The isotopic analysis of moderately volatile elements such as K have gained significant interest in recent years as they possess the potential to help us better understand solar system formation. Even so, the precise K isotopic composition of CI chondrites, the most chemically primitive chondrite, has remained elusive. As the K elemental composition of CI chondrites matches well with the solar photosphere, it is possible that their K isotopic composition represents the solar system initial value. Here, we investigate the CI chondrite K isotopic composition in order to determine the precise CI chondrite, and thus possibly solar system initial, & delta;41K value. In addition, we investigate the K isotope compositions of several other chondrite groups, evaluate all available chondrite K isotope data together, and use these data along with data from a range of other isotope systems to assess if nucleosynthetic variations, volatility related processes, or parent body processes can best explain the range of isotope variations. The & delta;41K composition of all nine CI chondrite pieces analyzed in this study show limited variation, ranging from -0.29%o to -0.17%o. When combined with the previous CI analysis, an overall mean CI & delta;41K value of -0.21 & PLUSMN; 0.05%o (2SE) is obtained. This K isotope composition is distinct from the Bulk Silicate Earth value of -0.43 & PLUSMN; 0.17%o (2SD), heavier than almost all other chondrite groups, and may represent the solar system initial K isotope composition. When comparing all chondrites broadly, ordinary chondrites show the lightest mean K isotope composition of -0.76 & PLUSMN; 0.06%o (H = -0.71 & PLUSMN; 0.12%o, L = -0.77 & PLUSMN; 0.04%o, LL = -0.81 & PLUSMN; 0.12%o), enstatite chondrites the middle composition of -0.39 & PLUSMN; 0.11%o (EH = -0.34 & PLUSMN; 0.05%o, EL = -0.45 & PLUSMN; 0.20%o), and carbonaceous chondrites the heaviest composition of -0.31 & PLUSMN; 0.08%o. For the carbonaceous chondrite groups CK (-0.42 & PLUSMN; 0.11%o), CR (-0.46 & PLUSMN; 0.05%o), and CV (-0.38 & PLUSMN; 0.07%o) chondrites show lighter & delta;41K compositions compared to CO (-0.20 & PLUSMN; 0.10%o), CM (-0.23 & PLUSMN; 0.11%o), and CI (-0.21 & PLUSMN; 0.05%o) chondrites. When these K isotope group averages are compared against the averages for other mass-dependent moderately volatile element isotope systems (& delta;87Rb, & delta;66Zn, & delta;71Ga, & delta;128Te) and mass-independent isotope systems (& epsilon;54Cr, & epsilon;64Ni, & epsilon;50Ti, & UDelta;17O, & epsilon;40K, and & epsilon;66Zn,), a range of correlations are observed. Across all chondrite groups & delta;41K shows correlations with & delta;87Rb, & delta;66Zn, and & delta;71Ga, and correlations with & epsilon;54Cr, & epsilon;64Ni, & epsilon;50Ti, & epsilon;40K, and & epsilon;66Zn. When comparing the CCs only, correlations are observed between & delta;41K and all four of the other moderately volatile elements assessed, while the mass-independent isotope systems show no strong correlations. Regarding the K isotope variations, these observations, along with other textural and chemical data, can be best explained by inherited isotopic variations form different precursor reservoirs (the cause of which is difficult to conclusively determine, though most likely related to the NC-CC dichotomy), and volatility related fractionation processes for the carbonaceous chondrite groups (most likely due to component mixing).

Coral reefs are highly diverse ecosystems of immense ecological, economic, and aesthetic importance built on the calcium-carbonate based skeletons of stony corals. The formation of these skeletons is threatened by increasing ocean temperatures and acidification, and a deeper understanding of the molecular mechanisms involved may assist efforts to mitigate the effects of such anthropogenic stressors. In this study, we focused on the role of the predicted bicarbonate transporter SLC4 gamma, which was suggested in previous studies to be a product of gene duplication and to have a role in coral-skeleton formation. Our comparative-genomics study using 30 coral species and 15 outgroups indicates that SLC4 gamma is present throughout the stony corals, but not in their non-skeleton-forming relatives, and apparently arose by gene duplication at the onset of stony coral evolution. Our expression studies show that SLC4 gamma, but not the closely related and apparently ancestral SLC4 gamma, is highly upregulated during coral development coincident with the onset of skeleton deposition. Moreover, we show that juvenile coral polyps carrying CRISPR/Cas9-induced mutations in SLC4 gamma are defective in skeleton formation, with the severity of the defect in individual animals correlated with their frequencies of SLC4 gamma mutations. Taken together, the results suggest that the evolution of the stony corals involved the neofunctionalization of the newly arisen SLC4 gamma for a unique role in the provision of concentrated bicarbonate for calcium-carbonate deposition. The results also demonstrate the feasibility of reverse-genetic studies of ecologically important traits in adult corals.

In order to characterize rhenium transport via infiltration of fluids in the Earth's interior, the solubility and solution mechanisms of ReO2 in aqueous fluids were determined to 900 & DEG;C and about 1710 MPa by using an externally-heated hydrothermal diamond anvil cell. In order to shed light on how Re solubility and solution mechanisms in aqueous fluids can be affected by interaction of Re with other solutes, compositions ranged from the comparatively simple ReO2-H2O system to compositionally more complex Na2O-ReO2-SiO2-H2O fluids. Fluids in the ReO2-SiO2-H2O, SiO2-H2O, Na2O-SiO2-H2O, and Na2O-ReO2-H2O systems also were examined. The presence of Na2O enhances the ReO2 solubility so that in Na2O-ReO2-H2O fluids, for example, Re solubility is increased by a factor of 10-15 compared with the Re solubility in Na2O-free ReO2-H2O fluids. The SiO2 component in ReO2-SiO2-H2O causes reduction of ReO2 solubility compared with ReO2-H2O fluids. The ReO2 solubility in the Na-bearing Na2O-ReO2-SiO2-H2O fluids is greater than that in fluids in both the ReO2-H2O and ReO2-SiO2-H2O systems. Rhenium is dissolved in aqueous fluid as ReO4-complexes with Re in fourfold coordination with oxygen. Some, or all, of the oxygen in these complexes is replaced by OH-groups depending on whether Na2O also is present. It is proposed that during dehydration of hydrated subduction zone mineral assemblages in the upper mantle, the alkali/alkaline earth ratio of the source of the released aqueous fluid affects the extent to which Re (and other HFSE) can be transported into an overlying peridotite mantle wedge. The infiltration of such fluids will, in turn, affect the Re content (and Re/Os ratio) of magma formed by partial melting of this peridotite wedge.

The Maaz formation consists of the first lithologies in Jezero crater analyzed by the Mars 2020 Perseverance rover. This formation, investigated from Sols (Martian days) 1 to 201 and from Sols 343 to 382, overlies the Seitah formation (previously described as an olivine-rich cumulate) and was initially suggested to represent an igneous crater floor unit based on orbital analyses. Using SuperCam data, we conducted a detailed textural, chemical, and mineralogical analyses of the Maaz formation and the Content member of the Seitah formation. We conclude that the Maaz formation and the Content member are igneous and consist of different lava flows and/or possibly pyroclastic flows with complex textures, including vesicular and non-vesicular rocks with different grain sizes. The Maaz formation rocks exhibit some of the lowest Mg# (=molar 100 x MgO/MgO + FeO) of all Martian igneous rocks analyzed so far (including meteorites and surface rocks) and show similar basaltic to basaltic-andesitic compositions. Their mineralogy is dominated by Fe-rich augite to possibly ferrosilite and plagioclase, and minor phases such as Fe-Ti oxides and Si-rich phases. They show a broad diversity of both compositions and textures when compared to Martian meteorites and other surface rocks. The different Maaz and Content lava or pyroclastic flows all originate from the same parental magma and/or the same magmatic system, but are not petrogenetically linked to the Seitah formation. The study of returned Maaz samples in Earth-based laboratories will help constrain the formation of these rocks, calibrate Martian crater counting, and overall, improve our understanding of magmatism on Mars.

Light organs (LO) with symbiotic bioluminescent bacteria are hallmarks of many bobtail squid species. These organs possess structural and functional features to modulate light, analogous to those found in coleoid eyes. Previous studies identified four transcription factors and modulators (SIX, EYA, PAX6, DAC) associated with both eyes and light organ development, suggesting co-option of a highly conserved gene regulatory network. Using available topological, open chromatin, and transcriptomic data, we explore the regulatory landscape around the four transcription factors as well as genes associated with LO and shared LO/eye expression. This analysis revealed several closely associated and putatively co-regulated genes. Comparative genomic analyses identified distinct evolutionary origins of these putative regulatory associations, with the DAC locus showing a unique topological and evolutionarily recent organization. We discuss different scenarios of modifications to genome topology and how these changes may have contributed to the evolutionary emergence of the light organ.

We applied single-crystal x-ray diffraction and Raman spectroscopy in a diamond-anvil cell up to 36 GPa and first-principles theoretical calculations to study the molecular dissociation of solid iodine at high pressure. Unlike previously reported, we find that the familiar Cmce molecular phase transforms to a Cmc21 molecular structure at 16 GPa, and then to an incommensurate polymeric Fmmm(00 & gamma; )s00 structure, which can be viewed as a mixture of molecular I2 and zigzag chains of three iodine atoms, at 20 GPa. The available data are consistent with metallization of iodine at the boundary between the commensurate Cmc21 structure and the incommensurate Fmmm(00 & gamma; )s00 structure at 20 GPa.