The Campito Formation is mainly composed of very fine to fine-grained quartzite, with small amounts of siltstone, getting up to 3,500 ft (1,100 m) thick.[3]
The formation is split into two distinct members, which are as follows, in ascending age:
Andrews Mountain Member: It is the thickest of the two members, getting up to 2,800 ft (850 m) thick. It is composed of olive-gray or greenish-gray very fine to fine grained silty quartziticsandstone or quartzite and interbedded layers of dark-greenish-gray siltstones, which weather to a greenish-black or just black. The quartzite layers are composed of sub-angular very fine to fine grains of quartz, feldspar and other metallic minerals, all set within a muscovite, chlorite, and biotite.[3]
Montenegro Member: It is the thinnest of the two members, only getting up to 1,000 ft (300 m) thick. It is composed of dark-greenish-gray and greenish-gray siltstone composed of a mixture of quartz, muscovite, and chlorite. The siltstone is evenly laminated to thin-bedded. There are also commonly occurring archeocyathid-bearing limestone beds in the upper sections of the member.[3]
^ abcdStewart, H. J. (2007). "Fallotaspidoid trilobite assemblage (Lower Cambrian) from the Esmeralda Basin (western Nevada, U.S.A.): The oldest trilobites from Laurentia". Alcheringa: An Australasian Journal of Palaeontology. 31: 123–140. doi:10.1080/03115510701586897.
^ abSignor, Philip W.; Mcmenamin, Mark A. S. (March 1988). "The Early Cambrian worm tube Onuphionella from California and Nevada". Journal of Paleontology. 62 (2): 233–240. doi:10.1017/S0022336000029863.
^ abcdefghiStewart Hollingsworth, J. (May 2005). "The earliest occurrence of trilobites and brachiopods in the Cambrian of Laurentia". Palaeogeography, Palaeoclimatology, Palaeoecology. 220 (1–2): 153–165. doi:10.1016/j.palaeo.2004.08.008.
^Skovsted, Christian B.; Balthasar, Uwe; Vinther, Jakob; Sperling, Erik A. (May 2021). "Small shelly fossils and carbon isotopes from the early Cambrian (Stages 3–4) Mural Formation of western Laurentia". Papers in Palaeontology. 7 (2): 951–983. doi:10.1002/spp2.1313.