Permian Sedimentary Rocks of the Black Mesa Basin Area H

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Permian sedimentary rocks of the Black Mesa Basin area H. Wesley Peirce, 1958, pp. 82-87 in: Black Mesa Basin (Northeastern Arizona), Anderson, R. Y.; Harshbarger, J. W.; [eds.], New Mexico Geological Society 9th Annual Fall Field Conference Guidebook, 205 p.

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PERMIAN SEDIMENTARY ROCKS OF THE BLACK MESA BASIN AREA

by H. WESLEY PEIRCE Arizona Bureau of Mines University of Arizona

GENERAL STATEMENT Figure No. 2 is an attempt to show the thickness dis- Information regarding Permian sedimentary rocks of tribution of the Supai formation in northeastern Arizona. the Black Mesa structural basin must be gathered from a In the area just south of the San Juan River all of the few drill holes and disconnected outcrops on the fringes of Cutler formation below the DeChelly sandstone has been the basin. From the center of the Black Mesa physio- considered Supai for all practical purposes. The figure graphic feature it is approximately 80, 72, 60, and 40 demonstrates the basining around the Holbrook area which miles south, west, north, and east respectively to the Mo- contrasts with the formational thinning onto the Defiance gollon Plateau, Grand Canyon, Monument Valley, and the and Mogollon Rim areas to the east and south respectively. Defiance Plateau where Permian sedimentary rocks crop The configuration of the zone of significant evaporite ac- out. As drill hole data are limited over most of the basin cumulation is not known to the north along the flank of area, projected trends through the basin are highly specu- the Defiance. Recent mapping in the Mogollon Rim to lative. the south has disclosed only minor beds of gypsum occurring PERMIAN BOUNDARIES near the top of the formation. Previous workers have emphasized the difficulty of The control point just southeast of Kaibito in the north- drawing a precise boundary between Pennsylvanian and central part of the area (fig. 2) is based on a log of a Permian sedimentary rocks in northern Arizona. That the test hole drilled by the Sinclair Oil Company in 1952. The Supai, lowermost of the Permian formations, crosses the log suggests that the interval between the top of the Rico Pennsylvanian-Permian boundary seems well established formation and the bottom of the DeChelly is only 580 feet by studies that have been made in parts of the Grand thick. This is the thinnest Supai (Organ Rock tongue of Canyon and Mogollon Plateau regions—Noble (1922), the Cutler fm.) in the area and creates the need for rep- Hughes 11950), Jackson (1951), Huddle and Dobrovolny resenting a northwest-southeast zone of thinned Supai that (1945), and Winters (1950). In western Grand Canyon trends toward the Black Mesa basin. and along portions of the Mogollon Rim the red sedimen- Evidently the paleogeographic framework that con- tary rocks of the Supai formation are interbedded with trolled the Supai formation was initiated during the Penn- marine limestones near the base in a manner that would sylvanian and continued into the Permian period. The seem to be analogous to the Rico "transition interval" de- floor of the deepening Pennsylvanian-Permian Supai basin scribed by Bailey (1955) in the Four Corners region. must have been sinking more rapidly than the previously In eastern Grand Canyon and at Jerome the Supai existing Defiance positive area and the area along the formation rests on the Mississippian Redwall limestone. present Mogollon Rim. Details of the configuration and extent of the latter type Cutler formation of contact are not known but undoubtedly it trends towards As indicated in the legend of figures 1-4, the Cutler the western margins of the Black Mesa basin. On the formation of the Monument Valley area is composed of Defiance Plateau as well as near St. Johns, Permian sedi- five members. Although Baker and Reeside (1929) be- mentary rocks are in depositional contact with granite and lieve that the Permian section in Monument Valley con- quartzite of probable Precambrian age (fig. 1). Permian trasts markedly with the Grand Canyon section, the writer sedimentary rocks are overlain by Triassic formations in suggests that except for the absence of the Kaibab forma- the Black Mesa basin but are truncated by upper Creta- tion and the insertion by them of the Hoskininni tongue ceous sandstones along parts of the Mogollon Rim to the at the top of the section, the stratigraphic sequences of the south. two disconnected provices have much in common (fig. 1 ). SOME ASPECTS OF PERMIAN STRATIGRAPHY The Cedar Mesa sandstone member of the Cutler formation Supai-Hermit formations passes laterally into red beds to the southeast, south, and The term "Supai" is currently used over all of northern probably southwest as this sandstone was not recognized Arizona except in the Four Corners area. As used it refers in the Sinclair test hole previously mentioned. The Organ to a multiple lithologic sequence dominated by reddish Rock and Halgaito red bed tongues thus coalesce to form clastics with varying modifications, but in large part sandy. a sedimentary sequence that cannot be readily differentiat- Although the formation contains some limestone, only the ed from the Supai formation of the Black Mesa basin area. prominent Ft. Apache limestone unit of the Mogollon Rim Baker and Reeside (1929) as well as Baker (1936) and area has been given a formal name. Evaporitic material Baker and Williams (1940) all picture the Cedar Mesa as well as evaporites seem to be concentrated in the and DeChelly sandstones as merging westward to form Holbrook to St. Johns region where the Supai formation the Coconino sandstone. McKee (1933) is not in agree- attains its greatest known thickness of approximately 2600 ment with this concept and the present writer is in agree- feet (figs. 1 and 2). ment with McKees views. It seems highly unlikely that The Hermit formation disconformably overlies the Supai the 57 feet of Coconino sandstone near Lees Ferry rep- formation in the Grand Canyon region and areas to the resents the 1300 feet of section from the top of the De- north. Evidently the Hermit merges laterally with the Supai Chelly sandstone to the bottom of the Cedar Mesa sand- southward towards Oak Creek Canyon as at this locality stone as shown in the Texas Company Hoskininni Mesa oil the Coconino sandstone, which overlies the Hermit in the test in western Monument Valley (fig. 1). Grand Canyon, is in gradational contact with sedimentary Coconino-DeChelly sandstones rocks of Supai lithology. The Hermit formation, as in the The Coconino sandstone of the Grand Canyon-Mogol- Grand Canyon area, is not known to extend into the Ion Plateau regions and the DeChelly sandstone of the Black Mesa basin. Defiance Plateau and Monument Valley areas everywhere NEW MEXICO GEOLOGICAL SOCIETY 0 NINTH FIELD CONFERENCE 83

EXPLANATION 7 PIO Mogollon Plateau Area Sections: 1-Argo Oil Co. St. No. 2 well 2-Franco-Ariz. Oil Co. Govt. No. 1 3-Gt. Basin Oil, Taylor-Fuller No. I

Grand Canyon Area Sections: 4-Oak Creek Canyon •sdc 5-Bass Trail Pik 6-Little Colorado River 7-Badger Canyon Ps MESA Ps Monument Valley Section: 8-Texas Co. Hoskininni Mesa test BASIN

Defiance Plateau Sections: 9-Canyon DeChelly area 10-Hunters Point 11-Pine Springs Pudc-Upper member DeChelly ss Pldc-Lower member DeChelly ss

Pc Gr- Granite Qtz- Quartzite

Stratigraphic symbols as shown in Ps previous figures.

Evaporitic sandy sits ss

Evaporite

Vertical Scale 1"= 1,000

0 18 36

FIGURE 1. Typical Permian sections surrounding the Black Mesa basin with possible relationships. Scale - Miles overlie, so far as is known, red sedimentary rocks. The Unequivocal solutions to problems of this sort are Coconino has been studied over a wide area by McKee difficult to establish when stratigraphic relationships can- (1933). McKee (1934) spent a few days working on not be traced and key beds such as the Kaibab-San Andres the DeChelly sandstone of part of the Defiance Plateau, limestone are absent in all known exposed outcrops in the particularly at the type section in Canyon DeChelly. Geol- Defiance area. Correlation in such cases must be based ogists who have worked in the areas of outcrop of these on relative stratigraphic sequence, lithologic details, and sandstones have expressed differing opinions as to the in this case particularly, the characteristics that may or relationship between them. Gregory (1917) named the may not reflect similarities in environments of deposition. DeChelly but did not attempt to make a correlation to the A critical analysis of these features has not been west. Darton (1925) mapped the sandstones on the De- published for all of the DeChelly sandstone as it is pres- fiance Plateau as Coconino and in his text he states: ently defined in the Defiance Plateau and Monument Valley "The sandstone (Coconino) is uplifted and exposed areas. The writer is not aware of a detailed analysis of over a considerable area extending from near Win- the Glorieta sandstone that compares with the studies that slow to Holbrook and into the Defiance uplift in the have been made of the Coconino sandstone. Until some central and northern part of Apache County where of the details are obtained correlation will largely be made there cannot be the slightest doubt as to its identity." from red-bed to red-bed and from sandstone to sandstone. Baker and Reeside (1929) refer this sandstone back The writer has had the opportunity to visit many of to the DeChelly suggesting that correlation with the Grand the outcrops of DeChelly sandstone in both the Defiance Canyon Coconino could not be definitely established. Mc- Plateau and Monument Valley regions. Regarding the Kee (1934) expressed the view that both a DeChelly and DeChelly sandstone it can be said that: (1) the sandstone a Coconino sandstone were recognizable and that the pinches out northward near the San Juan River in Utah Coconino sandstone graded laterally northward into the and that, in the opinion of the writer, pinch out is due upper part of the DeChelly sandstone. Read (1951) sug- largely to non-deposition and erosion in contrast to lateral gested that the sandstones exposed on the south and east gradation into red beds, (2) that the interval of the De- portion of the Defiance Plateau might well be called the fiance Plateau now called DeChelly sandstone is made Glorieta sandstone of the San Andres formation as seen up of units deposited in differing environments, (3) that in the Zuni area of New Mexico. the DeChelly thins to the south from near 800 feet at the

84 NEW MEXICO GEOLOGICAL SOCIETY 0 NINTH FIELD CONFERENCE

BLUFF

“",/,•,- ii;Ti -,,:;ili:" WZ.,.. •,iA I ■ ••■ 0 n 5 LEESL , FERRY Y \\ N 555555o \

,--- x : \ , \ 4.11TE N TA 1 •‘ III e / TO 1 1 li /...... , \ .s. EXPLANATION .5. i \ ...... -i5.. , 1 I ‘ . I.1\, , • 600\ . / , I 1 Grand Canyon-Central Ariz. : 5. , l000 / \ % .. \ -- - -- Pk-Kaibab fm. 55 5os+ if N i • / / I I \ ; i // j 1 , / Pt-Toroweap fm. / , / 1 I 1 1 • /, - I 1 BR SS TRAIL 00 • :--- I / ,----, Pc-Coconino ss. I I # • • — -" / // / /1 . Ph-Hermit fm. 1 000.540,, ,..,...\ 5 ;::::.. / I ro;. I i ;"tr!,-;-,"-2. 5 T14 ° ..• • // / / / "Si Ps-Supai fm. 1 /-5..75■...\, " T: : : 4117 ,1, :_., DLS, E R.r. S ...... 1 / / / I .5, , 5 / / / H...♦ % 1 i 1 i LT 5,•/ ... , ..H / / / ! i P . .es Monument Valley :5- ! I I 1 I l 1 = ■ / / / 1 1 I , I IA :::1_ , T. \ \ Cutler fm. 1 t S .....„____ ‘40 o .. II ■ 1 II Pho-Hoskininni tongue \ \ -.... 5 // // , /,111_,, ‘ „ \ ST,i ■ t ::::; II Ii I Pdc-DeChelly ss. ‘ 8 Ve,, ,/ / / / 1 i I k \ ‘ , d HUNTERS , Po-Organ Rock tongue : / / Pcm-Cedar Mesa ss. ‘ • \ _ _ ..... --- ti: / / , I ; ,?, ; \"\-°• PT1 : I Pht-Fialgaito tongue \ • ■ ‘,,,;.,... .■■:ecr . SELIGMAN \ . / / / r % ii „ . ...(0 -. : I WILLI AMS \ u•• • • =0./ / 1 I \ \ \ \\ \ : ..5.0 Defiance Plateau \ n ,:.::. \ C \ ,0 o ;; %LA:Sin F F ; / / / 1 I I oo !, Pdc-DeChelly ss. ,, _ \ %- O:o. I ... I- / / 0 , ■ \ •x Ps-Supai fm. "-"°: ) 1 0.. / . i// OS , 11( . , o I, ■ -5° -/- / ■ / o 1 `. I RMF . NOLSROO / , / / l,/,/ ,, En el; , I 5— .:VsEIDON A / 0 Vo 0 i O s, 1 20 // ! 220. _Fl....._o ,,-T,_o.s AREj...... 400:015 ,C , t , •=^— 2000 1 _ 0 5 30 .555 !ITT SCALE — MILES ,, t "72– - – ifoo- - - .....--i- i i

FIGURE 2. Thickness distribution of the Supai formation.

type section in Canyon DeChelly to near 300 feet at Andres formation, (3) that the changed aspect is totally Pine Springs with reason to suspect further thinning to the different from environments of deposition seen in the type south, (4) that this thinning is due (a) to a loss of the section and might be altogether a phase of the San Andres lower member by rapid lateral change to Supai lithology formation, and (4) that the changing aspect is not related a few miles south of Hunters Point between Oak Springs to either the Supai or San Andres formations but represents and Black Creek Canyon, and (b) to thinning of the upper a changing environment laterally gradational into type member from near 500 feet at Canyon DeChelly to near section DeChelly sandstone. 300 feet in the Pine Springs area. The manner of the The writer cannot readily choose between these pos- thinning of the upper member is not clear and is com- sibilities. Of considerable potential significance is a lith- plicated by the fact that the lithologic and sedimentary ologic log and samples from a water well on file at the structural characteristics over much of the east flank of the Museum of Northern Arizona at Flagstaff. These data Defiance is not a replica of the upper member character- indicate that there is a few feet of limestone between the istics as seen in Canyon DeChelly. The conspicuous differ- Moenkopi formation and the DeChelly sandstone at St. ence is the decided increase in the number and thickness Michaels near the east flank of the Defiance uplift. The of horizontally bedded sandstones and silty sandstones writer has looked at these samples and there is no doubt seen in sections on the eastern and southern sections of about the existence of limestone in the samples. It is the Defiance Plateau. This is in contrast with an almost gray, very dense and similar m general appearance to homogeneous development of large-scale cross-stratifica- some of the limestones in the San Andres formation in the tion as seen at Canyon DeChelly and at Nazlini Canyon Zuni area in New Mexico and to one phase of the Kaibab south of Canyon DeChelly on the west flank of the De- limestone that is exposed south of Showlow. A limestone fiance uplift. in this position has not been recorded elsewhere in the Four possibilities can be mentioned to account for Defiance area. It seems likely that many of the pecu- the changing aspect in the upper member of the DeChelly liarities in the stratigraphy on the east flank of the De- sandstone: (1) that the large scale cross-stratified sand- finance uplift may be related to the San Andres formation stones are intertonguing laterally with the Supai or equi- as partially suggested by Read (1951) when he considered valents, (2) that the large-scale cross-stratified sandstones some of the sandstones (Black Creek section) to be of are intertonguing laterally with some phase of the San Glorieta type. If the San Andres is represented then it NEW MEXICO GEOLOGICAL SOCIETY 4 NINTH FIELD CONFERENCE 85

WARE 1.17111. , j2,,,,,, , C•Irs; , 4 ‘I. RIVER RIP

na 6 - _

I. g ts ..,.. stitly AO./ • .-- iii17%• -----"--.-"- 111:•° I " .... I _ I I 0 • ° . IRVENTA I . ... .1 --- 2 0 ° 0 ti II ITO 50 V •-se EXPLANATION .00 -1.:, I to o 7 1 / / %.! Grand Canyon-Central Ariz. .•1 6° /, / i Pk-Kaibab fm. .1...... ,,,,- / •A S• TR•1 Pt-Toroweap fm. • )1 TA . / e /:;!1s Pc-Coconino ss. / (O., H ...•• II, ,.• 4:::,:._17,-/ -2 -_,,---,2::. / / ...I".. .. .0.6,) \"-.. Ph-Hermit fm. I .., ., . 0E•E1.71 0/ - VIEW 1, Ps-Supai fm. / I ■ -0; VY / ,.. 11/ Monument Valley / /. / . "A rT. / / 1 REIICV, ! Cutler fm. / I 1 Pho-Hoskininni tongue gig / / / L, .., ...... - - .., HUNTERS Pdc-DeChelly ss. ; 600 yo Po-Organ Rock tongue [v.-oes / , ,, ,—... Pcm-Cedar Mesa ss. ,..i / , . ,•. , , -ti.";- 111.141111111 “. Pht-Halgaito tongue ..! i- -v., , / .5 . 1 - , . • . ./ 5 lI .... 41 . • Oft• 470. i ■ ■•■ •■•0 . • , I Defiance Plateau : =0. r‘-CA" • . . :5 , i;

4 ..".. Pdc-DeChelly ss. Ps-Supai fm.

/fRIVER 01_” ■EDO. T. — -

/ I It i vRi.SCO TT • ° I 00 / 600 1-M.....7""Sw f? 0 30 "t5 I t. k./.... .5Q SCALE — MILES ..

,f4RV4/4,00„ — - — - • It.• GO I I

FIGURE 3. Thickness distribution of the Coconino-DeChelly sandstones. overlies the DeChelly sandstone with unclear lateral rela- supplied through study of well samples coupled with a tionship. knowledge of outcrop characteristics in Arizona and New McKee (1934) suggested that the Coconino sand- Mexico. stone overlies the DeChelly sandstone on the western flank of the Defiance uplift and that it grades laterally Kaibab-Toroweap formations into the DeChelly northward. The writer recognizes that The name Kaibab limestone, as officially recognized this might be the case at some places but is not secure today, was designated by Darton (1910). As this se- in the belief that it happens in outcrop on any part of quence of rocks contains a considerable proportion of fine the Defiance area. This problem involves many details grained sandstone and siltstone, it is suggested that the the significance of which are hard to evaluate. name Kaibab formation would be appropriate. In the Figure 3 is an attempt to represent the thickness dis- discussion that follows, the Kaibab-Toroweap interval will tribution of the Coconino and DeChelly sandstones. Sig- be referred to only as Kaibab formation. The Kaibab- nificant features include: (11 north to northwest thinning Toroweap formations have been thoroughly reviewed by of both sandstones, (2) southwestward thinning of both McKee (1938). Although the Kaibab formation is prob- formations, and (3) a suggested belt of maximum sand- ably not an important unit in the Black Mesa basin proper, stone development that trends northeast-southwest through it is included here for the sake of completeness. the Black Mesa basin. The overall form is suggestive of Figure 4 represents the thickness distribution of the a basin of deposition plunging to the southwest. The Kaibab formation. The suggested pinch out trend is orient- thickness trends in the northern part of the area on either ed in a north-south direction until it changes to east-west side of the dotted zone strongly indicate an intimate re- near Holbrook, and heads towards New Mexico. Although lationship between the DeChelly sandstone of the Monu- workers have correlated the Kaibab formation and the ment Valley area and the Coconino sandstone of the Grand limestone of the San Andres formation on a faunal basis, Canyon province. Such a relationship is not so easily the actual connection is not traceable in outcrop. The indicated in the southeastern part of the region. It is Kaibab of the Mogollon Rim region contains much sand- in the latter locality that the problems concerning the stone interbedded with limestone of varying degrees of Coconino-DeChelly-Glorieta sandstones become most criti- purity as well as more or less sandstone at the base over- cal. Data to be used in unraveling the picture must be lying the Coconino sandstone. Samples of Kaibab and 86 NEW MEXICO GEOLOGICAL SOCIETY O NINTH FIELD CONFERENCE

•LU LT

ti•T CHM AI BITO EXPLANATION I I Grand Canyon-Central Ariz. I I Pk-Kaibab fm. Pt-Toroweap fm. BASS SRI, Pc-Coconino ss. • o .22;2. Ph-Hermit fm. •,c c2 2. "2 Ps-Supai fm.

22.22.2, ! Monument Valley • FT. Cutler fm. Pho-Hoskininni tongue I Pdc-DeChelly ss. g 0 o NUM.. Po-Organ Rock tongue a o PT• i . 0 Pcm-Cedar Mesa ss. / t Pht-Halgaito tongue ..„ oL22,",22, ■ t I s`, , \ I WILLI•tAS Defiance Plateau I FLASST•FF .... •.-sso i • Pdc-DeChelly ss. o IvPs-Supai fm. ,...0,4‘L, 5•., ! , :::7,..; OLONCO ,_. f ---,, --,-.2.4.6, il.011•

•7:41,_/ sto "W • ,—__ — — .. P11.300 TT / 1:Ax. :;- 5 i / 0 IS 30 1 / . Me !,i-cil, , .,“ I / SCALE — MILES t 09-4., --, 1 ■s_ 1 4r; 0 • • • . . . ::. 4. - l• 1 1 ° , 1 ,.v ! OIL. us.

FIGURE 4. Thickness distribution of the Kaibab-Toroweap formations.

Coconino sandstone are alike in hand specimen and in drill the Permian seas may have more or less covered the De- cuttings. Sandstone belonging to the basal Kaibab forma- fiance area. The possibility increases when it is remem- tion encountered in drill holes is likely to be considered bered that erosion has removed some of the Permian strata as Coconino sandstone. The situation is unavoidable but below the Triassic formations. should be recognized. The development of sandstone in the San Andres formation of the Zuni area might be similar Total Permian to the development in the Kaibab formation. A reasonable Figure 5 is a summary of the thickness distribution question might be whether or not any of the sandstones of Permian sedimentary rocks in northeastern Arizona. It in the southern and eastern portions of the Defiance Plateau is not strictly a representation of only the Permian because are marine sandstones without the diagnostic interbedded Permian type lithology evidently extends into the Penn- marine limestones. Such a possibility is tenable, and, if sylvanian period. Available statistics are based largely such were the case, then the pinch out line representing on lithology, not time. As known total Permian thicknesses the maximum advance of the Kaibab sea would encroach are sparsely distributed, much of the control was used upon the Defiance area. Read (1951) suggests that the from a summation of the previous figures representing the Glorieta sandstone in the Defiance area represents mi- individual Permian formations. Such a procedure is not grating beaches and bars, which supports the idea that desirable but seemed necessary in this instance.

REFERE NCES

Bailey, J. S., 1955, A stratigraphic analysis of Rico strata in the Four , and Williams, J. S., 1940, Permian in parts of Rocky Moun- Corners regions, Univ. of Ariz., Thesis, 88 p. tain and Colorado Plateau Regions, Am. Assoc. Petroleum Geol. Bull., v. 24, p. 617-635. Baker, A. A., 1936, Geology of Monument Valley-Navajo Mountain Darton, N. H., 1910, A reconnaissance of parts of northwestern New region, San Juan County, Utah, U. S. Geol. Survey Bull. 865, 106 U. S. p., maps. Mexico and northern Arizona, Geol. Survey Bull. 435, p. 21, 28, 32. 1925, A resume of Arizona Geology, Univ. Ariz., Ariz. , and Reeside, J. B., Jr., 1929, Correlation of the Permian Bureau of Mines Bull. 119, 298 p. of southern Utah, northern Arizona, northwestern New Mexico, and Gregory, H. E., 1917, Geology of the Navajo Country: a reconnaissance southwestern Colorado, Am. Assoc. Petroleum Geol. Bull., v. 13, of parts of Arizona, New Mexico, and Utah, U. S. Geol. Survey Prof. p. 1413-1448. Paper 93, 161 p., maps.

NEW MEXICO GEOLOGICAL SOCIETY .0 NINTH FIELD CONFERENCE 87

/LOPE

BURN YES • IP

AliiTzAo"m A [ LEES FESS 1:71:g°

4ATENTA EXPLANATION

Grand Canyon-Central Ariz. ; Pk-Kaibab fm. , ‘ Pt-Toroweap fm. -- - - Pc-Coconino ss...... ,_/--711 o ; 0o Ph-Hermit fm. I e■,, % ZIT, °,- ‘,,,, , 000 / / 1/4A.i.;, I ar?..- ---2._:- Ps-Supai fm. Roo /1 X 1 , . —;.""I° II.° DESE4;, I I ...., I I, ,0 / I I I , , w. , , ,.,..w ,1 I , -.VI EW , I I I I 1, I 1 1 I I / p "-,_!■•100 ‘, 1 / / Monument Valley , 1 I I 1 I 1 t 1 ;ft:100. i --;g+ .., 1 ‘ .°°,, Cutler fm. \ .... I I: I : ::: tk0 o . i I I 4 "II FT. ,l ...... \ - _ ,,_ _ - - 1 1/ ,,,,e Pho-Hoskininni tongue 1 ‘ \ t I I I :1;•;;• 01, r 1;171OOS, Pdc-DeChelly ss. ? / / , I . . I \ Po-Organ Rock tongue ,,,, ..._,. og - ...- , , , I , I t, MU X T,ETS X o .., / ... 0 At I Pcm-Cedar Mesa ss. i 1,1as Pht-Halgaito tongue Ys "r(." / •_ o° / , /1 `. 1 – -" ..... - • 1,.- / , / .7,. / , SELIGIS•N \ \ / / ,/ -1 / I / I.to I " 2:6701j.z . 3 / Defiance Plateau WILLIAMS / A Co / 1■•-,o 0° I 1 / ; — -Ig ...IIZ I I FLAGSTAFF Pdc-DeChelly ss. 1 -wo I , c a ., 0 I i: r, Ps-Supai ...I. I i fm. ... l I I I I \ 3•••-. k-O \ I I 0 "-".ETS6 /e l I \- . eo ,3i:: t., 1007.5_51 „ ll. ::::.. `\ • , 0 , . 1 / ,/ 07 :- T1",;--:77.)1" ‘3 I 0 s°° .2 ,,,.„, I i..._, ----...= , ■-• , 1 "-7,1 .... mxoo „. 1,1i, SCO TT ..—.=;/- ...... ems., , 1.••• 1JOHMS At-woxi;. , 5 30 ro ou.ot:x 1,00 SCALE — MILES 1,00

TXXXXA,,,, ALL!. oM I /7

FIGURE 5. Thickness distribution of Permian sedimentary rocks.

Huddle, J. W., and Dobrovolny, Ernest, 1945, Late Paleozoic stratigraphy 1934, An investigation of the light-colored crossbedded of central and northeastern Arizona, U. S. Geol. Survey, Oil and sandstones of Canyon DeChelly, Arizona, Am. Jour. Sci., 5th ser., Gas Invest., Prelim. Chart 10. v. 38, p. 219-233. Hughes, P. W., 1950, The stratigraphy of the Supai formation in the , 1938, The environment and history of the Toroweap and Chino Valley area, Yavapai Couny, Arizona: Univ. Ariz., Thesis, Kaibab formations of northern Arizona and southern Utah, Carne- 95 p., maps. gie Inst. Wash. Pub. 492, 268 p. Jackson, R. L., 1951, The stratigraphy of the Supai formation along the Read, C. B., 1951, Stratigraphy of the outcropping Permian rocks around Mogollon Rim, central Arizona: Univ. Ariz., Thesis, 82 p., maps. Noble, .L. F., 1922, A section of the Paleozoic formations of the Grand the San Juan Basin, New Mexico Geol. Soc. Guidebook of the south Canyon at the Bass trails, U. S. Geol. Survey, Prof. Paper 131, p. and west sides of the San Juan Basin, New Mexico and Arizona, 23-73. p. 80-84. McKee, E. D., 1934, The Coconino sandstone — its history and origin, Winters, S. S., 1951, Permian Stratigraphy in eastern Arizona, Plateau, Carnegie Inst. Wash., Pub. 440, p. 77-115. v. 24, p. 10-16.