A 103 kg mass was seen and heard to fall in the daytime near the Benue River in Nigeria. The Geological Survey of Nigeria learned of the event in 1935 when the mass was recovered from a shallow hole six miles west of the railway station at Udei and 23 miles north of Makurdi. Some reports state that a second mass exists.
The IAB iron-meteorite complex, recently proposed by Wasson and Kallemeyn (2002), comprises iron meteorites from the former IAB-IIICD group, as well as numerous related irons. Many of the members contain silicate inclusions with roughly chondritic compositions. Udei Station is a low-Au member of the IAB complex that is closely related to the main group. On a NiAu diagram, a group of six meteorites has been resolved in an area close to the sLL subgroup, but with anomalous Ni contents; these meteorites were designated the Udei Station grouplet which includes Caddo County, Four Corners, Harlowtown, Thiel Mountains, Udei Station, and Zagora. Although theories of formation for these irons commonly attribute their origin to impact-melt pools, correlations between Ni abundance and several chemical and physical properties alternatively suggest an interaction with a crystallizing metallic core.
Udei Station is a medium octahedrite that contains a high proportion of silicates and troilite. Silicate inclusions range in size from single grains to as large as 8 cm, and they are composed of enstatite, olivine, oligoclase, and diopside representing various subchondritic rock types including basaltgabbro, feldspathic orthopyroxenite, lherzolite, and harzburgite. Some of the inclusions crystallized from a low degree partial melt (~310%) reaching a peak temperature of <1180°C, while others represent a partial melt residue (Ruzicka and Hutson, 2009). Identification of an FeO-poor, Na-rich gabbroic inclusion similar to one found in Caddo County is only the second discovery of such material. It was concluded that interstitial silicate melt migration and removal occurred, assisted by CO gas (now manifest as graphite), while low abundances of metallic melt (~37%) became trapped in veins between solid silicate assemblages (Ruzicka and Hutson, 2009). One plausible model involves impact processing within small melt pools that led to brecciation and mixing of rock clasts from different locations having different thermal histories (ranging from igneous to chondritic) with metallic melt. These melt pools were then slowly cooled, consistent with burial within a deep regolith.
A formation model that accounts for such a wide variety of inclusions and disparate petrographic evidence was proposed by Ruzicka and Hutson (2009) and Ruzicka (2014). They conceive of a major collisional disruption/jumbling of a partially molten, incompletely differentiated planetesimal. They consider winonaites to be derived from the outer layers of this body. At the same time, they envision the IAB complex irons that were more rapidly cooled, exhibit older IXe ages, and which are Ni-rich, to have derived from the middle layers, while those that were more slowly cooled, exhibit younger IXe ages, and which are Ni-poor, to have derived from the lowest layers. This was a severe impact that mixed material from different depths on the parent bodysolid subchondritic material from the cooler regions, and fractionated material from very hot regionscausing metallic melt to be injected into the silicates.
The absolute IXe retention age, relative to the Shallowater standard, was calculated to be ~4.558 b.y., while the metamorphic resetting of the KAr chronometer occurred ~4.31 b.y. ago (Bogard et al, 2005; Pravdivtseva et al, 2013). A PbPb age of 4.563 (±0.029) b.y. (isochron for all samples, see diagram below) was calculated by Litasov et al. (2019) for apatite grains in Udei Station and some other group IAB irons; a somewhat younger PbPb age was obtained when excluding several incongruent data points.
Diagram credit: Litasov et al., 82nd MetSoc, #6125 (2019)
Utilizing the short-lived 182Hf182W chronometer, corrected for neutron capture by 182W due to galactic cosmic rays, Hunt et al. (2018) derived the timing of metalsilicate separation of all genetically-related IAB irons (at least the MG and sLL subgroup [possibly also the sLM subgroup] and the ungrouped Caddo County [Udei Station grouplet] and Livingstone [Algarrabo duo]) to 6.0 (±0.8) m.y. after CAIs. Based on the constraints provided by the timing of metal segregation, they modeled the early history of the 120(+)-km-diameter IAB parent body as outlined in the following diagram:
Diagram credit: Hunt et al., EPSL, vol. 482, pp. 497 (2018, open accesslink)
'Late metalsilicate separation on the IAB parent asteroid: Constraints from combined W and Pt isotopes and thermal modelling'
Dey et al. (2019) employed 17O and ε54Cr values for several irons and their associated silicates/oxides to investigate i) if each iron and its associated phases originated on a common parent body (i.e., an endogenous mixture of core and mantle vs. an exogenous mixture through impact), and ii) if any genetic
connection exists between the irons and other meteorite groups (e.g., IAB with winonaites, IIE with H chondrites, and Eagle Station pallasites with CK chondrites). Three IAB irons were employed in the study, and it was demonstrated on a coupled diagram that although the ε54Cr values for the iron component plot in the winonaite field, values for the silicate component plot in a distinct region on an OCr coupled diagram (see diagram below). From these results they ascertained that the IAB silicated irons formed through an impact-generated mixture comprising iron from a winonaite-related parent body and silicate from an unrelated and otherwise unsampled parent body. Incorporation of the silicates into the FeNi-metal host took place at a depth greater than 2 km, allowing time for a Thomson (Widmanstätten) structure to develop during a long cooling phase. Fractional crystallization occurred in some large molten metal pools, followed by very slow cooling, which
produced the broad range of features found in certain IAB meteorites (e.g., silicate-poor, graphitetroilite-rich inclusions and extremely high Ni contents). Other results from their study can be found on the Miles and Eagle Station pages.
17O vs. ε54Cr for Irons and Pallasites
click on diagram for a magnified view
Diagrams credit: Dey et al., 50th LPSC, #2977 (2019)
Udei Station has a ClAr-based CRE age of 123 m.y. (Albrecht et al., 2000). It plots as an anomalous member of group IAB in several regards. It contains a clast best described as a peridotite, composed of the most Fe-rich mafic minerals found among IAB irons. Some variability in appearance is apparent in some members of this grouplet, as can be seen in the Four Corners meteorite. The specimen shown above is a 26.3 g partial slice exhibiting a high content of silicates.