Petrochronology and hygrochronology of tectono-metamorphic events

Abstract

U-Th-Pb petrochronology is based on the incontrovertible fact that the diffusion of radiogenic Pb is negligibly small relative to retrograde reaction rates. Multi-element maps demonstrate that patchy textures tightly correspond to (U+Th)-Pb age variations, requiring that fluid-induced dissolution/ reprecipitation is the principal cause of Pb mobility. Attempts to model intracrystalline core-rim Pb zonations as diffusive transport are not legitimate unless genuine bell-shaped diffusion profiles in minerals can be documented, which happens only exceptionally. Monazite and zircon intra-grain age maps confirm that coupled dissolution-reprecipitation and retrogression reactions assisted by fluids control (Th+U)-Pb ages, not temperature. The chemical zonations observed in many (Th+U)-bearing mineral chronometers (e.g. monazite, allanite, xenotime, zircon) provide petrological constraints. Linking petrology with textures and the isotope record allows reconstructing entire segments of the P-T-AX -D-t history of a rock and its geodynamic environment. The dearth of mathematically sound diffusion profiles equally applies to the isotope record of micas and feldspars. The tight link between petrology, microtextures, chemical composition and geochronology also pertains to Rb-Sr and K-Ar. Overdetermined multi-mineral Rb-Sr isochrons with excess scatter, and spatially resolved/stepwise release 39 Ar-40 Ar results, demonstrate ubiquitous correspondence between relict phases and isotopic inheritance. Many rock-forming minerals are highly retentive of Sr and Ar, unless they are obliterated by retrograde reactions. The rates of dissolution in fluid-controlled reactions are several orders of magnitude faster at upper and mid-crustal levels than diffusive reequilibration rates. Thus, as a rule Rb-Sr and K-Ar chronometers date their own formation. Accurately establishing P-T paths of monometamorphic rocks requires assessing petrologic equilibrium using multivariate thermodynamic software. Dating complex parageneses of polymetamorphic, unequilibrated rocks requires labor-intensive disentangling by: (i) qualitative identification of relicts, retrogression reactions, and chemically open systems by imaging techniques (e.g. cathodoluminescence, element maps, etc.); (ii) microchemical analyses at the µm-scale quantifying heterochemical disequilibrium phases and assigning them to a P-T-AX segment; (iii) spatially resolved/stepwise release, relating the chemical signature of the analyzed mineral to its age. K-Ar and Rb-Sr usually provide a different perspective on the P-T evolution of a rock than does (Th+U)-Pb, as K+Rb-rich minerals (phyllosilicates and especially feldspars) mostly form later and react/dissolve faster in the retrograde path than U-rich accessory phases (e.g. Mukai et al., 2014). The present paper reviews these general principles by means of well-understood examples, both successful and insuccessful in matching the independently known external constraints.

Kinematics and Timing Constraints in a Transpressive Tectonic Regime: The Example of the Posada-Asinara Shear Zone (NE Sardinia, Italy)

“…To obtain time constraints on the evolution of the studied sector, monazite geochronology was performed [84,85]. Grain locations, internal features (inclusions, fractures, etc.)…”

The Late Paleozoic Tectonometamorphic Evolution of Patagonia Revisited: Insights From the Pressure‐Temperature‐Deformation‐Time (P‐T‐D‐t) Path of the Gondwanide Basement of the North Patagonian Cordillera (Argentina)

“…In this sense, combined in situ petrologic and microstructural data allow to link deformation mechanisms, metamorphic reactions, and macroscopic structural features and to infer the relative timing of different mineral associations and microstructures (Goncalves et al, 2012;Hobbs et al, 2011;Johnson, 1999;Marsh et al, 2009;Oriolo et al, 2018;Skrzypek et al, 2011;Yakymchuk & Godin, 2012). The absolute timing of deformation and metamorphism, in turn, can be constrained by interpreting in situ geochronologic data in the light of microstructures, which provide insights into mineral equilibria, deformation mechanisms, and metamorphic reactions (Bosse & Villa, 2019;Gasser et al, 2015;Mulch & Cosca, 2004;Oriolo, et al, 2016;Oriolo et al, 2018;Schulz, 2017;Tchato et al, 2009;Villa et al, 2014;Williams & Jercinovic, 2012). Furthermore, the integration of structural, microstructural, petrologic, and geochronologic data permits reconstructing the crustal architecture of orogens and contributes on the understanding of their tectonic and geodynamic evolution (e.g., Endo & Wallis, 2017;Goscombe & Gray, 2009;Raimondo et al, 2010).…”

The Age, Origin, and Emplacement of the Tsiknias Ophiolite, Tinos, Greece

“…This contrasts with the Eocene high‐pressure metamorphic rocks in the Lower Unit, dated by 40 Ar‐ 39 Ar on Tinos (Bröker et al, ) and indirectly by correlative rocks on other islands at ~52–45 Ma by U–Pb zircon (Tomaschek et al, ) and Lu–Hf in garnet (Dragovic et al, , ; Lagos et al, ). However, there are inherent problems in determining what part of the rock's complex history is actually being dated with the K–Ar, 40 Ar– 39 Ar, and Rb–Sr methods (e.g., Kelley, ; MacDonald et al, ; Bosse & Villa, ). Here we present new U–Pb zircon dates for the timing of formation and emplacement of the Tsiknias Ophiolite within the Upper Unit.…”