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SAU 290

CH3 chondrite
standby for sau 290 photo
Found February 13, 2004
21° 04′ 31.6′ N., 57° 08′ 49.3′ E. During an expedition in Adam County, Oman, Rainer and Claudia Bartoschewitz found 64 fragments of a single meteorite lying on a limestone gravel plateau all within a distance of 10 meters (Bartoschewitz et al., 2005). The total weight of the constituted meteorite was 1.796 kg. The classification of SaU 290 was initially considered to be an anomalous E chondrite microbreccia with a weathering grade of W2, but the O-isotope composition of Sayh al Uhaymir 290 plots within the CH chondrite field, distinguishing it as a member of this very rare carbonaceous group.

The microstructure and microchemistry of a variety of FeNi-metal condensate particles from CH chondrites were examined by Goldstein et al. (2005). A portion of the metal particles were found to be zoned, with cores that are enriched in Ni and Co and depleted in P, Cr, and Fe. Other particles are unzoned and homogeneous, possibly reflecting diffusive equilibration during an extended period within the hot gas, a period of longer duration than that experienced by zoned particles. Ni-rich precipitates occur in a portion of both of these condensate types. In addition, a high-Ni metal grain identified as tetrataenite has been found. A silica-rich component similar to that observed in other CH chondrites was also identified (Zhang et al., 2007). CH-chondrite components originated from both highly reducing and highly oxidizing environments, constituting more than a single reservoir (Kimura et al., 2011).

A large N gas content has been found in SaU 290, residing in at least four components (Murty et al., 2007). The heavy N component (δ15N) is present in the same abundance as in other CH chondrites. Several carrier phases for the δ15N have been identified, including C–silicate aggregates, FeNi-metal+Fe–Cr-sulfide, Si-rich metal+FeS, and in hydrated areas; however, it is believed that a single carrier, the C–silicate aggregates, was the original δ15N source prior to its redistribution into metallic phases during a quick nebular heating event (Sugiura and Zashu, 2001). In their in-depth study of Bencubbin, Perron et al. (2007) proposed that water and 15N-bearing organics were degassed from the hydrated clasts during the impact of one or more chondritic objects. These hydrated clasts were agglomerated onto the Bencubbin parent body during its initial accretionary stages. The lower abundance of δ15N located within the hydrated areas is thought by some investigators to be the product of mixing of normal N and δ15N on the parent body. The presence of a carrier phase having a low abundance of δ15N has been seen in experiments, but has not yet been identified (Murty et al., 2007).

Based on a noble gas studies at the University of Tokyo (J. Park, K. Nagao, and R. Okazaki), SaU 290 was shown to contain the highest solar noble gas abundances among CH group members. The He and Ne isotopic ratios in SaU 290 are consistent with solar values. A 21Ne-based CRE age has been established at 1.2 m.y. The average Δ17O value of –2.2 (±0.6‰) is nearly identical to the values in most CH, CB, and CH/CB magnesian cryptocrystalline chondrules, indicating their likely formation from a common reservoir resulting from a single impact event (Nakashima et al., 2011). Given the range of O-isotopic values in those cryptocrystalline chondrules having anomalous values, it is proposed that they might have formed along with the type-I porphyritic chondrules.

A complete mineralogical inventory of the refractory inclusions and Al-rich chondrules present in SaU 290 has been prepared by Zhang and Hsu (2009). The CAI content of SaU 290 reflects the low abundance (0.1 vol%) and relatively small size (ave. ~40 µm) typical for other CH chondrites, but unlike those from other carbonaceous chondrite groups. The small CAI sizes are thought to be the result of either a nebular sorting mechanism or a mechanism which controlled the growth rates. The CH group CAIs are unique in composition from those of other carbonaceous chondrite groups and exhibit a highly refractory nature experiencing higher solar nebular peak temperatures of 1386–1074°C. They consist primarily of hibonite and grossite, along with melilite, spinel, fassaite, and anorthite, and various combinations thereof. While some CAIs exhibit igneous features consistent with crystallization from melt droplets, others have a layered texture indicative of nebular gas–solid condensation. An ultrarefractory inclusion was identified in SaU 290 by Zhang et al. (2015), which is composed of such ultrarefractory phases as panguite, davisite, and Sc-rich anosovite, together with the more typical refractory phases spinel, anorthite, and perovskite. This ultrarefractory CAI is depleted in 16O, which attests to its formation in the outer region of the protoplanetary disk where isotopic self-shielding during UV photolysis of CO preferentially produces an 16O-poor gas (Krot et al., 2009).

In addition, rare amoeboid olivine aggregates (AOAs) composed of olivine, Al-diopside, and anorthite have been identified in CH chondrites (Krot et al., 2014). These are texturally and mineralogically similar to AOAs in other carbonaceous chondrite groups that were formed as nebular condensates during the earliest stages of Solar System history. A suite of Al-rich chondrules compositionally unique to those of other carbonaceous chondrite groups have also been documented. These are likely products of melted precursor material derived from both CAIs and ferromagnesian chondrules. The study presented evidence for low degrees of both thermal metamorphism and aqueous alteration on the CH parent body, leaving the inclusions in a pristine state and reflecting the nebular conditions in which they were formed.

Further information about the CH group can be found on the Acfer 214 page. The specimen of SaU 290 pictured above is a 2.88 g partial end section with an unpolished cut face. The photo below shows the ~200 g fragment from which the above piece was cut.

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Photo courtesy of S. Turecki

For additional information on CH chondrite petrogenesis, read the PSRD article by G. Jeffrey Taylor: ‘The Oldest Metal in the Solar System‘, Sep 2000.

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NWA 4781

CH3 chondrite
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Purchased October 2006
no coordinates recorded A single highly weathered stone weighing 181 g was found in Northwest Africa. The stone was acquired by Moroccan meteorite dealer A. Habibi, and thereafter, sold to the Polish Meteorite Laboratory. Analyses of individual samples of this meteorite, conducted at both Northern Arizona University (T. Bunch) and the Muséum National d’Histoire Naturelle, Paris (M. Denise), resulted in a classification for NWA 4781 of CH3 chondrite.

John Kashuba’s excellent webpage on NWA 4781, utilizing petrographic thin section views and descriptions, can be seen here. Further information about the CH group can be found on the Acfer 214 page. The specimen of NWA 4781 pictured above is a 1.45 g partial slice. The photo below shows the ‘dinosaur-skin’ texture of the fusion crust sculptured by extensive terrestrial weathering, consistent with grade W4, along with a slice below.

nwa 4781
click on image for a magnified view
Photo courtesy of A. Habibi

Photo courtesy of A. Habibi

For additional information on CH chondrite petrogenesis, read the PSRD article by G. Jeffrey Taylor: ‘The Oldest Metal in the Solar System‘, Sept. 2000.

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CH3 chondrite
standby for acfer 214 photo standby for acfer 214 photo
Found September 30, 1991
27° 41.40′ N., 4° 22.72′ E. In the initial discovery in 1990, two pieces of an Fe-rich, fine-grained carbonaceous chondrite, weighing together 166 g, were found in the Algerian Sahara Desert and given the name Acfer 182. In 1991, additional pieces paired with Acfer 182 were found, including a 105 g piece designated Acfer 207 and two pieces with a combined weight of 612 g designated Acfer 214.

This meteorite has chemical, mineralogical, and textural similarities to the unique 11.9 g chondritic breccia ALH 85085, and has close affinities to the CR chondrites and the newly designated CB chondrites. In light of their high bulk iron and metal content, both Acfer 182 (and pairings) and ALH 85085 were initially designated as ‘HH chondrites’ (Bischoff et al., 1992). However, due to their many similarities to carbonaceous chondrites they were given the new designation of ‘CH chondrites’ (Bischoff et al, 1993). More recently, several separate finds from Antarctica were included in this rare CH group (EET 96238, PAT 91546, PCA 91467, and RKP 92435), as well as additional finds from northwest Africa (NWA 470, NWA 739, NWA 770, and NWA 4781) and Oman (SaU 290). These carbonaceous chondrite groups considered together have been termed the CR clan.

Acfer 214 is composed primarily of chondrules and chondrule fragments (~70 vol%). Interestingly, it has a much lower abundance of complete chondrules than chondrule fragments, with some fragments being derived from larger chondrules than those now present. Most chondrules in Acfer 214 and other CH members are significantly smaller than those in other chondrite groups. The majority of the chondrules (~80%) are of the much rarer cryptocrystalline texture rather than porphyritic, and they have a mean diameter of 0.03–0.15 mm, the largest measuring 1.1 mm in diameter. Most magnesian and ferroan cryptocrystalline chondrules in CH chondrites have identical chemical and O-isotopic values to those of CB cryptocrystalline chondrules, and the two groups are considered to be genetically related (Nakashima et al., 2010).

However, some cryptocrystalline and porphyritic chondrules in CH chondrites have anomalous isotopic values compared to other carbonaceous chondrite groups, inferring that these CH chondrules originated in a separate nebular region and/or during a different time period. Volatile depletions in these crptocrystalline chondrules suggest that they formed in high temperature conditions and cooled rapidly (Nakashima et al., 2011). An extremely 16O-rich, cryptocrystalline chondrule has been identified in Acfer 214 (Kobayashi et al., 2003). This chondrule, among others, condensed as a liquid directly from a nebular reservoir (Varela et al., 2011). It contains a lighter O signature than even refractory inclusions, and is the most 16O-enriched component discovered in a meteorite thus far.

Leitner et al. (2018) identified two presolar silicate grains (O-rich stardust grains) and four presolar SiC grains in the fine-grained material of the hydrated lithic clasts from the paired Acfer 182, representing a bulk abundance of 4 (+5/–2) ppm and 21 (+16/–10) ppm, respectively. Both of the silicate dust grains belong to group 1 of Nittler et al. (1997, article), which were derived from low-mass (1.2–2.2 M) AGB-stage red giant stars. They note that presolar silicate grains are susceptible to destruction by aqueous alteration while SiC grains are not, and infer that the lithic clasts are consistent with petrologic type 2.

Rare carbonaceous chondrite fragments present in Acfer 214 contain silica-rich spherules composed of nanocrystalline quartz formed at very high temperatures. The spherules subsequently underwent supercooling until rapid crystallization ensued. The consistently small size of this and all of the other components in this meteorite probably reflects aerodynamic size sorting in the nebula region prior to accretion, possibly through size-dependent interactions between gas drag pulling inward and photophoresis and radiation pressure pushing outward (Haack et al., 2006). Alternatively, size-sorting could have been controlled by the abundance of dust in the nebular region and by the number of chondrule remelting episodes that occurred (Rubin, 2010). According to thermal models of Scott et al. (2007), the accretion of CH chondrites is consistent with late accretion ~3–5 m.y. after CAI formation, at a time when radiogenic heating by 26Al was minimal. The formation location was likely in the outer region of the asteroid belt.

FeNi-metal is present in higher concentrations (~20 vol%) than in most other carbonaceous chondrites, which, taken together with the volatile- and sulfide-depletions observed, is indicative of an early accretion through condensation in a very hot (~1000°C at 10 Pa) nebular environment; these high temperatures are sustained by transient heating events associated with impact shocks. A nebular fractional condensation model is suggested by the widely varied patterns of zoning observed in some of these sub-mm-sized metal grains for the siderophile elements Ni, Co, Cr, P, Si, Au, Os, Ir, Ru, and Pd. To account for the preservation of these primitive zoned metal grains, as well as their virtual lack of Ga and Ge, it is necessary that these grains were isolated from the residual hot nebular gas before temperatures dropped below ~527°C. After condensing near 1 AU, these grains could have been radially transported to cooler nebular regions where oxidation, sulfurization, and thermal metamorphism effects were minimal, and cooling was rapid—measured in hours or days. Although a primary martensitic structure was retained in most of the FeNi-metal grains (Kimura et al., 2008), exsolution of Ni-rich taenite has been observed in some of the zoned metal grains, attesting to a brief period of reheating (hours to a day) and subsequent cooling at a reduced rate (Goldstein et al., 2007).

A population of unzoned metal grains that are depleted in Ni and refractory siderophile elements are present, possibly forming a continuum with zoned metal grains. These grains condensed at a later, lower-temperature stage than the zoned metal grains from a gas previously depleted in refractory elements. Moreover, they could have remained longer within the gas environment (> ~10 weeks) and undergone diffusive equilibration of metal (Campbell and Humayun, 2004). Some of these grains were plastically deformed and experienced a brief period of reheating (hours to a day), as evidenced by a recrystallized structure and Ni-rich taenite exsolution phases (Goldstein et al., 2007). It is considered likely that this reheating/exsolution stage occurred after the metal grains were incorporated into the precursor aggregate of the chondrules, where the heating is attributed to impact events. Ultimately, brecciation on the CH parent body brought together the various metal grains into the meteorites that we observe.

A silica-rich component (>65 wt% silica), which comprises <0.1 vol% of the meteorite, has recently been studied by Hezel et al. (2003). Based on the chemical compositions of these silica-rich objects, as well as on the sequence of layers that is recorded in one object, an origin through fractional condensation from an evaporated nebular gas was proposed. Initially, Ca–Al–Ti-rich minerals were isolated from the residual gas, followed in the condensation sequence by forsterite and enstatite, the formation of which left the residual gas enriched in SiO and infused with precursory silica-rich material. This precursor material was then reheated to temperatures above 1695°C, at which point several different silica-rich phases condensed—quartz, cristobalite, glass, and an unidentified polymorph—followed by rapid cooling to form the glassy objects, or slower cooling to form the crystalline objects. While the porphyritic chondrules may have been produced during this transient high-temperature reheating phase, evidence suggests that the cryptocrystalline chondrules were likely formed and isolated earlier during fractional condensation processes. Finally, each of these types of objects were accreted into the CH chondrite body.

A small component within Acfer 214 consists of dark, fine-grained inclusions with phyllosilicate-rich clasts. Since the other CH components did not experience alteration, aqueous alteration of these dark hydrated clasts occurred prior to their being incorporated into the CH parent body. Also present are very small (up to 0.45 mm), extremely refractory, rimmed CAIs that are high in grossite, melilite, hibonite, and perovskite occur throughout (~0.1 vol%); some CAIs are significantly less altered than those from other carbonaceous chondrites. An exceedingly rare phase, Ca-monoaluminate, has been identified in the CH group member NWA 470, the first time that this phase has been found in nature. This Ca-monoaluminate is thought to have condensed from a dust-enriched region of the nebula. Since these highly refractory CAIs are depleted in 26Mg, they probably condensed at a very early stage, prior to the injection of 26Al into the nascent solar nebula. Alternatively, production of this radionuclide may have been a more localized process that left it absent in the CAI condensation region. The remaining component of Acfer 214 consists of a sparse, fine-grained, chondritic matrix (~5 vol%) not present in other CH members, which has been terrestrially altered to a large degree. Due to extended weathering of the large metal component in Acfer 214, and its conversion to pore-filling iron oxide, the porosity was calculated to be 0 (Macke et al., 2011).

The presence of solar noble gases and the fragmental nature of the components indicates that the CH chondrites were once located in a brecciated surface regolith. Similar to bencubbinites, CH chondrites contain heavy 15N thought to have been accreted from interstellar molecular clouds. Although the actual source of the heavy N remains a source of study, it is thought to have been initially located within carbon-silicate aggregates, and then subsequently redistributed to other phases through shock heating or hydrous alteration. An alternative scenario proposed by Perron and Mostefaoui (2007) calls for the 15N to be delivered by a lagging portion of a hydrated cometary object impacting onto the CH parent body after some degree of cooling of the initial impact plume. They further argued that the data support an origin for the 15N within N-rich molecules rather than from meteoritic, carbonaceous material. In their in-depth study of Bencubbin, Perron et al. (2007) proposed that water and 15N-bearing organics were degassed from the hydrated clasts during the impact of a chondritic object(s). These hydrated clasts were agglomerated onto the Bencubbin parent body during its initial accretionary stages.

Extraterrestrial amino acids (13–16 ppm) were found to be present in a sampling of CH chondrites studied by Burton et al. (2013), abundances of which are similar to those found among CM2 chondrites. The types of amino acids are different from those identified in other carbonaceous chondrite groups and were likely synthesized through different chemical pathways under different environmental conditions (e.g., degree of aqueous alteration).

The relatively late formation of the CH chondrites is considered to have been concordant with, and related to the highly-energetic event that produced the CB chondrites, likely within an impact-generated plume. Mineral components studied in Acfer 214 and Acfer 182 are consistent with an accretionary origin from such an event (Krot et al., 2014). Further information about this collisional event can be found on the Bencubbin page. Also, see the HaH 237 page for a detailed scenario of the CB group formation process ascertained by Fedkin et al. (2015) through kinetic condensation modeling.

Acfer 182, 207, 214, and ALH 85085, along with several meteorites found more recently are designated CH chondrites. They constitute a group of volatile-poor, high-metal, carbonaceous chondrites that represent the most pristine nebular condensates known, or more likely, a late-stage condensate origin in a relatively high molecular weight gas such as a debris plume produced by a high-energy protoplanetary collision (Richter et al., 2014). It is notable that both Acfer 214 and NWA 739 share some anomalous features compared to the other CH chondrites, including larger-sized chondrules and O-isotopic compositions that plot outside of the CH field (they are also not concordant with each other). These two meteorites may represent a daughter parent body that is similar to, but separate from that of other CH chondrites.

The formation of Mercury from similar metal-rich chondritic material has been hypothesized to account for its high density and large core, just as have all of the inner planets to explain their volatile element depletions. Reflectance specta of asteroid 21 Lutetia (Xk or Xc type in Bus-DeMeo taxonomy, M-type in Tholen taxonomy) obtained by ESA’s Rosetta spacecraft is a very close match to laboratory spectra of CH3 chondrite PCA 91467 across a wide range of wavelengths for a variety of parameters, and it is considered to be a good candidate source body for this meteorite group (Trigo-Rodriguez et al., 2012; Moyano-Cambero et al., 2013, 2014, 2016). The data indicate that Lutetia may have a partially differentiated structure, with a metallic core, a silicate mantle, and a primitive chondritic crust. The degree of aqueous alteration on Lutetia is higher than for PCA 91467, which could reflect collisional exposure of deeper crustal regions on the asteroid subsequent to the impact ejection of CH chondrites (Moyano-Cambero et al., 2016). A density estimate for Lutetia is similar to the bulk density calculated for the metal-rich CH group (Moyano-Cambero et al., 2016 and references therein). It was inferred that the specific source location for the CH chondrites could reside near the northern equatorial region of this heterogeneous asteroid, or it could derive from an asteroid having similar properties (Moyano-Cambero et al., 2014).

The specimen of Acfer 214 shown above and in the top photo below is a 1.5 g partial slice exhibiting an abundance of metal grains throughout. The bottom photo shows the main mass, courtesy of Luc Labenne. standby for acfer 214 photo

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