CV3.3 (~3.6)oxB
standby for grosnaja photo
Fell June 28, 1861
43° 40' N., 45° 23' E.

A shower of stones fell after sonic booms at 7:00 P.M. in Grosnaja, Mekensk, USSR. Only one stone of about 3.5 kg was recovered, the remainder falling into the river Terek. It has been shocked to stage S3. The CV3 group was subdivided into the following three subgroups (McSween, 1977; Weisberg et al., 1997):

  1. Reduced subgroup: e.g., Arch, Efremovka, Leoville, Vigarano, and QUE 93429
  2. Oxidized-Allende subgroup: e.g., Allende, Axtell, Tibooburra, and ALH 84028
  3. Oxidized-Bali subgroup: e.g., Bali, Grosnaja, Kaba, and Mokoia

The CV-oxidized and CV-reduced subgroups are separated on the basis of metal abundances and the Ni content of sulfide (Howard et al., 2010). The previously used discriminator, magnetite abundance, has been shown to overlap between oxidized and reduced subgroups. The oxidized-Bali subgroup has a higher degree of aqueous alteration than oxidized-Allende. The subgroups reflect varying degrees of aqueous/oxidative alteration, which has been found to be correlated with the amount of ice-bearing matrix that was initially accreted (Ebel et al., 2009). For more mineralogical relationships, see Appendix I, Carbonaceous Chondrites).

Some investigators (e.g., Greenwood et al., 2003 and Wasson et al., 2013) have proposed that the CK chondrites could represent an extension of the CV group. This subgroup is considered to reflect varying degrees of metamorphism including impact-generated crushing, thermal alteration, and recrystallization processes (Wasson et al., 2013). In a subsequent study, Dunn et al. (2016) compared magnetite in a number of CK and CV chondrites, and presented geochemical, mineralogical, and petrographic evidence which is more consistent with separate CV and CK parent bodies; details of their study can also be found on the Dhofar 015 page.

A study was undertaken by Bonal et al. (2004, 2006) to refine the subtypes of several CV3 chondrites. They utilized several methods to obtain their data, including Raman spectrometry of organic material, a petrologic study of Fe zoning in olivine phenocrysts, presolar grain abundance, and a noble gas study. These methods are in contrast to that of TL sensitivity data of feldspar which is typically used to determine subtypes of ordinary chondrites, and which was previously applied to the CV3 chondrites. They suggest that TL sensitivity data is not applicable to aqueously altered carbonaceous chondrites because of loss of feldspars through dissolution, leading to an underestimate of the petrologic subtypes. They have redefined the petrologic subtypes of the common CV3 members as follows:

  Raman TL
Allende >3.6 3.2
Axtell >3.6 3.0
Grosnaja ~3.6 3.3
Mokoia ~3.6 3.2
Bali >3.6 3.0
Efremovka 3.1-3.4 3.2
Vigarano 3.1-3.4 3.3
Leoville 3.1-3.4 3.0
Kaba 3.1 3.0

These differences in petrologic subtype are explained by Greenwood et al. (2009) in their study of CV and CK chondrite relationships. They assert that there is a decoupling between the silicate and organic components with respect to measurements involving thermal metamorphism.

The finding of Allende-like oxidized lithologies in the reduced Vigarano breccia, as well as in the Bali-like oxidized member Mokoia, indicates that all four CV3 subgroups derive from a common heterogeneous asteroid. The Bali-like matrix mineralogy was formed by one or more mechanisms; in particular, asteroidal aqueous alteration of material similar to that of the primitive CV3 reduced subgroup at temperatures below 300°C, or re-condensation of vaporized, pre-accretionary, chondritic-rich dust. Grosnaja contains 51 vol% matrix component and exhibits a petrofabric of chondrule flattening (McSween, 1977); this is consistent within the CV group with a shock stage of ~S3 (Rubin, 2012).

The Bali-like mineralogy of Grosnaja includes the phyllosilicates saponite and sodium phlogopite replacing Ca-rich minerals in chondrules and CAIs. It is unique within its group for containing serpentine and chlorite group phyllosilicates, indicative of higher than normal temperatures during alteration. Other secondary minerals present include magnetite, fayalite, andradite, and Ca–Fe-rich pyroxenes. In the Allende-like lithologies which are present in all CV3 subgroups, virtually no phyllosilicate or fayalite is found in the chondrules or CAIs. Instead, nepheline, sodalite, fayalitic olivine, and Ca–Fe-rich pyroxenes are found indicating a higher temperature of alteration than that experienced in the Bali-like lithology on the CV parent asteroid.

The high content of magnetite in the Bali-like subgroup was instrumental in paleomanetism studies of type 3.0 Kaba by Gattacceca et al. (2013). Tentative results suggest a very early (~4.558 b.y. ago) parent body acquisition of a stable magnetic field, consistent with a core dynamo within a partially differentiated planetesimal.

Reflectance spectra have identified an asteroidal analog for the Bali-like meteorite Mokoia—the K-type asteroid 599 Luisa. Luisa is located near the 5:2 resonance at ~2.8 AU, supplying fragments into Earth-crossing orbits on short timescales. On the other hand, the ~39 km diameter, C-type asteroid 495 Eulalia was found to have spectral characteristics very similar to Grosnaja, including a "featureless" spectrum, a slight negative slope, and a virtually identical albedo (Fieber-Beyer et al., 2008). Moreover, Eulalia is located at the 3:1 Kirkwood gap (2.487 AU) and is predicted to rapidly deliver almost half of its ejected material to Earth crossing orbits; the timing is consistent with the 1.7 m.y. CRE age of Grosnaja. The above specimen of Grosnaja is a 1.5 g partial slice cut from a 20.5 g specimen formerly in the Natural History Museum, Humboldt University, Berlin.