No abstract

Reconstructs glacial history of the area (approx. 68-69 30 N, 147-162 W) on the basis of observations during 1944-1953 of the nature and extent of glacial deposits in the central part of the Range between Shainin and Itkillik Lakes and in the southern part of the Foothills Province from the Shaviovik River west to Etivluk River. Distribution is mapped and characteristics described of deposits from six glaciations for which a tentative chronological sequence is established: Anaktuvuk and Sagavanirktok of Pre-Wisconsin age; Itkillik and Echooka of Early Wisonsin; Alapah Mountain of Late Wisconsin; and Fan Mountain of Recent age. Terrace deposits and Pleistone alluviations are mentioned.

The 7,500-8,000-foot-thick Paleozoic section exposed in the Shainin Lake area, central Brooks Range, northern Alaska, is divided into 5 formations, 4 of which have not been described before. The 3,300-foot-thick, probably nonmarine, Kanayut conglomerate (new name), of Late Devonian age, overlies an unnamed shale and sandstone, also of Late Devonian age. Massive lower and middle members of the Kanayut conglomerate are 1,400 and 1,030 feet thick, respectively. The upper, 860foot-thick, Stuver member (revised name), consists of alternating beds of shale, orthoquartzitic sandstone, and orthoquartzitic conglomerate.The overlying Kayak shale (new name), 960 feet thick, consists of black shale with a quartzose sandstone member at the base and argillaceous-limestone beds, which contain early Mississippian fossils, in the upper part.The Lisburne group (revised name), about 2,200 feet of fossiliferous bioclastic limestone and dolomite, is composed of 2 formations. The Wachsmuth limestone (new name), the lower 1,230 feet of the Lisburne, is predominantly cherty limestone and dolomite with some shale. Early Mississippian corals, echinoderms, bryozoans, and brachiopods occur sporadically throughout. The Alapah limestone (new name), the upper 970 feet of the Lisburne, is limestone with some chert and is characterized by late Mississippian lithostrotionoid corals and Gigantoproductus.Topmost beds of the Lisburne group are covered by high-level gravel deposits; the contact with overlying Permian or Triassic rocks is not exposed. Structurally the area is characterized by imbricate thrust faulting and high-angle reverse faulting. Mississippian rocks apparently represent platform-type deposition in an east-trending late Paleozoic seaway.11952, Stratigraphy and paleontology of the Noatak and associated formations, Brooks Range, Alaska: Yale Univ., unpublished doctoral thesis, 209 p., 18 pis., 13 figs.EXPLORATION OP NAVAL PETROLEUM RESERVE NO. 4, ALASKA, 1944-53 * The terms "early" and "late" Mississippian are used here in the broadest sense, encompassing together the entire span of the Mississippian.

A new genus and two new species of late Paleozoic edrioasteroids, Giganticlavus bennisoni and G. gelasinus, are described from the Early Pennsylvanian of Oklahoma and New Mexico. Giganticlavus differs from other clavate edrioasteroids by its large size, extreme ambulacral length and ambital overlap, extreme thickness of interambulacral and recumbent zone plates, and the tessellate nature of the recumbent zone plating. The extreme length of ambulacra and thickness of the plating are interpreted as adaptations for increased size and rigidity.

Reef complexes of Mississippian, Pennsylvanian, and Early Permian age are conspicuous in the western escarpment of the Sacramento Mountains of southeastern New Mexico (Fig. 1). The coincidence of reef trends and the fault zone at the western front of the Sacramento Mountains appears to be significant. The basement fault zone on the western edge of the Sacramento block created platform margins along which Paleozoic shelf-edge reefs accumulated. Facies in Late Paleozoic formations were strongly controlled by structural trends in the Precambrian basement rocks. The Sacramento escarpment lies parallel to and adjacent to the western margin of the "Pedernal Landmass” (Pray, 1961) that trends northerly, as do the Sacramento Mountains. The La Luz Anticline (Pray, 1961) in the northern part of the Sacramento Mountains plunges to the north(Fig. 1). Beds on the west limb dip 8 to 12 degrees. Numerous deep canyons off this west flank expose thick sequences including nearly all the Paleozoic formations. Exposures perpendicular to the reef-trends thatare available in these canyons (Fig. 2) are unique. Facies Figure changes in the reef complexes are readily available to the field geologist. This area of the Sacramento Mountains is of extreme importance to students of carbonate rocks because of the excellent, numerous, and distinct exposures of the reef complexes.