Mg isotopic heterogeneity,Al‐Mg isochrons,and canonical 26Al/27Al in the early solar system

There is variability in the Mg isotopic composition that is a reflection of the widespread heterogeneity in the isotopic composition of the elements in the solar system at approximately 100 ppm. Measurements on a single calcium‐aluminum‐rich inclusion (CAI) gave a good correlation of ²⁶Mg/²⁴Mg with ²⁷Al/²⁴Mg, yielding an isochron corresponding to an initial (²⁶Al/²⁷Al)_o = (5.27 ± 0.18) × 10^?5 and an initial (²⁶Mg/²⁴Mg)_o = ?0.127 ± 0.032‰ relative to the standard. This isochron is parallel to that obtained by Jacobsen et al. (2008) , but is distinctively offset. This demonstrates that there are different initial Mg isotopic compositions in different samples with the same ²⁶Al/²⁷Al. No inference about uniformity/heterogeneity of ²⁶Al/²⁷Al on a macro scale can be based on the initial (²⁶Mg/²⁴Mg)_o values. Different values of ²⁶Al/²⁷Al for samples representing the same point in time would prove heterogeneity of ²⁶Al/²⁷Al. The important issue is whether the bulk solar inventory of ²⁶Al/²⁷Al was approximately 5 × 10^?5 at some point in the early solar system. We discuss ultra refractory phases of solar type oxygen isotope composition with ²⁶Al/²⁷Al from approximately 5 × 10^?5 to below 0.2 × 10^?5. We argue that the real issues are: intrinsic heterogeneity in the parent cloud; mechanism and timing for the later production of ¹⁶O‐poor material; and the relationship to earlier formed ¹⁶O‐rich material in the disk. ²⁶Al‐free refractories can be produced at a later time by late infall, if there is an adequate heat source, or from original heterogeneities in the placental molecular cloud from which the solar system formed.     

Mars: Chemical weathering as a massive volatile sink

Photostimulated oxidation weathering irreversibly removes both oxygen and hydrogen from the atmosphere at a rate of 10⁸ to 10¹¹ cm^?2sec^?1. This corresponds to a net loss of 10²⁵ to 10²⁸ molecules cm^?2 (10² to 10⁵ g cm^?2 of H₂O, assuming a uniform rate over geologic time. Additional H₂O is removed through hydration of Fe₂O₃ and clay minerals, but the loss is reversible and the extent of regolith storage is uncertain. CO₂ is irreversibly removed from the atmosphere through the formation of CaCO₃ at a rate of 10⁷?10¹⁰cm^?2sec^?1. Over geologic time this corresponds to a net loss of 10²⁴?10²⁷ molecules cm^?2 (10¹?10⁴g cm^?2) of CO₂. Previously, it was proposed that exospheric escape was the principal irreversible volatile sink, amounting to only 10²g cm^?2 of H₂O and 10⁰g cm^?2 of CO₂ over geologic time. A recent tentative identification of abundant argon on Mars suggests that the planet may have degassed up to 10⁵g cm^?2 of H₂O and 10⁴g cm^?2 of CO₂. If the amounts of H₂O and CO₂ removed by photostimulated oxidation are close to the upper limits proposed here, it is possible that chemical weathering may have had a major effect on limiting the supply of H₂O and CO₂ trapped in the regolith and polar caps.     

The production of nitrogen atoms on Mars and their escape

Quantitative calculations of the escape rate of nitrogen by photodissociation and photoionization, by photoelectron impact processes, by chemical reactions and by dissociative recombination are reported. It is shown that the predicted present escape rate of 2.0 × 10⁵ atoms cm^?2 S^?1 is consistent with the measured ¹⁵N/¹⁴N isotope ratio. A minimum of 4.0 × 10²² cm^?2 S^?1 is obtained for the initial reservoir of N₂. The production rates of N(⁴S) and N(²D) atoms in the atmosphere are obtained and the altitude profile of N(²D) is calculated.     

Lightnings and nitric oxide on Venus

In an updating of energy characteristics of lightnings on Venus obtained from Venera-9 and -10 optical observations, the flash energy is given as 8 × 10⁸ J and the mean energy release of lightnings is 1 erg cm^?2 s which is 25 times as high as that on the Earth. Lightnings were observed in the cloud layer. The stroke rate in the near-surface atmosphere is less than 5 s^?1 over the entire planet if the light energy of the stroke exceeds 4 × 10⁵ J and less than 15 s^?1 for (1–4) × 10⁵ J.The average NO production due to lightnings equals 5 × 10⁸ cm^?2 s^?1, the atomic nitrogen production is equal to 7 × 10⁹ cm^?2s^?1,the N flux toward the nightside is 3.2 × 10⁹ cm^?2s^?1, the number densities [N] = 3 × 10⁷cm^?3 and [NO] = 1.8 × 10⁶cm^?3 at 135 km. Almost all NO molecules in the upper atmosphere vanish interacting with N and the resulting NO flux at 90-80 km equals 5 × 10⁵cm^?2s^?1, which is negligibly small as compared with lightning production. If the predissociation at 80–90 km is regarded as the single sink of NO, its mixing ratio, f_NO, is 4 × 10^?8, for the case of a surface sink f_NO = 0.8 × 10^?9 at 50 km. Excess amounts, $\text{f}{}_{\mathrm{<mtext>NO</mtext>}}\text{? 4 × 10}{}^{\mathrm{?8}}$, may exist in the thunderstorm region.     

Radioactive Isotopes in Hoba West and Other Iron Meteorites

Abstract The radioactivities Be¹⁰, Al²6, Cl³⁶, Mn⁵³, Ni⁵⁹, and Co⁶⁰ and the rare gas isotopes were measured in a sample taken from the surface of the Hoba meteorite. The spallation-produced radioactivities indicate that the sample was at a depth of 35 to 40 cm when the body was in space. The Ni⁵⁹ activity indicates that the terrestrial age of Hoba is less than 80,000 years. Its Cl³⁶-Ar³⁶ exposure age is 263±40 million years. The Cl³⁶ and rare-gas isotopes were also measured in the Deelfontein meteorite; its Cl³⁶-Ar³⁶ exposure age is 400±40 million years. The Cl³⁶ and the Ni⁵⁹ were also measured in a sample of Sikhote-Alin. In both Hoba and Sikhote-Alin the Ni⁵⁹, which is a neutron-produced isotope, is higher than would be expected from the Cl³⁶ content. This indicates that solar flares contributed to the neutron-produced isotopes in these iron meteorites.     

Structure and time variations of the Jovian ionosphere

The problem of the ionospheric formation in the Jovian upper atmosphere is examined. By adopting two plausible atmospheric models, we solve coupled time-dependent continuity equations for ions H₂⁺, H₅⁺, H⁺, H₃⁺ and H_eH⁺ simultaneously. It is shown that both radiative and three body association of H⁺ to H₂ are important for the determination of the structure of the Jovian ionosphere. The maximum electron density in the daytime is found to be about 10⁵ cm^?3. It is also shown that diurnal variation with large-amplitude can exist in the Jovian ionosphere.     

Satellites and Riemannian geometry

In an axially symmetric three-dimensional Riemann-spaceg _ik(u ¹,u ²)?u ³ represents the cyclic parameter-, a gravitational potential ?(u ¹,u ²) is given. For all masspoints with equal total energy and equal angular momentum there exists a function Ψ(u ¹,u ²) by means of which the equations of motion can be reduced to a simple ordinary second-order differential equation. The function ? can be interpreted as the velocity with which the masspoint moves in the two-dimensional spaceu ¹,u ². Of particular interest is the case where the spaceu ¹,u ²,u ³ is Euclidean. Ifu ¹,u ² are Cartesian coordinates in a planeu ³=const., and if the tangent vector of the trajectoryu ¹(t)u ²(t) has the components cosω, sinω it is shown that the triple integral $$\smallint \smallint \smallint \psi du^1 du^2 d\omega $$ is an invariant integral in Cartan's sense, in other words, if the integral is extended over a domain in a meridian plane at timet=0, it keeps its value at any time.     

The atmosphere of Io from Pioneer 10 radio occultation measurements

The occultation of the Pioneer 10 spacecraft by Io (JI) provided an opportunity to obtain two S-band radio occultation measurements of its atmosphere. The dayside entry measurements revealed an ionosphere having a peak density of about 6 × 10⁴ elcm^?3 at an altitude of about 100 km. The topside scale height indicates a plasma temperature of about 406 K if it is composed of Na⁺ and 495 K if N₂⁺ is principal ion. A thinner and less dense ionosphere was observed on the exit (night side), having a peak density of 9 × 10³ elcm^?3 at an altitude of 50 km. The topside plasma temperature is 160 K for N₂^? and 131 K for Na⁺. If the ionosphere is produced by photoionization in a manner analogous to the ionospheres of the terrestrial planets, the density of neutral particles at the surface of Io is less than 10¹¹?10¹² cm³, corresponding to a surface pressure of less than 10^?8 to 10^?9 bars. Two measurements of its radius were also obtained yielding a value of 1830 km for the entry and 192 km for the exit. The discrepancy between these values may indicate an ephemeris uncertainty of about 45 km. The two measurements yield an average radius of 1875 km, which is not in agreement with the results of the Beta Scorpii stellar occultation.     

The energy flux number and three types of planetary dynamo

It is proposed that the existence and nature of a planetary dynamo can be characterized by a dimensionless number Φ ≡ F_eR/ϱλ²ω, called the energy flux number, where F_e is the energy flux available for dynamo generation, R is the core radius (or thickness of the dynamo generating region), ϱ is the fluid density, λ is the magnetic diffusivity and ω is the angular velocity. For Φ ≲ 1, there is no dynamo. For 1 ≲ Φ ≲ 10^2.5 there is an “energy-limited dynamo”, in which F_e is insufficient to enable the dynamo to reach the dynamically desirable state A ≡ B²/8πϱλω ∼ 1, where B is a typical field amplitude (in Gauss). For 10^2.5 ≲ Φ ≲ 10⁵, there is a dynamically determined dynamo (Λ ∼ 1) in which the magnetic Reynolds number of turbulent eddies is small. For Φ ≳ 10⁵, there is a turbulent dynamo. Probable planetary examples of these three dynamo states are Mercury (Φ ∼ 10²-10³), Earth (Φ ∼ 10⁴) and Jupiter (Φ ∼ 10¹¹), respectively.     

Mars’ atmospheric 40Ar: A tracer for past crustal erosion

Noble gas ⁴⁰Ar may be used as a tracer of the past evolution of volatiles in Mars’ crust, mantle and atmosphere. ⁴⁰Ar is formed by the radioactive decay of ⁴⁰K in the mantle and in the crust and is released from the mantle to the atmosphere due to volcanism and from the crust by erosion such as eolian and hydrothermal erosion. Furthermore, ⁴⁰Ar can escape from the atmosphere into space via atmospheric escape mechanisms. The evolution of the atmospheric abundance of ⁴⁰Ar thus depends on these three processes whose efficiencies vary with time.In the present study we reconsider atmospheric escape mechanism efficiencies and describe various possible scenarios of the evolution of ⁴⁰Ar with a model describing the three main reservoirs of ⁴⁰Ar, the mantle, crust and atmosphere. First, we show that atmospheric escape, which is stronger in the early evolution, does not significantly influence the present abundance of the atmospheric ⁴⁰Ar. In the early evolution the atmospheric concentration of ⁴⁰Ar is very low as the outgassing of ⁴⁰Ar from the mantle occurs relatively late in the martian evolution. Thus, the atmospheric ⁴⁰Ar concentration is essentially a tracer of Mars’ outgassing history and not of the escape processes. Second, using the results of the most recent published crustal formation models, the calculated present ⁴⁰Ar atmospheric abundance is smaller than its observed value. This discrepancy may be explained by a significant ⁴⁰Ar supply from the crust by erosion (16–30% of the ⁴⁰Ar content of the upper first 10 km of crust). The knowledge of the fraction of crustal ⁴⁰Ar outgassed to the atmosphere is an important constraint for any future global modelling of past Mars’ hydrothermal activity aiming at better characterizing the role of subsurface aqueous alteration processes in Mars climate evolution. One of the main sources of the uncertainty of these results is the present uncertainty in the measured atmospheric ⁴⁰Ar value (±20%). More precise measurements of ⁴⁰Ar and ³⁶Ar in the martian atmosphere are therefore required to better constrain the model.     

The influence of convection electric fields on thermal proton outflow from the ionosphere

The continuity, momentum and energy hydrodynamic equations for an O⁺-H⁺ ionosphere have been solved self-consistently for steady state conditions when a perpendicular (convection) electric field is present. Comparison of the H⁺ temperature profiles obtained with and without the electric field show that the effect of the electric field is to enhance the H⁺ temperature at high altitudes from about 3600 to 6400 K. Due to ion heating by the electric field, there is a net reduction of O⁺ in the F2-region as compared with the case of a non-convecting ionosphere. When the reduction of O⁺ is neglected, the electric field acts to increase the H⁺ outward flux from 8.3 × 10⁷ to 2.7 × 10⁸ cm^?2 sec^?1 for average ionospheric conditions. However, when the reduction of O⁺ is included, there is a net reduction in the outward H⁺ flux. Nevertheless, the convection electric field still results in an increase in the rate of depletion of the F-re m^?1 electric field.     

A Study on the CO Isotopic Lines of the Star Forming Region AFGL 5157

By the mapping observations simultaneously at the ¹²CO (J=1-0), ¹³CO (J=1-0), and C¹⁸O (J=1-0) lines on the area of 24’×24’ (12 pc×12 pc) of the star forming region AFGL 5157, we have obtained the distribution and averaged physical parameters for the respective ¹³CO and C¹⁸O cores of this molecu- lar cloud. At the edge of the molecular cloud, the isotopic abundance ratio is X [(¹³CO)/(C¹⁸O)] ≈ 10, close to the ratio of a giant molecular cloud. The viral masses of the ¹³CO and C¹⁸O cores are less than the masses of the molecu-lar cloud cores, so the molecular cloud cores are gravitationally unstable, and the C¹⁸O molecular cloud core is more easy to collapse. The column density distributions of the C¹⁸O molecular cloud core in the northeast and southwest directions are, respectively, 1.1 × 10²³× z^−0.43 and 4.6 × 10²⁵× z^−0.58, where z is the distance from the center of the molecular cloud core. The high velocity molecular out?ow has been con?rmed from our ¹²CO spectra, the mass loss rate of the out?ow has been estimated, and the mass-velocity relation of the out?ow is ?tted by a power-law function of m ∝ v^−1.8. The star formation rate of the ¹³CO molecular cloud core is as high as 23%, probably, under the in?uence of     

Nucleosynthesis in neutron star atmospheres

The composition of neutron star atmospheres is calculated as a function of time including effects of diffusion, cooling and thermonuclear reactions. A seven-component nuclear reaction network with includes He⁴, C¹², O¹⁶, Ne²⁰, Mg²⁴, Si²⁸ and Fe⁵⁶ is utilized. Neutron star models with different initial nuclear abundances are compared as to subsequent nucleosynthesis. It is found that the final abundances are independent of original composition assuming He⁴ as the major initial constituent. The final composition of the atmosphere is predominantly Fe⁵⁶. Mass loss from an evolving neutron star is examined as a possible source of cosmic rays. It is found that a neutron star contributes only Fe⁵⁶ significantly to the cosmic-ray spectrum.     

Quantitative estimation of helium-3 spatial distribution in the lunar regolith layer

³He (helium-3) in the lunar regolith implanted by the solar wind is one of the most valuable resources because of its potential as a fusion fuel. The abundance of ³He in the lunar regolith is related to solar wind flux, lunar surface maturity and TiO₂ content, etc. A model of solar wind flux, which takes account of variations due to shielding of the nearside when the Moon is in the Earth's magnetotail, is used to present a global distribution of relative solar wind flux over the lunar surface. Using Clementine UV/VIS multispectral data, the global distribution of lunar surface optical maturity (OMAT) and the TiO₂ content in the lunar regolith are calculated. Based on Apollo regolith samples, a linear relation between ³He abundance and normalized solar wind flux, optical maturity, and TiO₂ content is presented. To simulate the brightness temperature of the lunar surface, which is the mission of the Chinese Chang-E project's multichannel radiometers, a global distribution of regolith layer thickness is first empirically constructed from lunar digital elevation mapping (DEM). Then an inversion approach is presented to retrieve the global regolith layer thickness. It finally yields the total amount of ³He per unit area in the lunar regolith layer, which is related to the regolith layer thickness, solar wind flux, optical maturity and TiO₂ content, etc. The global inventory of ³He is estimated as 6.50×¹⁰⁸ kg, where 3.72×¹⁰⁸ kg is for the lunar nearside and 2.78×¹⁰⁸ kg is for the lunar farside.     

Calibration of cosmogenic noble gas production based on 36Cl‐36Ar ages. Part 2. The 81Kr‐Kr dating technique

We calibrated the ⁸¹Kr‐Kr dating system for ordinary chondrites of different sizes using independent shielding‐corrected ³⁶Cl‐³⁶Ar ages. Krypton concentrations and isotopic compositions were measured in bulk samples from 14 ordinary chondrites of high petrologic type and the cosmogenic Kr component was obtained by subtracting trapped Kr from phase Q. The thus‐determined average cosmogenic ⁷⁸Kr/⁸³Kr, ⁸⁰Kr/⁸³Kr, ⁸²Kr/⁸³Kr, and ⁸⁴Kr/⁸³Kr ratiC(Lavielle and Marti 1988; Wieler 2002). The cosmogenic ⁷⁸Kr/⁸³Kr ratio is correlated with the cosmogenic ²²Ne/²¹Ne ratio, confirming that ⁷⁸Kr/⁸³Kr is a reliable shielding indicator. Previously, ⁸¹Kr‐Kr ages have been determined by assuming the cosmogenic production rate of ⁸¹Kr, P(⁸¹Kr)_c, to be 0.95 times the average of the cosmogenic production rates of ⁸⁰Kr and ⁸²Kr; the factor Y = 0.95 therefore accounts for the unequal production of the various Kr isotopes (Marti 1967a). However, Y should be regarded as an empirical adjustment. For samples whose ⁸⁰Kr and ⁸²Kr concentrations may be affected by neutron‐capture reactions, the shielding‐dependent cosmogenic (⁷⁸Kr/⁸³Kr)_c ratio has been used instead to calculate P(⁸¹Kr)/P(⁸³Kr), as for some lunar samples, this ratio has been shown to linearly increase with (⁷⁸Kr/⁸³Kr)_c (Marti and Lugmair 1971). However, the ⁸¹Kr‐Kr ages of our samples calculated with these methods are on average ~30% higher than their ³⁶Cl‐³⁶Ar ages, indicating that most if not all the ⁸¹Kr‐Kr ages determined so far are significantly too high. We therefore re‐evaluated both methods to determine P(⁸¹Kr)_c/P(⁸³Kr)_c. Our new Y value of 0.70 ± 0.04 is more than 25% lower than the value of 0.95 used so far. Furthermore, together with literature data, our data indicate that for chondrites, P(⁸¹Kr)_c/P(⁸³Kr)_c is rather constant at 0.43 ± 0.02, at least for the shielding range covered by our samples ([⁷⁸Kr/⁸³Kr]_c = 0.119–0.185; [²²Ne/²¹Ne]_c = 1.083–1.144), in contrast to the observations on lunar samples. As expected considering the method used, ⁸¹Kr‐Kr ages calculated either directly with this new P(⁸¹Kr)_c/P(⁸³Kr)_c value or with our new Y value both agree with the corresponding ³⁶Cl‐³⁶Ar ages. However, the average deviation of 2% indicates the accuracy of both new ⁸¹Kr‐Kr dating methods and the precision of the new dating systems of ~10% is demonstrated by the low scatter in the data. Consequently, this study indicates that the ⁸¹Kr‐Kr ages published so far are up to 30% too high.     

A PROCESS OF STELLAR NUCLEOSYNTHESIS WHICH MIMICKS MASS FRACTIONATION IN P-XENON

The combination of the O-shell theory of Heymann and Dziczkaniec and the supernova theory of Woosley and Howard clearly identifies the astrophysical sites for the formation of the anomalous light Xe component in carbonaceous chondrites. These sites are the O- and Ne-shells, and possibly C-shell of a massive star. Most of the ¹²⁴Xe and ¹²⁶Xe are formed in the O-shell during hydrostatic core silicon-burning, when a seed of heavy nuclei is exposed to an effective temperature near T₉ = 2.0. ¹²⁸Xe is formed via ¹²⁸Ba in the O-shell, but the amounts appear too small to satisfy the deduced ¹²⁸Xe/¹²⁴Xe and ¹²⁸Xe/¹²⁶Xe yield ratios from the chondrites. However, substantial amounts of ¹²⁸Xe can be formed in the adjacent Ne- and C-shells during the explosion. The formation of ¹²⁸Ba in the O-shell would increase if the (γ, α) photodisintegration rate in ¹²⁸Ba is actually smaller than calculated by Woosley and Howard. Lewis et al. have proposed that the anomalous light Xe component is mass-fractionated normal Xe. It is in this sense that the process of stellar nucleosynthesis of the present paper mimicks mass-fractionation.     

COSMOGENIC RADIONUCLIDES AND NOBLE GASES IN THE WETHERSFIELD (1982) CHONDRITE

The Wethersfield (1982) chondrite was assayed for a suite of cosmogenic radionuclides shortly after fall. Data are reported for ⁷Be, ²²Na, ²⁶Al, ⁴⁶Sc, ⁴⁸V, ⁵¹Cr, ⁵⁴Mn, ⁵⁶Co, ⁵⁷Co, and ⁶⁰Co. A comparison is made with predicted results based on a scaling to the Deep River Neutron Monitor. Noble gases were also assayed in a sub-sample. The cosmic ray exposure age is estimated to be 45 million years.     

Measurements of positive ion conversion and removal reactions relating to the Jovian ionosphere

Measured rates are presented for the reaction of He⁺ ions with H₂ (and D₂) molecules to form H⁺, H₂⁺, and HeH⁺ ions, as well as for the subsequent reactions of H⁺ and HeH⁺ ions with H₂ to form H₃⁺. The neutralization of H₃⁺ (and H₅⁺) ions by dissociative recombination with electrons is shown to be fast. The reaction He⁺ + H₂ is slow (k = 1.1 × 10^?13 cm³/sec at300°K) and produces principally H⁺ by the dissociative charge transfer branch. It is concluded that there may be a serious bottleneck in the conversion of two of the primary ions of the upper Jovian ionosphere, H⁺ and He⁺ (which recombine slowly), to the rapidly recombining H₃⁺ ion (α[H₃⁺]?3.4 × 10^?7 cm³/sec at 150°K).     

Relative flow of H+ and O+ ions in the topside ionosphere at mid-latitudes

Theoretical results on the daily variation of O⁺ and H⁺ field-aligned velocities in the topside ionosphere are presented. The results are for an L = 3 magnetic field tube under sunspot minimum conditions at equinox. They come from calculations of time-dependent O⁺ and H⁺ continuity and momentum balance in a magnetic field tube which extends from the lower F2 region to the equatorial plane (Murphy et al., 1976).There are occasions when ion counterstreaming occurs, with the O⁺ velocity upward and H⁺ velocity downward. The conditions causing this counterstreaming are described: the H⁺ layer is descending whilst O⁺ is supplied from below either to increase the O⁺ concentration at fixed heights or to replace O⁺ ions lost by charge exchange with neutral H. It is suggested that the results of observations at Arecibo by Vickrey et al. (1976) of O⁺ and H⁺ concentrations and counterstreaming velocities are significantly affected by $\text{E}\text{×}\text{B}$ drift.     

Solar abundances of light nuclei and mixing of the Sun

Radial profiles of the light nuclei (A 15) are calculated in the non-mixing Sun, taking into account the changes of solar structure with time. The results are discussed in relation to models of solar mixing and compared with abundance determinations at the solar surface or in the solar wind. B cannot be depleted in the outer convective zone without producing a large increase in the He³/He⁴ ratio. A decrease in He³/He⁴ would be accompanied by changes in C¹³/C¹² and N¹⁵/N¹⁴ of a magnitude which is not observed.It is shown that boron could be depleted in the pre-main sequence period of the Sun, if mixing was on a time-scale of 10⁶ yr. The simultaneous small increase in He³/He⁴ does not contradict observation. However, Be would be depleted more strongly than B.A He³/He⁴ decrease is always accompanied by large changes in N¹⁵/N¹⁴ and C¹³/C¹². Since such changes are not observed, it is concluded that the He³/He⁴ ratio in the outer convective zone is a reliable upper limit for (He³ + D)/He⁴ in the solar nebula. Thus the D/H ratio in the protosolar material was much lower than it is in sea water or in carbonaceous chondrites.