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Flora of the Lower Cretaceous Cedar Mountain Formation of Utah and Colorado, Part I

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Flora of the Lower Cretaceous Cedar Mountain Formation of Utah and Colorado, Part I Great Basin Naturalist Volume 43 Number 3 Article 3 7-31-1983 Flora of the Lower Cretaceous Cedar Mountain Formation of Utah and Colorado, Part I. Paraphyllanthoxylon utahense G. F. Thayne Bureau of Land Management, Salt Lake City, Utah W. D. Tidwell Brigham Young University W. L. Stokes University of Utah Follow this and additional works at: https://scholarsarchive.byu.edu/gbn Recommended Citation Thayne, G. F.; Tidwell, W. D.; and Stokes, W. L. (1983) "Flora of the Lower Cretaceous Cedar Mountain Formation of Utah and Colorado, Part I. Paraphyllanthoxylon utahense," Great Basin Naturalist: Vol. 43 : No. 3 , Article 3. Available at: https://scholarsarchive.byu.edu/gbn/vol43/iss3/3 This Article is brought to you for free and open access by the Western North American Naturalist Publications at BYU ScholarsArchive. It has been accepted for inclusion in Great Basin Naturalist by an authorized editor of BYU ScholarsArchive. For more information, please contact [email protected], [email protected]. FLORA OF THE LOWER CRETACEOUS CEDAR MOUNTAIN FORMATION OF UTAH AND COLORADO, PART I. PARAPHYLLANTHOXYLON UTAHENSE G. F. Thayne', W. D. Tidwell", and W. L. Stokes' Abstract.— ParapItyUantJwxijIon utahense, sp. nov., is described from the Cedar Mountain Formation and com- pared with similar fossil and modern woods. Fossil angiosperm woods from the Early Cretaceous are of great interest because very few have been reported from strata of this age. This species demonstrates that the angiosperms had de- veloped many of their modern characteristics by Early Cretaceous time. The Lower Cretaceous Cedar Mountain between 10 (3.1 m) and 30 (9.2 m) feet below Fonnation is fossiliferous at several localities. the overlying Dakota Sandstone, which is Fossils reported from this formation include represented by 10 (3.1 m) to 20 (6.2 m) feet the wood of conifers, Tempskya, and cyca- of coarse brown sandstone that forms a cap deoids, charophytes, pelecypods, gastropods, rock in the area. ostracods, and fish scales (Stokes 1952, Young 1960, Thayn et al. 1973, Tidwell et al. 1976), as well as dinosaur bones (Bodily 1969). A species of dicotyledonous wood assigned to the genus Paraphyllanthoxylon Bailey 1924, is described in this report from the Ce- dar Moimtain Formation. This is the first re- port of petrified dicotyledonous wood from the diverse flora in this formation. These angiosperm woods are of great interest in that very few Early Cretaceous angiosperm woods have been previously reported. Since the Cretaceous Period is the assumed time for the origin of the angiosperms, a tax- onomic study of Early Cretaceous angio- sperm wood is significant in that it expands oiu- knowledge of the early members of this division. The petrified wood described in this study was collected from two localities. Lo- cality 1 is 6 road miles (3.7 km) east of Castle Dale, Utah, and Locality 2 is 9 road miles (5.6 km) east of Ferron, Utah (Figs. 1, 5, 6, 7). The Cedar Mountain Formation at Local- ity 1 is composed of brown to grey shales. It contains at least one horizon of nearly coali- fied material from which Tempskya has been collected in growth position (Tidwell and Hebbert 1976). The dicotyledonous woods studied here were collected from a horizon Fig. 1. Index map of collection sites. 'Bureau of Land Management, Salt Lake City, Utah 84112. 'Department of Botany and Range Science, Brigham Young University, Provo, Utah 84602. 'Department of Geology, University of Utah, Salt Lake City, Utah 84112. 394 July 1983 Thayne et al.: Cretaceous Flora 395 Ulah Prove Fig. 3. ParaphijUanthoxijlon i/ta/iense— Ilhistration of the transverse section showing the relative abundance of ray tissue (dark areas) and the size, shape, and arrange- ment of the vessel elements (open circles). Note the radi- al pore multiples. Arizono (Fig. 2). Stokes (1952) defined two members of the formation, the Buckhorn Con- glomerate at the base and the Cedar Moun- tain Shale at the top. At the type locality near Castle Dale, Utah, the Buckhorn Con- Fig. 2. Geographic extent of the Cedar Mountain glomerate is thick and massive, but it gener- Formation (after Young 1960). ally thins to the east and is absent on the eastern side of the San Rafael Swell. East of Specimens were collected from seven dif- the Colorado River a mudstone and con- ferent logs at Locality where the Cedar 2, glomeritic sandstone unit occupies the same Mountain Formation consists of a bed of coarse white sandstone underlaid by channel fills of yellow conglomeritic sandstones alter- nating with grey-green shales. These are, in turn, underlaid by a dark green nodular weathering shale (Figs. 5-7). The Dakota Sandstone is missing at this particular site, but reappears in the section about 3 miles (1.9 km) to the southeast. Dicotyledonous woods were found associated with Tempskya and fossil conifer wood at this locality. Stratigraphy of the Cedar Mountain Formation Stokes (1944) defined the Cedar Mountain Formation as those sediments lying between the Brushy Basin Member of the Upper Juras- sic Morrison Formation and the Lower Cre- taceous Dakota Formation. These strata were formerly considered part of the Morrison Fig. 4. ParaphijUanthoxijlon lita/iense— Illustration of Formation. Cedar Mountain deposits are the tangential section showing the size, shape, and ar- present over much of eastern Utah, western rangement of the rays (dark lines) and a vessel element Colorado, and northwestern New Mexico (center). 396 Great Basin Naturalist Vol. 43, No. 3 W" -* site, the lithology. Fig. 5. Ferron collecting showing Fig. 7. Petrified dicotyledonous wood shown as it is A is white sandstone cap, B is the surface of the yellow found weathered upon the surface of the Ferron site. conglomeritic channel fill from which the specimens were recovered, and C is the underlying grey-green listed the formation as Aptian, but it shale. (1960) may be only Albian or, most probably, may include rocks of both ages. relative position as the Cedar Mountain For- mation on the west side of the river. These rocks were termed the "Post-McElmo" beds Paraphyllanthoxylon utahense sp. nov. (Coffin 1921), but were later renamed the Figs. 3-4, 8-18 Burro Canyon Formation (Stokes and Phoe- Description.— This species is described nix 1948). Young (1960) proposed that the from several pieces of black petrified second- Burro Canyon Formation and the Cedar ary wood. The preservation is excellent, and Mountain Formation are a physically contin- fine stRictural detail can be observed. uous unit and should both be referred to as Growth rings: Lacking. Cedar Mountain Formation. Vessels: Diffuse porous, approximately Based on the presence of the pelecypods 12 /mm 2, solitary or more commonly in radial Protoelliptio douglassi, Unio farri, and the rows (pore multiples) of 2-3 up to 5 cells conifer Frenelopsis varians, as well as the long; individual vessels range from 204 jum stratigraphic position of the Cedar Mountain radial by 165 jum tangential diameter to 58 Formation, Young (1960) as well as Stokes jum radial by 48 jum tangential, average 105 (1952), suggested that it is Lower Cretaceous jum radial by 93 jum tangential diameter; per- in age. Another indication of its age is the forations exclusively simple, located on presence of Tempskya, which Read and Ash oblique end walls; thin-walled tyloses abun- (1961) considered to be an index fossil to the dant, obscuring the vessel length; vessel walls Lower Cretaceous (Albian). Fisher et al. 3 ium-5 jum thick; tangential pitting with nu- merous, often appressed, 6 jum-10 /xm diame- ter; alternate bordered pits with slitlike aper- tures and occasionally up to 12 |u,m long, slightly bordered pits with large elliptic aper- tures probably representing the vessel to pa- renchyma pitting; radial intervascular pitting similar to tangential; vessel to ray inter- vascular pitting similar to tangential; vessel to ray pitting consisting of small circular or large, up to 24 jum, scalariform, elliptic to an- gular slightly bordered pits; 3-6, occasionally more, pits per crossover field. Fig. 6. Overview of the Ferron collecting site. Snow- Axial Parenchyma: Rare, apotracheal dif- capped mountains in the background are in the Wasatch fuse or scanty paratracheal. Plateau. Dicotyledonous logs along with Tempskya were Rays: 12/mm2, heterogeneous with both collected from tlie uppermost layer of sediment shown in the foreground. uniseriate and multiseriate present; uniseriate July 1983 Thayne et al.: Cretaceous Flora 397 Fig. 9. Transverse section illustrating distribution of vessels and multiseriate rays (30X). Diffuse porous wood; vessels in radial rows (pore multi- ples); exclusively simple perforations; alternate inter- vascular pitting; elongate vessel to ray pitting; rays of two sizes, 1-7 seriate, heterocellular with 107 rows of Fig. 8. Transverse section illustrating solitary vessels upright border cells, rays commonly over I high, ax- and vessel chains with tyloses. Note that the axial paren- mm ial parenchyma lacking or scanty apotracheal diffuse, chyma is scarce (65X). scanty paratracheal, or combination of both; septate fibretracheids; vessels commonly with tyloses. rays rare, many partially biseriate, with both Paraphijllanthoxijlon utahense fits well with- procmnbent and upright cells, uniseriate rays in the boundaries of this genus. range from 2 cells (80 jum) to 6 cells (300 jum) high (average 5 cells, 200 jam-220 jum); mul- Comparison with tiseriate rays range from 9 cells (380 jum) to Described North American Species 33 cells (1360 [xm) high and 2 cells (30 jum) to 5 cells (100 jum), wide with 106 rows (com- Three species of ParaphyUanthoxylon have monly 2) of upright border cells; procumbent been described from Cretaceous strata in cells range from 25 jam-40 jum vertical, 50 North America. jum-80 jLim radial, and 25 jum-45 jUm tan- ParaphyUanthoxylon arizonense Bailey gential diameter; some cubodial cells present, 1924.—ParaphyUanthoxylon utahense differs approximately 40 jum in diameter; upright from the upper Cretaceous P.
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