Depositional Environments of the Mississippian ...

R O C K Y R W N T A ' L SECTION, S . E . P . M . R A T E N Z P K PAIEPFTPGPAHLY OF ® T - ' " E T I W . ! . (F)ITH> STATES H E S T - R E R W L U I I T E D STATES

EOTEOGPAPHY S Y T T O I H I 1

T, D. KUH AND E. R. WATrlA'l, ETJITORS EJVER, COLORADO, J L f E 1 9 8 0

DEPOSITIONAL ENVIRONMENTS OF THE MISSISSIPPIAN REDWALL LIMESTONE IN NORTHEASTERN ARIZONA

W . Norman Kent and Richard R. Rawson Union Oil Co., Box 6247, Anchorage, Alaska 99502; and Geology Department, Northern Arizona University, Flagstaff, Arizona 86011

ABSTRACT

(fig. 1). Noble (1922) redefined the Redwall to its present configuration which includes all rocks of Mississippian age. Gutschick (1943) subdivided the Redwall into four informal members and in 1963 McKee formally named these members in ascending order: The Whi.tmore Wash, Thunder Springs, Mooney Falls, and Horsehoe Mesa Members {fig. 2). McKee and Gutschick (1969) later presented one of the most inclusive and definitive works on the Redwall. Many other paleontologists and stratigraphers too numerous to mention here, have contributed to the understanding of the Redwall and have been cited by McKee and Gutschick (1969). More recent work by Smith (1974), Kent (1975), and Purves (1976) has focused on facies analysis of the Redwall Limestone. The work of Smith (1974) and Kent (1975) form the basis of this paper.

Facies analysis of the Redwall Limestone suggests two major transgressive sequences in northeastern Arizona. The first major transgression of the sea spread slowly from the west and was followed by a rapid regression. The second major transgression consisted of three rapid transgressions in northeastern Arizona separated by relatively slow partial regressions caused by prograding sedimentation. Facies geometry of the first transgression best fits the Shaw-Irwin model of epeiric deposition with welldeveloped transgressive and regressive facies whereas the second transgression best fits Coogan's asymmetrical model of epeiric deposition with poorly developed transgressive facies. Textural analysis of the Redwall Limestone to determine facies relations and depositional environments included differentiation of the carbonate grain types into the following textural rock types: dolomite, stromatolitic wackestone, pi soli ti c wackestone, calcispheric packstone, pelletal packstone, oolitic packstone and grainstone, foramini feral grainstone, crinoidal grainstone and packstone. These textural rock types may be grouped into four depositional facies: Facies I, crinoidal packstone--open marine; Facies II, crinoidal and foraminiferal grainstone-open "intratidal"; Facies III, oolitic grainstone and packstone, and pelletal packstone—protected "intratidal"; Facies IV, algal (calcispheres, stromatolites, pisolites) packstone and wackestones and dolomite--supratidal.

U

T

A

H

INTRODUCTION The Redwall Limestone in northern Arizona was deposited on a cratonic shelf during the Mississippian Period. This shelf was subject to at least four marine transgressions and regressions. The depositional dynamics of the Redwall in northern Arizona are demonstrated in this paper by facies analysis of carbonate rock textures.

INDEX MAP 0

20mi

0

33km

Previous Work Figure 1. Index map showing the area discussed in this paper, including type sections, well control, and major cities. See figure la for list of wells used for stratigraphic control.

The Redwall Limestone, named by Gilbert in 1875, originally included rocks both older and younger than Mississippian in age. Darton (1910) selected a type section in a canyon of the Shinumo drainage basin of the Grand Canyon and named the canyon "Redwall Canyon"

101

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KENT AND RAWSON Well 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32

Name

Location

Texaco 1 Navajo Mobil 1 Navajo Cactus 1 Navajo Buttes 1-14 Navajo Gulf 1 Navajo-Texaco Amerada 1 Navajo Wilson-Cranmer 2 Gulf 1 Navajo Pan Am 1 N.M. & A LD Tenneco 1 Fed B Tenneco 1 Navajo Skelly 1 Hopi Amerada 1 Hopi Atlantic 9-1 Hopi Texaco 1 Hopi - A General Pet 14-6 Pan Am 1 Aztec - A Pan Am 1 Aztec - B Eisele 1 McCauley Tenneco 1 X Sinclair 1 Navajo Underwood 1-32 Jacob L. Collins - Cobb 1-X Lockhart 1 Babbit Black Mesa 1 Stat. 3 Ray Terry 1 State Pickett 1 Padre Canyon Willet 1 State Stienberg 1A Flowalt Eastern Moqui Bardo Cathedral 1 Fed Western 1 Valen-Fed.

Sec- 16- 41N- 25E Sec- 26- 39N- 25E Sec- 23- 36N- 24E Sec- 14- 07N- 09W Sec- 11- 04N- 07W Sec- 03- 31N- 23E Sec- 21- 02N- 06W Sec- 21- 29N- 24E Sec- 12- 13N- 25E Sec- 04- 10N- 24E Sec- 24- 38N- 19E Sec- 35- 30N- 17E Sec- 08- 29N- 19E Sec- 09- 29N- 15E Sec- 15- 26N-• 16E Sec-•06- 19N- 23E Sec- 05- 16N- 20E Sec-•09- 16N-•18E Sec-•01- 16N-•16E Sec-•31- 10N- 21E Sec-•28-•37N-•14E Sec- 32-•39N-•02E Sec-•22-•34N-•08E Sec-•21-•27N-•09E Sec-•27-•25N-•02E Sec-•34-•25N-•08W Sec-•26-•20N-•10E Sec-•24-•20N-•05E Sec-•24- 19N-•10E Sec- 10- 14N- H E Sec-•16-•17N-•05E Sec-•31-•38N-•05W

490'

150m

67'

20m

245

75m A A A BEDDED C H E R T A CHERT NODULE

^ PELLET STROMATOLITE

9> FORAW ® OOJD

)f CRIN01D ^

FOSSILS

iJS FOSSIL MOLD

-UCOJfrORMlTY 27m

88'

Figure la. List of 32 wells and locations used for stratigraphic control. See figure 1 for location of wells.

27m 1 5 - r 5 0 '

J

O-LO'

Methods

Figure 2. Stratigraphic section of the Redwall Limestone on the south Kaibab Trail, Grand Canyon (After McKee, 1969, and Kent, 1975).

Our findings are largely the result of detailed petrologic studies of well samples and cores from 32 wells located in northeastern Arizona (see fig. 1). Detailed descriptions of carbonate rock textures are based on Dunham's (1962) classification. Textural rock types are grouped into mappable facies using subsurface well control. The Shaw (1964)-Irwin (1965) epeiric sea model proved to be very useful for explaining the dynamics of Redwall deposition and for establishing time surfaces for constructing facies maps and- interpreting the depositional history.

N E V A D A

9

50

Antler Highland

A

100

' F E W

Flyaeh

Trough

Cratonic

Shelf

MONTE CRISTO GROUP PEERS SPRING FORM. - CHAIlOlAa SHAI2 - JOAWA LIMESTONE

STRATIGRAPHY The Redwall Limestone was deposited on a cratonic shelf that covered an area extending from the hinge line near the Nevada-Arizona border into New Mexico (fig. 3). The shelf extended through much of the Rocky Mountain region during Mississippian time (Rose, 1976). The Redwall in northern Arizona includes most all of the rocks formed on this shelf during Mississippian time. At the type section in Redwall Canyon (fig. 1), the Redwall unconformably overlies the Cambrian Muav Limestone, but nearby, it locally overlies channelfill deposits of the Devonian Temple Butte Limestone.

M E X I C O

ISO 2 0 0 2 SO KM

I

NBYADA ! UTAH | COLORADO ^ I

Figure 3. Cross section from Nevada through northern Arizona into New Mexico showing the relationship of the Redwall Limestone to other Mississippian units to the west (From Rose, 1976).

102

MISSISSIPPIAN REDWALL LIhESTCME IN NORTHEASTERN ARIZONA In central and northwestern A r i z o n a , the Redwall was deposited unconformafaly on the Devonian Martin Form a t i o n , and in northeastern Arizona overlies the Devonian Ouray Limestone. The Redwall Limestone is conformably overlain by the Pennsylvanian.Molas Formation in the subsurface of northeastern Arizona and by the Pennsylvanian Watahomigi Formation (Supai G r o u p , M c K e e , 1975) in central and northwestern Arizona. Figure 1 is an index map of the area covered by this paper and figure 4 shows the isopachs of the "Redwall Limestone for this area. Other isopach and facies maps in this paper cover the same area shown on the index m a p .

View Point (fig. 1). McKee (1963) measured 12 m (38 ft) at the type section and described the rock as being mostly aphanitic limestone. Kent (1975) had difficulty recognizing the member in the subsurface due to post-Redwall pre-Supai dissolution, w e a t h e r i n g , and erosion removing much of the unit.

Whitmore Wash Member The type section is located (fig. 1) in the study area just north of the Colorado River in Whitmore Wash on the upthrown side of the Hurricane Fault where McKee and Gutschick (1969) measured 31 m (101 ft) of thickly bedded, f i n e - g r a i n e d dolomite. In other areas lime m u d s t o n e s , pisolites, peloids, and skeletal fragments have been reported from this member (Kent, 1975; S m i t h , 1974). The Whitmore Wash ranges in thickness from an erosional zero edge (fig. 5) in the east to a maximum thickness of over 60 m (200 ft) at Iceberg Ridge near the Arizona-Nevada border on the Colorado River. Thunder Springs Member The type section is located (fig. 1) in the .study area at the head of Thunder River, about 3 km (2 m i ) north of the Colorado River in central Grand Canyon (McKee, 1963). McKee described the member as consisting of thin-bedded carbonate rock and interbedded chert. In the subsurface of northeastern A r i z o n a , this member is typically a coarse-grained dolomite with interbedded tripolitic chert (Kent, 1975). The isopach map (fig. 6) of the Thunder Springs indicates a thickening to the north. Kent reports a thickness of 71 m (235 ft) from the Underwood 1-32 Well (Sec. 3 2 , T 3 9 N , R2E) drilled near Jacob Lake on the Kaibab Plateau (Well no. 2 2 , fig. 1).

Figure 4. Isopach map of the Redwall Limestone. See figure 1 for well control (black circles).

Mooney Falls Member The type section is located (fig. 1) in the study area in Havasu Canyon at Mooney Falls 6.7 km (4 m i ) south of the Colorado River on the Havasupai Indian Reservation. McKee (1963) measured 95 m (312 ft) of Mooney Falls at the type section. Kent (1975) reported approximately 137 m (450 ft) of this member in the Western #1 Valen-Fed. well located in s e c . 3 1 , T. 38 N . , R. 5 W . (fig. 7). At the type section McKee and Gutschick (1969) described skeletal limestone with dolomite beds near the base. In northeastern Arizona Kent (1975) reported an abundance of grain types including a l g a e , p e l l e t s , o o i d s , foraminifers, and crinoids. The absence of chert in the member helps distinguish it from the underlying Thunder Springs Member (McKee and Gutschick, 1969, and Smith, 1974).

Figure 5. Isopach map of'the Whitmore Wash Member (After Kent, 1975). See figure 1 for well control (black circles).

Horseshoe Mesa Member The type section is located at Horseshoe Mesa on the south rim of the Grand Canyon below Grand

103

KENT AND RAWSON of northeastern Utah and northwestern Colorado depositing the Doughnut Formation (Rose, 1976).

U T A H

Age and Correlation McKee and Gutschick (1969) concluded that the age of the Redwall ranges from late Kinderhookian to Chesterian based on fossil work done by themselves and others. The Redwall correlates with the Madison, Leadville, Escabrosa, Lake Valley, and Monte Cristo Formations or Groups of the Rocky Mountains and Great Basin.

PETROLOGY The Redwall Limestone includes a variety of limestone and dolomite types. Smith (1974) and Kent (1975) have classified these types into two major categories: non-skeletal and skeletal. Non-skeletal types include those composed of pellets, o o i d s , pelo i d s , lime m u d s t o n e , intraclasts, lithoclases, dolomite mudstone, stromatolites, and pisoliths. Skeletal types include crinoids, foraminifers, bryozoans, ostracodes, brachiopods, bivalves, gastropods, cora l s , arthropods, and calcispheres. Kent (1975) recognized ten textures in the Redwall as having depositional significance. These include the following: dolomite mudstone, stromatolitic wackestone, pi sol l ti c wackestone, calcispheric packstone, pelletal packstone, oolitic packstone, oolitic grainstone, foraminiferal grainstone, crinoidal grainstone, and crinoidal packstone. Each one of these textures is described briefly below.

Figure 6 . Isopach map of the Thunder Spring • Member (After Kent, 1975). See figure 1 for well control (black circles).

Dolomite Grain size is less than 0.1 rim and the rock is light brown to light gray in color. It may be laminated or contain peloids. This textural type is found at the base of two transgressive depositional units in the Redwall. The dolomite by-facies relationships is interpreted as having formed in a supratidal or sabkha environment. Stromatolitic Wackestone Figure 7. Isopach map of the Mooney Falls Member (After Kent, 1975). See figure 1 for well control (black circles).

Stromatolites are not abundant in the Redwall, but are found a t the base of the Whitemore Wash and within the Mooney Falls Members. Although widespread in several modern environments, stromatolitic textures are rarely preserved in rocks except in the high intertidal to supratidal environment. In other environments they are destroyed by burrowing organisms. The stromatolitic wackestone overlies the dolomite and is considered to have formed in or near a supratidal environment.

Post-Horseshoe Mesa Member A fifth, unnamed member has been found in channels cut into the Horseshoe Mesa Member. McKee and Gutschick (1969) reported a Chesterian fauna from an uppermost limestone in the Redwall near the Bright Angel Trail on the south rim of the Grand Canyon. Later work by Skipp and McKee (1978) and Billingsley (1979) has verified a late Chesterian transgression that filled erosional channels in the Horseshoe Mesa Member with marine limestones containing Chesterian fossils. This transgression appears to be widespread and may correspond in time with similar transgressions that occurred in the Williston Basin forming the Big Snowy Group (Rawson, 1968) and in the Doughnut Trough

Pisolitic Packstone Pisolitic packstone consists of pisoliths and pellets in a matrix of micrite or neomorphic spar. Pisoliths are rare in the Redwall. Where found, they consist of a core of intraclasts or peloids surrounded by irregular crenulated laminations. The pisoliths range in size from 2 m m to 5 m m . They appear to be algal in origin and are not similar to Dunham's (1969)

104

MISSISSIPPIAN REDWALL LIhESTCME IN NORTHEASTERN ARIZONA vadose pisolites. The pi soli ti c packstone is interpreted as having formed in pools within the protected upper neritic zone in which wind-generated currents were able to roll the grains about.

Crinoidal

Grainstone

Crinoid ossicles represent the m o s t abundant skeletal components of the Redwall Limestone. They range in size from 1 mm to 4 m m . Crinoidal grainstone may also contain an abundance of bryozoans, foraminifers, and various other skeletal grains. The lack of micrite suggests that winnowing by currents.

Calcispheric Packstone Calcispheres consist of a thin w a l l , surrounding a spherical chamber filled with sparry calcite. Outside diameter is about 0.5 m m . The origin of these grains is unknown. Rupp (1967) suggested that the smooth forms closely resemble the reproductive cysts of modern dasycladacian Acetabularia. These grains are also found in the crinoidal and pelletal packstones. This rock type in the Redwall includes a mixture of pellets and algal structures and is interpreted as having been formed, in a lateral and vertical sense, between the pisolitic and pelletal packstones. The environment of deposition was a lowenergy neritic zone.

Crinoidal

Packstone

In this rock type the components are crinoid ossicles, fossil debris, pellets, and micrite. The presence of micrite and associated components would suggest along with spatial relationships to other rock types that this was formed seaward of the crinoidal grainstone.

FACIES ANALYSIS Pelletal

Packstone

From the analysis of rocks in a vertical seq u e n c e , the rock types discussed above can be grouped into four facies. that have environmental significance Kent (1975). Walther's Law of Facies indicates that only those facies can be superimposed that can be observed laterally adjacent at the present time (Middlet o n , 1973). Studies of recent carbonate sediments indicate that rock textures that occur vertically in the Redwall do exist adjacent to each other in modern carbonate environments. One exception is the crinoids which are uncommon in shallow-water nearshore environments.

This rock type consists of grain-supported pellets and fossil debris (brachiopods, ostracodes, etc.) with intergranular m i c r i t e . Pellets are roughly elliptical with no internal structure. Average diameter ranges from 0.1 mm to 0.25 m m . The pellets formed in a n e r i t i c , moderate-energy environment with abundant animal life. Micritic envelopes were formed on skeletal fragments associated with this texture, indicative of algal bores (Bathurst, 1975).

Oolitic Packstone

The four facies, their respective textural types and inferred environments of deposition (see fig. 8) in the Redwall are: Facies I. Crinoidal p a c k s t o n e — open marine; Facies II. Crinoidal and foraminiferal g r a i n s t o n e — o p e n "intratidal"; Facies III. Oolitic grainstone and packstone, and pelletal p a c k s t o n e — protected "intratidal"; Facies IV. Algal (calcispheres, stromatolites, pisolites) packstones and wackestones and d o l o m i t e — s u p r a t i d a l . (The term "intratidal" as used here is defined as that area subject t o w a v e and tidal effects but not exposed as in the intertidal zone.) Facies I developed seaward below wave base. Facies II and III were formed in a zone between wave base and the landward limit of the tidal effect. Facies IV formed in a zone landward from the effects of marine-generated waves and tides.

The rock type is composed of o o i d s , pellets, and fossil debris including crinoids. Ooids are usually cream or yellowish white in color in well samples. Most nuclei are crinoid ossicles, but in the Mooney Falls Member some ooids contain foraminifers as nuclei. Ooid diameters in the Redwall usually range from 0.2 mm to 1.0 m m . The oolitic packstones formed where wave energy or currents were capable of conveying ooids shelfward into a lower energy environment. The lower energy of this environment is indicated by the presence of intergranular micrite. Oolitic Grainstone The oolitic grainstones are composed almost-exclusively of ooids cemented by sparry calcite. In places uncoated crinoids or other fossil fragments are found in association. This rock type is interpreted as having formed in an environment of strong marine currents and wave action as indicated by the absence o f m i c r i t e . Foraminiferal

DEPOSITIONAL MODELS Two models appear to best fit the data from the Redwall: the Shaw (1964)-Irwin (1965) epieric sea model (fig. 9) and Coogan's (1972) asymmetric carbonate cycle (fig. 10). The Redwall was deposited in two major transgressive-regressive cycles. The lower cycle deposited the Whitmore Wash and Thunder Springs Members. The Mooney Falls and Horseshoe Mesa Members constitute the upper depositional cycle. Both cycles are marine and have similar facies, but the manner in which the facies were displaced indicates a difference in depositional dynamics.

Grainstone

Laterally and vertically the foramini feral grainstones are found between the oolitic grainstones and the crinoidal grainstones which may indicate that foraminifers were able to inhabit areas of higher energy than crinoids. The types and abundance of foraminifers in the Redwall were well covered by Skipp in McKee and Gutschick (1969).

105

KENT AND RAWSON

FACIES

^

Figure 8. The relation of depositional textures to environments of deposition and resulting depositional facies. Facies patterns of right column are used on other figures (Figures 10 through 17).

ENERGY ZONES

hundreds o f miles wide

tens o f miles wide

X LOW ENERGY (marine currents)

HIGH ENERGY (waves and t i d e s )

SEDIMENTATION ZONES I RUIN'S

I s i l t size skeletal fraynents

IDEAL

11 sand size skeletal fragments

Figure 10. Comparison of the Irwin (1965) and Coogan (1972) models for carbonate rocks using the facies developed for the Redwall Limestone. See figure 8 for facies patterns.

tens to hundreds o f miles wide

ENVIRONMENT

Z LOW ENERGY ( l i t t l e circulation;tides r e s t r i c t e d seaward; absent Shoreward; local storm wave action only) sediments b a s i c a l l y chemical

wave base III

IV

algal & skeletal carbonates grading from sand-----nud

penecontempo raneo us chalky dolomite

LIMESTONE

*—crinoidal ooli tic grainstones

•

pelletal— —skeletal packs tones

algal packs tones

SHELF

marine

v

open intratidal protected

oolites--pel1ets

crinoidal pelletal packs tones

SHELF EDGE

open

CASE

REDWALL

Regression

intratidal dolomlte

eroded

supratidal ^

Figure 11. Schematic cross section of idealized lower depositional cycle of the Redwall Limestone showing relationship of the Ouray Limestone to the Redwall. Lithofacies are shown along with two time lines, R1 and T1 (After Kent, 1975).

Figure 9. Comparison of Irwin's model to the Redwall facies sequence (After Irwin, 1965, and Kent, 1975). Lower Depositional Cycle

gressions (compare fig. 13 with figs. 15, 16, 17). Throughout much of northern Arizona the Thunder Springs Member is dolomitized and the overlying Mooney Falls is not. Much of the dolomite in the Thunder Springs appears to be late diagenetic dolomite as evidenced by the relics of typical marine facies being dolomitized. It appears that the dolomitization occurred after the transgression of the sea that deposited Thunder Springs. Along and beneath the surface of the exposed carbonate rocks ideal conditions would have existed to promote dolomitization by the mixing of marine and fresh water as proposed by Badiozamani (1973) in his Dorag dolomitization model.

The transgression that occurred during the lower depositional cycle crossed a peneplain. Kent (1975) suggested that there was a minor regression of the sea prior to the major Redwall transgression. Once the sea had reached its maximum transgression a regression and/or progradation occurred as illustrated in Figure 11. The facies reversal at the base of the Redwall (R-l) and the major reversal after maximum transgression (T-l) provide two time surfaces (Irwin, 1965) upon which facies maps have been constructed (see figs. 12, 13). The major transgression that occurred during the lower cycle was the most extensive of Redwall trans-

106

MISSISSIPPIAN REDWALL LIhESTCME IN NORTHEASTERN ARIZONA

Upper Depositional Cycle The depositional textures of the Mooney Falls suggest that transgression was fairly rapid and regression and/or depositional progradation was comparatively slow. Facies were not established until maximum transgression was attained and then as progradation of sediments occurred, possibly accompanied by subsidence, facies were established and retreated in a marineward direction. There were at least three transgressions (fig. 14) in the upper cycle, each one overstepping the preceding one (figs. 15, 16, 17). The extent of maximum transgression in the upper cycle (T-4) was much less than that in the lower cycle (T-l) (compare fig. 13 to fig. 17). The upper cycle of the Redwall best fits the carbonate model proposed by Coogan (fig. 10) of rapid transgression followed by slow regression and/or progradation.

ENVIRONMENT

SHELF EDGE

supratidal Figure 12. Facies map constructed on R1 time surface of lower Redwall (After Kent, 1975). See figure 1 for control and figure 8 for facies patterns.

SHELF

-

protected intratidal

/ / j

open intratidal

/

/

Upper Redwall

fact**

I

open

— — —"T 3

marine

Figure 14. Schematic cross section of idealized upper depositional cycle of the Redwall Limestone showing the three transgressive pulses and facies shift. Lithofacies are shown along with three time lines (T2, T 3 , T4) just above the transgressive pulse after it reached its maximum position (After Kent, 1975).

SUMMARY The Redwall Limestone in northern Arizona was deposited by an epeiric sea that covered a broad cratonic shelf. A variety of carbonate rock textures were formed, documenting depositional environments which ranged from below-wave base to supratidal. Facies maps indicate that the Redwall for the most part was deposited by two major transgressive-regressive cycles. The early cycle was the most extensive and appears to have been formed by slow transgression and regression. The late cycle was marked by three fairly rapid transgressions interspersed with three slow regressions.

Figure 13. Facies map constructed on T1 time surface of lower Redwall (After Kent, 1975). See figure 1 for control and figure 8 for facies patterns.

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KENT AND RAWSON

T 4 FACIES

Figure 17. Facies map constructed of upper Redwall on T4 time surface of figure 14 (After Kent, 1975).


REFERENCES CITED Badiozamani, K., 1973, The Dorag dolomitization model-application to the Middle Ordovician of Wisconsin: Journal of Sedimentary Petrology, v. 43, p . 965-984. Bathurst, R . G . C., 1975, Carbonate sediments and their diagenesis: Elsevier Scientific Publishing Company, Amsterdam, 658 p. Billingsley,. G., 1979, Preliminary report of buried valleys at the Mississippian—Pennsylvanian boundary in western Grand Canyon iji Beus, S . , and Rawson, R., (eds.), Carboniferous stratigraphy in the Grand Canyon country northern Arizona and southern Nevada, American Geological Institute, Falls Church, Virginia, p. 115-117. Coogan, A . , 1972, Recent and ancient carbonate cycle sequences, in, Elam, J. G . , and Chuber, S . , (eds.), Cyclic sedimentation in the Permian Basin--a symposium: West Texas Geological Society, 2nd Edition, p. 5-16. Darton, N. H., 1910, A reconnaissance of parts of northwestern New Mexico and northern Arizona: U.S. Geological Survey Bulletin 435, 88 p. Dunham, R. J., 1962, Classification of carbonate rocks according to their depositional texture. jn_ Ham, W . E., (ed.), Classification of carbonate rocks: American Association of Petroleum Geologists Memoir 1, p. 108-121. Gilbert, G . K., 1875, Report on the geology of portions of Nevada, Utah, California, and Arizona: U.S. Geographical and Geological Survey west of 100th Meridian (Wheeler), v. 3, pt. 1, p. 17-187.

T 3 FACIES


108

MISSISSIPPIAN REDWALL LIhESTCME IN NORTHEASTERN ARIZONA Rawson, R. R., 1968, The "Kibbey Limestone" of the Williston Basin and central Montana: Wyoming Geological Association of Earth Science Bulletin, September 1968, p . 35-47. Rose, P. R., 1976, Mississippian carbonate shelf margins, western United States: U.S. Geological Survey Journal of Research, v . 4 , no. 4 , p . 449-466. Rupp, A . , 1967, O r i g i n , structure, and environmental significance of recent and fossil calcispheres: Geological Society of America Special Paper 101, p . 186 (Abstract). S h a w , A . B . , 1964, Time in stratigraphy: New York, McGraw-Hill Book Company, 365 p . S k i p p , B . , 1969, Foraminifera. i_n M c K e e , E . D., and Gutschick, R. C . , History of the Redwall Limestone of Northern Arizona: Geological Society of America Memoir 114, p . 173-255. and M c K e e , E . D., 1978, Transgressions and regressions of Redwall S e a , Northern A r i z o n a , related to calcareous foraminifera! faunas: Geological Society of America Abstracts with Programs, v . 1 0 , number 3 , p . 147. S m i t h , J . W . , 1974, The petrology of the Mississippian Redwall Limestone in northern Yavapai County, Arizona: Northern Arizona University unpublished M.S. thesis, 88 p .

Gutschick, R. C . , 1943, The Redwall Limestone (Mississippian) of Yavapai County, Arizona: Plateau, v. 16, no. 1, p. 1-11. Irwin, M . D . , 1965, General theory of epeiric clear water sedimentation: American Association of Petroleum Geologists Bulletin, v . 4 9 , p . 445-459. Kent, W . N . , 1 9 7 5 , Facies analysis of the Mississippian Redwall Limestone in the Black Mesa region: Northern Arizona University unpublished M . S . thes i s , 186 p . M c K e e , E.- D . , 1963, Nomenclature for lithologic subdivisions o f the Redwall Limestone, Arizona: U.S. Geological Survey Professional Paper 4 7 5 - C , p . C21C23. , 1 9 7 5 , The Supai G r o u p — s u b d i v i s i o n and nomenclature: U.S. Geological Survey Bulletin 1395-J, p . J1-J11. and Gutschick, R . C . , 1 9 6 9 , History of the Redwall Limestone of northern Arizona: Geological Society of America Memoir 1 1 4 , 612 p . Middleton, G . U . , 1973, Johannes Walther's law of the correlation of facies: Geological Society of America Bulletin, v . 8 4 , p . 979-988. N o b l e , L. F., 1 9 2 2 , A section of the Paleozoic formations of Grand Canyon at Bass T r a i l , U.S. Geological Survey Professional Paper 131-B, 42 p . Purves, W . J . , 1 9 7 6 , Possible Arizona faulting as suggested by Mississippian facies analysis and plate t e c t o n i c s — a stratotectonic approach: Arizona Geological Society Digest, v . 1 0 , March 1 9 7 6 , p . 259-

286.

109