Stillwater igneous complex
The Stillwater igneous complex is a large layered mafic intrusion (LMI) located in southern Montana in Stillwater, Sweet Grass and Park Counties. The complex is exposed across 30 miles (48 km) of the north flank of the Beartooth Mountain Range. The complex has extensive reserves of chromium ore and has a history of being mined for chromium. More recent mining activity has produced palladium and other platinum group elements.
The Stillwater complex is a large layered intrusion with many similarities to the Bushveld igneous complex of South Africa. The complex was intruded into existing gneisses during the Archean at about 2700 Ma. Host rocks on the northern side are Archean sedimentary rocks while the southern boundary includes Precambrian rocks of granite, granite gneiss and schist . The Precambrian rock on its southern side is mostly provided by the Beartooth Mountains. The region had a quartz monzonite intrusion and underwent extensive metamorphism, faulting and folding during the Archean at about 2500 Mya. The area was intruded by north trending mafic dikes before being unconformably covered by a middle-Cambrian sedimentary rock sequence. The intrusion forms a linear body stretching some 30 miles (48 km) and striking roughly N 60 °W and dipping from 50° to near 90° to the northeast. The exposed thickness is around 18,000 feet (5500 m) with an additional estimated 5,000 to 15,000 feet (1524 to 4572 m) having been removed from the top by pre-Cambrian erosion. 
- The basal zone consists of a chilled fine grained gabbro overlain by gabbro, norite and feldspar pyroxenites. Thickness up to 700 feet (210 m).
- The ultramafic zone is composed of a lower peridotite member consisting of alternating dunite, chromitite, harzburgite and bronzite pyroxenite. The upper third is massive bronzite pyroxenite. The ultramafic zone averages around 3500 feet (1100 m) in thickness.
- The banded zone is composed of alternating norite, gabbro and anorthosite. The banded zone has a maximum thickness of 14,000 feet (4300 m).
The chromium orebodies are restricted to the peridotite member of the ultramafic zone. The platinum group orebodies are located in the lower part of the banded zone within a horizon referred to as the J-M reef.
The J-M Reef is similar to the Merensky Reef of the Bushveld complex of South Africa. It is a continuous layer near the base of the banded zone. It consists of one to three meter thick pegmatitic peridotite and troctolite with disseminated sulfide minerals. Common sulfides include pyrrhotite, pentlandite (containing up to 5% Pd), and chalcopyrite along with lesser amounts of moncheite ((Pt,Pd)(Te,Bi)2), cooperite ((Pt,Pd,Ni)S), braggite ((Pt,Pd,Ni)S), kotulskite (Pd(Te,Bi)1-2) and platinum-iron alloys. Overall the reef contains an average of 20-25 ppm platinum plus palladium in an average two meter thickness. It has a Pd/Pt ratio of about 3.6.
In July 1972, the area was used by NASA to geologically train the Apollo Astronauts in recognizing a coarse grained igneous intrusion. Astronauts who would use this training on the Moon included Apollo 16's John Young and Apollo 17's Gene Cernan and Jack Schmitt. Notable geologist instructors included William R. Muehlberger.
- The Stillwater Complex: A review of the geology by I. S. McCallum http://serc.carleton.edu/files/NAGTWorkshops/petrology03/McCallum.Stillwater.doc
- American Mineralogist, Volume 75, pages 37-45, 1990 The Stillwater Complex and its anorthosites: An accident of magmatic underplating? GERALD K. CZAMANSKE, STEVEN R. BOHLEN http://www.minsocam.org/ammin/AM75/AM75_37.pdf
- "Igneous and tectonic structures of the Stillwater complex, Montana". 1960. doi:10.3133/b1071h.
- Jackson, Everett D., The Chromite Deposits of the Stillwater Complex, Montana in Ore Deposites of the Unitrd States, 1933-1967 (The Graton-Sales Volume) Vol. 2, pp. 1495-1509, 1968
- Stanton, R. L., 1972, Ore Petrology, Ch 11 Ores of Mafic and Ultramafic Association, pp. 305-351, McGraw Hill
- Phinney, William (2015). Science Training History of the Apollo Astronauts. NASA SP -2015-626. pp. 253–254.