U.S. DEPARTMENT OF THE INTERIOR MISCELLANEOUS FIELD STUDIES MAP MF–2412 U.S. GEOLOGICAL SURVEY Version 1.0

A CORRELATION OF MAP UNITS INTRODUCTION STRUCTURAL GEOLOGY hhc hbu Mb Main body (Upper to Lower , Meramecian-Osagean)—Medium- to thick- hhg 3 hhg bedded, chert-bearing bioclastic limestone. Limestone is light to medium gray on fresh Rocks within the map area were mildly deformed by a system of faults and folds. Structure contours on hbl This map summarizes the geology of the Ponca 7.5-minute quadrangle in the Ozark Plateaus hhc 6 hhc surfaces and generally coarsely crystalline with interspersed crinoid ossicles. A 1–3-ft- the base of the Boone Formation illustrate the location of structures and their vertical offset. The structure 2 Mp Qty region of northern (fig. 1). The quadrangle is near the transition between two physiographic 3 (0.3–1-m-) thick bed of oolitic limestone is common at the top of the Boone Formation. contours conform to elevations at 345 control points on the lower or upper contacts of the Boone 2 14 hhc hhg h hbl hc provinces, the and the Springfield Plateau, and it contains a deep valley cut by the Dense beds of limestone are present in the upper third of the unit. Beds are typically Formation that were located on the topographic base map using one or a combination of a global position Buffalo River. The exposed bedrock of this region comprises an approximately 1,600-ft- (490-m-) 6 Qtm Qc medium to thick and parallel planar to wavy. The chert content varies within the Boone system receiver, a barometric altimeter, or a distinctive topographic contour pattern. A 390 ft (119 m) 12 Mfw thick sequence of , Mississippian, and carbonate and clastic sedimentary Formation and is greatest in the northwestern part of the map. Chert forms lenticular to hhg ha 950 Mp thickness for the Boone Formation was used to project the elevation of the basal contact from points on h rocks (fig. 2) that have been mildly deformed by a series of faults and folds. hg 900 anastomosing lenses. Chert-rich horizons are generally poorly exposed and form slopes the upper contact, based on the average of several traverses across stratigraphic sections near the Buffalo hbu 3 Qto The geology of the Ponca quadrangle was first mapped by Purdue and Miser (1916) at 1:125,000 littered with float of white weathered chert that in uppermost part of unit contains large hhc hbl Mf River (Hudson, 1998). scale and later by Morrison (1971) at 1:24,000 scale. The current map confirms many features of brachiopods casts. Thickness is 310–375 ft (95–114 m) The vertical offset across structures can be estimated from the elevation difference of formation h h Unconformity these previous studies but it also identifies new structures and employs a revised stratigraphy. Mbs St. Joe Limestone Member (Lower Mississippian, Osagean to Kinderhookian)—Thin- hg 3 hg contacts across the structures. Lateral offset is difficult to measure due to the lack of piercing points, but hbl bedded, coarse-crystalline bioclastic limestone with ubiquitous 3–6-mm-diameter crinoid 4 1340 kinematic data suggest that strike-slip offset was important on small faults associated with the Adds Creek fragments. Limestone is commonly pink to red due to hematite staining, but its color and and Hanner Point monoclines. Fault striations that are sparsely preserved on planes of some mapped Mf 2 Mbv ha Atokan h hematite concentrations vary with location. Beds are thin and wavy in form. Chert nodules bl TOM TH 5 DESCRIPTION OF MAP UNITS faults, or on adjacent, parallel, small-scale faults were used to infer the slip direction in some locations. hbu 4 UMB M 1320 are uncommon but, where present, are tabular and reddish. The contact with the ONOC Small cataclastic faults, or deformation bands (Aydin and Johnson, 1978), were commonly developed in hbu LINE h overlying main body of Boone Formation is gradational. The middle part of the St. Joe hhg Mfw 4 bu porous Everton Formation sandstone in and adjacent to structures. Slip sense for mapped faults was 1280 Qty Younger terrace and active-channel alluvial deposits (Quaternary)—Unconsolidated h Limestone Member forms a local topographic flat on a slightly shaley limestone interval inferred either from offset of bedding, from asymmetric minor fault-plane features, or from the geometry bl sand and gravel of the Buffalo River. Terrace deposits are principally composed of light- h that commonly overlies a low limestone ledge above the basal unconformity. Base of unit of conjugate sets of deformation bands in adjacent rock. Faults of normal, reverse, and strike-slip sense are 1100 900 bl PENNSYLVANIAN 1050 950 brown fine sand and have smooth upper surfaces that are as much as 20 ft (6 m) above is a 1.5–3-ft- (0.5–1-m-) thick sequence of phosphate-pebble-bearing tan sandstone and all present within the map area. Mp 1260 Morrowan the base-flow level of the river. Active-channel gravel deposits are composed of overlying greenish-gray shale that, although thin, is laterally persistent throughout much of The Kyles Landing fault is a reverse fault that dies out in the Bee Bluff monocline north of the Buffalo 1000 4 1250 subangular to rounded rock clasts of mixed lithology along drainages and they hhg northwestern Arkansas (McKnight, 1935). The member is approximately 30–50 (9–15 m) River. Beds of Everton and Boone Formations and Batesville Sandstone dip moderately to steeply adjacent hhc are interspersed with bedrock exposures (not mapped). Deposits are as thick as 20 ft (6 ft thick h to the fault, defining a nearly horizontal model fold axis that trends south-southeast (fig. 3A). The hg hhg m) Of Fernvale Limestone (Upper Ordovician)—Thin- to medium-bedded, coarse-crystalline 1240 h orientation of this fold axis and the geometry of sparse small-scale reverse faults (fig. 3B) and conjugate hc Qtm Medial terrace and alluvial deposits (Quaternary)—Unconsolidated gravel and sand 1150 1260 bioclastic limestone. Limestone is light to medium gray on fresh surfaces and it contains deformation bands (fig. 3C) in hanging wall Everton Formation indicate that the fault has reverse motion. hbl 3 deposits adjacent to the Buffalo River. Deposits are poorly exposed and are principally a ha Unconformity abundant cylindrical to barrel-shaped crinoid ossicles 3–10 mm in diameter. Continuous The plane of the Kyles Landing fault is not exposed but, assuming a south-southeast strike, its trace over 6 lag of brown-weathered, subrounded to rounded Paleozoic rock clasts of mixed lithology hhc outcrop of this unit is restricted to the southwest part of the quadrangle but local lenses topography suggests that it dips steeply west-southwest (cross section B–B′). Traced southward, the Kyles hbu that are as high as 40–60 ft (12–18 m) above the base-flow level of the river. Thickness 1220 1240 Mp are recognized farther east in quadrangle. Thickness reaches 20 ft (6 m) in southwestern Landing fault and adjacent folded strata are unconformably overlain by Cane Hill Member, indicating that 8 uncertain but probably as much as 20 ft (6 m) Mf corner of map (McFarland, 1982) this structure formed in Late Mississippian-Early Pennsylvanian time. To the north, the Bee Bluff Mfw 850 Qto Older terrace and alluvial deposits (Quaternary)—Unconsolidated gravel and sand Mf Everton Formation (Middle Ordovician)—Interbedded sandstone, dolomite, and limestone monocline is interpreted to abut against a west-northwest continuation of the coeval Web monocline, Mfw deposits adjacent to the Buffalo River. Deposits are poorly exposed and are principally a 5 h Mp sequence divided into upper part, Newton Sandstone Member, and lower part. Unit is although this interpretation is conjectural because the inferred connection is concealed beneath bl Mbv Chesterian lag of brown-weathered, subrounded to rounded Paleozoic rock clasts of mixed lithology hbl 1240 310–350 ft (95–107 m) thick Pennsylvanian rock. Small strike-slip and normal faults were observed locally within the north-facing Web hhg Mf that are 100–120 ft (30–37 m) above the base-flow level of the river. Thickness Oeu 6 Mb Upper part—The upper part of Everton Formation contains 3–20-ft- (1–6-m-) thick light- to monocline in the adjacent Jasper quadrangle (Hudson and others, 2001), suggesting that it probably uncertain but probably no more than 5 ft (1.5 m) dark-gray dolomite and limestone beds interbedded with sandstone. Fine crystalline, light- 1200 MISSISSIPPIAN formed over a transtensional fault. 1240 Qc Colluvial deposits (Quaternary)—Unconsolidated deposits of angular blocks as large as 20 gray, limestone as thick as 10 ft (3 m) is present near top of unit in southwestern part of hhc Mbv Normal faults are the predominant structures within the map area. In surface exposures the normal 900 ft (6 m) in diameter that are mostly derived from the basal sandstone of the upper Bloyd map. Sandstone is light tan to white quartz arenite containing well-sorted, well-rounded, faults dip from 50° to 85°, averaging 71° dip for 15 measurements. Seven west-northwest-striking, en Unconformity Formation. Colluvium in southeast corner of map is a continuation of a thick deposit and fine- to medium-grained quartz grains. Sandstone is variably cemented by dolomite or echelon normal faults form a 2-km-wide, N. 60° W.-trending zone that crosses the center of the area and Mbv Meramecian- centered on Boulder Creek in adjacent Jasper quadrangle (Hudson and others, 2001). calcite and is transitional from carbonate sandstone to sandy carbonate; carbonate crystals 5 Mb intersects the east-northeast-striking Compton fault and the northeast-trending Hanner Point monocline. 950 850 Osagean Colluvium deposit in east-central part of map (sec. 13, T. 16 N., R. 22 W.) conceals 7 locally envelop sand grains. Sandstone generally has medium to thick planar beds. This en echelon pattern of normal faults is like that produced in analog models of low-angle oblique rifts ha probable erosional truncation of Pitkin Limestone and Wedington Sandstone Member of 4 Osagean- Dolomite is light to dark gray, fine to medium crystalline, and thin to medium bedded with (Withjack and Jamison, 1986), suggesting that the zone may have developed over a basement weakness. 4 ha 1000 the beneath Cane Hill Member of the Hale Formation. Colluvial 4 3 Mbs Kinderhookian common sandstone stringers and beds. Dolomite is typically laminated and forms intervals Striations on the individual mapped faults within this zone have high rakes (fig. 3D), indicating extension 1210 deposits present elsewhere are not mapped. Thickness uncertain but probably more than 1–10 ft (0.3–3 m) thick. Includes Jasper Member and the informal “Member C” of 1050 Unconformity was essentially normal to their strike. Likewise, conjugate sets of deformation bands measured in Everton 10 ft (3 m) Everton Formation of Suhm (1974). Unit is 80–100 ft (24–30 m) thick 1250 14 1210 Formation sandstone at a footwall site (36° 3.99’ N, 93° 18.77’ W) adjacent to the California Point fault Upper ha Atoka Formation (Middle Pennsylvanian, Atokan)—Interbedded shale, siltstone, and 1100 Of Oen Newton Sandstone Member—Thick sandstone interval within the Everton Formation that 10 hhg Qty Ordovician (fig. 3E) also indicate south-southwest extension. Within the zone, maximum down drop lies within the Jim sandstone. Unit forms highest hills of map area and is poorly exposed. Sandstone is tan, forms prominent bluffs along the Buffalo River. The unit is quartz arenite containing well- 1300 h Unconformity Bluff graben, whose strata are about 600 and 450 ft lower than correlative strata on adjacent northern and hg thin to medium bedded, fine to very fine grained, and holds up topographic ledges. Beds sorted, well-rounded, and fine- to medium-grained quartz grains. Sandstone is light tan to 7 1150 southern zone flanks, respectively. The Compton fault dips steeply southeast and has normal throw of over 8 Mf are typically ripple-trough laminated, and locally bioturbated. Less commonly, sandstone 7 1350 Mfw Oeu white and variably cemented by dolomite or calcite; carbonate crystals locally envelop sand 300 feet in its central part (cross-section A–A′), but this offset decreases abruptly at its eastern end. 1800 is medium to coarse grained and contains white quartz granules. Siltstone is thin bedded Mb grains. Sandstone breaks with sugary texture. The sandstone generally has medium to Conjugate sets of deformation bands (fig. 3F) observed at a hanging wall site (36° 4.57’ N, 93° 19.89’ W) hbu 1400 Mbv 5 Mf 5 Mp with ripple cross-lamination. Shale is dark gray to black. Thickness of unit is as much as thick planar beds. Newton Sandstone Member of the Everton was defined by McKnight 3 h Middle adjacent to the eastern part of the Compton fault are consistent with north-northwest extension on this 1200 hc Oen 100 ft (33 m) 1450 Ordovician (1935). Unit is 90–100 ft (24–30 m) thick fault, but the deformation bands at this site are crosscut by small-scale strike-slip faults (fig. 3G) that suggest 6 3 1220 6 2 ORDOVICIAN Bloyd Formation (Lower Pennsylvanian, Morrowan)—Interbedded sequence of Oel Lower part—Interbedded sandstone, limestone, and dolomite. Upper part of unit is mostly 4 4 hhc h that the fault was probably reactivated under north-northwest shortening. Mapped normal faults within the 1500 Mbs 1510 bl 1250 Oel sandstone, siltstone, shale, and thin limestone beds separated into lower and upper limestone interbedded with sandstone. Limestone is light gray, finely crystalline, thin to 9 1760 quadrangle affect all Paleozoic strata and thus they were active after Middle Pennsylvanian time. The 1880 parts. As much as 380 ft (116 m) thick 3 medium bedded, commonly laminated, and locally stromatolitic. Limestone is 1–10 ft normal faults accommodated north-directed extension that was probably caused by flexure of the foreland hbl Mf Oeu Unconformity h 1530 3 bu Upper part—Dominantly sandstone with interbedded siltstone and shale. Upper part of (0.3–3 m) thick. Limestone-rich part of the lower Everton is a common host of paleokarst 6 of the developing to the south (Hudson, 2001). 10 1540 7 7 sequence is poorly exposed and contains dark-gray to black shale beds that form hhg hbl Mbv 1300 Op features that consist of vertical columns of highly fractured or brecciated sandstone The northeast-trending Adds Creek and Hanner Point monoclines in the western part of the map area Mbv 1820 topographic flats and sandstone and siltstone beds that hold up ledges 3–6 ft (1–2 m) 4 8 1550 h h Lower collapsed from overlying horizons. Sandstone is quartz arenite containing well-sorted, well- are associated with a zone of short mapped faults and small-scale faults having strike-slip as well as dip-slip h 11 10 hc 4 h hg hc 9 Mbs 7 2 1350 a Ordovician high. At least one bed of coal from 4 to 19 in (0.1 to 0.48 m) thick is interbedded with rounded, and fine- to medium-grained quartz grains. Sandstone is light tan to white and 7 4 1400 Mp offset. Together with a northeast alignment of lead-zinc mines near Ponca (McKnight, 1935) and Mb 1960 1930 Oc black shale and siltstone at the top of the sequence in the northwestern part of the area h 1600 Mbv 1850 1820 h hbu variably cemented by dolomite or calcite. Poorly cemented sandstone breaks with sugary topographic features on and beyond the quadrangle, these structures lie within a N. 30° E.-trending zone hg 5 1590 Oel 3 a h 2000 OME Oeu 1460 (J.D. McFarland, oral commun., 2000). Upper sandstone beds are tan, mostly fine to texture. The sandstone has medium to thick planar beds. The lower part of unit is light- to hbl hg EEK D 1620 that has been called the Ponca lineament (McFarland, 1988). It is likely that this lineament formed over a S CR 1620 Op 3 very fine grained, ripple-cross laminated to planar bedded, and locally bioturbated. Base dark-brownish-gray dolomite grading to sandy dolomite interbedded with sandstone. EED 74 1300 Mf 850 preexisting fault zone in basement that was partly reactivated with strike-slip and down-to-the- 6 1950 12 SN 1620 7 1300 89 hhc of unit is crossbedded sandstone as thick as 100–150 ft (33–50 m) that forms prominent 84 Oel Mbs 1450 1000 Dolomite is fine to medium crystalline, thin to thick bedded, commonly laminated, and Oen 82 1800 950 900 southeast motion to form the overlying monoclines and associated small faults. The left step between the 1600 Oeu 79 Mbv cliffs in most of the area. Basal sandstone is white to light-brown, fine- to medium- 1250 1620 1360 h may be stromatolitic. Dolomite beds present as intervals 1–10 ft (0.3–3 m) thick. Contact Adds Creek and Hanner Point monoclines is similar to what might form above en echelon Riedel faults 1600 3 1620 Oeu bl 8 Mp 18 12 Mbv Mb 1430 grained quartz arenite that has a sharp erosional base and is commonly a composite of with underlying Powell Dolomite is placed at lowest bed of sandstone or sandy dolomite. 1875 Mb 1240 1450 within a buried northeast-trending dextral fault zone (Tchalenko, 1970). The Adds Creek and Hanner 1510 1360 1840 1450 several 1–3-ft- (0.3–1-m-) thick tabular and trough-crossbed sets. Sandstone contains 38 18 1350 1380 Lower part of Everton equivalent to informal “Member B,” Kings River Sandstone Point monoclines and associated faults affect all Paleozoic strata and thus they were active after Middle 11 15 66 5 1400 1430 1840 3 4 Mf ULT Mf Mf 43 1500 concentrations of white quartz pebbles and casts of wood fragments. In the west-central Member, and the Sneeds Dolomite Member of the Everton Formation of Suhm (1974). 1550 17 FA 1230 1320 10 5 Pennsylvanian time. 1500 2 4 6 12 WEB MONOCLINE part of the map area, the basal sandstone is interbedded with shale and does not form a N 1565 Oel 11 1890 hbl 3 Unit is 100–140 ft (30–43 m) thick hbl TO Mbs Oel 1370 Mf 8 1780 hhc The Sneeds Creek dome (Purdue and Miser, 1916) is an east-northeast-elongated, doubly plunging 4 P 24 17 15 13 Oen Oeu 1480 h Mbs Op prominent cliff. Thickness of unit is about 275 ft (84 m) OM 8 Mbv Mbs 1150 8 hg Oeu h 5 Op Powell Dolomite (Lower Ordovician)—Fine-grained, argillaceous to silty, gray dolomite with 36 C 14 13 CA 1450 Oel 2 1780 1700 h Mf hc h anticline in the footwall of the Compton fault within which rocks of the quadrangle achieve their highest 2 h 36 LIFO 1910 hg 16 3 9 bl Lower part—Dominantly dark-gray to black shale and siltstone interbedded with thin beds dark-gray shale interbeds. Dolomite beds are thin to medium, wavy, commonly laminated 32 a Oeu 3 RN 1450 Mf 1400 elevation. Although this fold probably initiated as an extensional forced fold (Withjack and others, 1990) h 19 1120 IA 1825 1520 E Mfw of sandstone and limestone. Sandstone beds locally exposed as ledges as much as 10 ft hg 21 31 INE 4 1150 8 1530 PO 4 Oen 1410 3 and stromatolitic. Contact with overlying Everton Formation is unconformable and 15 NCL 1150 1250 4 Mbs h INT FAULT 7 IN above the Compton normal fault, the presence of a small, south-southeast-vergent thrust fault in the fold SY 1200 hhc 1140 bl 8 1580 L (3 m) high. Sandstone varies from tan, very fine to fine grained, thin bedded with ripple 10 1200 1620 C 1100 beneath it Powell beds may be truncated with slight local angular unconformity. Unit is 4 45 OW 9 Oeu 1340 O 10 1400 core (Sec. 6, T. 16 N., R. 22 W.) suggests that this fold also accommodated some north-northwest LL 8 3 11 11 1190 6 18 h N 1050 marks to orange brown, medium grained, thin to medium bedded with local basal 43 HO 1350 1620 1150 1200 hg Oc 5 O about 200 ft (60 m) thick in the only complete section exposed in Hemmed-In Hollow shortening. We interpret that the Sneeds Creek dome probably was tightened during later reactivation of S 9 22 1300 3 8 h 1570 66 8 1460 N 1670 hhc hg M 1490 1000 conglomerate lenses containing clasts of sandstone and shale and rounded white quartz Oc Cotter Dolomite (Lower Ordovician)—Brownish-gray dolomite with sparse chert nodules. 52 A 8 2 1200 76 8 Oel 1530 the Compton fault in response to north-northwest-directed compression at the end of the Ouachita G 3 hhc 8 Oeu h 1510 RO h 20 30 12 h 1620 1250 3 1220 5 bl 1700 Mbv pebbles. The Brentwood Limestone Member at the base of the formation (not mapped) Chert composed of concentric, alternating dark-gray and white bands within elongate G bu 14 1790 hg 1570 Mbv 1150 1500 orogeny. 1840 14 6 3 3 1200 Oen is a 5–20-ft- (1.5–6-m-) thick, reddish-gray, coarse bioclastic limestone. Unit is 1630 F 1420 nodules that are concentrated in dolomite beds in the upper part of the formation. Only 41 6 1525 3 1410 Dips of bedding within folds in the map area are generally greater than 5° and have consistent 18 70 1825 2 1520 Mf Oel F 1390 1250 Mbs 1250 1600 conformable with the underlying Hale Formation. Forms moderate to steep slopes and is 7 1150 the upper 20–30 ft (6–9 m) of unit are exposed along Hemmed-In Hollow

1540 NE 1780 1640 1250 Mb 1150 1510 Oeu 1300 U directions. Away from structures, where structure contours indicate little dip of the base of the Boone 1200 LI 9 L 980 1250 1400 1450 NTIC 1780 9 Mbs Qty 1690 Mb poorly exposed. Unit is 40–100 ft (12–30 m) thick A Mf Mbv 78 B Formation, dips of bedding at the surface are mostly low and variable in direction. These dispersed 40 LLOW 1480 3 Mbv Oen Oeu 2 1000 O 1500 1180 E Hale Formation (Lower Pennsylvanian, Morrowan)—Interbedded sequence of sandstone, hbl F H 8 1190 1170 10 F 10 1660 E attitudes can be attributed to local subsidence caused by karst dissolution within the abundant limestone 15 CLI Oen 7 1350 Oeu 1170 1280 Mbs 960 Oel 11 B Mbs Oeu 93°22'30" 93°15' 93°07'30" 93°00' siltstone, shale, and thin limestone that consists of Prairie Grove Member and Cane Hill Contact 1430 Mf 1120 1270 1150 and dolomite rock units and to unrecognized rock creep. Oel 5 3 Oen 3 Mbv 3 36°15' Member. Formation is 110–150 ft (35–46 m) thick 4 Mb Oeu 980 1090 Oeu 81 62 7 h h Oel 960 OSAGE NE GAITHER HARRISON h Joints within the map area (406 joints measured) are distributed in two dominant strike sets (fig. 3H), hg 6 bu 1200 1150 1080 Oel 1190 8 hg Prairie Grove Member—Brown to reddish-brown, fine- to medium-grained, thick-bedded, 6 Mbs hbl 62 12 1060 7 Oeu QUAD. QUAD. QUAD. Fault—Dashed where inferred; dotted where concealed; ball and bar on downthrown side; northeast and north. A less prominent joint set strikes east. Joint planes within limestone and dolomite 1140 1100 63 Oen 1276 4 20 1000 1100 Oeu Harrison 1840 1050 Of Op calcite-cemented sandstone. May contain bioclastic limestone interbeds and, at its base, 1445 1280 3 JIM BLUFF 1180 Oeu Mb 12 Qto Oeu Mbs showing fault dip (arrow) and rake (diamond-headed arrow); paired arrows indicate relative formations, such as the Boone Formation, are commonly enlarged due to dissolution. 1410 3 1580 Oen 1360 Oen 6 3 4 Mb quartz pebbles. Beds are planar or crossbedded and crossbeds may have bi-directional GRABEN 1150 Qty 1700 1200 right-lateral strike-slip movement 1350 69 950 1400 1350 72 900 46 dips. Weathered sandstone forms massive, rounded surfaces with elliptical cavities as E 1300 Oeu Mbv Mb 850 1240 Mbs N 1710 940 10 975 65 Reverse fault—Dashed where inferred; dotted where concealed. Rectangles on upper plate LI 26 4 1240 1140 large as 8 in. (20 cm) long. The sandstone forms steep slopes that may be covered by C Mbs 70 5 ECONOMIC GEOLOGY O Mf 7 1270 1310 1360 hhc Mb Oeu Op 43 Thrust fault—Teeth on upper plate N 1700 Mb 1325 1280 Oen 3 960 slope debris from overlying units. Unit is 20–60 ft (6–18 m) thick 6 3 1250 6 Oen ha O h 7 Oen Oeu Oel hhc Cane Hill Member—Interbedded sequence of shale, siltstone, and sandstone. The upper M hc 1300 1260 960 hbl Oen 980 Structure contours drawn on base of Boone Formation—Dashed where approximately Lead and zinc were mined intermittently within the Ponca-Boxley district from the 1860’s through the 5 Oeu 1280 1305 Oen T 3 1300 1200 Mf Mbv 80 Qtm part of the Cane Hill Member is poorly exposed and composed mostly of dark-gray shale 1950’s (McKnight, 1935; McFarland, 1988). Within the map area, the mines are located near Ponca and N 1700 Oeu Of 3 4 Mb 6 Qty located. Contour interval 50 ft I Oeu 6 Qtm 80 Qty BOONE COUNTY 3 1250 CARROLL COUNTY 1350 and thin-bedded siltstone that form gentle to moderately steep slopes. The lower part is O Mbv 1320 Qty 12 980 1390 7 30 align in a northeast trend that is collinear with the Adds Creek monocline. McKnight (1935) reported that P Oen 3 hbu 10 10 Strike and dip of inclined bedding 5 1000 1680 850 Oeu 77 a 10–40-ft- (3–12-m-) thick sandstone interval with siltstone and shale interbeds. about 4,000 tons of concentrates of galena, zinc carbonate, and zinc silicate were produced from the Op 1200 31 1100 1200 Oeu 980 4 R Of 1240 1450 Qty 11 1000 Horizontal bedding E Mf 1150 25 Sandstone varies from reddish brown, poorly sorted, fine to medium grained in medium 1750 N 7 Oeu 1284 39 1390 Ponca-Boxley district. All ore zones precipitated at or near the contact between upper Boone Formation hbu 6 Oel 1150 Mb N 9 1580 39 hhg Qtm 1395 B′ to thick beds that may contain trough crossbeds, to tan to olive brown, very fine to fine Anticline h 5 A 1710 1020 BOONE COUNTY and Batesville Sandstone, and most are associated with zones of fracturing and small strike-slip faults h bl H 1330 Qty hhc 34 ° hg 14 900 21 36 07'30" NEWTON COUNTY grained, thin bedded with ripple cross-lamination or parallel lamination. Lower (McKnight, 1935). 1320 950 7 Syncline 1750 1700 Op 1500 1090 1250 hhc hbl Mbs PONCA sandstone beds may contain wood as carbonized fragments or as casts and angular 1300 3 1100 Mbs 1050 12 1570 Monocline 8 5 Oel 21 QUADRANGLE mudstone intraclasts, and also contain local conglomerate lenses with clasts of 1760 1680 1120 1130 Mbv BUFFALO Mf Oen Oen Mbs 13 5 Oen 1150 1070 1130 Axis of minor anticline showing direction and amount of plunge ACKNOWLEDGMENTS Mbv Oeu Oen 1180 Mbv NATIONAL sandstone, shale, and crinoid-bearing limestone. Sandstone beds locally display soft- 2 1290 Op 1680 1700 1100 1160 1200 6 Qc 8 2 1310 Mbs 3 6 Oel Mb 1220 1404 RIVER sediment slump folds. Unit unconformably overlies the Pitkin Limestone, the Wedington 1325 Control point showing elevation in feet on lower or upper contact of Boone Formation 7 1305 1300 4 1250 4 Mfw Mbs 1300 Mb 2 This work was conducted in a cooperative project between the U.S. Geological Survey and the U.S. 1650 1600 Oel 3 1260 Oen 1250 K 7 Member of the Fayetteville Shale, and the main body of the Fayetteville Shale. Unit is Oel Mbv Oeu B 1240 1230 1570 Y 1370 1300 L Mp National Park Service. Special thanks go to the private owners who allowed access onto their land during 5 7 1315 Oeu 1615 1250 80–140 ft (24–43 m) thick 1660 1620 1650 E Mf 1230 h 1270 S this study. We thank J.D. McFarland, III, D.N. Mott, and D.L. Zachry for helpful discussions during the Oen 1580 1300 hc 1700 1150 Mp Pitkin Limestone (Upper Mississippian, Chesterian)—Generally medium- to dark-gray, 1300 1660 1580 16 12 8 Oen 1300 1220 11 L er 4 Mf Mbv A iv course of the study. Helpful reviews were provided by W.R. Page, K. Kellogg, and J.D. McFarland, III. Op lo R fetid limestone. Limestone varies from micritic to coarse grained and is locally oolitic. Mb 1600 N ffa STRATIGRAPHY Oeu 1250 7 Oel Mf Bu 1370 Oel 1600 Mf 8 D 0 5 km Limestone beds may contain abundant crinoids, brachipods, corals, and Archimedes. Oeu Mbv I h 1540 1320 N hg 7 Mb 1700 hbl hhc The unit commonly forms a prominent ledge. Distribution of Pitkin is restricted to the The study area preserves a 1,600-ft- (490-m-) thick record of early and late Paleozoic deposition on 1200 1150 1200 Oen h 1160 G 1620 hc 3 4 northeastern part of the map area. The basal contact with the Fayetteville Shale is what is now the southern margin of the North American continent. Stages for Pennsylvanian and REFERENCES 4 1200 1290 1150 1150 82 F Ponca 12 1680 A JASPER HASTY 1285 Mbv 1550 Qty Mf 78 43 Mississippian units are from McFarland (1988). 1160 U hbl Jasper QUAD. QUAD. conformable, although rarely exposed. Upper contact with Cane Hill Member is Mf 3 ° 1720 Oeu Mbv 1260 Mbs Mbv h L 36 00' unconformable and Pitkin was eroded beneath the unconformity in the western part of Pennsylvanian sandstone and shale of the upper part of the Bloyd Formation and the Atoka Formation Angelier, Jacque, 1990, Inversion of field data in fault tectonics to obtain the regional stress, III, A new 4 4 Mbs Oen 1525 hg T h 1270 1660 1680 1150 Mbs hc Oeu Mbs 1250 7 63 were originally called Winslow Formation by Purdue and Miser (1916), with the basal Greenland Sandstone rapid direct inversion method by analytical means: Geophysical Journal International, v. 103, p. 1170 3 hbu 73 the area. Its thickness varies from 0 to 60 ft (0 to 18 m) 1270 1220 Oeu 1260 Oel 1690 1590 Mf Fayetteville Shale (Upper Mississippian, Chesterian)—Consists of fine-grained sandstone Member of the Atoka (Henbest, 1953) representing the prominent cliff-forming crossbedded sandstone. 363–376. 1290 2 1300 1260 Mf 1280 1250 Oeu 17 81 94°00' 92°00' 90°00' hbl 62 and siltstone of Wedington Sandstone Member that grade downward into black, slope- Morrison (1971) followed this convention. Zachry (1977), however, concluded that the cliff-forming Aydin, A., and Johnson, A.M., 1978, Development of faults as zone of deformation bands and as slip 6 13 1250 4 Oen 1650 hhc 6 9 Mbv forming shale of the main body of the unit. Thickness varies from 10 to 360 ft (3 to 110 sandstone was a time-equivalent unit with the Woolsey Member of the Bloyd Formation farther west and surfaces in sandstone: Pure and Applied Geophysics, v. 116, p. 931–942. Mb 1220 1220 1245 83 3 Mf 6 Mb 1240 85 9 Mbv 12 Oen 1240 1330 Ozark Dome St. Francois m) designated it with the informal term “middle Bloyd sandstone.” This sandstone interval comprises the basal Henbest, L.G., 1953, Morrow group and lower Atoka Formation of Arkansas: American Association of 1300 3 1695 Mountains Mfw Wedington Sandstone Member—Brown, well-indurated, calcite-cemented sandstone and interval of the upper part of the Bloyd Formation as used here. The contact between the Atoka and Bloyd Petroleum Geologists Bulletin, v. 37, p. 1935–1953. 1580 3 1270 9 Salem Plateau Formations on the map is located within alternating shale and sandstone intervals and is indistinct. Atoka Horner, G.J., and Craig, W.W., 1984, The Sylamore Sandstone of north-, with emphasis h Oeu 50 37°00' KANSAS siltstone that form a distinctive unit in the upper part of the Fayetteville Shale. The hc Oeu Qty 15 1650 1250 1650 87 OKLAHOMA Wedington Sandstone Member caps a steep slope and is separated from overlying Pitkin Formation is interpreted to be preserved within the map area because the aggregate thickness of strata on the origin of its phosphate, in McFarland, J.D., III, ed., Contributions to the geology of Arkansas, 1200 1620 Mbs h Springfield Mbs 1220 1230 a 1250 25 31 Limestone by a rarely exposed, thin, black shale that commonly forms a bench. above the Hale Formation is as great as 500 ft (152 m), much greater that the typical 100-150 ft (30–46 v. 2, Arkansas Geological Commission, p. 51–85. 1570 Plateau MISSOURI 5 Oeu hhg Sandstone is fine- to very fine grained and is present in thin to thick planar beds with m) thickness of the Bloyd Formation 60 km to the west in Washington County where the presence of the Hudson, M.R., 1998, Geologic map of parts of the Jasper, Hasty, Ponca, Gaither, and Harrison INE 1190 1620 1290 ARKANSAS L 1200 2 1200 1280 C Mbv 3 1210 internal parallel laminations and locally developed low-angle crossbeds in highest beds. Kessler Limestone Member at the top of the Bloyd Formation allows separation of the Bloyd and Atoka quadrangles in and adjacent to Buffalo National River, northwestern Arkansas: U.S. Geological Survey 4 N 1590 1200 Formations (Zachry, 1977; Zachry and Sutherland, 1984). Where it has been studied in Washington Open-File Report 98–116, scale 1:24,000. 1260 O Oen 3 Mb Sandstone grades downward into siltstone beds that are ripple cross-laminated and 1620 Mf Boston M KM 1190 Oen oun bioturbated. Distribution of the sandstone is restricted to the northeastern part of the County, lower Atoka Formation is a marine sequence (Zachry and Sutherland, 1984). Within the map Hudson, M.R., 2001, Coordinated strike-slip and normal faulting in the southern Ozark dome of northern E tains Oeu Oeu 1200 map area and is thickest in the northeast corner of the map. Contains limestone area, the presence of a thin coal bed approximately 250 ft (76 m) above the base of the upper part of the Arkansas: deformation in a late Paleozoic foreland: Geology, v. 28, p. 511–514. 1215 1580 1180 1600 Arkoma Basin interbeds south of the Buffalo River. The unit was probably eroded from the western Bloyd Formation indicates deposition of these beds in a non-marine setting. Thus, the Bloyd-Atoka contact Hudson, M.R., Murray, K.E., and Pezzutti, D., 2001, Geologic map of the Jasper quadrangle, Newton and SCRE 1190 2 ° TENNESSEE D 1610 35 00' was placed above this horizon. Boone Counties, Arkansas: U.S. Geological Survey Miscellaneous Field Studies Map MF–2356, D 1550 Mb Oeu MISSISSIPPI part of the map area before deposition of the Cane Hill Member of the Hale Formation. A 1160 Oeu Mbv 1550 The Wedington grades downward into main body, and its basal contact is placed at the The base of the Morrowan Cane Hill Member of the Hale Formation represents a major erosional 1:24,000 scale. hbu 1170 untains 5 Mo first outcrop of dominantly siltstone or sandstone beds. Thickness is 0–20 ft (0–6 m) unconformity within the map area. Late Mississippian-Early Pennsylvanian erosion removed the Pitkin McFarland, J.D., III, 1982, A small bitumen deposit near Ponca, Arkansas, in McFarland, J.D., III, editor, 1530 Mf Ouachita 1550 1600 1100 Mf Main body—Below the Wedington Sandstone Member, the main body of the Fayetteville Limestone, the Wedington Sandstone Member, and much of the main body of the Fayetteville Shale in the Contributions of the Geology of Arkansas: Arkansas Geological Commission Miscellaneous Publication Qty Oen Mf hhg hbl 1590 Mississippi Embayment 950 Shale is black shale that is poorly exposed. The lower part of the Fayetteville Shale western part of the map (fig. 2). This truncation is most abrupt across the Kyles Landing fault south of the 18, p. 43–44. 1205 h 1150 a outcrops along stream gullies where it consists of black fissile shale that may contain Buffalo River (cross section B–B′), indicating that movement on this fault was pre-Pennsylvanian and that it McFarland, J.D., III, 1988, The Paleozoic rocks of the Ponca region, Buffalo National River, Arkansas, in hhc 1150 Mbs hhg 1050 rocks TEXAS hhg Mbv 1000 medium- to light-gray, fetid septarian concretions as large as 2 ft (0.6 m) in diameter. caused differential erosion across the fault. North of the river, truncation of the Pitkin Limestone at the Hayward, O.T., Centennial Field Trip Guide, v. 4: Geological Society of America, Boulder, Colorado, Mbs 1150 1600 hhg h 1520 1100 hc Unit is susceptible to landslides. Formation thickness varies from 10 to 340 ft (3 to 110 Web monocline suggests that this structure was also active before Pennsylvanian time. In addition to p. 207–210. 5 Mb 1130 3 ° m). Large variation in thickness of unit partly results from Late Mississippian-Early structural uplift, a sea-level drop at the end of the Mississippian Period (Sutherland, 1988) also was McKnight, E.T., 1935, Zinc and lead deposits of northern Arkansas: U.S. Geological Survey Bulletin 853, hbu h 1560 ha 33 00' hbl hc Pennsylvanian erosion beneath unconformity at base of the Cane Hill Member of the probably a key factor in development of the unconformity. Above the unconformity, the heterogeneous 311 p. 1120 hbl Hale Formation nature of the basal sandstone interval of the Cane Hill Member of the Hale Formation, as well as its Morrison, J.D., 1971, Bedrock geology of the Ponca quadrangle, Newton County, Arkansas: Fayetteville, Oeu 1160 Figure 1. Location of study area within northern Arkansas, in and adjacent to the western part Mbs Mbv Batesville Sandstone (Upper Mississippian, Chesterian)—Fine- to very fine grained, light- content of conglomerate and wood fragments, suggests that this interval includes non-marine fluvial Arkansas, University of Arkansas Masters thesis, 108 p. Mf of Buffalo National River. Lower regional map illustrates geological and selected physiographic deposits that were deposited ahead of a Morrowan sea-level rise. Limestone clasts within conglomerates of Purdue, A.H., and Miser, H.D., 1916, Descriptions of the Eureka Springs and Harrison quadrangles: U.S. 1480 1500 ha provinces of Arkansas and adjacent areas. to medium-brown, calcite-cemented sandstone with interbedded limestone. Thin to medium beds are typically parallel laminated with low-angle crossbeds common in upper the basal Cane Hill Member were probably derived from Pitkin Limestone. Geological Survey Atlas, Folio 202, scale 1:125,000. Mbv 1100 4 Mbv 1560 part of unit. Sandstone commonly contains burrows on bedding plane surfaces and The main part of the Boone Formation within most of the study area does not contain as much chert Suhm, R. A., 1974, Stratigraphy of Everton Formation (early Medial Ordovician), northern Arkansas: Mbv 1110 breaks into tabular blocks. One or more discontinuous, 1–3-ft- (0.3–1-m-) thick, medium- as described elsewhere in northern Arkansas. As a consequence, its contact with underlying St. Joe American Association of Petroleum Geologists Bulletin, v. 58, p. 685–707. Of Mf 1100 Oeu 1510 5 to dark-gray, fetid, fossiliferous limestone beds are locally interbedded with sandstone. Limestone Member, which elsewhere is based on a marked increase in chert, is indistinct. This study did Sutherland, P.K., 1988, Late Mississippian and Pennsylvanian depositional history in the Arkoma basin Mb 3 1530 3 The Hindsville Limestone Member (Purdue and Miser, 1916) is present in the northeast not confirm major thinning of the Boone Formation in the area of the Sneeds Creek dome, as proposed area, Oklahoma and Arkansas: Geological Society of America Bulletin, v. 100, p. 1787–1802. 1090 1550 hhg hbu hhc map area at the base of the formation and is as much as 5 ft (1.5 m) thick in the Cecil by Morrison (1971). Instead, apparent thinning can be attributed to offset between the base and top of the Tchalenko, J.S., 1970, Similarities between shear zones of different magnitudes: Geological Society of 1080 Qc Creek drainage. Hindsville Limestone Member is distinguished by the presence of Boone Formation across a newly recognized northeast-striking normal fault. Although thin, the phosphate- America Bulletin, v. 81, p. 1625–1640. 1510 hbl 1520 Oeu hhc subangular clasts of white chert that range in size to as much as 2 in. (5 cm). Limestone nodule-bearing sandstone and overlying thin shale at the base of the St. Joe is persistent throughout much Withjack, M.O., and Jamison, W.R., 1986, Deformation produced by oblique rifting: Tectonophysics, v. Mbs Mbv Mf 1550 h beds of the Batesville contain crinoids and brachiopods. Sandstone and limestone beds of northern Arkansas (McKnight, 1935). Based on petrography, Horner and Craig (1984) supported a 126, p. 99–124. 1480 h bl 1500 Mf hg contain 2–10-mm-diameter oxidized pyrite framboids that weather to reddish-brown correlation of the basal sandstone with the Sylamore Sandstone that was deposited as a transgressive lag Withjack, M.O., Olson, J., and Peterson, E., 1990, Experimental models of extensional forced folds: hhg 1480 5 1080 Of 1150 during sea level rise in Late time. Strata of uppermost Ordovician through Devonian age are American Association of Petroleum Geologists Bulletin, v. 74, p. 1038–1054. 6 2 9 spheres. The Batesville commonly forms a topographic ledge that forms small waterfalls hhg 5 7 Mb 1340 Mf h 9 along streams. Where stripped of overlying Fayetteville Shale, the top of the Batesville is missing beneath the unconformity at the base of the St. Joe Limestone Member, although strata of these Zachry, D. L., 1977, Stratigraphy of middle and upper Bloyd strata (Pennsylvanian, Morrowan), Qty h hg bu hbl 1150 h typically a topographic flat that hosts sinkholes formed by collapse into dissolution ages are preserved both to the east and west of the map area. northwestern Arkansas, in Sutherland, P.K., and Manger, W.L., eds., Upper Chesterian-Morrowan h bl hbu 1100 h bl Oeu Mb hc hhc 1000 cavities in underlying Boone Formation. Thickness is 3–30 ft (1–9 m) and is greatest in Suhm (1974) divided the Everton Formation into several formal and informal members that within the stratigraphy and the Mississippian-Pennsylvanian boundary in northeastern Oklahoma and hbl 1050 Mbv 4 0 Mbv the northeastern part of the area map area include, from top to bottom, the Jasper Member, B member, Newton Sandstone Member, C northwestern Arkansas: Oklahoma Geological Survey Guidebook 18, p. 61–66. Of 1480 1520 Mf Mbs ha 1480 1480 ha Mf Boone Formation (Upper to Lower Mississippian)—Formation consists of limestone and member, King River Sandstone Member, and Sneeds Dolomite Members. Only the Newton Sandstone Zachry, D.L., and Sutherland, P.K., 1984, Stratigraphy and depositional framework of the Atoka hbl Mf hhg Mbv 950 Mb Mb cherty limestone of main body that grade into the basal St. Joe Limestone Member. The Member, that forms a prominent cliff in much of the area, is mapped separately here. Suhm (1974) Formation (Pennsylvanian), Arkoma basin of Arkansas and Oklahoma, in Sutherland, P.K., and A′ Boone Formation is a common host of caves and sinkholes. The total thickness of the interpreted the mixed sandstone and carbonate interval of the Ordovician Everton Formation as barrier Manger, W.L., eds., The Atokan series (Pennsylvanian) and its boundaries—a symposium: Oklahoma formation is 380–405 ft (116–122 m) islands and adjacent tidal-flat environments. Geological Survey Bulletin 136, p. 9–17.

1 Base from U.S. Geological Survey, 1967 6 /2 SCALE 1:24 000 Geology mapped by M.R. Hudson intermittently during 1996–2000 Universal Transverse Mercator, Zone 15 1 1/ 2 0 1 MILE Digital database compilation by K.E. Murray during 2001–02 ARKANSAS Digital cartography and map layout by Gayle M. Dumonceaux and Nancy Shock 10000 1000 2000 3000 4000 5000 6000 7000 FEET Edited by F. Craig Brunstein

TRUE NORTH 10.5 1 KILOMETER

MAGNETIC NORTH Manuscript approved for publication January 3, 2003 MAP LOCATION APPROXIMATE MEAN CONTOUR INTERVAL 20 FEET DECLINATION, 1967 NATIONAL GEODETIC VERTICAL DATUM OF 1929

Figure 3. Structural data for the map area. (A) Equal-area Kyles Landing fault projection of poles to bedding adjacent to the Kyles Landing fault, with model fold axis. (B) Striated faults within the hanging wall of the Kyles Landing fault. Great circles and dots are lower hemisphere projections ABN N CN of fault planes and their slip lines, respectively. Small arrows show movement sense, with greater head ornamentation indicating higher West Northeast confidence on slip determination. Open five-, four-, and three-pointed stars represent orientation of maximum, intermediate, and least principal paleostress axes, respectively, estimated from analysis of Angelier (1990). Large black arrows show azimuth of maximum 500 horizontal compression. (C) Poles and orientation density contours for 1600 deformation bands in hanging wall of Kyles Landing fault. Contour SYSTEM PROVINCIAL SERIES SYSTEM A A' PROVINCIAL SERIES levels are multiples of standard deviations. Two density highs define ATOKA N Sneeds Creek dome Compton fault Grogans Hollow syncline Cliff Hollow anticline Hanner Point monocline S conjugate sets from which orientation of principal stress axes were FORMATION h constructed by bisecting obtuse and acute angles to find maximum bu c ccc FEET and least principal paleostress axes. (D) Striated map-scale faults ha Upper part FEET h hhg h h from en echelon zone trending west-northwest across map area. bu h bl bu 1400 h h hbl hhc h hg hhg hbl hbu Fold Axis 2000 bl bu hbl hbl hhg Mbv bu h 2000 Large black arrows show azimuth of least horizontal compression. hhg hhg Mbv hc hhg hhc Mf hhc hhc N = 35 Other conventions as in B. (E) Poles and orientation density contours h h Mf N = 35 hc bl Mf hhc 400 Upper part Mf Mbv Mbv for deformation bands at a site in footwall of California Point fault.

Mbv BLOYD FORMATION Lower part Mf Mbs Mb Mbv Mf poles to bedding small faults and striations poles to deformation bands Large black arrows show azimuth of least horizontal compression. 1500 Mb Mb 1500 Mbv Mb Oeu Morrowan Mb Mbs Mb Mbs Mb Mbs Prairie Grove Member Other conventions as in C. (F) Poles and orientation density contours Mbs Oen Mbs Mb 1200 Buffalo River Buffalo Oeu Mbs BLOYD FORMATION Lower part for deformation bands at a site in hanging wall of the Compton fault. Oel Oeu Mb PENNSYLVANIAN (part) Oen Cane Hill Member Oeu Oen Qty Oeu Morrowan Atokan Large black arrows show azimuth of least horizontal compression. HALE

1000 Oel Op 1000 PENNSYLVANIAN (part) Oen Oel Oen Prairie Grove Member Mapped ENE-striking California Point fault Other conventions as in C. (G) Striated small-scale secondary faults Oel Op Oel FORMATION Oc Op normal faults from site in hanging wall of the Compton fault. Large black arrows Op Cane Hill Member PITKIN LIMESTONE Oc Op HALE Oc Wedington Sandstone Member DEN N show azimuth of maximum horizontal compression. Other conventions

Oc FORMATION 500 Oc 500 300 1000 FAYETTEVILLE SHALE as in B. (H) Rose diagram of strike frequency of joints recorded within BATESVILLE SANDSTONE Hindsville Limestone Member of Batesville the map area. Chesterian FAYETTEVILLE 2 × vertical exaggeration SHALE Chesterian

800 BOONE FORMATION Meramecian- Osagean BATESVILLE SANDSTONE Cross-bedded Hindsville Limestone Member of Batesville sandstone N 200 MISSISSIPPIAN H 600 St. Joe Limestone Member FERNVALE LIMESTONE Sandstone BOONE MISSISSIPPIAN Osagean- Meramecian- Osagean FORMATION

Kinderhookian N = 38 EVERTON B B' FORMATION Shale, siltstone faults and striations poles to deformation bands 400 Newton Sandstone Member W E 10% 100 Compton fault FEET FEET Limestone St. Joe Limestone Member 2000 2000 F N G N Osagean- Kyles Landing fault h Kinderhookian hhc Mf hc Mp 200 EVERTON hhc Dolomite FORMATION

Mfw ORDOVICIAN 1500 Mbv Mbv Mf Mf 1500 POWELL DOLOMITE Newton Sandstone Member Mf Mb Mb N = 406 Mb Mbs Chert Mbv Oeu Oeu Mb Mbs Oeu Mb Mbs ccc ORDOVICIAN joints Oen Oen Oeu 1000 1000 COTTER DOLOMITE Coal Oel Oen Oeu 0 m 0 ft Oel Oen Op Op Oel Oc Op 500 Oc 500 Oc Figure 2. Stratigraphic columns for Paleozoic rocks of the map area. Column for west area generally reflects exposed stratigraphy near Hemmed-In Hollow. Column for northeast area reflects stratigraphy exposed in the Cecil Creek drainage. Provincial series are from Purdue and Miser (1916) and McFarland (1988).

2× vertical exaggeration N = 21

poles to deformation bands late small faults and striations

Any use of trade names in this publication is for GEOLOGIC MAP OF THE PONCA QUADRANGLE, NEWTON, BOONE, AND CARROLL COUNTIES, ARKANSAS descriptive purposes only and does not imply endorsement by the U.S. Geological Survey By For sale by U.S. Geological Survey Information Services Box 25286, Federal Center, Denver, CO 80225 Mark R. Hudson and Kyle E. Murray This map was produced on request, directly from digital files, on an electronic plotter. It is also 2003 available as a PDF file at http://pubs.usgs.gov