DHOFAR 1988

A relatively fresh, partially crusted carbonaceous chondrite weighing 59 g was found in the Dhofar desert region of Oman by M. Cimala and L. Smula (see in situ photos below). A sample was sent for analysis to the Natural History Museum in Berlin (A. Greshake) and the University of New Mexico (oxygen isotopes; K. Ziegler), and Dhofar 1988 was classified as C2-ungrouped.

Dhofar 1988 and three other possibly paired brecciated meteorites were found within 3 km of each other (see Google Earth image below). These include the anomalous CM chondrite Dhofar 735 (oxygen isotope plot; photo courtesy of Thomas Witzke), the CM2 chondrite Dhofar 955, and the ungrouped carbonaceous chondrite Dhofar 2066 (oxygen isotope plot; photo courtesy of Lukasz Smula).

A petrographic component analysis of Dhofar 1988 was conducted by Suttle et al. (2021, 2023) and presented in terms of area% as follows: ~60–70% matrix, ~15–20% coarse-grained chondrules (ave. 530 µm; compare to typical ave. size in CM chondrites of ~270–300 µm) and CAIs, and ~10–20% sulphides and carbonates. An XRD-based modal mineral analysis gave abundances of 73 vol% olivine (11 vol% primary and 62 vol% secondary), 14 vol% troilite, 7 vol% pyroxene, and 5 vol% calcite. Most of the chondrules in Dhofar 1988 have experienced at least partial aqueous alteration, whereas others have become pseudomorphs during a dehydration/recrystallization stage in which phyllosilicates were transformed into secondary olivine at temperatures of at least 500–750°C—heating stage IV of Nakamura (2005) and Kimura et al. (2009) (see table below). Suttle et al. (2023) found that heating was relatively brief (minutes to days), consistent with an impact origin. Suttle et al. (2021) determined that the primary olivine, which is present in chondrule cores and as large matrix grains, has a Mg-rich (Fo81.0–99.7; ave. Fo97.4) composition. They were able to infer that the former phyllosilicate matrix was predominantly an Al-poor serpentine with the chondrule cores having a higher Al content, and that an intermixed matrix component identified as micron-scale FeNi-sulfide grains reflects the former presence of abundant tochilinite–cronstedtite intergrowths (TCI, formerly PCP or "poorly characterized phases"). A comparison of aqueous alteration degree for CY chondrites based on the phyllosilicate fraction (PSF) scheme of Howard et al. (2015) is shown in the diagram below, where Dhofar 1988 is a subtype 1.3 within a range that encompasses 1.6–1.0; this is equivalent to subtype 2.2 in the scheme of Rubin et al. (2005).

Dhofar 1988 has an O-isotopic composition enriched in heavy oxygen (18O, 17O), and has a plot very close to the C2-ungrouped Tagish Lake (oxygen isotope plot) and to the CM/CI-like, thermally metamorphosed/dehydrated Antarctic meteorite group termed 'CY' by Y. Ikeda (1992 [Consortium Summary]), which consists of Belgica 7904 (C2-ung), Y-82162 (C1/2-ung), Y-86029 (CI1), Y-86720 (C2-ung), Y-86789 (C2-ung, likely paired with Y-86720), and Y-980115 (CI1); see the MetBull oxygen isotope plot and diagrams below.

Other possibly related dehydrated CM-like meteorites include WIS 91600 (CM2.2 [CI]), EET 96010 (CM2), and PCA 02012 (CM2). Furthermore, Nakamura (2006) identified two regolith breccias, Y-793321 (CM2) and A-881458 (CM2), that contain solar-wind-implanted noble gases and belong to this dehydrated group, while M.M.M. Meier (2014) found that the meteorite Diepenveen (CM2-an) also contains similar trapped solar gases. Both Y-86737 and Y-980134, which are classified as CI1, have similar oxygen isotopes (King and Russell, 2019). In addition, Goodrich et al. (2019) revealed that clast 28 in the polymict ureilite NWA 10657 has an O-isotope composition which plots near the CY group, and a Cr-isotope composition which is unique but plots near the CI group (see diagrams below). Cr isotopes should be obtained for other CY chondrites in the future for comparison. Notably, The CM-an Dhofar 225 has many features and an oxygen isotopic composition like Dhofar 735, which along with Belgica 7904, Y-86720, and PCA 02012 have experienced the highest temperatures (~900°C) over a brief time interval (PCA 02012 estimated at tens of hours; Nakato et al., 2013) compared to other members of the CY group.

Ebihara et al. (2025) investigated the elemental composition of twelve Antarctic meteorites that were recognized as members of the proposed CY group: five have petrologic and mineralogic affinities to the CI chondrites (CI-like, dehydrated-CI), and seven have affinities to the CM chondrites (CM-like, dehydrated-CM; see table below). Abundances were obtained for 15 major elements in each of the meteorites, but the values for Mn and S, which are resistant to change during parent body aqueous and thermal processing, were found to be instrumental in distinguishing two separate groupings among the twelve CY chondrites. The two groupings, representing Mn and S inheritence from two distinct parent bodies, were termed 'CYi' and 'CYm' (see top diagram below). The CYi members have experienced parent body conditions similar to the CI chondrites, while the CYm members formed under conditions intermediate between CM and CI chondrites. Further analyses of these meteorites by both Schrader et al. (2025) and Zhu et al. (2025), have verified through petrographic, geochemical, and isotopic data that they represent two distinct parent bodies: 1) the CYi members are thermally metamorphosed CI lithologies produced in an impact shock event, during which both lithologies were ejected, and 2) the CYm members represent similar heating/dehydration processes on a parent body unique from that of CM chondrites (see bottom diagrams below). Zhu et al. (2025) also recommend that the CYi members should be termed the 'CI1T' chondrites (the "T" indicating a brief reheating stage), and the CYm members should be termed the 'CY' chondrites, forming a unique group after comprising five members.

It was experimentally demonstrated by Lindgren et al. (2020) that the slope of 0.48, which represents the increase in heavy oxygen isotopes from heating of CM chondrite ALH 83100 to 800°C, does not intersect the CY compositional field (see diagram below). Therefore, they concluded that CY chondrites cannot be derived from CM2 chondrites through any thermal process.

Hu et al. (2026) presented nucleosynthetic Ti and Cr isotope data as part of their analyses showing that a four-component mixing model best explains the heterogeneous composition of CC chondrites. Specifically, these four components are (1) matrix composed of volatile-rich CI-like dust and water ice, (2) chemically fractionated, metal-depleted, silicate-rich NC dust, (3) "Normal" CAIs (average CAI and AOA composition with ε⁵⁰Ti ~9), and (4) ultra-refractory "Chondrule-related" CAIs (with ε⁵⁰Ti ~4). See their Fig. 1 showing the mixing relationships among CC groups, with a full explanation in the open access article. Their data is also useful as a basis for comparison of the CY1 and CY2 chondrites with the CI and CM groups as shown in the table below, which additionally includes nucleosynthetic Ti, Cr, and Fe isotope data obtained by Schönbächler et al. (2026) for several CM and CI chondrites and for the CI-related asteroid Bennu. Based particularly on the available ε⁵⁰Ti and ε⁵⁴Cr data, CY2 chondrites have a close affinity with CM group members. Comparable high-precision nucleosynthetic Fe (and Zr, Ru, Nd) isotope data for CY1 and CY2 chondrites should help resolve any genetic relationships.

Ti–Cr–Fe Isotope Data for CY1, CY2, CI, and CM Chondrites
(Data is from Hu et al. [2026] except as noted)

	ε46Ti	ε48Ti	ε50Ti	ε53Cr	ε54Cr	ε54Fe	ε58Fe
CY1
Y-82162	0.43 (±0.30)	0.00 (±0.28)	2.02 (±0.32)	0.03 (±0.04)	1.43 (±0.11)
Y-86029	0.31 (±0.32)	0.13 (±0.13)	1.75 (±0.19)	0.15 (±0.02)	1.42 (±0.10)
Y-980115	0.26 (±0.15)	0.13 (±0.08)	1.48 (±0.12)	0.08 (±0.06)	1.41 (±0.11)
CY2
B-7904	0.33 (±0.21)	0.06 (±0.06)	2.49 (±0.15)	0.09 (±0.07)	1.11 (±0.10)
Y-86720	0.42 (±0.12)	0.03 (±0.08)	2.97 (±0.16)	0.17 (±0.06)	1.38 (±0.08)
Y-86789	0.37 (±0.29)	0.02 (±0.19)	2.00 (±0.22)	–0.01 (±0.06)	0.97 (±0.07)
CI
CI bulk (Wölfer et al., 2026)	0.32 (±0.05)		1.91 (±0.06)	0.29 (±0.06)	1.60 (±0.08)
Orgueil (Schönbächler et al. (2026)	0.32 (±0.09)	0.00 (±0.02)	2.03 (±0.05)	0.13 (±0.06)	1.37 (±0.05)	0.09 (±0.06)	0.00 (±0.14)
Orgueil (Schönbächler et al. (2026)	0.33 (±0.11)	–0.07 (±0.05)	1.83 (±0.07)	0.20 (±0.04)	1.35 (±0.12)	0.07 (±0.07)	0.02 (±0.13)
Bennu (OReX-800117-110) (Schönbächler et al. (2026)	0.33 (±0.06)	0.01 (±0.04)	1.95 (±0.13)	0.20 (±0.06)	1.33 (±0.08)	0.04 (±0.04)	0.06 (±0.14)
Bennu (OReX-800117-111) (Schönbächler et al. (2026)	0.42 (±0.12)	–0.03 (±0.04)	1.80 (±0.08)	0.19 (±0.05)	1.20 (±0.09)	0.05 (±0.08)	0.05 (±0.12)
Ryugu (ave.) (Schönbächler et al. (2026) Data from Tables S1-4	0.25 (±0.14)	–0.03 (±0.07)	1.78 (±0.13)	0.46 (±0.16)	1.54 (±0.11)	2.20 (±3.33)	10.80 (±4.60)
CM
CM bulk (Wölfer et al., 2026)	0.51 (±0.04)		3.00 (±0.11)	0.19 (±0.04)	0.96 (±0.06)
Murchison	0.35 (±0.16)	–0.01 (±0.08)	2.57 (±0.08)	0.31 (±0.04)	1.20 (±0.09)
Murchison (Schönbächler et al. (2026)	0.59 (±0.11)	–0.04 (±0.07)	3.13 (±0.10)	0.23 (±0.07)	0.90 (±0.06)	0.23 (±0.07)	–0.11 (±0.16)
Mighei	0.28 (±0.12)	0.11 (±0.04)	3.34 (±0.07)	0.20 (±0.05)	0.97 (±0.10)
Murray	0.34 (±0.17)	0.05 (±0.06)	2.86 (±0.11)	0.23 (±0.08)	1.10 (±0.19)
Aquas Zarcas (Schönbächler et al. (2026)	0.59 (±0.08)	–0.04 (±0.06)	2.94 (±0.11)			0.23 (±0.09)	–0.12 (±0.20)

Employing position-sensitive-detector X-ray diffraction (PSD-XRD), King et al. (2015) determined the modal mineralogy of a suite of CI and CY chondrites (see diagrams below). The total phyllosilicate abundances, ~83 vol% (81–84 vol%) for CI and ~79 vol% (including potentially back-transformed olivine) for CY, indicates that both parent bodies experienced similar extensive aqueous alteration to near completion. However, there is a significant difference in sulfide abundances between the two groups, ~6 vol% for CI and 19 vol% for CY, which reflects a difference in primary S content for the respective protoliths. King et al. (2015) also found a difference in the modal abundance of magnetite between the two groups, ~7–9 vol% for CI and 2 vol% for CY. Based on this data they inferred that the two groups likely originated on separate parent bodies.

Employing micro-Computer Tomography along with high-precision triple oxygen isotope analysis, Suttle et al. (2020) investigated a number of the largest (>500 µm), least melted, and least weathered micrometeorites from the Transantarctic Mountains (TAM) collection. They found that two intensely hydrated 16O-poor micrometeorites, TAM50-25 and TAM19B-7, share a common oxygen isotope trend line with CO, CM, and CY chondrites, possibly reflecting differences in accumulated isotopically-heavy water ice (see diagram below). Although the two micrometeorites have significantly lower sulfide abundances as well as smaller chondrules compared to the CY chondrites, they maintain that the micrometeorites could have originated from the CY parent body.

Comparative analyses of the known asteroid types and a suite of ungrouped and rare meteorites in multiple forms (bulk, powder, polished section), including NWA 2066 (paired with NWA 1988), were conducted by Krämer Ruggiu et al. (2021) utilizing petrographic, spectroscopic, and albedo data. They concluded that the best matches to NWA 2066, and by association NWA 1988, are the X-type asteroids Xc, Xe, and Xk; this is the first meteorite match to Xe-type asteroids (see diagram below).

Amsellem et al. (2020) utilized Rb–Sr systematics to date the thermal metamorphism and dehydration experienced by a number of CM chondrites, including MIL 07675, PCA 02010, PCA 02012, PCA 91008, and QUE 93005. For each of the meteorites they found that the heating was a late-stage event (<2 b.y. ago), possibly associated with a collisional disruption resulting in the formation of a C-type asteroid family (see diagram below).

Further information about the thermally metamorphosed CM-like chondrites and the CY group can be found on the Dhofar 225 page. The specimen of Dhofar 1988 shown above and below is a 2.73 g slice that exhibits a brecciated texture. It is comprised of monomict dark clasts (CY1; Zhu et al., 2026 #5007) hosted within a CY2 lithology consisting of chondrules with Fe-sulfide mantles, along with a significant distribuion of CAIs.