Abstract Nucleosynthetic isotope variability among solar system objects provides insights into the accretion history of terrestrial planets. We report on the nucleosynthetic Fe isotope composition (μ54Fe) of various meteorites and show that the only material matching the terrestrial composition is CI (Ivuna-type) carbonaceous chondrites, which represent the bulk solar system composition. All other meteorites, including carbonaceous, ordinary, and enstatite chondrites, record excesses in μ54Fe. This observation is inconsistent with protracted growth of Earth by stochastic collisional accretion, which predicts a μ54Fe value reflecting a mixture of the various meteorite parent bodies. Instead, our results suggest a rapid accretion and differentiation of Earth during the ~5–million year disk lifetime, when the volatile-rich CI-like material is accreted to the proto-Sun via the inner disk.

INTRODUCTION Terrestrial planet formation is thought to occur in stages, where first-generation bodies of a few hundred kilometer radii form rapidly by streaming instabilities, followed by growth dominated by gas drag–assisted accretion of millimeter-sized particles onto these bodies (1) to form Mars-sized planetary embryos during the protoplanetary disk stage. In the inner solar system, these embryos are inferred to have formed from thermally processed and, hence, dry and reduced solids. After dissipation of the gas, the terrestrial planets are assembled over several tens of millions of years via large collisions between embryos (2), many of which will have differentiated into metal cores and silicate mantles. In these models, water and other volatile elements are inferred to have been delivered to Earth and oxidized its mantle during the last phase of accretion after core formation, possibly by volatile-rich, outer solar system bodies scattered inward by the outward migration of Jupiter (3–5). However, a recent study of the isotope composition of the siderophile element ruthenium in solar system objects, including Earth and the parent bodies of chondrite meteorites, suggests that Earth’s volatile element budget may have been acquired much earlier (6), perhaps during its main accretion phase. Moreover, new planet formation models based on the rapid accretion of pebbles onto asteroidal seeds suggest that Earth’s main accretion phase may have been completed within the ~5–million year lifetime of the protoplanetary disk (1). Elucidating the accretion history of Earth, including the timing of addition of volatile elements, is critical for a full understanding of the timescales of terrestrial planet formation. Mass-independent isotope variability of nucleosynthetic origin among early solar system objects can be used to track the source and nature of the material precursor to the terrestrial planets. In particular, iron is a redox-sensitive, siderophile major element whose partitioning between mantle and core is a proxy of the overall oxidation state of a planet. Iron readily oxidizes in the presence of water, substantially lowering its partitioning into the metal core (7, 8). Therefore, if Earth became more oxidized during accretion and core formation, the mass-independent Fe isotope composition of Earth’s mantle is predicted to be dominated by that of the late accreting material. The existence of nucleosynthetic Fe isotope variability in solar system objects can thus provide a powerful tool to fingerprint the source of the material responsible for the delivery of water to Earth and the subsequent oxidation of Earth’s mantle.

RESULTS CI chondrites are believed to best represent the bulk solar system composition for most elements and, hence, that of the Sun (9). Thus, CI chondrites best approximate the average composition of the molecular cloud material that collapsed to form the Sun and its planets. To evaluate the nucleosynthetic iron isotope variability in the solar system, we have subjected the Ivuna CI chondrite to a stepwise leaching procedure that provides a crude chemical separation of its various mineralogical components (10). This experiment reveals the existence of two main carriers of Fe nucleosynthetic variability, expressed as the μ54Fe value (see Materials and Methods), each comprising about half the total iron budget in this meteorite (Fig. 1A and Table 1). Labile phases dissolved in the early dissolution steps (L2 to L7) exhibit elevated μ54Fe values of around +46 parts per million (ppm) with respect to Earth’s mantle, which we interpret as reflecting the average composition of phases isotopically homogenized during parent body processes. Later dissolution steps (L8 to L12) contain both negative and positive μ54Fe values that range from −82 to +273 ppm in dissolution steps L8 and L11, respectively. This provides evidence for the presence of presolar carriers of nucleosynthetic Fe isotope heterogeneity. Hence, variable incorporation of these carriers in disk solids, including asteroidal and planetary bodies, could impart resolvable solar system–wide iron isotope heterogeneity. Fig. 1 μ54Fe data of a stepwise dissolution experiment of the CI chondrite Ivuna and bulk silicate Earth, stony and iron meteorites, chondrites, and chondrules. (A) Plot of μ54Fe values measured in steps of increasing acid strength (L2 to L12) of a dissolution experiment of ~3 g of the CI chondrite Ivuna (10). Width of spheres indicates the relative proportion of iron in dissolution steps. Uncertainties for individual measurements are typically smaller than the symbols and not shown (Table 1). (B) Average μ54Fe values for each group of samples from distinct solar system reservoirs (Table 2), where n denotes the number individual samples measured. The uncertainties shown for individual data points reflect either two times the SE (2 SE) of the average of the mean of the analyses or the 2 SE of the sample analysis if the group only consists of one sample without replicate analyses. The vertical dotted line and shaded area represent the mean value for terrestrial standards (10 individual analyses) and the 2 SE of these data. Table 1 Mass-independent μ54Fe and mass-dependent δ56Fe values for sequential dissolution steps of the CI chondrite Ivuna. The combined average iron isotope signature of the individual dissolution steps is consistent with the whole rock data. The number of repeat analyses of each dissolution steps is indicated by n. View this table: To determine the μ54Fe composition of the disk material that may have contributed to the growth of terrestrial planets, we measured the μ54Fe value of various classes of chondrites and their main constituents, namely, individual chondrules, as well as that of meteorites originating from differentiated parent bodies (Fig. 1B and Table 2). Apart from CI chondrites, which have a μ54Fe indistinguishable from Earth’s mantle, all chondrites are characterized by resolvable excesses in μ54Fe ranging from +6.4 ± 0.7 ppm to +28.8 ± 4.4 ppm relative to Earth’s mantle. Similarly, samples of differentiated bodies represented by iron meteorites record μ54Fe excesses, in agreement with an earlier report (11). The ordinary and CR2 chondrite chondrules are also all variably enriched in 54Fe comparable to their host meteorites, where the two CR2 chondrules exhibit the highest μ54Fe values of the analyzed samples (Fig. 1). Collectively, our data establish that apart from CI chondrites, none of the meteorites analyzed here, including all main chondrite groups, match the terrestrial composition. A CI-like composition of Earth’s mantle is not observed for other siderophile nucleosynthetic tracers such as Mo and Ru. However, these elements are much more siderophile than Fe and, as such, their compositions can be easily modified by late accretion events such as the Moon-forming impact and/or addition of the later veneer material. Unlike Fe, which records the dominant source of the material that accreted to Earth after the onset of core formation, Mo and Ru are understood to only track the last ~10% of the terrestrial accretion. Hence, the observation that the bulk of the Fe in the terrestrial mantle is indistinguishable from CI chondrites has far-reaching implications for understanding the accretion history of Earth. Table 2 Iron isotope compositions of bulk meteorites and chondrules. Summary of the mean mass fractionation–corrected (μ54Fe) and mass-dependent (δ56Fe) iron isotope composition of cores and mantles of asteroidal and planetary bodies, chondrites, and individual chondrules. The number of individual analyses including distinct samples or repeat analyses of the same sample is indicated by n. Results for individual analyses can be found in table S1. View this table:

DISCUSSION Earth’s main accretion phase is understood to have occurred via stochastic collisional accretion of embryos and planetesimals over several tens of millions of years (2, 12). In this model, oxidation of Earth’s mantle occurs toward the end of the accretion by increased addition of oxidized, outer solar system impactors, once the initially more reduced proto-Earth has differentiated and reached approximately 80% of its current mass (3–5, 13–15). Thus, if Earth’s mantle iron content was derived from the accretion of oxidized outer solar system bodies, the μ54Fe composition of the terrestrial mantle should be dominated by an average carbonaceous chondrite-like composition. However, the only chondrite group that matches the terrestrial composition is CI chondrites. Apart from the metal-rich carbonaceous chondrites, which may have accreted beyond the orbits of the gas giants, most carbonaceous chondrites are believed to have formed near the snow line beyond Jupiter or, alternatively, in the outer asteroid belt (16). Thus, it is highly improbable that scattering of outer solar system bodies by the inward migration of Jupiter would result in the selective delivery of only one type of the outer solar system material to Earth’s feeding zone, namely, CI chondrites. Alternatively, the bulk of the iron in Earth’s mantle could originate from the impact of a single body with a CI-like composition such as, for example, the Moon-forming impact. However, using the most conservative estimates for the μ54Fe composition and iron concentration of the proto-Earth as well as that of the impactor (see Materials and Methods), mass balance arguments require at least a body with a mass of approximately 15 to 20% of that of the proto-Earth, which corresponds to a planetary embryo. As planetary embryos are understood to grow by the combined effect of pebble and planetesimal accretion (1), it is unlikely that this process will result in a purely CI-like μ54Fe composition given the extent of nucleosynthetic diversity that exists among outer solar system bodies (Fig. 1). Thus, the CI chondrite composition of Earth’s mantle is inconsistent with the idea that Earth’s main accretion phase before the Moon-forming impact was dominated by stochastic collisional accretion of planetesimals and planetary embryos. Moreover, a CI-like Moon-forming impactor as the origin of the CI-like composition of Earth’s mantle is also inconsistent with the titanium and calcium isotopic similarity of Earth and Moon (17, 18). Current giant impact models cannot achieve the very high degree of isotopic equilibration between the two bodies required in the case of a carbonaceous impactor (19). Thus, we conclude that the CI-like composition of Earth’s mantle cannot result from a carbonaceous, outer solar system Moon-forming impactor. The only epoch in the history of the solar system when the CI-like material is readily available within the terrestrial planet–forming region is during the lifetime of the protoplanetary disk. This period represents the time when the in-falling envelope material of CI composition is channeled through the disk to fuel the growth of the proto-Sun and is estimated to have lasted approximately 4.8 ± 0.3 million years (Ma) (20). It has been suggested that the nucleosynthetic variability of the lithophile element calcium (μ48Ca) observed among inner solar system bodies, including Mars and proto-Earth, reflects the progressive admixing of the in-falling CI-like material during the disk’s lifetime (18). In this framework, the dry and reduced material is rapidly locked into sizeable asteroidal bodies and planetary embryos, which continue to grow by the accretion of pebbles with a CI-like composition. Thus, the μ48Ca isotope composition of terrestrial planets reflects mixtures of two reservoirs, namely, the thermally processed (and reduced) inner disk material and the pristine, volatile-rich CI-like envelope material. In this model, ureilite meteorites, which are characterized by the lowest μ48Ca values among bulk solar system materials, are our best proxy for the isotope composition of the reduced, thermally processed inner disk material before admixing of the volatile-rich CI material (18). This mixing relationship between the CI-like material and ureilites is broadly consistent with that deduced from other lithophile nucleosynthetic tracers (see the Supplementary Materials). In Fig. 2, we show that the μ48Ca and μ54Fe systematics of the inner solar system material that avoided core formation like ordinary and enstatite chondrites as well as individual ordinary chondrite chondrules are coupled and form a simple mixing line. This observation is consistent with the idea that their compositions primarily result from binary mixing. However, given the distinct geochemical behavior of Fe and Ca, core formation occurring early in the accretion history of a planetary body, especially during accretion under reducing conditions, will result in decoupling of the μ48Ca-μ54Fe systematics. Notably, the mantle μ48Ca-μ54Fe systematics of Vesta (the parent body of howardite-eucrite-diogenite meteorites) and Mars are not decoupled, considering the level of precision of our data. This is consistent with the accretion of Mars under oxidizing conditions, where iron is more lithophile, and the very early and fast accretion of Vesta such that little accretion occurred after segregation of its core (Figs. 2 and 3). In contrast to μ48Ca, the μ54Fe value of the terrestrial mantle is dominated by a CI composition. This observation points to substantial decoupling of the terrestrial μ48Ca-μ54Fe systematics and requires that the bulk of the iron in the proto-Earth was already partitioned into a metallic core before the admixing of the CI-like material. Fig. 2 Plots of μ54Fe versus μ48Ca values of bulk and bulk silicate solar system objects. (A) μ48Ca (10, 18, 38) versus μ54Fe plot of carbonaceous (outer solar system) and noncarbonaceous (inner solar system) objects. (B) μ48Ca versus μ54Fe plot of inner solar system objects plus CI chondrites. The linear regression includes ordinary chondrite chondrules, the ureilite parent body (UPB), as well as ordinary, enstatite, and CI chondrites, where the shaded area represents the 95% confidence interval. Uncertainties for both μ54Fe and μ48Ca are the 2 SE of the mean apart from μ48Ca values for CO and CV, where they are the 95% confidence interval. Fig. 3 Plot of μ48Ca versus μ54Fe of silicate mantles of inner solar system asteroids and planets and CI chondrites with possible accretion trajectories. μ54Fe values are shown versus μ48Ca data (10, 18) for the mantles of Earth, Mars, Vesta, and the UPB, where an increase in μ48Ca represents addition of CI-like solids to the planetary objects (18). Symbols and uncertainties are the same as in Fig. 2. Shown trajectories for the evolution of the μ48Ca-μ54Fe mantle composition of a growing planetary body in the inner solar system assume either no core formation or core formation on a planetary body with initially UPB-like composition and subsequent addition of CI-like dust with distinct degrees of iron partitioning between core and mantle [D(Fe) metal/silicate ] that are held constant throughout accretion. We show the isotopic evolution of a putative mantle composition in μ48Ca-μ54Fe space for three D(Fe) metal/silicate values: one reflecting iron partitioning similar to that recorded by Earth today [D(Fe) metal/silicate = 13.66], as well as for accretion under more reducing [D(Fe) metal/silicate = 27.4] or under more oxidizing [D(Fe) metal/silicate = 5.5] conditions. For simplicity, partitioning values are calculated by partitioning of only iron and nickel [D(Ni) metal/silicate = 26.5] into the core. Earth’s mantle CI-like iron isotope composition also constrains the timing of the Earth’s oxidation, as it implies that the iron budget of the mantle was established during the lifetime of the protoplanetary disk when pebble accretion could operate. The proto-Earth accreting under more oxidizing conditions than today (21–23), however, is not compatible with the CI-like iron isotope composition of Earth’s mantle (Fig. 3). Although the μ48Ca-μ54Fe systematics do not rule a constant oxidation state throughout Earth’s accretion, this would require early and instantaneous core formation, followed by the accretion of only the CI-like material (Fig. 3), making this scenario unlikely. An initially more reduced proto-Earth relaxes these constraints and only requires that Earth oxidized (i.e., acquired most of its mantle iron budget) by the accretion of CI-like dust. Water is the key ingredient for oxidation (7, 8), and as such, our results are consistent with the accretion of a component of Earth’s water and other volatile elements during the protoplanetary disk’s lifetime. This may be achieved via the direct accretion of water adsorbed to dust (24, 25) or reflects the fact that the snowline will be inside of Earth’s orbit toward the end of the protoplanetary disk’s lifetime (5), allowing direct accretion of ice during this stage. Early accretion of a fraction of Earth’s water budget is in excellent agreement with the detection of primordial water in Earth’s deep mantle (26). Our proposed timescale for the main phase of Earth’s accretion and differentiation is shorter than typically inferred from 182Hf-182W model ages of core formation (27). However, these ages are primarily controlled by the last reequilibration of the mantle during the Moon-forming impact event and are highly susceptible to model assumptions (28). Critically, the rapid timescales proposed here can be reconciled with Earth’s mantle 182W isotope composition if the Moon-forming impact occurred at least 40 Ma after the main accretion and differentiation of the proto-Earth (29). A late Moon-forming impact is supported by radiometric age dating of lunar anorthosites, which indicate that the crystallization of the lunar magma ocean occurred between 4.34 and 4.37 billion years ago (30).

MATERIALS AND METHODS Iron isotope analyses Whole rock samples weighing a few to hundreds of milligrams were digested using Savillex beakers with concentrated HF-HNO 3 mixtures on a hotplate at 130°C. To ensure complete dissolution of enstatite and carbonaceous chondrite samples, they were further digested in Parr bombs at 210°C. Iron isotope composition of individual chondrules was determined using aliquots from which Zn (31) and Ca (18) have been previously separated. For the individual dissolution steps of Ivuna, iron was extracted from dissolution steps from which previously Sr (32), Cr (33), Mg (10), and Ca (10) have been separated and measured for their isotopic composition. The detailed dissolution procedure is fully described in (10). Iron was separated from the matrix following published methods (34) using AG1-X4 anion exchange resin. Each iron separate typically consisted of several tens to hundreds of micrograms of iron, whereas procedural blanks are magnitudes lower, making blank correction inconsequential for our results. The Fe isotope compositions were measured using the Thermo Fisher Neptune Plus MC-ICP-MS (Multicollector–inductively coupled plasma mass spectrometry) at the Natural History Museum of Denmark in the medium-resolution mode. Samples were introduced to the plasma source using a stable introduction system (SIS, wet plasma) or an ESI Apex HR sample introduction system with an uptake of 25 μl min−1 and analyzed at signal intensities of 0.30 to 0.45 nA on mass 56 for ~10-ppm iron solutions. Iron isotope data were acquired in static mode using four Faraday collectors setup as follows: 58Fe and 57Fe in the high-2 and high-1 collector on the high mass side of the axial Faraday, respectively; 56Fe in the axial collector; and 54Fe in the low-2 collector on the low mass side of the axial Faraday. Alongside the iron signal, the 60Ni and 53Cr beams were measured in the high-4 and low-4 collectors, respectively, to correct for direct isobar interferences on 54Fe and 58Fe from 54Cr and 58Ni, respectively. All Faraday cups collecting iron signals were connected to amplifiers with a 1011-ohm feedback resistors, whereas the Faraday cups collecting the 60Ni and 53Cr signals were connected to amplifiers with 1012-ohm feedback resistors. Measurements were made in the medium-resolution mode (M/ΔM > 5000 as defined by the peak edge width from 5 to 95% full peak height) to resolve potential molecular interferences on the high-mass side (e.g., 40Ar16O+). We report our data relative to the IRMM-014 Fe isotope standard in the μ-notation, where the reported data represent the mean and SE of 10 individual standard-bracketed sample analyses, each comprising 25 ×16.7 s of on-peak baseline measurement and 100 × 16.7 s of sample measurement for all whole rock samples and stepwise dissolution steps where sufficient iron was available. The μ54Fe notation refers to the deviation in the 54Fe/56Fe ratio when corrected for natural kinetic mass fractionation using a 57Fe/56Fe ratio of 0.023261 (35). In table S1, we also report the 57Fe/56Fe ratio normalized using a 54Fe/56Fe ratio of 0.062669 (35), which results in isotope variations and their uncertainties that are systematically halved but otherwise exhibiting the same relative variations, demonstrating that the choice of isotope ratio does not influence the interpretation of our results. Although the 58Fe signal was monitored, we do not report the data, as the typical signal intensities during our analysis do not allow us to measure this isotope markedly above the noise level threshold of our 1011-ohm feedback resistors. Moreover, the precision of the 58Fe data is further compromised by a time variant interference correction from 58Ni, which is introduced from the measured signal on 60Ni. The 54Cr signal contributing to the total 54Fe signal was typically less than 1 ppm and, thus, negligible. On the basis of repeat analyses of processed iron separated from peridotite olivine (J12), DTS-2b and BHVO-2b standards (n = 10 including repeat analyses; 2 SD = 5.9 ppm) and intergroup isotopic variability between ureilites (n = 8 including repeat analyses; 2 SD = 7.9 ppm), ordinary chondrites (n = 9; 2 SD = 7.7 ppm), and CI chondrites (n = 9 including repeat analyses; 2 SD = 8.2 ppm), we estimate the external reproducibility of a single μ54Fe measurement to be better than ±8.2 ppm (2 SD) (table S2). Some mass-dependent fractionation of iron during planetary differentiation may occur by a nonkinetic process (i.e., equilibrium fractionation), and as such, our mass independent data for achondrites may include apparent nucleosynthetic variability arising from inappropriate mass fractionation correction, as we assume that mass-dependent fractionation occurred via kinetic processes. For example, Elardo and Shahar (36) suggested that iron isotope fractionation during core formation on terrestrial planets resulted in isotopically light mantles, which may have affected the mass bias–corrected iron isotope signatures determined for the mantles of Earth, Mars, Vesta, and the ureilite parent body determined here. Notably, Elardo and Shahar (36) argue that the terrestrial mantle is not fractionated relative to chondrites, and as such, their proposed mechanism cannot account for the CI-like iron isotope signature of Earth. We also note that average δ56Fe compositions of noncarbonaceous achondrites reported here vary by only 0.07‰, which equates to a possible effect of less than 2 ppm, if the difference in mass-dependent isotope signature was solely due to equilibrium fractionation effects. This isotope effect is not resolvable given the current precision of our data and, critically, much smaller than the μ54Fe variability of 14.6 ppm for the same samples. Hence, we conclude that nonkinetic mass fractionation cannot account for the vast majority of the observed μ54Fe variability and is best understood as being primarily of nucleosynthetic in origin. Calculation of hypothetical CI chondrite impactor mass Growth via planetary collisions is the traditionally assumed mechanism of terrestrial planet growth. Only CI chondrites match the iron isotope signature of Earth’s mantle. Thus, this isotope similarity may imply that most of the iron in the Earth’s mantle today was delivered via a late impactor with CI chondrite composition after Earth’s core had formed. To provide a conservative estimate of the mass of such a hypothetical impactor, we first determined the required minimum contribution of CI chondrite-like iron to Earth’s mantle iron budget via a mixing calculation between CI (μ54Fe = −2.0 ± 2.7 ppm) and EL chondrites (μ54Fe = +6.4 ± 0.7 ppm). EL chondrites are, apart from CI chondrites, the meteorite group that is isotopically most similar to composition of Earth’s mantle for μ54Fe and, thus, serve as conservative proxy of the pre-impact mantle composition. Using these two end-members, we derived that approximately 70% of the iron in Earth’s mantle today had to originate from the CI chondrite impactor. To estimate the relative mass of a hypothetical CI chondrite impactor based on the required iron contribution to the mantle, we assumed that 67% of the current mass of Earth is in the mantle and contains 6.26% iron (37). For the CI chondrite impactor, we used an iron abundance of 18.66% (9). Using these constraints, we calculated that the CI impactor was at least Mars sized but may have been substantially larger if the impactor metal did not fully equilibrate with the mantle. Mixing calculations for continuous accretion We calculated the isotopic evolution of an accreting Earth via addition of CI-like solids to an already formed planetesimal seed with iron and calcium isotope signatures akin to ureilites. For simplicity, we assumed a constant iron concentration in the mantle and core during accretion. Accretion was simulated by adding material with a CI chondrite composition (9) to the growing Earth incrementally, and full isotopic equilibration between mantle and the accreted material was assumed in each step. Mixing calculations either consider a constant D(Fe) metal/silicate of 5.5, 13.66, or 27.4 to simulate Earth’s accretion under more oxidizing, similar or more reducing conditions than that of Earth today. We also partitioned nickel (Ni) into the core assuming a constant D(Ni) metal/silicate = 26.5. Given that calcium does not partition into the core, we used 48Ca isotope data from (18) to calculate the evolving 48Ca isotope signature of the accreting terrestrial mantle parallel to the 54Fe signature. A terrestrial 48Ca value (= 0) indicates that the mass the hypothetical Earth has accreted and, thus, at this point the calculated 54Fe signature should also match that of the Earth’s mantle today (= 0). Thus, this model provides a test for the approximate lower limit of D(Fe) metal/silicate of Earth during its accretion via addition of CI-like solids. Without ongoing core formation before and during the accretion of the CI-like material, the iron and calcium isotope compositions would evolve along a linear mixing line between ureilites and CI chondrites and cannot generate an isotopic match in 54Fe-48Ca space for Earth. Our approach allows us to constrain the major end-members that contributed to the growing Earth based on their isotopic signature, whereas their actual bulk chemical composition (e.g., C, N, and H 2 O) may have been somewhat distinct from that preserved in the meteoritic record today. Hence, our model describes a general process rather than a precise chemical recipe.

SUPPLEMENTARY MATERIALS Supplementary material for this article is available at http://advances.sciencemag.org/cgi/content/full/6/7/eaay7604/DC1 Supplementary Text Table S1. Mass-independent μ54Fe and μ57Fe and mass-dependent δ56Fe values for terrestrial and extraterrestrial materials relative to IRMM-14. References (39–57)

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Acknowledgments: Funding: Financial support for this project was provided by the Danish National Research Foundation (DNRF97) and the European Research Council (ERC Consolidator Grant Agreement 616027—STARDUST2ASTEROIDS) to M.B. Author contributions: M.S. designed and performed the research. M.S. and M.B. analyzed the data and wrote the manuscript with input from J.S. Competing interests: The authors declare that they have no competing interests. Data and materials availability: All data needed to evaluate the conclusions in the paper are present in the paper and/or the Supplementary Materials. Additional data related to this paper may be requested from the authors.