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DEPARTMENT OF THE INTERIOR UNITED STATES GEOLOGICAL SURVEY GEOLOGY OF THE SEDIMENTARY ROCKS OF. THE MORRISON QUADRANGLE COLORADO By J. Hiram Smith MISCELLANEOUS GEOLOGIC INVESTIGATIONS MAP I-428 PUBLISHED BY THE U. S. GEOLOGICAL SURVEY WASHINGTON, D. C. ~ 1964 ::s< DEPARTMENT OF THE INTERIOR TO ACCOMPANY. MAP 1-. 428 UNITED STATES OEOLOOICAL SURVEY GEOLOGY OF THE SEDIMENTARY ROCKS OF THE MORRISON QUADRANGLE, COLORADO By J. Hiram Smith The Morrison quadrangle is in Jefferson County, interbedded volcanic flows of early Cenozoic age. These about 10 miles west of Denver, Colo. The rugged west­ rocks are mantled by alluvium and colluvium of Quater­ ern one-third of the quadrangle along the eastern flank nary age. The sedimentary rocks consist of 15 for­ of the Front Range is underlain by Precambrian crys­ mations that range in age from Pennsylvanian toTer­ talline rocks. The eastern two-thirds, with which this tiary (table 1) and have a combined thickness of about account is concerned, lies in the Colorado Piedmont 13,000 feet. The contact of the Precambrian crystal­ section of the Great Plains and is underlain by sedi­ line rocks with the overlying Fountain Formation is mentary rocks. Prominent topographic features on sharply unconformable, and locally the crystalline the plains include (1) the long sinuous hogback formed rocks beneath it are deeply weathered. by the Dakota Group; (2) South Table Mountain, a broad Paleozoic sedimentary rocks.--The Paleozoic is relatively flat mesa at the north edge of the quadrangle; represented by the Fountain Formation, Lyons Sand­ (3) Green Mountain, a broad gently rounded conspicuous stone, and part of the Lykins Formation. The Foun­ eminence in the east-central part of the quadrangle; tain and Lyons are resistant to erosion and form bold and (4) Mt. Carbon, a flat-topped remnant of a middle outcrops. The contact between them is gradational, Pleistocene pediment south of Bear Creek. The prin­ the characteristic lithologies of the two formations cipal streams-Clear Creek, which crosses the north­ interfingering within a 30-foot transition zone. The west corner of the quadrangle, and Mount Vernon and Lykins Formation was subdivided by LeRoy (1946) Bear Creeks -have cut deep canyons in the Front into three shale members separated by two thin lime­ Range. Clear Creek and Bear Creek flow eastward stone members. The uppermost orStrainShaleMem­ from the mountain front across the sedimentary rocks ber constitutes about two-thirds of the formation; its of the Piedmont and into the South Platte River, but upper part is of Triassic(?) age. Most of the Lykins Mount Vernon Creek is diverted by the hogback formed is not resistant to erosion, and, except for the Glennon by the Dakota and empties into Bear Creek at Morri­ Limestone Member, forms· a broad valley. The Glen­ son. non forms a narrow sharp hogback. The basal contact The author has benefited from many discussions of the Lykins probably is disconformable. The Lykins with Richard Van Horn. Dr. H. D. MacGinitie of Hum­ is the brightest red bed in the quadrangle. boldt State College contributed helpful suggestions con­ Mesozoic sedimentary rocks.--Rocks ofMesozo­ cerning the Cretaceous-Paleocene boundary and iden­ ic age include those from the upper part of the Lykins tified fossil leaves from the Denver and Green Moun­ Formation to the lower part of the Denver Formation. tain Formations. The Cretaceous invertebrate fossils The lower contact of the Ralston Creek Formation is were identified by W. A. Cobban, and the zones of the not exposed but is disconformable in adjoining areas. Pierre Shale were mapped by G. R. Scott. Scott and The dis conformity marks a hiatus encompassing Early, Cobban collected most of the fossils by which the zones Middle, and part of Late Jurassic time. The Ralston of the Pierre Shale were mapped. Creek locally forms a low ridge. The Morrison For­ Geologic observations in this area were made as mation forms a steep smooth slope interrupted by small early as 1869 by the Hayden Survey, but the earliest ledges of sandstone and limestone. A basal sandstone comprehensive geologic study was made by Emmons, of the Morrison locally lies in channels in the Ralston Cross, and Eldridge ( 1896). More recent studies were Creek Formation and indicates a minor unconformity. made by Johnson ( 1931) on paleontology, Lovering and Near Morrison, the formation has yielded many fossil Goddard (1938) and Waldschmidt (1939) on the Table bones of giant dinosaurs (Marsh, 1877). Mountain flows, LeRoy (1946) and Van Horn (1957) on The Dakota Group was divided by Waag~ (1955, general geology, Brown (1943) and Reichert (1954) on p. 18-19} into the Lytle and South Platte Formations, the Tertiary sedimentary rocks, Waag~ (1955) on the and the South Platte was subdivided into five members. Dakota Group, Scott and Cobban (1959) on the Pierre Although all these units are recognizable locally in Shale, Maughan and Wilson (1960) and Hubert (1960) on the Fountain and Lyons Formations, and Berg (1962) the Morrison quadrangle, they were not mapped sep­ on the Golden fault. arately. Almost the entire group is exposed along the Alameda Parkway, but eisewhere exposures are incom­ The bedrock of theMorrison quadrangle com­ plete. The basal contact iR disconformable, the lower­ prises Precambrian metamorphic and intrusive rocks, most conglomerate beds of the :Ly~Ie lying in channels which were not mapped, sedimentary rocks of Paleo­ cut into the Morrison. Sandstone units in the Dakota zoic and Mesozoic age, and sedimentary rocks and Group form a prominent hogback. The Benton Shale contains recognizable equiva­ lying Laramie. The conglomerate is regarded as an lents of the Graneros Shale, Greenhorn Limestone, and orogenic deposit derived from the rising Front Range Carlile Shale but was mapped as a single unit because on the west. The Denver Formation is exposed only of poor exposures. The Benton forms a broad east­ on steep slopes and in gullies. The base of the for­ ward-sloping belt between the hogback of Dakota and mation is selected at the base of the lowest bed con­ one made of limestone at the base of the Niobrara For­ taining andesite pebbles and probably is disconform­ mation. The Benton is conformable and transitional able. with the underlying Dakota. Cenozoic rocks.--Rocks of Cenozoic age consist The Niobrara Formation is divided into the Fort of the upper part of the Denver Formation and the Hays Limestone and Smoky Hill Shale Members. The Green Mountain Conglomerate of LeRoy (1946). The Fort Hays forms a small sharp hogback, arid chalk upper part of the Denver Formation includes inter­ beds in the middle and at the top of the Smoky Hill bedded flows of latite, which form a gently sloping cap form low ridges locally. The basal contact of the Nio­ on South Table Mountain. To the north, in the adjoin­ brara is disconforrhable. ~ohnson (1930, p. 789) re­ ing Golden quadrangle, Van Horn (1957) distinguished ported phosphatic nodules and other evidence of a dis­ three such flows, but only the two he designated as conformity near P u e b 1 o, Colo., and Cobban and numbers 2 and 3 are present in the Morrison quad­ Reeside (1952, p. 1029 ahd chart lOb) showed that sev­ rangle. The Green Mountain Conglomerate crops out eral fossil zones known in other areas are absent at only on the upper slopes of Green Mountain. The base the contact along the "Front Range. of the formation is marked by trees which grow there because· water seeps from the conglomerate. The ba­ The Pierre Shale, by far the thickest formation in the quadrangle, is easily eroded and poorly exposed, sal contact probably is conformable and is marked by a change in the composition of the gravel, from pre­ although a part of the Hygiene Sandstone Member, in the middle part of the formation, locally forms a hog­ dominantly andesitic in the Denver to predominantly granitic in the Green Mountain, back. The Pierre grades into the underlying Niobrara. A persistent ledge-forming limestone bed is regarded The Morrison quadrangle is on the east limb of as the top of the Niobrara, and nearly 100 feet of cal­ the large north-trending Front Range anticline. Sed­ careous shale above it is assigned to the Pierre. Fau­ imentary rocks therefore dip sharply eastward at the nal zones within the Pierre Shale have been depicted mountain front, but they flatten abruptly eastward and on the map with the aid ofW. A. Cobban and G. R. Scott. generally dip gently beneath the plains (section A-A'). In order of increasing age, these zones are: The Golden fault.--The Golden fault, the most Baculites clinolobatus Elias prominent in the area, crosses the quadrangle from Baculites grandis Hall and Meek northwest to southeast, It is a reverse fault that dips Baculites baculus Meek and Hayden west at an angle of 45°, or more, and has a predomi­ Baculites eliasi Cobban nantly dip-slip component of movement. The fault Baculites cuneatus Cobban locally includes wedges of sedimentary rock. Minor Didymoceras cheyennense (Meek and branch faults extend northwest from the main fault Hayden) and one can be traced into the Precambrian rocks. Didymoceras stevensoni (Whitfield) Strata on both sides of the fault commonly are over­ Didymoceras nebrascense (Meek and turned. Hayden) Stratigraphic throw of the fault decreases from Baculites scotti Cobban 8,000 feet where the Fountain is against the Pierre, Anapachydiscus complexus (Hall and Meek) at the north edge of the quadrangle, toO near Mt. Car­ Baculites gregoryensis Cobban bon, where the fault is in the Pierre and all the faunal Baculites perplexus Cobban zones of the Pierre are present. From Mt. Carbon Baculites asperiformis Meek (called B. northward, the fault roughly parallels the uppermost obtusus in the broad sense in the adjoin­ or Baculites clinolobatus faunal zone but cuts strati­ ing Indian Hills quadrangle) graphically downward across the older faunal zones, The Fox Hills Sandstone makes a low hogback at and finally, across older formations.

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