share a history in the same nappe complex, instead the Ulsteinvik metapelite is a constituent of the Seve‐Blåhø Nappe, whilst the Fjørtoft metapelite shares its history within a separate nappe complex.

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