Presentation on theme: "Geochronometry-Isotope tracing-Age of the Earth"— Presentation transcript:
1Geochronometry-Isotope tracing-Age of the Earth Geochronometry (methods)Nuclear synthesisMeteoritesAge of the Earth accretionPbFormation of the coreFormation of the core (energy considerations)Formation of crustPlate tectonics starts
2Geochronometry Radiogenic isotopes Decay mechanisms (α decay, β decay, electron capture)Main isotopic systems for datingRb-SrK-ArU-PbTh-PbOther isotopes used mainly for “tracing” (Sm-Nd, Re-Os, …)
5Geochronometry (hypotheses) Parent -> daughter decay probability λMineral closes at temperature (depends on type: zircons 800 deg, feldspars 350, …)No daughter present at closure (or it can be accounted for)No loss or gain of parent or daughter after mineral closesCounting P/D gives the time that elapsed since the system closed
6Geochronometry (particulars) K->Ar is a branching decay K40 -> Ar 40 or Ca 40U -> Pb two different isotopes of same element give two independent age estimates (must be concordant)Rb/Sr requires different minerals with variable Rb/Sr ratios (same for Sm-Nd). Methods yield initial isotopic ratio of Sr87/Sr86 (important for tracing)
7Same equations and method for other systems (U-Pb, Sm-Nd)
18Xe129 Xe129 product of short half life I129 Meteorites formed shortly after nucleosynthesis.Xe129 in earth atmosphere (I129 in primitive earth) comes from degasing of mantleEarth and meteorites have ~ same age
21Meteorites All meteorites have about the same age 4.55 Ga Some meteorites that have younger ages come from the moon. They were ejected after impact.A few are much younger (1.1 Ga). They are assumed to have been ejected by Mars after a large impact
27Moon samplesNasa has collected samples for dating Ages range between 3.0 and 4.5 Ga (see PDF document)
28Time series of a Moon-forming impact simulation Time series of a Moon-forming impact simulation. Results are shown looking down onto the plane of the impact at times t = 0.3, 0.7, 1.4, 1.9, 3, 3.9, 5, 7.1, 11.6, 17 and 23 hours (from left to right); the last frame is t = 23 hours viewed on-edge. Colour scales with internal energy (shown on the colour bar in units of 6.67 times 108 erg g-1), so that blue and dark green represents condensed matter, and red particles signify either the expanded phase or a hot, high-pressure condensed phase; pressures at intermediate energies are computed by an interpolation between the Tillotson15 condensed and expanded phases. We form initial impactors and targets in hydrostatic equilibrium by pre-colliding smaller bodies together at zero incidence, resulting in realistically evolved internal energies, stratified densities (basalt mantle + iron core) and consistent pressures. Each particle's internal energy is evolved due to the effects of expansion/compression and shock dissipation, with the latter represented by artificial viscosity terms that are linear and quadratic in the velocity divergence of converging particles; effects of mechanical strength and radiative transfer are ignored. The momentum of each particle is evolved due to pressure, viscous dissipation and gravity. Gravity is computed using a binary tree algorithm, reducing the N2 calculation of particle–particle attractions into an NlogN calculation25. We use a beta spine kernel to define the spatial distribution of material represented by each SPH particle. The scale of each particle, h, is automatically adjusted to cause overlap with a minimum of 40 other particles, ensuring a 'smoothed' distribution of material even in low-density regions. The code is explicit, requiring a Courant-limited timestep Deltat < (c/h) where c is the sound speed. For a full description of the technique, see ref. 26, from whose efforts our present algorithm derives.
29Rappel Geochronometry hypotheses Nucleosynthesis (6 to 4.6 Ga) Age of meteorites 4.55 GaMeteorites follow shortly end of nucleosynthesisEarth followed shortly end of nucleosynthesisMoon samples 3.2 to 4.5 GaOldest rock on Earth 4 GaAge of Earth from Pb 4.55 Ga
32Dating core formation Hafnium Hf and Tungsten W Hf182 -> W182 (half life 9 Myears)Hf180 referenceHf stays in mantleW goes in coreInitial ratio Hf182/Hf180 in solar system different from that of mantle
33εw values of carbonaceous chondrites compared with those of the Toluca iron meteorite and terrestrial samples analysed in this study. The values for Toluca, Allende, G1-RF and IGDL-GD are the weighted averages of four or more independent analyses. Also included are data from ref. 16 (indicated by a), ref. 30 (b), and ref. 2 (c). For the definition of εw see Table 1. The vertical shaded bar refers to the uncertainty in the W isotope composition of chondrites. Terrestrial samples include IGDL-GD (greywacke), G1-RF (granite) and BB and BE-N (basalts).
34εw versus 180Hf/184W for different fractions of the H chondrites Ste Marguerite (a) and Forest Vale (b). NM-1, NM-2 and NM-3 refer to different nonmagnetic fractions, M is the magnetic fraction. We interpret the positive correlation of εw with 180Hf/184W as an internal Hf–W isochron whose slope corresponds to the initial 182Hf/180Hf ratio at the time of closure of the Hf–W system.
35Time of core formation in Myr after CAI condensation for Vesta, Mars, Earth and Moon versus planet radius as deduced from Hf–W systematics. For the Moon, the two data points refer to the endmember model ages. The Moon plots distinctly to the left of the correlation line defined by Vesta, Mars and Earth, suggesting a different formation process.
36Timing of core formation Timing of core formation. The Earth formed through accretion, absorbing planetesimals (lumps of rock and ice) through collisions. Did the Earth accrete undifferentiated material that then separated into shell and core — in which case, did the planet reach its present mass before differentiating, or was it a more gradual process? Alternatively, core formation might have happened rapidly inside growing planetesimals, so that the Earth's core is a combination of these previously formed cores. Isotopic evidence supports the latter model, and now Yoshino et al.1 demonstrate a mechanism for the physical process.
37Core formation (conservation laws) Gravitational potential energy decreases when core formsMoment of inertia decreasesAngular velocity of rotation increasesRotational energy increasesIncrease in energy of rotation < Decrease in gravitational potential energyTotal energy must be conservedDifference goes into heatEstimates: Core formation -> K temperature increase
42He It is assumed that volatiles were lost during accretion Very little He in atmosphere (too light, lost to space)He in mantleHe3 is primitive, He4 primitive + decay of radioelementsHe4/He3 ratio (initial ratio same as that of universe)He4/He3 ratio grows with timeSome degasingShows mantle is not well mixed