redeposited in the southwestern facies with clasts either derived in situ or from nearby sources. The black pelite unit overlying the chert-carbonate unit of the Black Stuart Group is Middle Devonian and may range from Lower to Upper Devonian. Its contact with the chert-carbonate unit is sharp and suspected to be conformable. Environmental stratigraphic detail in- cludes: 1) fine grain, 2) even, finely laminated bedding, 3) occasionally graded silt lenses and laminae, 4) absence of ripples, crosslaminations, dewatering and density inversion structures, evidence of burrowing organisms, and fossils other than Amphipora and conodonts, 5) moderate to high carbon content, 6) low to moderate silicification, 7) variable quantities of thin black carbo- nate bands, and 8) presence of an oolitic grey limestone. Intercalated within the black unit are the Waverly and Guyet formations. The black pelite of this unit is similar to the graptoli- tic shale, except it is more carbonaceous and siliceous. There are no physical paleobathymetric indicators which suggest deep water, though the basin would have been quiet and restricted with little clastic input. The conodonts from the upper Middle Devonian carbonates are all spe- cies of Polygnathus, which is suggestive of deep water environments (Chatteron, 1976) but the sample is far too limited to support this conclusively. Chatterton attrib- utes a diverse fauna of Polygnathus with poor represen- tation of other forms to a low energy basin or slope environment. The intercalation of the Waverly Formation volcanics into this succession may indicate a shallowing of the basin because the Waverly is directly overlain by the grey oolitic limestone of the black pelite unit. Laminated grey lime- stone breccia fragments are found within the basalts of the Waverly. The laminated limestone is suspected to have been derived from a similar environment as the oolitic limestone. The oolites indicate wave-action; usually less than 10 to 15 m below sea level. Above the oolitic lime- stone are more black shales indicating a calming of cur- rent action which may have resulted from deepening of the water synchronous with a waning of the effects of Waverly volcanism. The Waverly Formation is overlain by both the black pelite unit of the Black Stuart Group and the Guyet Formation conglomerate. Sedimentological detail of the Guyet Formation in- cludes: 1) angular to rounded polymictic clasts, 2) grading displayed by decrease from pebble-clast size to the per- vasive quartzite-chert-sand matrix, 3) erosion contacts at the base of coarse beds, 4) interbedding of muddy and sandy conglomerate, 5) changes in clast content, 6) even bedding, where seen, 7) massive sandstones, 8) suspen- sion of solitary large clasts in finer massive matrix, and 9) general fining upsection in thick sequences. The envi- ronment of deposition is not obvious from this scanty information. Several other observations are useful: 1) the conglom- erate is intercalated in the black pelite unit of the Black Stuart Group, 2) the contact between these two units is only partly erosional, and 3) clast types possibly from the Black Stuart Group are scarce. These points imply the Guyet Formation conglomerate was deposited into a moderately deep-water environment. Sutherland Brown (1963) suggested (from the size of the clasts) that the Guyet was probably deposited at the mouth of a torren- tial stream. Such a stream must be erosional and the Guyet conglomerate does not record that erosion. Large clasts supported in a mud matrix (muddy conglomerate) is a textural anomaly for a conglomerate deposited in a fluviatile environment. The conglomerate is considered instead to have been brought to the depositional site as debris flows travelling into moderately deep water. The texture and grading characteristics of the conglomerate are features of proximal debris flows (see Krause and Oldershaw, 1979, and Walker, 1978). Overlying the Guyet conglomerate are the black pelite and sandstone units in the Black Stuart Mountain area and the Greenberry limestone to the north. The upper black pelite unit is considered have been deposited pene- contemporaneously with the northern Guyet Formation conglomerate and to be deposited in an environment simi- lar to that of the older black pelite unit. The sandstone unit suggests a change of conditions with current induced sedimentary structures and a coarsening of grain size. The water was no longer stagnant but its depth need not have been different than during the time of deposition of the black pelite unit. Greenberry Formation Elevation of the Greenberry limestone member of the Guyet Formation to a formation, as originally suggested by Johnston and Uglow (1926), is proposed. Sutherland Brown (1957) made the Greenberry a member of the Guyet Formation because he believed it was thin, discon- tinuous and volumetrically unimportant, but the Green- berry is more continuous than he thought, and is distinct from, and everywhere overlies, the conglomerate of the Guyet Formation. The Greenberry Formation consists of crinoidal lime- stone, and is locally altered to dolostone and chert. It is distinguished in the field from older limestone by its abun- dant crinoid fragments, but not so easily from the Sugar limestone of the Barkerville Terrane which is also crinoidal. The Greenberry Formation is poorly exposed, under- lying a narrow zone from Big Valley Creek in the north- west to Mount Tinsdale in the southeast. Any of its local- ities display the general characteristics of the unit and no type section is suggested. Its bedded character is best dis- played north and east of Tinsdale Creek. The Greenberry Formation is reserved for the Mississippian crinoidal limestone of the Cariboo Terrane. The Greenberry For- mation may be up to 30 m thick, but averages about 10 m thick. The lower contact is rarely exposed but where seen is sharp against a thin shale bed on Guyet Formation con- glomerate. It contains minor clasts of chert similar to 33