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1.

The

^{40}Ar/^{39}Ar dating technique requires the use of neutron fluence monitors (standards). Precise calibrations of these standards are crucial to decrease the uncertainties associated with^{40}Ar/^{39}Ar dates. Optimal calibration of^{40}Ar/^{39}Ar standards should be based on K/Ar standards having independent isotope dilution measurements of^{40}K and^{40}Ar*, based on independent isotope tracers (spikes) because this offers the possibility to eliminate random interlaboratory errors. In this study, we calibrate the widely used Fish Canyon sanidine (FCs) standard based on four primary K/Ar standards (GA-1550, Hb3gr, NL-25, and GHC-305) on which K and Ar* concentrations have been determined in different labs with independently calibrated tracers. We obtained a mean age of 28.03 ± 0.08 Ma (1*σ*; neglecting uncertainties of the^{40}K decay constants) for FCs, based on the decay constant recommended by Steiger and Jäger [Steiger R.H., Jäger. E. 1977. Subcommission on geochronology: convention of the use of decay constants in geo- and cosmochronology.*Earth Planet. Sci. Lett.***36**, 359-362.]. This age corresponds to a mean^{40}Ar*/^{40}K value of (1.6407 ± 0.0047) × 10^{−3}. We also discuss several criteria that prevent the use of previous calibrations of FCs based on other primary standards (LP-6, SB-3 and MMhb-1). The age of FCs obtained in this study is based on the^{40}K decay constants of Steiger and Jäger (1977) but we anticipate the imminent need for revision of the value and precision of the^{40}K decay constants (representing the main source of uncertainties in^{40}Ar/^{39}Ar dating). The^{40}Ar*/^{40}K result of FCs obtained in this study allows therefore a rapid calibration of the age of FCs with uncertainties at the 0.29% level but perhaps more importantly this value is independent of any particular value of the^{40}K decay constants and may be used in the future in conjunction with revised decay constants. 相似文献2.

William S. Cassata Paul R. Renne David L. Shuster 《Geochimica et cosmochimica acta》2009,73(21):6600-416

Plagioclase is not only the most abundant mineral in the Earth’s crust, but is present in almost all terrestrial tectonic settings and is widespread in most extraterrestrial material. Applying the K-Ar system to this common mineral would provide a powerful tool for quantifying thermal histories in a wide variety of settings. Nonetheless, plagioclase has rarely been used for thermochronometry, largely due to difficulties in simultaneously acquiring precise geochronologic data and quantifying argon diffusion kinetics from a mineral with low-K concentration. Here we describe an analytical technique that generates high-precision

^{40}Ar/^{39}Ar data and quantifies Ar diffusion kinetics of low-K minerals. We present results of five diffusion experiments conducted on single crystals of plagioclase from the Bushveld Complex, South Africa. The observed diffusion kinetics yield internally consistent thermochronological constraints, indicating that plagioclase is a reliable thermochronometer. Individual grains have activation energies of 155-178 kJ/mol and ln(*D*_{0}/*a*^{2}) varies between 3.5 and 6.5. These diffusion parameters correspond to closure temperatures of 225-300 °C, for a 10 °C/Ma cooling rate. Age spectra generally conform to single-domain diffusive loss profiles, suggesting that grain-scale diffusion dominates argon transport in this fairly simple plagioclase. Conjointly examining several single-grain analyses enables us to distinguish episodic reheating from slow cooling and indicates that the Bushveld Complex cooled rapidly and monotonically from magmatic temperature to <300 °C over 3 Ma, followed by protracted cooling to ambient crustal temperatures of 150-200 °C over ∼600 Ma. 相似文献3.

New

^{40}Ar/^{39}Ar thermochronology results and thermal modeling support the hypothesis of Hollister et al. (2004), that reheating of the mid-Cretaceous Ecstall pluton by intrusion of the Coast Mountains Batholith (CMB) was responsible for spatially variable remagnetization of the Ecstall pluton.^{40}Ar/^{39}Ar ages from hornblende and biotite from 12 locations along the Skeena River across the northern part of the Ecstall pluton decrease with proximity to the Quottoon plutonic complex, the nearest member of the CMB to the Ecstall pluton. The oldest^{40}Ar/^{39}Ar ages are found farthest from the Quottoon plutonic complex, and are 90 ± 3 Ma for hornblende, and 77.9 ± 1.2 Ma for biotite. The youngest^{40}Ar/^{39}Ar ages are found closest to the Quottoon plutonic complex, and are 51.6 ± 1.2 Ma for hornblende, and 45.3 ± 1.7 Ma for biotite. No obvious relationship between grain size and age is seen in the Ecstall pluton biotites. Spatial trends in^{40}Ar/^{39}Ar ages are consistent with model results for reheating by a thermal wall at the location of the Quottoon plutonic complex. Although no unique solution is suggested, our results indicate that the most appropriate thermal history for the Ecstall pluton includes both reheating and northeast side up tilting of the Ecstall pluton associated with intrusion of the Quottoon plutonic complex. Estimates of northward translation from shallow paleomagnetic inclinations in the western part of the Ecstall pluton are reduced to ∼3000 km, consistent with the Baja-BC hypothesis, when northeast side up tilting is accounted for. 相似文献4.

^{40}Ar/

^{39}Ar and K-Ar geochronology have long suffered from large systematic errors arising from imprecise K and Ar isotopic data for standards and imprecisely determined decay constants for the branched decay of

^{40}K by electron capture and β

^{−}emission. This study presents a statistical optimization approach allowing constraints from

^{40}K activity data, K-Ar isotopic data, and pairs of

^{238}U-

^{206}Pb and

^{40}Ar/

^{39}Ar data for rigorously selected rocks to be used as inputs for estimating the partial decay constants (

*λ*and

_{ε}*λ*) of

_{β}^{40}K and the

^{40}Ar∗/

^{40}K ratio (

*κ*

_{FCs}) of the widely used Fish Canyon sanidine (FCs) standard. This yields values of

*κ*

_{FCs}= (1.6418 ± 0.0045) × 10

^{−3},

*λ*= (0.5755 ± 0.0016) × 10

_{ε}^{−10}a

^{−1}and

*λ*= (4.9737 ± 0.0093) × 10

_{β}^{−10}a

^{−1}. These results improve uncertainties in the decay constants by a factor of >4 relative to values derived from activity data alone. Uncertainties in these variables determined by our approach are moderately to highly correlated (cov(

*κ*

_{FCs},

*λ*) = 7.1889 × 10

_{ε}^{−19}, cov(

*κ*

_{FCs},

*λ*) = −7.1390 × 10

_{β}^{−19}, cov(

*λ*,

_{ε}*λ*) = −3.4497 × 10

_{β}^{−26}) and one must take account of the covariances in error propagation by either linear or Monte Carlo methods.

^{40}Ar/

^{39}Ar age errors estimated from these results are significantly reduced relative to previous calibrations. Also, age errors are smaller for a comparable level of isotopic measurement precision than those produced by the

^{238}U/

^{206}Pb system, because the

^{40}Ar/

^{39}Ar system is now jointly calibrated by both the

^{40}K and

^{238}U decay constants, and because

*λ*(

_{ε}^{40}K) <

*λ*(

^{238}U). Based on this new calibration, the age of the widely used Fish Canyon sanidine standard is 28.305 ± 0.036 Ma. The increased accuracy of

^{40}Ar/

^{39}Ar ages is now adequate to provide meaningful validation of high-precision U/Pb or astronomical tuning ages in cases where closed system behavior of K and Ar can be established. 相似文献

5.

Thermochronometry based on radiogenic noble gases is critically dependent upon accurate knowledge of the kinetics of diffusion. With few exceptions, complex natural crystals are represented by ideal geometries such as infinite sheets, infinite cylinders, or spheres, and diffusivity is assumed to be isotropic. However, the physical boundaries of crystals generally do not conform to ideal geometries and diffusion within some crystals is known to be anisotropic. Our failure to incorporate such complexities into diffusive models leads to inaccuracies in both thermal histories and diffusion parameters calculated from fractional release data. To address these shortcomings we developed a code based on the lattice Boltzmann (LB) method to model diffusion from complex 3D geometries having isotropic, temperature-independent anisotropic, and temperature-dependent anisotropic diffusivity. In this paper we outline the theoretical basis for the LB code and highlight several advantages of this model relative to more traditional finite difference approaches. The LB code, along with existing analytical solutions for diffusion from simple geometries, is used to investigate the affect of intrinsic crystallographic features (e.g., crystal topology and diffusion anisotropy) on calculated diffusion parameters and a novel method for approximating thermal histories from crystals with complex topologies and diffusive anisotropy is presented. 相似文献

6.

7.

The New CLOCIT Irradiation Facility for 40Ar/39Ar Geochronology: Characterisation,Comparison with CLICIT and Implications for High‐Precision Geochronology

*下载免费PDF全文* Daniel Rutte Tim A. Becker Alan L. Deino Steven R. Reese Paul R. Renne Robert A. Schickler 《Geostandards and Geoanalytical Research》2018,42(3):301-307

The Cadmium‐Lined Outer‐Core Irradiation Tube (CLOCIT) is a new irradiation facility for

^{40}Ar/^{39}Ar geochronology at the Oregon State University TRIGA^{®}reactor. We report fluence (i.e., time‐integrated flux) parameters from the first four CLOCIT irradiations and compare them with the existing Cadmium‐Lined Inner‐Core Irradiation Tube (CLICIT). CLOCIT provides an average neutron flux equivalent of 1.45–1.53 × 10^{?4}*J*h^{?1}; about 55% of CLICIT. Radial fluence gradients were on the order of 0.2–4.2% cm^{?1}. A planar fit of*J*‐values results in residuals in the range of uncertainty in the*J*‐value, but systematic deviations resolve a non‐planar component of the neutron flux field, which has also been observed in CLICIT. Axial neutron fluence gradients were 0.6–1% cm^{?1}, compared with 0.7–1.6% cm^{?1}for the CLICIT. Production rate ratios of interfering reactions were (^{40}Ar/^{39}Ar)_{K}= (4 ± 6) × 10^{?4}and (^{38}Ar/^{39}Ar)_{K}= (1.208 ± 0.002) × 10^{?2}, (^{36}Ar/^{37}Ar)_{Ca}= (2.649 ± 0.014) × 10^{?4}, (^{38}Ar/^{37}Ar)_{Ca}= (3.33 ± 0.12) × 10^{?5}and (^{39}Ar/^{37}Ar)_{Ca}= (9.1 ± 0.28) × 10^{?4}, similar to the CLICIT values. 相似文献8.

Jonathan Levine Paul R. Renne Richard A. Muller 《Geochimica et cosmochimica acta》2007,71(6):1624-1635

We have studied lunar impact spherules from the Apollo 12 and Apollo 14 landing sites, examining the isotopic composition of argon released by stepwise heating. Elsewhere, we reported the formation ages of these spherules, determined by the

^{40}Ar/^{39}Ar isochron method. Here, we discuss solar and cosmogenic argon from the same spherules, separating these two components by correlating their partial releases with the releases of calcium-derived^{37}Ar on a “cosmochron” diagram. We use the abundances of cosmogenic argon to derive a cosmic ray exposure age for each spherule, and demonstrate that single scoops of lunar soil contain spherules which have experienced very different histories of exposure and burial. The solar argon is seen to be separated into isotopically lighter and heavier fractions, which presumably were implanted to different depths in the spherules. The abundance of the isotopically heavy solar argon is too great to explain as a minor constituent of the solar particle flux, such as the suprathermal tail of the solar wind. The fact that the spherules have been individually dated allows us to look for possible variations in the solar wind as a function of time, over the history of the Solar System. However, the isotopic composition and fluence of solar argon preserved in the lunar spherules appear to be independent of formation age. We believe that most of the spherules are saturated with solar argon, having reached a condition in which implantation by the solar wind is offset by losses from solar-wind sputtering and diffusion. 相似文献9.

Fred Jourdan<sup> Jennifer P. Matzel Paul R. Renne 《Geochimica et cosmochimica acta》2007,71(11):2791-2808

The

^{40}Ar/^{39}Ar dating technique requires the activation of^{39}Ar via neutron irradiation. The energy produced by the reaction is transferred to the daughter atom as kinetic energy and triggers its displacement, known as the recoil effect. Significant amounts of^{39}Ar and^{37}Ar can be lost from minerals leading to spurious ages and biased age spectra. Through two experiments, we present direct measurement of the recoil-induced^{39}Ar and^{37}Ar losses on Fish Canyon sanidine and plagioclase. We use multi-grain populations with discrete sizes ranging from 210 to <5 μm. One population consists of a mixture between sanidine and plagioclase, and the other includes pure sanidine.We show that^{39}Ar loss (depletion factor) for sanidine is ∼3% for the smallest fraction. Age spectra of fractions smaller than ∼50 μm show slight departure from flat plateau-age spectrum usually observed for large sanidine. This departure is roughly proportional to the size of the grain but does not show typical^{39}Ar loss age spectra. The calculated thickness of the total depletion layer*d*_{0}(sanidine) is 0.035 ± 0.012 (2*σ*). This is equivalent to a mean depth of the partial depletion layer (*x*_{0}) of 0.070 ± 0.024 μm. The latter value is indistinguishable from previous values of ∼0.07-0.09 μm obtained by argon implantation experiments and simulation results.We show that it is possible to adequately correct ages from^{39}Ar ejection loss provided that the*d*_{0}-value and the size range of the minerals are sufficiently constrained. As exemplified by similar calculations performed on results obtained in a similar study of GA1550 biotite [Paine J. H., Nomade S., and Renne P. R. (2006) Quantification of^{39}Ar recoil ejection from GA1550 biotite during neutron irradiation as a function of grain dimensions.*Geochim. Cosmochim. Acta***70**, 1507-1517.], the*d*_{0}(biotite) is 0.46 ± 0.06 μm. The significant difference between empirical results on biotite and sanidine, along with different simulation results, suggests that for biotite, crystal structures and lattice defects of the stopping medium and possibly subsequent thermal degassing (due to ∼150-200 °C temperature in the reactor or extraction line bake out) must play an important role in^{39}Ar loss.The second experiment suggests that^{37}Ar recoil can substantially affect the age via the interference corrections with results that suggest up to ∼98% of^{37}Ar can be ejected from the ∼5 μm grain dimension.Further investigation of silicates of various compositions and structures are required to better understand (and correct) the recoil and recoil-induced effects on both^{39}Ar and^{37}Ar and their influences on^{40}Ar/^{39}Ar dating. 相似文献10.

In order to better constrain the thermochronological evolution of the IAB parent body we performed a

^{40}Ar/^{39}Ar age study on individual silicate inclusions of the IAB irons Caddo County, Campo del Cielo, Landes, and Ocotillo. In contrast to earlier studies, several plagioclase separates of different grain sizes and quality grades were extracted from each inclusion to reduce the complexity of the age spectra and study the influence of these parameters on the Ar-Ar ages. In nearly all inclusions we found significantly different Ar-Ar ages among the separates (Caddo County: 4.472 ± 0.02-4.562 ± 0.02 Ga; Campo del Cielo 2: 4.362 ± 0.04-4.442 ± 0.03 Ga; Landes 2: 4.412 ± 0.05-4.522 ± 0.04 Ga; Ocotillo: 4.382 ± 0.04-4.462 ± 0.03 Ga). These ages were calculated using the new^{40}K decay constant published by [Mundil R., Renne P. R., Min K. and Ludwig K. R. (2006) Resolvable miscalibration of the^{40}Ar/^{39}Ar geochronometer.*Eos Trans.*AGU 87, Fall Meet. Suppl., Abstract V21A-0543]. The ages did not systematically correlate with the respective grain size of the separate as expected, i.e., smaller grains did not necessarily show younger ages due to later closure to Ar diffusion or easier re-opening of the system in the course of a reheating event compared to larger grains. Based on the large range of Ar-Ar ages we suggest that the individual inclusions are composed of silicate grains from different locations within the IAB parent body. While some grains remained in a hot (deep) environment that allowed Ar diffusion over an extended time period—in some cases combined with grain coarsening—, others cooled significantly earlier (near surface) through the K/Ar blocking temperature. These different grains where brought together during an impact followed by mixing and reassembly of the debris as proposed by Benedix et al. [Benedix G. K., McCoy T. J., Keil K. and Love S. G. (2000) A petrologic study of the IAB iron meteorites: constraints on the formation of the IAB-Winonaite parent body.*Meteorit. Planet. Sci.***35**, 1127-1141]. Due to rapid cooling after the impact some of the age differences among the grains could be preserved. Based mainly on our Caddo County Ar-Ar age information, the IAB parent body was destroyed by impact and reassembled between ∼4.5 and 4.47 Ga. However, IAB silicate Ar-Ar ages should depend much more on the pre- and post-impact cooling rate and burial depth than on the time of the actual impact. This is supported by a compilation of our and literature IAB and winonaite Ar-Ar ages ranging smoothly from the time of accretion of the chondritic IAB parent body down to the time of its final cooling through the K-Ar blocking temperature after impact and reassembly, instead of showing a peak in Ar-Ar ages at the time of the destructive impact. 相似文献