Stratigraphy and Geologic History of Pennsylvanian and Permian Rocks, Mogollon Rim Region, Central Arizona and Vicinity

Stratigraphy and geologic history of Pennsylvanian and Permian rocks, Mogollon Rim region, central Arizona and vicinity

RONALD C. BLAKEY Department of Geology, Box 6030, Northern Arizona University, Flagstaff, Arizona 86011

ABSTRACT INTRODUCTION northwest to southeast): (1) western Grand Canyon, (2) Aubrey Cliffs, (3) Chino Valley Stratigraphie, paléontologie, sedimentolog- The Problem (Seligman to Hell Canyon), (4) upper Verde ic, and pétrographie data are used to con- Valley (Hell Canyon to Sycamore Canyon), struct a revised system of correlation and Recent regional stratigraphie and sedimento- (5) western Mogollon Rim (Sycamore Canyon stratigraphie nomenclature for Pennsylvanian logic studies demonstrate a need for major revi- to West Clear Creek), (6) central Mogollon Rim and Permian rocks of central and northern sion in correlation and nomenclature for Penn- (Fossil Creek to Colcord Canyon), (7) eastern Arizona and adjacent regions. The resulting sylvanian and Lower Permian rocks on the Mogollon Rim (Canyon Creek to Fort Apache). scheme emphasizes major tectonic and depo- southern Colorado Plateau in the Mogollon Rim Collectively, elements 3-7 and the immediately sitional events but also provides for recogni- region. The proposed changes, combined with adjacent subsurface are referred to as the "Mo- tion of local to regional minor events. By recent analysis of sedimentary facies, provide a gollon Rim region." recognizing stratigraphie spikes in the rock new interpretation of late Paleozoic depositional The escarpment comprises Pennsylvanian and record and combining these with available and tectonic setting of the region. Regional fa- Permian rocks, with or without a cap of Tertiary biostratigraphic data, regional correlation is cies changes caused by nonsynchronous subsi- basalts, along most of its length. Key Permian established in spite of a sparsity of fossils, dence in several major basins and sporadic units can be directly traced into Grand Canyon complex cyclic lithologie units, abrupt facies movement on intervening arches and platforms along the Aubrey Cliffs northwest of Seligman. changes, sporadic subsurface data, and dras- complicate the stratigraphie interval and, Upper Paleozoic rocks are buried or removed tic differences in quality and extent of coupled with widely separated outcrop belts and between the Mogollon Rim and the Monument outcrops. an overall poor fossil record, have caused geolo- upwarp, Defiance Plateau, Zuni Mountains, and Highlights of the proposed correlation and gists to erect a complicated nomenclature. southeast Arizona outcrops. The interval of nomenclature include the following. The Mogollon Rim region of central Arizona study ranges from the unconformity overlying 1. Differentiation of Supai and Naco For- lies southeast of Grand Canyon, south of the the Mississippian Redwall Limestone (or older mations and restriction of use of the term Monument upwarp, southwest of the Defiance rocks where the Mississippian is absent) through "Supai." upwarp, west of the Zuni Mountains, and north the Coconino Sandstone (Fig. 2). The interval, 2. Correlation of the Supai Group and the of upper Paleozoic outcrops in southeastern which averages about 800 m in thickness, con- Hermit Formation into the western part of Arizona. Each of the five surrounding regions sists of red beds, quartzarenite, carbonate, and central Arizona (as far east as Sedona). has separate nomenclature for Pennsylvanian conglomerate; it ranges in age from Morrowan 3. Formal definition of a new stratigraphie and Permian rocks, and nomenclature from to Leonardian. unit, the Schnebly Hill Formation, and sev- each of these regions has at some time been Methods eral formal members. applied in the Mogollon Rim region. This paper 4. Correlation of Pennsylvanian and Per- briefly evaluates previous nomenclature and An important aspect of this paper is regional mian strata of the Grand Canyon and De- correlation and formally proposes modified no- correlation. To facilitate this end, Pennsylvanian fiance Plateau with rocks in central Arizona menclature for the region. and Permian rocks were studied using both out- (Mogollon Rim and adjacent areas). crop and subsurface data in moderate to, in local Area and Interval of Study With a clearer concept of stratigraphy and cases, extreme detail in southern Nevada, south- nomenclature, the resulting sedimentologic The southern escarpment of the Colorado ern Utah, northern Arizona, and southeastern and tectonic history of the region can be de- Plateau stretches across Arizona from western Arizona (appendix tables).1 Forty-six detailed ciphered. The resulting interpretation of Grand Canyon and Lake Mead to near Fort geologic history provides a foundation for re- Apache, a distance of 450 km (Fig. 1). The east- lating tectonic and sedimentologic events of ernmost two-thirds of this escarpment forms the 'Measured sections and well control are listed in the appendix, available free of charge by requesting Sup- the Colorado Plateau to the evolution of Mogollon Rim. Throughout this paper, I refer to plementary Data 9014 from the GSA Documents southwestern North America. the following elements of the escarpment (from Secretary.

Additional material for this article (an appendix) may be obtained free of charge by requesting Supplementary Data 9014 from the GSA Documents Secretary.

Geological Society of America Bulletin, v. 102, p. 1189-1217, 16 figs., 1 table, September 1990.

1189

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measured sections form the data base for the Figure 1. Index map of study area, showing locations of measured sections. Inset is Mogollon Rim region; approximately 100 other enlargement of area of concentrated study, Sedona area and vicinity. See Data Repository surface and subsurface sections across the south- information (Supplementary Data 9014) for list of localities. (Note overlap.) ern Colorado Plateau have been examined, pho- tographed, and sampled during the course of this field work (appendix; Fig. 1). At most locations, the section was studied laterally as well as vertically. Thousands of outcrop photographs were made, hundreds of pétrographie thin sections were studied, and all available fossil data were incorporated into the study. The already complex nomenclature is kept as simple as possible, and old terms have been retained as much as possible, although many have been reassigned in rank. A major tool used to construct the regional correlation presented in this paper was the recognition of major depositional sequences. Sedi- mentologic methods have been used to interpret the processes of deposition at many of the outcrops, and depositional trends were established (for example, see Blakey, 1984; Blakey and Middleton, 1983). Lateral and vertical facies patterns were defined and compared with physical stratigraphy. Major facies changes related to given depositional sequences were identified and used to aid in regional correlation. Particularly important to the stratigraphie interpretation are changes from cross-stratified sandstone to wavy- bedded sandstone to red silty sandstone and mudstone formed by transition from eolian erg center to erg margin to noneolian, respectively. Recent studies (Blakey, 1988; Blakey and others, 1988) have demonstrated that nearly all eolian sandstone units on the Colorado Plateau grade laterally into noneolian units. Typically, noneolian or eolian-margin sandstone units can be traced many miles beyond the margin of the main eolian sandstone. Their sedimentologic characteristics vary laterally in a predictable manner; therefore, the stratigraphie position of an eolian sandstone can be determined within an adjacent noneolian red-bed or carbonate package. This method proved to be of great value in correlating the De Chelly and Schnebly Hill Formations.

Previous Work

An extensive literature review and appraisal is beyond the scope of this paper; recent evalua- tions of the literature have been provided (Bla- key, 1979a, 1979b, 1980). A review of the history of nomenclature as it pertains to this report, however, is necessary. Two early critical papers appeared in 1945. McKee (1945), in a general description of the rocks of Oak Creek Canyon, assigned all rocks between the Redwall Limestone and Coconino Sandstone to the Supai Formation (Darton, 1910), a Grand Can- yon term (Fig. 2). He informally recognized three members, in ascending order, C, B, and A.

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menclature and proposed nomen- V— L.X clature of this report. : la. almi?? Coconino SS

o „ COCL

Cocon ino Schnebly Hill Fm

>mE

o —

Hi 5

V) a>

% 5 Redwall Ls WESTERN MOGOLLON RIM AT PICACHO BUTTE

90-r 300

SEDONA - SYCAMORE •200 60- CANYON

Redwall Ls 30- •100 FOSSIL CREEK

m O-l-o ft CARRIZO CREEK- FORT APACHE'

Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/102/9/1189/3380878/i0016-7606-102-9-1189.pdf by guest on 02 October 2021 Huddle and Drobovolny (1945) also recognized the Supai Formation in the same interval in Oak Creek Canyon. They recognized and correlated three members, lower, middle, and upper, from Sedona to Fort Apache. From Fossil Creek eastward, they assigned a carbonate-rich interval at the base of the section to the Naco Formation, a southeastern Arizona term. Thus, "Supai" and "Naco" are firmly established names in the Mo- gollon Rim. Neither paper clearly related the formations to their respective type sections, a problem that would plague Mogollon Rim stratigraphy for 35 yr. Jackson (1952) subdivided the Naco and Supai into several members in the central Mo- gollon Rim and correlated each with rocks as far west as Las Vegas, Nevada (Fig. 3). Jackson's correlation within the central and eastern Mo- gollon Rim is similar to that used in this paper; however, the correlation he proposed with rocks in the Sedona area and in the Grand Canyon and southern Nevada has been completely revised by recent studies (Blakey, 1979a, 1979b, 1980; Lane, 1977, 1979). Winters (1963), in local study of the Fort Apache area, formalized several members in the Supai. Most of his terms are used in this report, although they are reassigned to a new formation. Brew (1965), in a biostratigraphic study of the Naco Formation in the central and eastern Mogollon Rim, provided the first substantial paleontologic data for regional correlation. Baars (1962) correlated the Permian rocks of Mogollon Rim to those in southern Utah and proposed terminology that was brought in from the Defiance and Monument upwarps. Al- though his proposed terminology in the Mogol- lon Rim region has not been accepted by subsequent workers, one critical aspect of his correlation is accepted in this paper; most of the Supai Formation (of previous workers) in the Mogollon Rim is younger than the type Supai of Grand Canyon. Ross (1973), in a regional biostratigraphic study, raised the Naco in the Mogollon Rim to group status and recognized the Horquilla Limestone and Earp Formation, southern Arizona terms, in the Naco Group. Peirce and others (1977) felt that previous work had thoroughly confused regional terminology, and so they proposed a simplified informal scheme, based on work by McKee (1945) and Huddle and Dobrovolny (1945). McKee (1975) raised the Supai of Grand Can- yon to group status and named four new This paper and Read and Wanek interpret formations. McKee made no mention concern- zone of intertonguing; ing the status of, or correlation to, the Supai of Peirce interpreted as the Mogollon Rim in either the 1975 paper or channel fill. the comprehensive recent study (McKee, 1982). Recent studies (Blakey, 1979a, 1979b, 1980; SOUTH DEFIANCE PLATEAU Blakey and Knepp, 1989) have shown that McKee's four formations can be correlated into Figure 2. (Continued). the study area. Elston and DiPaolo (1979) pro-

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PREVIOUS WORKERS (Generalized)

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Figure 3. Restored simplified cross sections of Pennsylvania and Permian strata from posed new terminology and interregional corre- southern Nevada to the eastern Mogollon Rim. Upper section shows correlation and terminol- lation for rocks in the western Mogollon Rim. ogy of this report; lower section shows previous correlations and terminology. Note significant Their terminology and correlation are unique differences in correlation of Supai, Naco, and Hermit rock-stratigraphic units. Key to numbers: (Rg. 2). 1, type Pakoon Limestone of McNair (1951); 2, Queantoweap Sandstone of McNair (1951); 3, Esplanade Sandstone (member) of many workers; 4, alleged pinch-out of Hermit, although Summary of Proposed Nomenclature never specifically located by previous workers; 5, some workers including Jackson (1952) and Elston and DiPaolo (1979) recognized Naco as far west as Sycamore Canyon. 6, lower or C; Nomenclature and correlation proposed for 7, middle or B; 8, upper or A members of Supai Formation of many previous workers. Elston the Mogollon Rim region are shown in Figures and DiPaolo correlated 8 with the Esplanade of Grand Canyon. 9, position of Hermit Shale of 2, 3, 4, and 5. Highlights include the formal Elston and DiPaolo; 10, Packard Ranch Member, the zone of intertonguing between the Supai proposal of a new formation, the Schnebly Hill and Naco of Jackson (1952); 11, Oak Creek Member (Jackson, 1952), Cibecue Member Formation, and modification of usage of the (Finnell, 1966a, 1966b), Amos Wash Member (Winters, 1963) of Supai Formation; 12, Big A Supai Group and Formation and the Hermit [Butte] Member of Supai Formation (Jackson, 1952; Winters, 1963); 13, Corduroy Member of Formation. The Coconino Sandstone is formally Supai Formation (Jackson, 1952; Winters, 1963); 14, approximate location and correlation of divided into two members in the Sedona-Oak Pennsylvanian-Permian boundary of H. W. Peirce (1988, personal commun.). Creek area, and the Supai-Naco boundary is moved down section to conform with earlier usage and definition of Huddle and Dobrovolny (1945).

Figure 4. Time-rock section of Pennsylvanian and Permian rocks of central Arizona and adjacent regions. Format and unconformity designations from Ross (1973). Supai Group includes Watahomigi through Esplanade in Grand Canyon and western Mogollon Rim; Naco Group includes Horquilla through Earp and Horquilla through Concha in southeastern Arizona; Cutler Group includes Elephant Canyon-Hal- gaito through De Chelly-White Rim in Monument Valley and southeastern Utah. Stratigraphic sequences: MAM, Morrowan-Atokan marine; DMM, Desmoinesian-Missourian marine; VR, Virgilian red bed; WSS, Wotfcampian sandstone; WLR, Wolfcampian-Leonardian red bed; LSR, Leonardian sandstone-red bed; LQ, Leonardian quartzarenite.

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BLUE MTN. CHINO PICACHO CATHEDRAL HELL BEAR PERKINS- SYCAMORE DRY (MCKEE, 1962) POINT „ BUTTE ,„ CAVES „ CANYON CANYON VILLE CANYON CREEK 30 13 13 13 |3 4 8 12

SEDONA ARCH Base Morrowon REDWALL LIMESTONE

a GRAND CANYON EMBAYMENT

Figure 5. Detailed columnar cross sections of Pennsylvanian and Permian rocks from western Grand Canyon to eastern Mogollon Rim; a, top of Redwall Limestone to top of Hermit Formation (datum); b, base of Schnebly Hill Formation (datum is Fort Apache Member) into Coconino Sandstone. Numbers between sections equal distance in miles.

Problems in Regional Stratigraphy nature and lack penultimate solutions. To some the conclusions of this paper. Summary of pa- extent, their solution is based more on trends of leontological data is provided in Table 1, and Some of the problems concerning regional stratigraphic usage than on hard data. Figures 2 the age constraints are used in the construction stratigraphy of Pennsylvanian and Permian and 3 compare and contrast the present and pre- of Figure 4. rocks in northern Arizona relate to the following vious interpretations of these four controversies; The following ages are assigned to rocks of four controversies: (1) correlation and age of the justification for the correlations proposed in this the study area based directly on analysis of con- Hermit Formation, (2) position of the Pennsyl- paper is a major goal of this study. tained fauna and flora (older nomenclature in vanian-Permian boundary, (3) position of the parentheses). Supai-Naco boundary, and (4) upward extent of STRATIGRAPHY 1. The Naco Formation in the central Mogol- the Supai Formation or Group. lon Rim is Desmoinesian and Missourian (Brew, The first two represent problems that have Introduction 1965; Brew and Beus, 1976; Ross, 1973). solutions based on stratigraphic and paleonto- 2. The uppermost Naco Formation along the logic data. Therefore, as more data are accumu- Paleontologic Control. Although data for easternmost Mogollon Rim is Virgilian (Brew, lated, interpretations are subject to modification. correlation in this report are chiefly lithologic, 1965; Ross, 1973). The two latter problems are more subjective in the meager fossil data available strongly support 3. The lower part of the Supai Formation in

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OAK FOSSIL SHARP CARRIZO CREEK CREEK 33 CREEK 35 43 CREEK

SUPAI FORMATION (upper part)

SUPAI FORMATION (lower part)

NACO ^ FORMATION

60- -200

30- -100 CENTRAL m 0 •0 ft ARIZONA SHELF

Figure 5. (Continued).

the easternmost Mogollon Rim is Virgilian Ray Douglass (1980, personal commun.) re- the Aubrey Cliffs (McKee, 1982). The Espla- (Ross, 1973). This is the lower Supai Formation ported Virgilian fusulinids within several meters nade can be traced directly into the Sedona area. of Huddle and Dobrovolny (1945) and the of Atokan fusulinids. It appears that Desmoines- 8. On the basis of a molluscan fauna, Win- upper Naco Formation of Winters (1963). ian and Missourian strata are absent from the ters (1963) considered the Fort Apache Lime- 4. The lower Supai Group in Chino Valley Grand Canyon region and western Mogollon stone to be latest Wolfcampian to Leonardian contains probable Early Pennsylvanian brachio- Rim (Oak Creek Canyon to Seligman). in age. Weisman (1986) reported late middle pods (Hughes, 1952). Physical correlation of the 6. Strata assigned to the Supai Formation in Leonardian conodonts from the Fort Apache fossil-bearing limestone into western Grand this report in the central Mogollon Rim yield an near Pine, Arizona. Similar conodonts were re- Canyon with the Watahomigi Formation Early Permian flora (Blazey, 1971; Canwright, covered from the Fort Apache south of Sedona (McKee, 1982) confirms a Morrowan age for 1978). H. W. Peirce (1987, personal commun.) (S. S. Beus, 1987, personal commun.). The Fort the unit. This carbonate marker can be physi- has collected a gastropod fauna from this unit Apache is herein assigned to the middle of the cally traced eastward to Sycamore Canyon. that is either latest Pennsylvanian or earliest Schnebly Hill Formation. 5. The lower two-thirds of the Supai Group Permian in age. Four strong conclusions result from the above in western Grand Canyon yields faunas of Mor- 7. A rich Wolfcampian fauna is reported paleontologic data. All bear strongly on the rowan, Atokan, and Virgilian ages (McKee, from the Pakoon Limestone; the Pakoon inter- correlations proposed in this report. 1982). I carefully collected and examined the fingers eastward with the lower Esplanade a. Most rock units of the Supai and Naco section at Iceberg Ridge on Lake Mead, and Sandstone in western Grand Canyon and along Groups (or Formations) are of different ages.

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PICACHO UPPER SYCAMORE LOY HARTWELL BOYNTON CAPITOL WEST SOUTH BUTTE GRINDSTONE CANYON BUTTE CANYON CANYON BUTTE SCHEUR-SCHEUR-

33 CANYON 18 5 2 3 2 2 MAN 1 MAN MTN. MTN.

HERMIT FORMATION

Figure 5. (Continued).

They are not principally coeval facies as has topmost unit in the Supai Group of Grand Can- ian age of the Fort Apache is considerably been suggested by Jackson (1952) but rather yon. It also defines the top of the Supai Group in younger than the age presently assigned to the are partially separated by major unconformities. the Mogollon Rim, where it lies some 450 m Supai Group in Grand Canyon. Only the Virgilian part of the Pennsylvanian below the top of the previously recognized Lithologic Control. The columnar cross sec- section crosses the Sedona arch. The lower "Supai Formation." tion (Fig. 5) shows the distribution of various Supai is Morrowan-Atokan, and the Naco c. The Hermit Formation in Grand Canyon Pennsylvanian and Permian rock units across Formation is Desmoinesian-Missourian and is Lower Permian (White, 1929), and it can be the entire Mogollon Rim region. The diagram is partially Virgilian. physically correlated into the Sedona area. constructed from 46 measured stratigraphic sec- b. The Pakoon-Esplanade is mostly, if not d. The Schnebly Hill Formation contains the tions between Seligman and Fort Apache, and entirely, Wolfcampian. The Esplanade is the Fort Apache Member. The late middle Leonard- correlation is based on physical tracing of

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BELL BEAVER WEST FOSSIL SHARP CARRIZO ROCK CREEK CLEAR CREEK CREEK CREEK CREEK

Figure 5. (Continued).

marker horizons. Physical stratigraphie relations creases somewhat to the west and substantially merous local unconformities are present in are supplemented with the above paleontologie to the east. Sections in the Grand Canyon region Pennsylvanian and Permian rocks of central and control as well as sedimentologie and pétro- at Iceberg Ridge, Toroweap, Thunder River northern Arizona (Ross, 1973; Peirce and graphie studies. The best outcrops with respect trail, Supai, Bass trail, Hermit trail, and Kaibab others, 1977; McKee, 1982; Blakey and Knepp, to quality of exposure, fewest and shortest gaps trail were examined and compared with pub- 1989). The former provide help with regional between sections, continuity of exposure, and lished sections by McKee (1982). Data gathered correlation, whereas the latter reflect local proc- completeness of section occur in the upper here were used for comparing the Supai Group esses and controls. Major unconformities of Verde Valley and Sedona areas. Here, abrupt of Grand Canyon with that of the Mogollon regional extent mark the base of the Pennsylva- facies changes and complex stratigraphie rela- Rim region. nian, the Morrowan-Atokan boundary within tions are well exposed. Quality of outcrop de- Unconformities. Several regional and nu- the Watahomigi Formation (McKee, 1982), the

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Stratigraphic interval

Reported age This paper

Fossil Creek Marine invertebrates; Early Desmoinesian Naco-alpha Naco East Verde R. fusulinids key group for do Naco-beta Naco Tonto Creek do Naco-beta Naco Kohl Ranch do Naco-beta Naco Big Springs Canyon do-Virgtlian Naco-beta Naco Red Rock House do-do Naco-beta Naco Carrizo Creek do-do Naco-beta/gamma Naco-Supai Amos Wash do-do Naco-beta/gamma Naco-Supai White River Missourian-Virgilian Naco-beta/gamma Naco-Supai Black River Missourian Naco-beta Naco

Brew and Koh! Ranch Marine Early Desmoinesian Naco Naco Beus, 1976 invertebrates

Nonmarine Early Permian Lower Supai Supai Can wright, 1978 flora

Big Black Mesa- Brachiopods Early Lower Supai Watahomigi Hughes. 1952 Chino Valley Pennsylvanian?

Wells south and Marine fauna; Early Desmoinesian, Supai-Naco Naco-Supai Lokke, 1962 east of Holbrook fusulinids Virgilian

Molluscs, Middle to late Ft. Apache Ft. Apache Weisman, 1986 Pine conodonts Leonardian

Molluscan Late Wolfcampian Ft. Apache Ft. Apache Winters, 1963 Ft. Apache area fauna to Leonardian

Microflora, Wolfcampian (=Abo Supai Supai Blazey, 1971 Central Rim pollen, spores Formation)

NW ARIZ W. GRAND CANYON CHINO PT SEDONA E. MOGOLLON RIM SE ARIZ

Kaibab Formation Concha Ls

'.•'Scherrer-:'.-] Fm

s Hermit Formations :8- Epitaph I w Dol A ^Colina Ls 'Formation^-— Imu

Earp Ages: Imu: Leon., mid-up ¿Supai: llw: low Leon.-Wolf. v: Virgilian Fm .. llw I mo: Missourian Principle Lithology dm: Desmoinesian "M at: Atokan ' Horquilla Sandstone mr: Morrowan dm mo

Redbeds Regional Unconformities Physical and Ls paleontological: can be dm\ 400 Limestone picked on outcrop 120 1^0 1(^ 20 30 miles Chiefly paleontological: at difficult to pick on outcrop

meters 0 0 feet "o 1020 30 Kilometers 250 kms —- mr

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Desmoinesian-Missourian boundary within the Naco Formation (Brew, 1965; Ross, 1973), the base of the Virgilian (Ross, 1973; McKee, 1982), the base of the Permian (McKee, 1982; Blakey and Knepp, 1989), and the base of the Coconino Sandstone or Schnebly Hill Forma- tion, likely within the Leonardian (Blakey, 1980; Blakey and Knepp, 1989). Numerous local unconformities, some of which could prove to be of regional extent, are present throughout the section. Unfortunately, presence or absence of conglomerate, relief, or contrast in lithology has little to do with the extent or amount of time missing at a given unconformity. Regional unconformities are determined by regional paleontologic, stratigraphic, and sedimentologic data (Fig. 6).

Tectonic Setting

The diversified tectonic setting of the Colo- rado Plateau in the late Paleozoic coupled with worldwide eustatic changes are responsible for the complex lithologic sequences and abrupt fades changes that characterize the Pennsylvanian and Permian systems. Three separate basins and Fig. 10 several intervening shelves and arches controlled local sedimentation patterns (Fig. 7). Not all the %% basins were active at the same time, and thus deposits of one basin are not necessarily the Fig. 9 same age as similar deposits in another basin (Blakey, 1980; Blakey and Knepp, 1989). De- posits along the western Mogollon Rim were oTUCSON chiefly influenced by the Grand Canyon em- 50 100 I bayment, an eastward-projecting negative area Km ^ PEDREGOSA off the Cordilleran miogeocline (Fig. 8). Major f N. BASIN periods of subsidence took place during Morro- '"1 wan, Atokan, Wolfcampian, and early Leonar- dian time (Fig. 4). Figure 7. Late Paleozoic tectonic elements of Arizona and adjacent areas. Also shown are The central and eastern Mogollon Rim region locations of areas shown in Figures 8,9, and 10. was influenced by subsidence on the Mogollon shelf during the Pennsylvanian Period (Fig. 9). The Mogollon shelf opened southeastward into the strongly negative Pedregosa basin (Ross, Formation) are not present in the Grand Can- Supai Group 1973; Blakey, 1979a, 1980; Blakey and Knepp, yon region. The Paradox basin in southeastern 1989). Subsidence in the eastern Mogollon Rim Utah had less direct effect on sedimentation in The Supai Group (Pennsylvanian and Lower was strongest during Desmoinesian and Mis- central Arizona, but nevertheless, it was an im- Permian) is present throughout west-central, sourian time. Permian rocks in this area are portant tectonic element that influenced sedi- northwest, and north-central Arizona generally closely related to subsidence in the Holbrook ment dispersal to the south. The Grand Canyon west of the Sedona arch (Fig. 7) from Sedona basin (Fig. 10). Facies patterns strongly reflect embayment is separated from the Mogollon and Flagstaff northward to the Utah-Arizona the short-lived but intense Leonardian subsi- shelf and Holbrook basin by the Sedona arch state line at 111° west longitude (Fig. 8). The dence, and rocks of this interval (Schnebly Hill (Blakey, 1979b, 1980). The Sedona arch was Supai Group consists of the following four for- slightly negative to have preserved thin deposits mations, each of which is absent or unrecogniz- throughout parts of the Pennsylvanian and Per- able east of the above line: Watahomigi mian, but sufficiently positive to reflect facies Formation (Morrowan, Atokan), Manakacha patterns (Figs. 8, 9, and 10) and is the site of Formation (Atokan), Wescogame Formation numerous important unconformities (Fig. 4). (Virgilian), and Esplanade Sandstone (Wolf- Broader views concerning late Paleozoic tec- campian). The contacts between these forma- Figure 6. Restored cross section of Penn- tonics of southwestern North America are pro- tions may be difficult to pick, even in the Grand sylvanian and Permian rocks, emphasizing vided by Burchfiel and Davis (1975) and Blakey Canyon where exposures are mostly spectacular. relations of regional unconformities. Note (1980). Late Paleozoic eustacy is discussed by This problem is further compounded in the large gap between Mogollon Rim and south- Heckel (1980) and Blakey and Middleton study area where outcrop is less continuous and eastern Arizona. (1983). less well exposed (Figs. 1 la, 1 lb, and 1 lc).

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lain by carbonate ledges and mudstone slopes of the upper part of the Watahomigi Formation. 112° — —I _ The exact position of the contact between the Watahomigi and overlying Manakacha Forma- tion is difficult to pick consistently but is marked Si S by an upward increase in bright orange, biotur- °0 1/ bated, rounded ledge-forming, very fine-grained calcareous sandstone. In general, this interval consists of several repetitive cycles of sandstone J à % and cherty, typically jasper-bearing carbonate. It Si forms a distinctive banded steep slope within o A' which McKee (1982) placed the contact be- / tween the Watahomigi and Manakacha Forma- tions. Distinctive outcrops of this interval on the Kaibab and Hermit trails in Grand Canyon are igman 1 •v.. APPRO X EAST EDGE correlated with nearly identical outcrops 0Kingman ' gF'agstaff /^ . o 0R AT<)K throughout Chino and Upper Verde Valleys. In 35;PERCE^JT CARBONATE' both the Grand Canyon and western Mogollon 2 U I o Sedona Rim, the slope-forming Watahomigi Formation 50 h ' 7 is overlain by a persistent cliff and slope se- '«y/ quence that makes up the Manakacha and Wes- 0 km so o ^J^Prescott cogame Formations. A typical complete section of the Supai Group is well exposed at Hell Can- yon. There, the Watahomigi Formation is succeeded by red-orange, cross-stratified, cal- Figure 8. Generalized fades of Pennsylvanian rocks of Supai Group, northern Arizona, careous sandstone of the Manakacha Forma- showing isopachs, percent carbonate, and east edge of each series. Virgilian rocks probably tion; reddish-brown to tan sandstone, limestone, covered entire area. See Figure 7 for location. and mudstone of the Wescogame Formation; and ledge- and cliff-forming calcareous cross- stratified sandstone and subordinate mudstone The basal Supai Group consists of reworked Supai Group is overlain by one to as many as of the Esplanade Sandstone. A mudstone and material from the underlying Redwall Lime- three prominent marine cherty limestone ledges sandstone slope marks the lower part of the stone; of variable thickness, it consists of basal that crop out from Picacho Butte to Sycamore Hermit Formation. Correlation of these units conglomerate or breccia, chiefly composed of Canyon. The ledge or ledges form a unit that and their probable relations to the Supai Group chert clasts and overlying bluish-gray to pale averages 5-10 m thick. Faunal and lithologie in Grand Canyon are shown in Figure 5a. reddish-brown mottled mudstone to claystone. characteristics and stratigraphie position indicate The best outcrops of this poorly exposed unit are that this is the Morrowan limestone unit of the Although lacking the continuity of exposure in man-made cuts in the Jerome area. The basal Watahomigi Formation. The limestone is over- afforded in Grand Canyon, physical characteristics and stratigraphic succession of the Supai Group in the western Mogollon Rim confirm Flagstaff ir.e - ^ f&c\£S the extension of the four formations into the REOBeo^P Sycamore Canyon area. From Sycamore Can- yon to Dry Creek, the group thins rapidly and marker beds disappear and the upper Esplanade Sandstone overlies the lower Supai Group Figure 9. Generalized (undivided). facies of Pennsylvanian rocks of Naco Forma- Naco Formation tion, east-central Arizona, showing isopachs, per- The Naco Formation (Desmoinesian, Mis- cent carbonate, and north sourian, Virgilian) is recognized in the Mogollon edge of each series. Virgil- Rim and adjacent subsurface from Fossil Creek ARIZONA ian rocks probably cov- eastward (Figs. 9 and lie). The Naco Forma- ered entire area. See Fig- x tion has received thorough paleontologic and 0 / SHELF V ure 7 for location. biostratigraphic study (Brew, 1965; Ross, 1973; Brew and Beus, 1976) but awaits detailed sedi- Florence mentologic and petrographic study. In the cen- N o tral and eastern Mogollon Rim, Huddle and Safford Dobrovolny (1945) recognized the Naco For- mation from Fossil Creek eastward. They re- o Km 50 stricted the Naco to ledge- and slope-forming,

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intercalated light gray limestone; nodular bluish- gray to pinkish limey mudstone; gray to purplish to locally reddish sandy mudstone; and rare tan to pinkish sandstone. Biostratigraphic information in Figure 5a is after Brew (1965) and Ross (1973), although their thicknesses for the Naco are adjusted slightly. As defined, the Naco ranges in thickness from 100 m (330 ft) at Fossil Creek to more than 200 m (660 ft) in the Fort Apache area (Brew, 1965; Finnell, 1966a, 1966b; McKay, 1972; Ross, 1973). The increase in thickness is primarily due to slight regional southeastward tilting of the strata, so that succes- sively younger rocks are beveled to the northwest beneath the sub-Virgilian unconformity (Ross, 1973), but southeastward thickening due to increased subsidence is also evident (Fig. 5a). If the biostratigraphic data of Ross (1973) are considered, the upper boundary of the Naco Formation as defined herein lies at an unconformity or series of unconformities. According to Ross, the first widespread Supai lithofacies is Prescoft ' O his format K, and it overlies his unconformity 11. He has shown a series of local unconformities (1 la, 1 lb, 1 lc) in the Mogollon Rim region ZERO EDGE beneath and within this first major red-bed FT. APACHE MBR. pulse. The change from predominantly gray and 34° + purplish-gray limestone and mudstone below to 100ft. CONTOUR FT, APACHE MBRr"*\ o Ft. Apache reddish-brown sandstone and mudstone above marks the Supai-Naco boundary of Huddle and Drobovolny (1945) and the one followed in this Figure 10. Generalized fades of Permian rocks of Schnebly Hill Formation and De Chelly report. The 40-70 m of rocks in question, var- Sandstone, northeastern Arizona, showing isopachs. See Figure 7 for location. iously assigned to the Supai Formation, Earp Formation, Naco Formation, or B-2 (see Fig. 2), is a complicated, very poorly exposed sequence formations. Few aspects of the formation are mussen, 1987, personal commun.), indicate that of sandstone, limestone, and fine-grained red unequivocal; its age, facies distribution, and the formation is present southeast of where beds. Their age (based on a late Virgilian fauna), depositional history are all imperfectly under- Peirce postulated the zero edge. Thickness trends stratigraphic position, and lithologic character stood. White (1929) assigned an age of late are irregular, and the Hermit is less than 20 m suggest both Supai and Naco affinities. The Early Permian (Leonardian) to the formation, thick in several wells, but it can be correlated in preference herein to assign the rocks to the Supai and McKee (1982, p. Ill) further supported wells near Flagstaff. I have measured nearly 100 Formation (lower part) is perhaps a moot point, this assignment, based on a fossil plant Callip- m of Hermit Formation on Mount Elden at given the poor outcrops and difficulty of estab- teris arizonae also found in the Bone Springs Flagstaff. From there, it is less than 35 km south lishing mappable contacts. Limestone of Leonardian age in southeastern to extensive Hermit outcrops in the Sedona- New Mexico. Obvious southeastward thinning Oak Creek Canyon area. These data do not Hermit Formation of the unit led Hughes (1952), Jackson (1952), preclude the possibility that the Hermit is absent and Peirce (1989) to postulate a wedgeout of the locally on the structurally high Kaibab upwarp, The Hermit Formation (Wolfcampian to Hermit between the Aubrey Cliffs-Grand Can- but on a regional scale, it is present across north- Leonardian) extends across northwestern Ari- yon regions and the Mogollon Rim region. central Arizona. zona from the Sedona area (Fig. lid), and it Extension of thickness trends to locate edges of Throughout the Grand Canyon-Aubrey Cliffs crops out in the Grand Canyon and the western stratigraphic units, although a widely used strat- area, the Hermit Formation lies between two Mogollon Rim, into the Aubrey Cliffs. Because igraphic practice, can be misleading in some prominent sandstone units, the Esplanade Sand- of problems outlined previously, the Hermit cases. A detailed examination of the postulated stone below and Coconino Sandstone above. At Formation is no longer recognized in the central pinchout of the Hermit Formation is critical to Chino Point, the southern extremity of the Au- or eastern Mogollon Rim, and partially equiva- some of the correlations in this report. brey Cliffs, this relation holds, and the formation lent rocks in these areas are assigned to the Peirce (1989) used outcrop trends and a sin- is 30 m (100 ft) thick. Exposures are very poor, Supai Formation (Fig. 5). Misnamed a shale, the gle borehole south of Grand Canyon to postu- and facies analysis at this location is impossible, unit is mostly sandy mudstone, sandy siltstone, late the zero edge of the Hermit Formation. but continuity with better exposed and thicker and very fine-grained sandstone. The Hermit More recent data, however, based on very tight sections a few kilometers northwest is unequivo- Formation everywhere forms a steep slope, gen- drilling throughout the region south of Grand cal. At Picacho Butte, 14 km to the southeast, erally mostly covered by debris from overlying Canyon by Energy Fuels Nuclear (Jim Ras- the entire pre-Kaibab Paleozoic section is mod-

Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/102/9/1189/3380878/i0016-7606-102-9-1189.pdf by guest on 02 October 2021 Figure 11. Outcrops of Supai Group and Supai, Hermit, and Naco Formations, central and western Mogollon Rim area. A. Lower Supai Group near U.S. Mine (loc. 19); light carbonate at base near top of Watahomigi Formation, dark ledges and slopes in Manakacha Formation, light ledges at top in Wesco- game Formation. B. Entire Supai Group on east side of Syca- more Canyon; lower slopes and ledges are Watahomigi through Wescogame Formations, undivided; upper cliff is Esplanade Sandstone. C. Gradational and intertonguing contact between Esplanade Sandstone (lower half of photograph) and Hermit Formation (upper half of photograph) at Red Butte (loc. 15). D. Hermit Formation between lower cliff of Esplanade Sandstone and upper cliff of Schnebly Hill Formation near Grasshopper Point in Oak Creek Canyon (loc. 59). E. Naco Formation in Fossil Creek (loc. 81). Lower part of cliff yields fossils of Des- moinesian age.

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erately exposed. The Esplanade Sandstone con- sures are so poor that it cannot be determined mation above contains rocks of Virgilian and tains the same stratigraphic, petrographic, and whether a similar transitional interval is present. Early Permian age (Table 1; Fig. 4). Although sedimentologic characteristics seen along the Unit E is the main 35-m-thick body of the the upper part of this sequence contains rocks Aubrey Cliffs and at Chino Point. Approxi- Hermit Formation. Lithofacies are similar to temporally equivalent and lithologically similar mately 60 m (300 ft) of moderately to poorly those of the Hermit in central Grand Canyon to the Hermit Formation, the problems of estab- exposed slope- and ledge-forming siliciclastic and along the Aubrey Cliffs. lishing a recognizable lower contact or other- strata separates the Esplanade Sandstone from Unit F is an altered zone, local to the Picacho wise consistently subdividing the sequence have the overlying Coconino Sandstone. The follow- Butte area. It probably represents an altered convinced me to drop the term "Hermit Forma- ing description uses informal letter designations zone at the top of the Hermit. tion" east of the Sedona area. I propose that the to define units within this critical interval (see Unit G is the westernmost exposure of the entire package between the Schnebly Hill and Fig. 2). Schnebly Hill Formation; the Schnebly Hill Naco Formations be assigned to the Supai Unit A. This unit overlies cross-stratified cal- gradually thickens into the Sedona area. Formation. careous sandstone and calcareous hybrid sand- The Hermit Formation is next exposed to the stone of the Esplanade Sandstone. Unit A southeast at the head of a small draw in the Hell Supai Formation consists of 14 m (47 ft) of intercalated reddish- Canyon-Limestone Canyon area on south Big brown sandstone, sandy siltstone, and limey silt- Black Mesa, sec. 22, T. 19 N., R. 2 W. Here, The Supai Formation (undivided) includes stone. Beds are faintly ripple laminated and 10-20 m of the formation is exposed between rocks of Virgilian, Wolfcampian, and possibly display a mottled appearance due to bioturba- the underlying Esplanade Sandstone and an Leonardian age and is recognized across the tion and diagenetic alteration. The unit forms overlying Tertiary basalt flow. The Esplanade- Mogollon Rim from Fossil Creek eastward, in slopes and weak ledges. Hermit contact is again transitional. The Hermit the adjacent subsurface, and northward onto the Unit B. This unit is cross-stratified, calcareous, Formation is partially to completely exposed in Defiance Plateau (Figs. 2, 3, 4, and 5). The hybrid sandstone 5 m (17 ft) thick and forms a a number of outcrops in the upper Verde Valley, Supai Formation consists of a poorly studied reddish-orange cliff. including Grindstone Canyon, MC Canyon, red-bed sequence and has been inconsistently Unit C. This unit comprises 11 m (36 ft) of Red Butte, and Bear Canyon (Fig. 1). In the subdivided and assigned to various stratigraphic sandstone and siltstone like those in unit A and Bear Canyon area, moderately well-exposed units (Fig. 2). The treatment of the unit herein is forms a slope. outcrops show the same relations as seen at Pi- considered a compromise, because further de- Unit D. This unit is similar to unit B and cacho Butte; several ledges of Esplanade-like tailed study will likely result in more precise forms a ledge 2 m (8 ft) thick. rocks are intercalated with slopes of Hermit definition, correlation, and subdivision. Unit E. This is another slope-forming mudstone. At least two sedimentary-pebble Two parts can generally be recognized in the sequence of sandstone and siltstone similar to conglomerate beds are also exposed in this area central and eastern Mogollon Rim. The lower units A and C. It is 35 m (122 ft) thick. Near within the Hermit Formation. Broader expo- part is assigned a Virgilian age, based on fossils the top of unit E are two limestone-pebble sures occur throughout the Perkinsville, Syca- found in the eastern part of the area (Brew, conglomerates. more Canyon, and Sedona areas. A relatively 1965; Ross, 1973). The strata are varied but Unit F. This unit consists of 13 m (41 ft) of sharp contact is between the two units in some consist chiefly of limey and nodular very fine- somewhat altered, purplish limey sandstone and areas, whereas gradation and probable inter- grained structureless sandstone, trough cross- siltstone. Alteration appears to have been caused tonguing is observed elsewhere. stratified sandstone and conglomerate, and by diagenesis and bioturbation. In the western Mogollon Rim region, the limey mudstone to the west with addition of Unit G. Consisting of 15 m (50 ft) of wavy- to Hermit Formation consists of two major facies. micritic and calcarenitic limestone to the east. ripple-laminated, noncalcareous sandstone to The first includes typical Hermit strata of the The unit is primarily reddish gray to reddish silty sandstone and intercalated cross-stratified type section area in Grand Canyon and is pre- brown to locally pale grayish orange in color sandstone, this unit forms an orange cliff be- dominant from Chino Point to the western side and forms ledges, steep slopes, and local cliffs. neath the overlying Coconino Sandstone. The of Sycamore Canyon. It consists of alternating, Thickness averages 90 m (300 ft). Local large- Coconino consists of noncalcareous, cross- very fine-grained, faintly ripple-laminated, cal- scale, cross-stratified, calcareous sandstone of stratified, very pale grayish-orange sandstone. careous to slightly calcareous sandstone and in- possible eolian origin is present in parts of the Apparently, the intercalated sandstone units distinctly bedded sandy siltstone and mudstone. Fossil Creek area. B, D, and G led Hughes (1952) to believe that Where exposure permits, about a dozen cycles The lower part of the Supai Formation is the thin Hermit at Chino Point was absent at of sandstone and mudstone can be identified, probably temporally equivalent to parts of the Picacho Butte, because he assigned this interval most on the order of several meters thick. Wescogame Formation farther west, although (units A-G) to the undivided Supai Formation. Limestone-pebble conglomerate is present but the uncertain location of the Pennsylvanian- I interpret the section differently. As previously rare in this facies. The second major facies con- Permian boundary and lack of datable fossils in discussed, the Watahomigi, Manakacha, Wes- tains numerous beds of limestone-pebble con- the lower Supai Formation add uncertainty to cogame, and Esplanade are each present below glomerate. Best developed in the Sedona area, this. The interbedded, cross-stratified sandstone and mark the position of the Supai Group. Units the lateral change to facies one is exposed in the and red beds in the Fossil Creek area are litho- A through D are similar to rocks marking the Sycamore Canyon area. logically very similar to the Wescogame at the Esplanade-Hermit transition in Grand Canyon. From Sedona westward, the Hermit crops out Hermit and Kaibab trails in Grand Canyon. The At some locations (for example, Hermit and between the cliff-forming Esplanade Sandstone sandstone is not present in the southeastern Fos- Kaibab trails), this transition is associated with below and Schnebly Hill Formation or, west of sil Creek area nor in outcrops farther southeast channeling at the top of the Esplanade, and in Picacho Butte, Coconino Sandstone above. The along the Mogollon Rim. This suggests that the other places (for example, Toroweap Valley), a Esplanade Sandstone is absent east of Sedona, Fossil Creek area is transitional between typical probable area of intertonguing between the two and so the lower contact cannot be accurately or Virgilian Wescogame to the northwest and Vir- units is present. Units A and C are typical of the consistently established. From Fossil Creek gilian strata of the Supai Formation in the Mo- Hermit, and units B and D are typical of the eastward, the slope-forming interval between the gollon Rim east of Fossil Creek. Esplanade Sandstone. At Chino Point, expo- Naco Formation below and Schnebly Hill For- The upper part of the Supai Formation is a

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complex assemblage of red beds. Sandstone and cirudites of the Supai Formation at Fossil Creek eolian) to wavy-bedded sandstone decreases in conglomerate content, composition of conglom- and Hermit Formation at Sedona. Given that abundance up section and to the north. erates, and bedding styles vary across the region. the Hermit Formation is Permian, the upper Previous terminology applied to this interval in- Supai at Fossil Creek and presumed equivalents Coconino Sandstone cludes Hermit Formation (Blakey, 1980; Blakey farther east are also Permian. and Knepp, 1989), Amos Wash Member of Only the upper part of the Supai Formation is The Coconino Sandstone (Leonardian) ex- Supai Formation (Winters, 1963), Cibecue believed to be present on the Defiance Plateau. tends (or once extended) across all of northern Member of Supai Formation (Finnell, 1966a, There, the formation consists of channels of and central Arizona south of a line from the 1966b), middle member of Supai Formation sandstone, conglomerate, and conglomeratic southern Defiance Plateau to south of the pres- (Huddle and Dobrovolny, 1945), and B-l sandstone and intercalated limey nodular ent Monument upwarp. East of a north- (Peirce and others, 1977). The poor exposures mudstone. south-trending line running through approxi- and abrupt lateral changes and lack of traceable mately Fossil Creek, the Coconino Sandstone is key marker beds led Ross (1973) to state that Schnebly Hill Formation undivided (Fig. 3). West of this line, the upper the Amos Wash Member is of local extent, ap- part of the Coconino Sandstone and equivalent parently led Finnell (1966a, 1966b) to propose The Schnebly Hill Formation (Leonardian) is White Rim Sandstone in Utah grade westward new nomenclature for this part of the section, recognized throughout the Mogollon Rim re- into the Toroweap Formation (Irwin, 1971, and has led me to withdraw the use of "Hermit gion and adjacent subsurface, and northward to 1976; Rawson and Turner-Peterson, 1980; Bla- Formation" east of the Sedona area. Physical the Defiance Plateau (Fig. 10). The Schnebly key and others, 1988). correlation presented in this paper suggests a Hill was deposited in response to rapid subsi- The Coconino Sandstone is the highest Per- Wolfcampian to possibly Leonardian age for the dence in the Holbrook basin and is not present mian unit studied in detail for this report. It upper Supai Formation. Included flora sug- in the Grand Canyon region (Blakey, 1979a, sharply, and probably unconformably, overlies gested an Early Permian age to Blazey (1971) 1979b, 1980). Sedimentology, lithology, faunal the Hermit Formation and gradationally overlies and Canwright (1978). H. W. Peirce (1987, per- content, and stratigraphic position serve to sepa- the Schnebly Hill Formation or De Chelly sonal commun.) has collected a molluscan fauna rate the Schnebly Hill Formation from the Supai Sandstone. The Coconino Sandstone consists of from the base of the interval that could be either Group or Formation. The Schnebly Hill Forma- cross-stratified, noncalcareous quartzarenite of latest Pennsylvanian or earliest Permian. Clear- tion is a heterogeneous sequence, generally red- eolian origin (Fig. 13a). In the Sedona and Mar- ly, this part of the section is in need of careful dish brown to reddish orange in color, with ble Canyon areas, it is divisible into two formal additional study. several distinctive types of sandstone, silty sand- stratigraphic units. To further confuse matters, a complex of flu- stone, mudstone, evaporite sequences, and lime- The lower Coconino Sandstone is continuous vial channels, bleached sandstone and mudstone and dolomite (Fig. 12). At all outcrops, throughout the Mogollon Rim region. The stone, carbonaceous material, and anomalous the basal contact is sharp and lacks transition of upper part of the Coconino Sandstone abruptly high radioactivity is present near the middle of any kind, and probably is a regional unconform- grades westward into the Toroweap Formation the Supai Formation, probably at or near the ity. The upper contact is everywhere a zone of along Sycamore Canyon; this change is also ex- Pennsylvanian-Permian boundary. Peirce and gradation or intertonguing. The formation posed in Marble Canyon (Rawson and Turner- others (1977) described and correlated this in- thickens from all directions into the subsurface Peterson, 1980). In order to emphasize these terval throughout the central and eastern Mogol- near Holbrook, where it is nearly 600 m (2,000 stratigraphic relations and the resulting differ- lon Rim and into the adjacent subsurface. At ft) thick. Sandstone content increases, and car- ences between the two parts of the Coconino Fossil Creek, the complex fills a northwest- bonate, mudstone, and evaporite content de- Sandstone, the formation is formally divided trending channel roughly 1 km wide and 10-25 creases both up section and to the west, into two members. These members can be easily m deep. This channel, or paleovalley, is filled northwest, and north. The Schnebly Hill Forma- and consistently mapped and recognized in the with fine- to very fine-grained quartz sandstone tion defines a broad, nearly circular basin Sedona area and in Marble Canyon. East of and limestone-pebble conglomerate. Thin-sec- rimmed by eolian sandstone with evaporite and Marble Canyon and the southern Sedona area, tion analysis of six samples reveals a lack of carbonate in its center. the two units cannot be differentiated and the anomalous feldspar or other extrabasinal lithic Coconino Sandstone remains undivided. West material and suggests a soil-derived origin for De Chelly Sandstone of Sycamore Canyon and in Grand Canyon, the carbonate grains. Several fining-upward cy- only the lower member is present and the forma- cles, trough and epsilon cross-stratification, and The De Chelly Sandstone (Leonardian) is tion is likewise undivided. associated plant debris suggest a fluvial origin recognized across northeastern Arizona and vi- The lower subdivision of the Coconino Sand- for the channel-fill sequence. The complex over- cinity north of a line from the southern Defiance stone is herein formally named the Harding lies several conglomerate units, one of which is Plateau to the subsurface east of Marble Can- Point Member of the Coconino Sandstone. The very prominent in the area, and is overlain by yon. It overlies the Organ Rock Formation unit extends throughout the Sedona-Oak Creek several more conglomerate beds. Regional cor- (Hermit equivalent) on the Monument upwarp Canyon area, where it consists of approximately relations presented in this paper suggest that the and overlies and grades laterally into the Schne- 180 m (600 ft) of cross-stratified quartz sand- channeled complex lies at or near the Pennsyl- bly Hill Formation to the south. The De Chelly stone of eolian dune origin. The lower contact vanian-Permian boundary. Peirce (1989) pre- Sandstone comprises several types of cross- with the Schnebly Hill Formation is everywhere ferred to locate the boundary higher in the stratified sandstone intercalated with ripple- gradational to intertonguing; the upper contact is section and suggested that it might be as high as laminated to wavy-bedded sandstone and silty a sharp horizontal surface marked by a promi- the base of the Schnebly Hill Formation. My sandstone. Sedimentary structures document an nent zone of vegetation, the so-called "green arguments are based on the similarity of lithol- eolian erg and erg-margin origin. The erg- line" (Fig. 13a). The type section is on the ogy and stratigraphic position of the upper cal- margin ripple-laminated (both subaqueous and southeast face of Harding Point, sec. 28, T. 19

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N., R. 6 E., Coconino County, Arizona (Moun- tainaire quadrangle). Complete sections of the member are difficult to measure; well-exposed sections form vertical cliffs, and climbable slopes are covered with debris and heavy forest. The lower half of the member is easily studied in excellent outcrop on the spur immediately north of the junction of West Fork of Oak Creek and Oak Creek, and so this serves as the chief reference section. The Harding Point Member is recognized from the east side of Sycamore Canyon south- o-t-o eastward to the Beaver Creek area, then SCALE: northward to the Flagstaff area. Southeastward, A-C the "green line" apparently disappears, and so the two parts of the Coconino Sandstone are not TONGUE OF BELI divisible. ROCK HERMIT FM J The upper part of the Coconino Sandstone is formally named the Cave Spring Member of the Coconino Sandstone. From the type section and southeastward throughout the Sedona area, the unit displays similar characteristics to the Hard- ing Point Member, although more flat-bedded sandstone is generally present; however, between Oak Creek and Sycamore Canyon, the unit undergoes a rapid lateral change to sabkha deposits of the Toroweap Formation (Rawson HERMIT and Turner-Peterson, 1980). The suggested western extent of the term "Cave Spring" is at Buck Ridge, the eastern margin of Sycamore Canyon, sec. 35, T. 19 N., R. 4 E. The unit SANDSTONE•• x-strat, large SANDSTONE : wavy to ripple cannot be differentiated southeast of the Beaver scale, undifferentiated laminated, silty Creek area. SANDSTONE: x-stratified, The Cave Spring Member ranges in thickness MUDSTONE: sandy from 54 m (180 ft) near Buck Ridge to 90 m trough (300 ft) at Cave Spring. The type section is in SANDSTONE: x-strat, com- Oak Creek Canyon 600 m southeast of Cave Z=Z DOLOMITE Spring near the section corner of sees. 27, 28, pound, herringbone 33, 34, T. 19 N„ R. 6 E., Coconino County, Arizona (Munds Park quadrangle). The member SANDSTONE: x-strat, is fully exposed and easily accessible. Its upper planar, large scale contact with the overlying Kaibab Formation is sharp and marked by the appearance of sandy Figure 12. Columnar section of A, type Schnebly Hill Formation; B, type Sycamore Pass dolomite. Member; C, type Bell Rock Member; and D, type Rancho Rojo Member. Note that A-C have The Cave Spring Member marks the eastern different scale than does D. phase of the Toroweap Formation (Rawson and Turner-Peterson, 1980) and is probably the only part of the Coconino Sandstone directly equiva- through Marble Canyon and into southern Utah Cheevers and Rawson (1979) and Hopkins lent to the White Rim Sandstone in Utah (Blakey and others, 1988). The line is defined by (1990). (Blakey and others, 1988). A similar relation a sharp facies change from upper Coconino Cutler Group. The Cutler Group is widely between the Coconino and Toroweap is well Sandstone-White Rim Sandstone to carbonate, distributed across the Four Corners region in exposed in Marble Canyon, but it is perhaps sandstone, and red beds of the Toroweap. The both the outcrop and subsurface. It consists of premature to extend the Oak Creek Canyon regional stratigraphy and origin of the Toro- the Halgaito Formation (Wolfcampian), Cedar nomenclature into this area. weap Formation are described in Rawson and Mesa Sandstone (Wolfcampian), and Organ Turner-Peterson (1980). Rock Formation (Wolfcampian-Leonardian) Other Stratigraphic Units Kaibab Formation. The Kaibab Formation in southeasternmost Utah and adjacent Arizona (Leonardian to possibly Guadalupian) is the (Baars, 1962). Toroweap Formation. The Toroweap For- youngest Permian unit on the southern Colo- Cutler Formation. Southeast of a line from mation (Leonardian) is recognized west of a line rado Plateau. Regional stratigraphy, sedimen- Flagstaff, Arizona, to Bluff, Utah, the Cedar that runs from Sycamore Canyon northward tology, and carbonate petrology are presented in Mesa Sandstone and equivalent Esplanade

Figure 13. Outcrops of Schnebly Hill Formation and De Chelly Sandstone. A. Hermit by subsidence of the Holbrook basin and re- Formation (Ph), Schnebly Hill Formation (Ps), and Coconino Sandstone (Pc) in upper Dry peated marine transgressions and regressions Creek, Boynton Canyon (loc. 39) in background; 1, Bell Rock Member; 2, tongue of (Blakey and Middleton, 1983). Thinning of the Sycamore Pass Member; 3, Fort Apache Member (in notch); 4, Sycamore Pass Member; Hermit Formation in the western Mogollon Rim 5, Harding Point Member; 6, Cave Spring Member. Kaibab Formation (Pk) caps middle and the abundance of caliche nodules and asso- cliff. B. Type Schnebly Hill Formation (loc. 55) with lower Bell Rock Member, upper Syca- ciated carbonate-pebble conglomerate in the more Pass Member, and medial Fort Apache Member (arrows). C. Rancho Rojo Member at Sedona area are related to slight tectonic ad- Red Tanks Wash south (loc. 75), overlying covered slope of Hermit Formation. D. Intertongu- justment along the Sedona arch (Blakey, 1980; ing between Sycamore Pass Member (cross-stratified sandstone cliffs) and Corduroy Member Duffield, 1985). (slopes), West Clear Creek (loc. 80). Ledge at base of photograph (arrow) is carbonate tongue. Fort Apache Member is 50 m below base of photograph. E. Supai Formation (about 70 m DEFINITION OF THE SCHNEBLY thick) overlying Precambrian rocks and overlain by Schnebly Hill Formation (above arrow) at HILL FORMATION Hunters Point south (loc. 98). F. Schnebly Hill Formation (slickrock slope) with prominent dolomite (arrow) overlain by cliff of De Chelly Sandstone at Black Creek (loc. 96). To north 30 Type Section km, entire coeval section is cross-stratified eolian rocks of De Chelly Sandstone (see Fig. 15). The type section of the Schnebly Hill Forma- tion is on the south side of Casner Canyon at its junction with Oak Creek, Schnebly Hill area, sec. 3, T. 17 N., R. 6 E., Munds Park quadran- Sandstone undergo facies change to gypsiferous Hill-De Chelly are apparently related to paleo- gle, Coconino County, Arizona (Figs. 12 and red beds. In this region, which includes the sub- geography. Eolian deposits of the Supai were 13). The type section was measured along the surface of the southern Four Corners region, the formed on a windward coast that faced north- prominent slickrock spur in section 3 to the top entire Permian section comprises red beds. Baars west, the predominant Permian wind direction. of the butte in the south-central part of the sec- (1962) suggested that the term "lower Cutler Winds blew off the inland sea and across coastal tion and is accessible from Schnebly Hill Road Formation" (undivided) be assigned to these flats (Blakey, 1980). There, undersaturated (Coconino National Forest Road 153) or U.S. rocks. The Cutler Formation is Lower Permian winds picked up sand, much of it carbonate, and Highway 89A. The type section provides 100% and is recognized north of the Kaibab arch and blew the grains inland. Thin sections show that rock exposure and is fully visible from the Midg- east of the Monument upwarp (Fig. 6). Equiva- some sandstone units contain 60%-80% carbon- ley Bridge area on U.S. 89A (Fig. 13b). Pre- lent rocks to the southwest are assigned to the ate grains. viously, the Schnebly Hill Formation has been Supai Formation. In contrast, the Schnebly Hill and De Chelly assigned to various members of the Supai For- eolian sandstones formed on a leeward coast. mation or the Yeso Formation and De Chelly Sedimentologic Criteria The coast faced southeastward, and eolian sand Sandstone (Fig. 2). grains traveled hundreds of kilometers from the The physical correlations, supported by pa- north before reaching the sea (Baars, 1962; Bla- Lithology and Contacts léontologie data, provide the basis for the no- key, 1980, 1990). Even though the Schnebly menclature proposed in this report. In addition, Hill eolian units intimately intertongue with ma- The Schnebly Hill Formation is predomi- detailed pétrographie and sedimentologic studies rine and coastal deposits, not one grain of car- nantly a siliciclastic red-bed sequence with have yielded a regional picture of Pennsylvanian bonate has been found in the eolian units; the minor carbonate and local evaporite. Figure and Permian paleogeography (Lane, 1977; Bla- sand grains were derived from inland, not from 10 shows the distribution of lithology in the key, 1979a, 1979b, 1980, 1984; Blakey and the coast. formation. Middleton, 1983; Blakey and Knepp, 1989; The Hermit Formation in the Mogollon Rim The lower contact is everywhere sharp, prob- McAllen, 1984; Gallaher, 1984; Duffield, 1985). contains abundant carbonate concretions inter- ably unconformable, and sharply contrasts the These studies have provided a series of checks preted as caliche nodules by Duffield (1985). lithology, color, and outcrop characteristics of on previous hypotheses and have strengthened Similar nodules are present in Grand Canyon. the underlying Hermit or Supai Formations with the stratigraphie conclusions. The six lithofacies recognized by Duffield near those of the overlying Schnebly Hill Formation Several lines of pétrographie data support Sedona are also present in Grand Canyon, al- (Fig. 13). The upper contact is everywhere a physical correlation. Sandstone units in the though relative distribution appears to be differ- zone of gradation and/or intertonguing with the Supai Group are chiefly calcareous hybrid ent in the two areas. overlying De Chelly or Coconino Sandstones. quartzarenites. Carbonate and fossil content Sedimentologic studies have defined deposi- The contact with the Coconino Sandstone is a gradually increases westward along the western tional systems and trends within these systems. transition marked by change in sandstone strati- Mogollon Rim (McAllen, 1984) and into west- Facies changes in the Supai and Naco Groups fication style, decrease in ripple-laminated to ern Grand Canyon (McKee, 1982). Sandstone are related to position of depositional sequences wavy-bedded sandstone, and change in color units of the Schnebly Hill and Coconino are with respect to northwestward- and southeast- from reddish orange below to pale orangish tan noncalcareous and petrographically are easily ward-sloping shelves, respectively (Blakey, above (Blakey and Middleton, 1983). The ac- distinguished from most sandstone in the Supai 1980). The abrupt appearance of a sandstone tual contact is marked at the top of the highest Group. Sandstone in the Naco Group is similar marker bed at the base of the Schnebly Hill ripple-laminated, wavy-bedded, or flat-bedded to Supai sandstone but is finer grained and typi- Formation southeast of Sedona is related to the red silty sandstone and is everywhere within cally more silty. development of a marine sandwave sequence several meters of the color change. The reasons for the contrasting pétrographie (Blakey, 1984). Abrupt facies changes in the The contact with the De Chelly Sandstone is characteristics of the eolian sandstones in the Schnebly Hill Formation are related to eolian- marked both vertically and laterally by change Supai Group with those of the Schnebly shallow-marine processes that were controlled from reddish-brown, ripple-laminated to wavy-

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bedded sandstone and silty sandstone (Schnebly by ripple-laminated, very fine-grained sandstone present in some carbonate units. The member is Hill) to cross-stratified to wind-ripple-laminated, and silty sandstone. Averaging approximately poorly exposed in steep wooded slopes through- light grayish-orange to reddish-orange, fine- 150 m (500 ft) thick in the Sedona and Beaver out the eastern Mogollon Rim. grained sandstone (De Chelly). Creek areas, the Bell Rock Member gradually The Big A Butte Member ranges to about 150 thins eastward as it grades into the Big A Butte m (500 ft) thick in the Fort Apache area and Geometry and Extent Member. At many localities, the Bell Rock thins eastward owing to intertonguing with the Member overlies the Rancho Rojo Member Bell Rock Member. It is not recognized west of The Schnebly Hill Formation forms a south- with sharp transition. The westernmost extent of Fossil Creek, although thin silty and muddy eastward-thickening mass of strata that ranges the main body of the Bell Rock Member is the units in the Beaver Creek area probably repre- from a few meters thick on Picacho Butte to Dry Creek area; however, tongues of the unit sent westernmost tongues of the unit into the nearly 300 m in the central and eastern Mogol- extend westward into the Sycamore Canyon Bell Rock Member. The Big A Butte Member lon Rim (Fig. 10). The thickest known section is area (Fig. 5). The member forms slickrock coun- overlies the Bell Rock Member and is succeeded in the subsurface in the Holbrook basin, where try over much of the outcrop area. East of by the Fort Apache Member. nearly 600 m of strata are reported (Peirce and Beaver Creek, exposures are limited by heavy The Fort Apache Member was named the others, 1977). The formation is absent at Chino vegetation and onlapping Tertiary sediments "Fort Apache Limestone" by Stoyanow (1936) Point and at all locations in Grand Canyon but and basalts. In the Fort Apache area, good out- and assigned to the Supai Formation. It was is present in wells east of Grand Canyon (Baars, crops are limited to steep canyon walls. formally considered a member of the Supai 1962). Outcrops are restricted to the Mogollon The newly proposed Rancho Rojo Member is Formation by Jackson (1952), Winters (1963), Rim region, Mount Elden near Flagstaff, the named for Rancho Rojo Subdivision on High- and Gerrard (1969). Gerrard formally dropped Defiance Plateau, and possibly some flagstone way 179, 13 km (8 mi) south of Sedona. The the term "limestone," and that recommendation quarries north of Williams. type section is on the south flank of Wild Horse is followed herein. I formally assign the Fort Mesa, 0.7 km (2,000 ft) west of Arizona High- Apache Member to the Schnebly Hill Forma- Definition of Members way 179 along the jeep trail that winds up Dry tion because of the new correlations and reas- Beaver Creek, sec. 30, T. 16 N., R. 6 E., Yavapai signment of strata in this paper. The Sycamore Pass Member is herein defined County, Arizona (Sedona quadrangle). The The Fort Apache Member comprises lime- for extensive cross-stratified sandstone at Syca- Rancho Rojo Member forms a very distinctive stone, dolomite, limey siltstone, and in the more Pass, sec. 24, T. 18 N., R. 3 E., Yavapai light orange cliff in most areas of outcrop (Fig. subsurface, evaporite. Gerrard (1969) showed County, Arizona. The type section is along the 13c). It is composed of cross-stratified, very fine- that limestone increases to the southeast, dolo- Sycamore Pass (Dogie) trail and along the grained quartzarenite to subfeldspathic arenite. mite to the north and west, and evaporite to the southwest ridge of Casner Mountain (Sycamore Very large-scale compound cross-stratification is north in the Holbrook basin. Much of the unit is Basin and Loy Butte quadrangles). The member present at many outcrops. The master set is fossiliferous, and a paleontologic study by Win- is characterized by nearly 100% cross-stratified commonly as much as 7 m (24 ft) thick with ters (1963) demonstrated a Leonardian age for sandstone (Fig. 12b). It is 225 m (740 ft) thick at low- and medium-angle (7°-20°), wedge- or the unit. the type section and thins abruptly to the tabular-planar, cross-stratification with super- The Fort Apache Member pinches out be- northwest and southeast. Thinning to the imposed small to medium, irregular cross- tween clastic units at Boynton Canyon near northwest is due to the thinning and pinchout of stratification; broad, low-angle trough cross- Sedona. It thickens to more than 30 m (100 ft) the Schnebly Hill Formation, and thinning to stratification is also abundant (Blakey, 1984). in the Fort Apache area. It overlies the Bell the southeast is due to facies changes and inter- The member is present from the Dry Beaver Rock and Big A Butte Members and is overlain tonguing with other members (Fig. 5). Between Creek drainage area eastward to Fossil Creek. by the Sycamore Pass and Corduroy Members. Sycamore Pass and Bell Rock, a distance of North and south extent is unknown. It generally Boundaries are generally sharp. The Fort about 22 km (15 mi), the lower 150 m (500 ft) ranges from 6-12 m (20-40 ft) thick, but despite Apache Member forms a prominent cliff or part of Sycamore Pass Member grades, by inter- the thinness of the unit, it forms an easily map- of a cliff throughout its extent and is easily tonguing, into the Bell Rock Member. South pable, easily identified outcrop. Because of its mappable, even where thin, and is useful as a and east of Sedona, the Sycamore Pass Member distinctiveness, relative thinness, and ease of structural marker bed. overlies the Fort Apache Member, and east of mapping, the Rancho Rojo Member can be con- The Corduroy Member was named and as- Beaver Creek, it overlies the Corduroy Member. sidered a key bed and is useful for mapping signed to the Supai Formation by Winters The Sycamore Pass Member thins abruptly numerous faults in the Dry Beaver and Beaver (1963) and is herein reassigned to the Schnebly southeast of Fossil Creek. At most localities, the Creek areas. Both upper and lower contacts are Hill Formation. The type section is along Cor- Sycamore Pass Member forms towering cliffs, sharp; the latter is probably unconformable. duroy Creek. Lithologically, it is similar to the and the cross-stratified sandstone allows for easy The Big A Butte Member was originally as- Big A Butte Member, comprising siltstone, mud- recognition from adjacent members. From Fos- signed to the Supai Formation by Winters stone, gypsum, and carbonate; however, in the sil Creek westward to Picacho Butte, spectacular (1963). Because of the revised correlations in subsurface in the Holbrook basin, the member is intertonguing with the overlying Coconino this paper, the unit is reassigned to the Schnebly dominated by halite and other evaporites (Peirce Sandstone makes separation locally difficult. Hill Formation. The member is also restricted and Garrard, 1966). Like the Big A Butte The Bell Rock Member is herein named for slightly at the type section, Big A Butte on the Member, the Corduroy Member thins west- excellent exposures on Bell Rock, a prominent Fort Apache Indian Reservation, because the ward, where its stratigraphic position is replaced butte 11 km (7 mi) south of Sedona in sec. 12, lowest few tens of meters are assigned to the Bell by cross-stratified sandstone of the Sycamore T. 16 N., R. 5 E., Yavapai County, Arizona Rock Member. The Big A Butte Member com- Pass Member. It is generally not recognizable (Sedona quadrangle). At the type section and prises reddish-brown sandy siltstone, mudstone, west of Fossil Creek, although silty beds in the throughout its extent, the member is dominated gypsum, and carbonate. A molluscan fauna is Sycamore Pass Member near Beaver Creek

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~~sw * NE~~

~~3 2 o O o oi s£ a. o z I o<~~

~~beds at MESOZOIC ROCKS MOENKOPI Fort Defiance - KAIBAB~~

~~TOROV/EAPJH~~

~~|: ;'•.;• | DOMINANTLY CLASTIC ROCKS BASE ATOKAN' | 1 DOMINANTLY CARBONATE ROCKS~~

* PALEOZOIC ROCKS MISSING BETWEEN STARS [NOT TO SCALE)

~~CORDILLERAS MIOGEOCLINE GRANO CANYON EMBAYMENT MOGOLLON INNER SHELF PEDREGOSA BASIN~~

~~. MOENKOPI~~

~~. TERTIARY BASALT POST-PERMIAN EROSION /CONCHA LSj. .. SANDSTONE COCONINO.'. SCHERRER F.M. .~~

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~~• • • —? * • • — ,n& MPW » _q7 /COLIN# A LimwLIMESTONi viiEu~~

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Figure 14. Schematic southwest-northeast and northwest-southeast restored cross sections of Pennsyivanian and Permian rocks, Arizona and adjacent areas, showing time and lithologie relations of stratigraphie units recognized in this report.

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probably represent westward tongues of the stratigraphic record that are reflected region- thereby favoring widespread carbonate deposi- Corduroy Member. Winters (1963) reported a wide. For example, lowstands of sea level that tion. Typically, thin dolomite beds mark the ma- thickness of 111 m (370 ft) at the type section. exposed broad lowlands, influx of quartz sand rine highstand well beyond the limits of normal from the north, and favorable climatic condi- shallow-marine deposition. INTERPRETATION, DEPOSITIONAL tions yielded several widespread episodes of eo- Sharp tectonic uplift in areas such as the An- HISTORY, AND SIGNIFICANCE lian deposition (Blakey, 1988; Blakey and cestral Rockies or perhaps even the Ouachita- others, 1988; Chan and Kocurek, 1988). Not Marathon belt (see Armin, 1987) can generate Event Stratigraphy only does the eolian sequence contrast with sed- widespread fluvial events. Several fluvial events iments formed by most other depositional sys- are known to have occurred in the late Paleozoic Although lithologic and biostratigraphic con- tems, but the eolian dune deposits of the in the vicinity of the southern Colorado Plateau. trol are not fully adequate for making medium- sand-sea center pass laterally into eolian erg- This line of reasoning leads to the recognition and long-range correlations in Pennsylvanian margin facies, also a distinctive sedimentologie of various stratigraphic intervals, separated from and Permian rocks on the southern Colorado sequence (Porter, 1986). Thus, in many cases, each other by sharp to diffuse boundaries. Defi- Plateau, the very nature of the heterogeneity and the eolian interval can be correlated far beyond nition of these intervals will constantly evolve as cyclicity provides another tool for correlation: the typical cross-stratified sandstone. more detailed sedimentologic work is done. If the stratigraphic pulse. Unusual or extreme Conversely, highstands of sea level cut off carefully defined and interpreted, intervals of events, caused by eustasy, tectonics, climate, or lanes of eolian transport (Chan and Kocurek, relatively small scale, perhaps less than 30 m a combination thereof, may cause changes in the 1988) and trap fluvial sediment in river mouths, thick, may be correlated over long distances.

~~SELIGMAN CHINO VALLEY SYCAMORE-SEDONA FOSSIL CREEK HOLBROOK~~

~~52 27, 45 53 GG,HH EE FF DO~~

~~- IOOO~~

~~240- ACCESSORY, MI SC.: 500 120 oooooo extrabasinal HOLBROOK BASIN intrabasinal } Pebbles ++ + + Salt xl casts~~

~~m O-l-O ft Gypsum~~

50 mi Figure 15. Restored section of Pennsylvanian and Permian rocks from the Mogollon Rim H to the Defiance Plateau and Monument upward. See Figure I for location of data points. 40 80 km (Note overlap in center.)

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Stratigraphie Sequences tems in which both local and regional trends this paper and is directly responsible for the match details of the local section (Fig. 14). The complex physical stratigraphy manifested as The tectonic conditions discussed above re- data gathered at the local section form the foun- complex facies changes and cyclic sedimenta- sulted in several genetically related, informally dation of this report. Another aspect of this point tion. It controlled the position and behavior of defined, units of rock called "sequences" (Bla- is the close relation between late Paleozoic tec- shorelines, eolian sand seas, rivers, and sabkhas. key, 1979a, 1979b, 1980). These sequences fa- tonic elements and the deposition systems that The fact that red beds increase throughout the cilitate understanding of the complex stratig- formed during this time. Blakey (1988) detailed section and rocks thin across this structure is no raphy and help to demonstrate the independent these relations across the southern two-thirds of coincidence. It is the merging of these red beds or interdependent depositional histories of the the Colorado Plateau. Tectonic elements are de- and the wedgeout of intervening fossiliferous stratigraphie units discussed in this paper. Strati- fined from the geometry of the stratigraphie se- carbonate units that have created the problems graphic sequences for Pennsylvanian and Per- quences. If the stratigraphy of the local section of correlation facing physical stratigraphers. For- mian rocks of central and northern Arizona does not match the depositional and tectonic tunately, several incursions of eolian deposition were defined by Blakey (1980) and are not re- model, then the model must be modified; the punctuate the section across the Sedona arch. peated herein; their interpretation is provided at data of the local section do not change. These eolian deposits differ in detail of facies, the end of this paper. Isopachs and facies patterns of Pennsylvanian petrology, and geometry and provide powerful and Permian rocks demonstrate beyond doubt information for interpreting the regional stratig- Facies Assemblages the presence of the Sedona arch, with its raphy. If these details are overlooked in making northeast-southwest trend across central Ari- local and regional correlation, then errors will The geometry of the correlated sequences and zona (Blakey, 1980, 1988). This structure result in the interpretation. the facies they contain define depositional sys- affected every stratigraphie interval discussed in All of the Permian eolian sand migrated into

*OOK S. DEFIANCE PLATEAU CANYON DE CHELLY MONUMENT VALLEY

~~D 105 108~~

~~ASIN SANDSTONE: (HI X-bed., chiefly large-scale, eolian~~

~~X-bed., w/ red SS, MS Figure 15. (Continued). I'.•./.•.'• '• I Wavy to ripple laminated~~

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the study area from the northwest and north Wescogame Formations, Esplanade Sandstone); Schnebly Hill Formation and lower Coconino (Baars, 1962; Blakey, 1988; Blakey and others, three times, the sand was derived from inland Sandstone are dominated by distinctive wavy- 1988; Johansen, 1988; Parrish and Peterson, and was blown toward southeast-facing coasts to ripple-laminated sandstone to silty sandstone, 1988; Peterson, 1988). As previously discussed, and consists of quartzarenite (lower and upper typically reddish brown to pale orange in color, sand derived from northwest-facing coastlines, Schnebly Hill Formation and equivalent De that forms thin to thick continuous sheet-like the predominant depositional pattern during the Chelly Sandstone, lower Coconino Sandstone). bodies between cosets of eolian sandstone; bases Pennsylvanian and Wolfcampian, contains abun- The upper Coconino Sandstone bordered a are always erosional, and tops typically grade dant carbonate grains (peloids, abraded fossils, broad coastal sabkha adjacent to the Toroweap upward into the overlying eolian sequence (Bla- oolites). Sand derived from inland sand seas and Sea (Rawson and Turner-Peterson, 1980), key and Middleton, 1983). Salt-crystal casts, blown onto southeast-facing coastlines, the pre- which apparently lacked material that could slumping, and invertebrate burrows are locally dominant pattern during the middle Leonardian, form carbonate grains. present. Although the units may fill broad scours lacks carbonate grains. Seven times during the Each of the above eolian sequences contains thought to be formed by eolian scouring (blow- Pennsylvanian and Permian, eolian sandstone adjacent associated erg-margin and noneolian outs), sharp channel-like features are rare. In was deposited on the flanks of or across the facies. These also differ in detail from each other contrast, erg-margin and noneolian deposits as- Sedona arch (Figs. 15 and 16); three times, the and can be used to differentiate and correlate sociated with eolian deposition in the Supai eolian deposits were related to northwest-facing red-bed sequences. Although a complete discus- Group include structureless mudstone with or coasts (Blakey, 1990) where abundant carbon- sion of this is beyond the scope of this paper, without nodular limestone concretions, limey ate grains were available and consist of carbon- several key features will serve as example. Erg- sandstone with planar to low-angle lamination, ate hybrid quartzarenite (Manakacha and margin and noneolian facies associated with the and nodular, limey, structureless to faintly lami-

~~NORTHWEST SOUTHEAST W. GRAND CANYON CHINO VALLEY SEDONA FOSSIL CREEK FT. APACHE~~

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~~EXPLANATION Eolian sandstone~~

~~ggg ^^MANAKÀCHÀ ra Marine carbonate Pebbles : Intraformational Redbeds, includes some ss extraformational • Gray to tan mudstone oo0oo m Unconformity~~

~~Figure 16. Time-stratigraphic diagram showing general extent, facies, and relations to unconformities of Pennsylvanian and Permian rocks of central Arizona.~~

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nated very fine-grained sandstone. Each of these Outcrops between Sycamore Canyon and Fossil Cordilleran miogeocline and northward in the is generally reddish gray to dark reddish brown, Creek clearly show the facies patterns on the Paradox basin. commonly with purplish cast. The geometry of west side of the basin (Blakey and Middleton, Virgilian Red-Bed Sequence. Virgilian rocks these deposits ranges from broad sheets to nar- 1983), and exposures on the central and south- consist chiefly of fine-grained red clastic detritus, row ribbon-like bodies. Overall, bedding is ern Defiance Plateau (Fig. 15) have very similar lighter cross-stratified sandstone, and interbedded much more irregular than that associated with sedimentologic patterns on the north side of the carbonate. They were deposited across the entire the Schnebly Hill Formation and Coconino basin. Subsurface data show coeval basinal pat- area of study (Figs. 4 and 5). From Sedona Sandstone, and channel-like geometry is com- terns and define highstands and lowstands of sea north and west into Grand Canyon (Wescogame mon. These characteristics serve to separate pre- level downwind from the sequences of eolian Formation), the sequence gradually thickens dominantly red-bed units of the Supai Group progradation. toward the Cordilleran miogeocline, and marine from those associated with eolian deposits of the deposits increase. Southeastward in the central Schnebly Hill Formation and Coconino Sand- Depositional History and eastern Mogollon Rim (lower part of Supai stone. Although no single criterion is foolproof, Formation), carbonate and fossil content in- when they are used together in moderate or bet- Correct lithostratigraphic correlation coupled creases. Scattered fossils and physical character- ter outcrops, the units are clearly distinguishable. with a consistent, simple, and comprehensive istics suggest that the red beds formed in Red beds in the Hermit Formation and Supai nomenclature system is paramount to correct in- shallow-marine and coastal-lowland conditions Formation (undivided) have overall characteris- terpretation of geologic history, presented here (Ross, 1973; Blakey, 1980; McKee, 1982) and tics similar to those of the Supai Group. In sev- by stratigraphic sequence. that the cross-stratified sandstone formed under eral areas, for example Toroweap Valley in Morrowan-Atokan Marine Sequence. In eolian conditions (Blakey and others, 1988). Grand Canyon and Picacho Butte and Oak the area of study, Morrowan and Atokan rocks The eolian sandstone and hybrid sandstone are Creek Canyon in the Mogollon Rim region, eo- are distributed west of the Sedona arch in the similar in form and origin to those of the Mana- lian sandstone bodies occur as much as 50 m Grand Canyon embayment. Outcrops are along kacha Formation. above the base of the Hermit. In poor or isolated the Mogollon Rim west of Sedona and can be Wolfcampian Sandstone Sequence. A per- outcrops, these sequences could be difficult to correlated into western Grand Canyon (Figs. 4 sistent blanket of sandstone covered the region separate from the Esplanade Sandstone, but in and 5). The sequence comprises limestone, mud- west of the Sedona arch and northward into most areas, the fact that the Esplanade is domi- stone, and basal conglomerate (Watahomigi southern Utah. Indirectly but probably accu- nated by ledge-forming sandstone and the Her- Formation) and upper chiefly cross-stratified rately dated as Wolfcampian by stratigraphic mit by slope-facing red beds serves to distinguish quartzose to hybrid sandstone (Manakacha position and intertonguing relations, the cross- the two units. Formation). A marine, coastal, and eolian origin stratified sandstone (Esplanade Sandstone in Slope-forming units in the Naco Formation is documented by scattered marine fossils, strati- Arizona, Cedar Mesa Sandstone in Utah) may be very similar to those in the Supai For- graphic sequences, and sedimentary structures formed in a variety of eolian, shallow-marine, mation and Group and Hermit Formation, ex- (Blakey, 1980; McKee, 1982; Blakey and others, and estuarine conditions (Blakey, 1980, 1990; cept that they tend to be less red in color and 1988). Work in progress (Blakey, 1990) sug- McKee, 1982; Loope, 1984; McAUen, 1984). may have a higher carbonate content. Com- gests that much cross-stratified sandstone and The Esplanade-Cedar Mesa complex forms a monly, Naco Formation fine-grained siliciclastic limestone (including carbonate-grain hybrid broad eolian coastal-dune and inland-erg com- units are tannish, to grayish, to purplish gray. sandstone) in the Manakacha Formation formed plex sandwiched between shallow-marine and Because of poor outcrops, their geometry is not as linear eolian dunes during low stages of sea coastal-plain deposits to the northwest and well understood, but they appear to crop out as level. Northwest winds blowing over exposed fluvial red beds of the Cutler, Organ Rock, and broad sheets. carbonate shoals transported carbonate and Hermit Formations to the east and southeast. quartz grains into coastal dune complexes. Intercalations of marine and eolian deposits Correlation between Mogollon Rim and Atokan rocks are also present in parts of the have been interpreted as resulting from eustatic Defiance Plateau Paradox basin of the Four Corners, and Mor- sea-level changes (Loope, 1984, 1985), and rowan and Atokan rocks are present in the eolian-fluvial interactions have been related to Perhaps no topic of regional upper Paleozoic Pedregosa basin of southeastern Arizona. flooding of interdunal areas by fluvial processes (Langford, 1987). stratigraphy is more controversial than the corre- Desmoinesian-Missourian Marine Se- lation of Pennsylvanian and Permian rocks of quence. Desmoinesian and Missourian rocks Wolfcampian-Leonardian Red-Bed Se- the Mogollon Rim with Permian rocks of the are restricted to the Mogollon Rim east of the quence. The Wolfcampian-Leonardian red-bed Defiance Plateau. Published correlations by Sedona arch across the Mogollon shelf (Figs. 4 sequence is the most widespread sequence in the Baars (1962), Blakey (1980), and Peirce and and 5). They can be directly correlated into the study area; this fluvial interval bears Early Per- others (1977) vary significantly. The correla- Pedregosa basin (Ross, 1973). Numerous fossils mian plant and vertebrate remains. It was depos- tions presented in this paper (Fig. 15) have used document widespread shallow-marine condi- ited across the western Mogollon Rim and all available surface and subsurface data and rely tions (Brew, 1965; Brew and Beus, 1976; Ross, Grand Canyon region (Hermit Formation). heavily on the stratigraphic principles discussed 1973). The cyclic carbonate and mudstone se- The chiefly red sandstone and mudstone also in the preceding pages. Most significant are the quence (Naco Formation) thins abruptly west- blanketed the Mogollon Rim east of Sedona facies patterns that resulted when eolian erg- ward against the Sedona arch and does not (upper part of Supai Formation) and much of center and erg-margin deposits prograded across intertongue with Supai clastic rocks as assumed southern Utah (Organ Rock Formation). It ex- adjacent basin and basin-margin sabkha and by some authors (Jackson, 1952). Rocks of this tended westward well into the Cordilleran mio- shallow-marine deposits of the Holbrook basin. age were deposited west of Grand Canyon in the geocline and is probably represented by

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unnamed red beds in the Keystone thrust of these events and speculate as to some of their tectonic framework emerges, which consisted of southern Nevada (Bissell, 1969). It is present as causes or significance. intervening arches and shelves that separated the upper part of the Earp Formation in the Major sedimentologic pulses and intervening major basins. Sedimentation and the resulting Pedregosa basin (Ross, 1973). The sequence unconformities are shown in Figure 16. These stratigraphy were related to tectonic setting. was deposited in fluvial and coastal-plain set- patterns show the stratigraphic sequences dis- Strong differences in timing, strength, and dura- tings (White, 1929; Baars, 1962; Ross, 1973; cussed previously. Note the smaller pulses tion of the various tectonic elements greatly Blakey, 1980; Duffield, 1985). within some of the stratigraphic units. Some, complicated the stratigraphy. Leonardian Sandstone and Red-Bed Se- such as the carbonate tongues of the Wata- 3. During Morrowan, Atokan, Virgilian, and quence. The Leonardian sandstone and red-bed homigi, Naco, Pakoon, Schnebly Hill, and Wolfcampian time, strata of the Supai Group sequence is dated on the basis of marine fossils, Toroweap Formations, represent marine high- were deposited west of the Sedona arch in the including conodonts. It was deposited across stands. Eolian tongues and pulses probably are Grand Canyon embayment. Only Virgilian and east of (but not west of) the Sedona arch related to lowstands of sea level (Chan and strata are physically continuous with the Naco (Figs. 4 and 5). The sequence is centered about Kocurek, 1988). Unconformities may represent Group to the southeast. The Naco comprises the Holbrook basin and displays a classic basinal marine lowstands but also likely reflect local to rocks of Desmoinesian, Missourian, and Vir- bulls-eye facies pattern (Blakey, 1980). The regional upwarp. Basal conglomerates immedi- gilian age, which were deposited east of the deposits (Schnebly Hill Formation) consist of a ately overlying regional unconformities support Sedona arch on the Mogollon shelf. western and northern fringe of cross-stratified this latter contention. Note that many con- 4. Uppermost Wolfcampian to lower Leo- eolian sandstone (Blakey and Middleton, 1983) glomerates are of intraformational origin or nardian rocks of the Hermit Formation can be that grades basinward into red beds, evapo'rite, have and reflect local sedimentary processes correlated from western Grand Canyon through- and marine carbonate (Fort Apache Member). rather than regional tectonic or climatic events. out the Mogollon Rim region. The term "Her- Northward in the Four Corners, the upper part Armin (1987) was one of the first workers to mit" is not used east of Sedona because of of the unit constitutes the De Chelly Sandstone directly relate a late Paleozoic depositional event difficulties in establishing a consistent lower and eastward in New Mexico the Yeso Forma- in Arizona with external tectonic events. He re- boundary. tion. Work in progress and shown in Figure 15 lated a middle to upper Wolfcampian conglom- 5. The Holbrook basin was a strongly nega- suggests that pulses of eolian sandstone into the erate sequence in the Pedregosa basin to fore- tive element during the Leonardian. The Schneb- Holbrook basin can be correlated basin-wide. bulge development in response to foreland basin ly Hill Formation is present within and to the These pulses thus provide potential regional loading adjacent to the Marathon orogeny. The west, southwest, and south of this feature. The stratigraphic correlation. Eolian-margin sedi- distal effects of this event may be reflected in the De Chelly Sandstone is present on the northern mentation extends well beyond the limit of red beds and conglomerate of the Hermit For- and eastern flanks. dune deposition and is reflected well out into mation and upper Supai Formation. Closer to 6. Stratigraphic terminology reflects the basinal sabkha deposits. Conversely, during northern Arizona, the tectonic effects of the Un- uniqueness of each of the above stratigraphic highstands of sea level, dolomitic marker beds compahgre element of the Ancestral Rocky sequences and tectonic elements. One new for- extended into eolian dune complexes. Mountains may be reflected in the rocks of the mation, the Schnebly Hill Formation, is for- Leonardian Quartzarenite Sequence. The study area. The Monument and Sedona arches mally proposed. Three new members are Leonardian quartzarenite sequence forms the and Defiance upwarp may be forebulges related recognized, and three members, previously as- top of the interval of study and was deposited to Ancestral Rockies foreland basin develop- signed to the "Supai Formation," are reassigned throughout the Mogollon Rim and Grand Can- ment. Direct correlation between timing of An- to the Schnebly Hill Formation. yon. The sequence (Coconino Sandstone) thins cestral Rockies tectonic events and distal 7. The broadest regional correlation is com- in all directions from the central Mogollon Rim sedimentation in northern Arizona cannot be prehensively shown in Figure 15. It reflects the region. It correlates with the Glorieta Sandstone made at present. latest data and interpretations available. The of New Mexico and the Scherrer Formation of The correlations presented in this paper along depositional sequences discussed in this paper southeastern Arizona. An eolian origin has been with depositional events and stratigraphic pulses stand out as distilled and filtered intervals of documented for much of the sequence (McKee, apparent within the correlation provide a foun- deposition with logical and explainable facies 1983; Blakey and Middleton, 1983). The upper dation for further research. It may soon be pos- changes. In spite of seemingly complex repeti- part of the Coconino Sandstone (White Rim sible to refine sea-level curves, date orogenic tive lithologic intervals typically seen at the local Sandstone in Utah) grades westward into the events, and define climatic cycles within the late outcrop, the forest can be seen through the trees. Toroweap Formation (Irwin, 1976; Rawson Paleozoic of the southern Colorado Plateau. and Turner-Peterson, 1980). ACKNOWLEDGMENTS CONCLUSIONS Tectonic Significance A number of individuals assisted in the prep- 1. Stratigraphic, paleontologic, lithologic, aration of the paper. Various drafts were re- The correlations presented herein clearly petrographic, and sedimentologic data provide viewed by Don Baars, Stan Beus, Doug Brew, show regional to subregional sedimentologic powerful constraints to which any local, sub- C. Dennis Irwin, Wes Peirce, and Fred Peterson. and tectonic events. Although the relation of regional, and regional correlation of Pennsyl- Financial support was provided by the Organ- these events to the overall tectonic evolution of vanian and Permian strata of central and ized Research Committee and the Bilby Re- southwestern North America is beyond the northern Arizona must conform. search Center, both of Northern Arizona scope of this paper, it is appropriate to identify 2. From these data, an interpretation of the University.

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