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51

MAP EXPLANATION

Contact

Normal fault—Dashed where approximately located, 

 dotted where concealed, bar and ball on downthrown block 

Normal, right-lateral, strike-slip fault—Dashed where 

 approximately located, bar and ball on downthrown block,

 arrows show relative motion

Normal, left-lateral, strike-slip fault—Dashed where 

 approximately located, bar and ball on downthrown block,

 arrows show relative motion

Fault movement—Away from viewer (left), toward viewer (right),

 shown in cross sections only

Anticline

Syncline

Monocline

Strike and dip of bedding

Inclined

Horizontal

Line of equal elevation showing base of Boone Formation,

 contour interval 50 ft 

Control point showing elevation in feet on base or

 top of Boone Formation 

900

900

N N

n = 70

N

Strike-slip faults

N

Normal faults

A

B

C

Figure 4. Structural data from the Maumee 

quadrangle. Number of data are “n”. (A) Rose 

diagram of strike frequency (left) and stereoplot of 

poles and orientation density contours (right) for fault 

planes measured in outcrop within quadrangle. 

Contour levels are multiples of standard deviations. (B) 

Striated faults with slip sense that are compatible with 

normal (left) and strike-slip (right) paleostress regimes. 

Arcs and dots are lower hemisphere projections of 

fault planes and their slip lines, respectively. Small 

arrows show movement sense of hanging-wall block. 

Open five-, four-, and three-pointed stars represent 

orientation of maximum, intermediate, and least 

principal paleostress axes, respectively, from analysis 

of Angelier (1990). Gray slip symbols are faults 

excluded from calculation due to slip misfits > 45°. 

Large black arrows show azimuth of least horizontal 

compression. (C) Rose diagram of strike frequency of 

joints recorded within the map area. 

N

n = 918

10 2 KILOMETER

McKinney Hollow fault

Pilot Mountain

 

South Tomahawk

 fault

Tomahawk fault

Copper Mine Hollow

syncline

Ranch fault

North Rocky Creek fault

South Rocky Creek 

fault

Caney Hollow fault

Davy Crockett fault

Baker Spring

monocline

Water Creek

monocline

Davis Hollow fault

Tomahawk

graben

fault 

N

N

N

N

O

N

N

N

N

O

S N

S

S

S

S

S

S

S

O

Figure 3. Shaded-relief digital elevation map of quadrangle with structural features and sites 

where faults (squares) were observed. Where determined, slip senses for faults at sites are 

indicated as normal, N (rake 90° to 60°); oblique, O (rake 59° to 30°); and strike-slip, S (rake 

29° to 0°). 

36°07'30"

92°45' 92°37'30”

36°00'

Anticline

EXPLANATION

Fault site

Syncline

Monocline

Fault—Dashed where approximately

 located, dotted where concealed,

 bar and ball on downthrown side

200

400

600

800

300

200

100

0 0

1,000

1,200

Whiterockian

Cincinnatian

LudlowLlandovery

OsageanKinderhookian MeramecianOsagean Mohawkian Chesterian

BOONE

FORMATION

EVERTON

FORMATION

BATESVILLE SANDSTONE

St. Joe Limestone Member

CASON SHALE

Silurian rocks, undivided

FERNVALE LIMESTONE

PLATTIN LIMESTONE

ST. PETER SANDSTONE

Jasper Member

FAYETTEVILLE

SHALE

Wedington Sandstone Member Upper part Lower part

ORDOVICIAN MISSISSIPPIAN

SILURIAN SYSTEM

SERIES ANDPROVINCIALSERIES

FORMATION

Figure 2. Stratigraphic column for Paleozoic rocks within the quadrangle. Provincial series are from Purdue and Miser 

(1916), Craig (1993), and McFarland (1988).

METERS FEET

Sandstone

Shale, siltstone

Limestone

Dolomite

Chert

EXPLANATION

0 5 10 KILOMETERS

Figure 1. Location of study area within northern Arkansas, adjacent to the western part of Buffalo National River. Other U.S. 

Geological Survey geologic maps in area (Hudson, 1998; Hudson and others, 2001; Hudson and Murray, 2003, 2004; Hudson and 

others, 2006; Hudson and Turner, 2007, 2009) are listed by publication number. U.S. Geological Survey publication series 

abbreviations are: Open-File Report (OFR), Miscellaneous Field Studies Map (MF), and Scientific Investigations Map (SIM). Lower 

regional map illustrates geological and selected physiographic provinces of Arkansas and adjacent areas. 

Harrison

Jasper

Buffalo

River

36°00’

36°15'

35°52’30”

36°07’30”

 93°15'

93°30’ 92°45'

93°00'

Buffalo

National

43 7

65

River

MF 2356

OFR 98–116

MF 2412

OSAGE NE

OSAGE SW

GAITHER HARRISON

JASPER WESTERN GROVE

BOXLEY MURRAY MT. JUDEA EULA

HASTY

PARTHENON

PONCA ST. JOE MAUMEE

MARSHAL

SIM 2847 SIM 2921 SIM 3074 THIS STUDY

SIM 2991

Ozark Dome

94° 92° 90°

Mississippi Embayment

Arkoma Basin

St. Francois

Mountains

Salem 

Plateau

Plateau

Cretaceous

 rocks

Springfield

37°

35°

33°

KANSAS

MISSOURI

TEXAS

ARKANSAS

TENNESSEE

MISSISSIPPI

OKLAHOMA

SNOWBALL

Ouachita Mountains

Boston Mountains

INTRODUCTION

This map summarizes the geology of the Maumee 7.5-minute quadrangle (fig. 1) in 

northern Arkansas. The map area is in the Ozark plateaus region on the southern flank of 

the Ozark dome (fig. 1). The Springfield Plateau, composed of Mississippian cherty limestone, overlies the Salem Plateau, composed of Ordovician carbonate and clastic rocks, with 

areas of Silurian rocks in between. Erosion related to the Buffalo River and its tributaries, 

Tomahawk, Water, and Dry Creeks, has exposed a 1,200-ft-thick section of Mississippian, 

Silurian, and Ordovician rocks (fig. 2) mildly deformed by faults and folds. An approximately 

130-mile-long corridor along the Buffalo River forms the Buffalo National River that is 

administered by the National Park Service.

McKnight (1935) mapped the geology of the Maumee quadrangle as part of a larger 

1:125,000-scale map focused on understanding the lead and zinc deposits common in the 

area. Detailed new mapping for this study was compiled using a Geographic Information 

System (GIS) at 1:24,000 scale. Site location and elevation were obtained by using a Global 

Positioning Satellite (GPS) receiver in conjunction with a U.S. Geological Survey 7.5-minute 

topographic map and barometric altimeter. U.S. Geological Survey 10-m digital elevation 

model data were used to derive a hill-shade-relief map used along with digital orthophotographs to map ledge-forming units between field sites. Bedding attitudes were measured in 

drainage bottoms and on well-exposed ledges. Bedding measured at less than 2° dip is 

indicated as horizontal. Structure contours constructed for the base of the Boone Formation 

are constrained by field-determined elevations on both upper and lower formation contacts.

DESCRIPTION OF MAP UNITS

Alluvial and active channel deposits of tributary drainages (Quaternary)— 

Tributaries to the Buffalo River include Tomahawk, Dry, and Water Creeks. 

Active-channel deposits include gravel deposits, composed of subangular to 

rounded Paleozoic rock clasts of predominantly chert and sandstone, and 

sandy point bar deposits composed mostly of rounded fine sand. Low 

terraces and active flood plain composed of light-brown, fine sand are 

locally present adjacent to creeks and extend up to about 20 ft above creek 

level. Unmapped bedrock exposures are interspersed along channels. As 

thick as 10 ft 

Young terrace and active channel alluvial deposits (Quaternary)—Active 

channel deposits consist of gravel bar and sandy point bar deposits of the 

Buffalo River. Gravel bar deposits composed of rounded to subrounded 

pebble- to cobble-sized clasts of Paleozoic chert, dolostone, and sandstone, 

and sandy point bar deposits composed of fine to medium, rounded to 

well-rounded sand grains. Terrace deposits are principally light-brown, fine 

sand with lesser interspersed silt and have smooth upper surfaces that are 

about 20–40 ft above the base-flow level of river. Unmapped bedrock 

exposures are located along channel. Deposits are as thick as 20 ft 

Landslide deposits (Quaternary)—Slump block of shale from main body of 

Fayetteville Shale (Mf) and minor sandstone blocks derived from Wedington 

Sandstone Member (Mfw) of Fayetteville Shale in west central part of map. 

Generally back-tilted into hillside and forms hummocky terrain. Probably 

no more that 60–80 ft thick

Medial terrace and alluvial deposits (Quaternary)—Unconsolidated sand 

deposits adjacent to Buffalo River. Deposits are poorly exposed and are 

principally brown-weathered, fine sand. Terrace surfaces are flat to gently 

sloping as high as 60 ft above base-flow level of river. Thickness uncertain 

but probably as much as 20 ft

Old terrace and alluvial deposits (Quaternary)—Unconsolidated gravel and 

sand deposits adjacent to Buffalo River. Deposits are poorly exposed and 

are principally lag gravel of brown-weathered, subrounded to rounded, 

pebble- to cobble-sized clasts of Paleozoic rocks in a sandy matrix. Clasts 

are primarily composed of very fine grained tan sandstone and chert. 

Terrace surface generally rounded 80–120 ft above base-flow level of river. 

Thickness about 5–10 ft

Remnant block deposits (Quaternary)—Remnant erosional blocks of Batesville Sandstone (Mbv) in sinkholes and along faults within the underlying 

main body of the Boone Formation (Mb). Deposits are characterized by 

tabular sandstone blocks with moderately rounded edges 1 to 4 ft in 

diameter and interspersed with chert. Deposits interpreted to be related to 

more recent, late-stage karst development because blocks are not encased 

in paleokarst features such as calcified collapse breccia. Relationship to 

faults is unknown 

Very old terrace and alluvial deposits (Quaternary)—Poorly exposed, 

unconsolidated gravel and sand deposits adjacent to Buffalo River. Deposits are principally a lag of weathered, rounded to well-rounded Paleozoic 

clasts of very fine grained tan sandstone and chert in a sandy matrix 

230–260 ft above base-flow level of river. Thickness about 5–10 ft

Fayetteville Shale (Upper Mississippian, Chesterian)—Fine-grained 

sandstone and siltstone of Wedington Sandstone Member (Mfw) that 

grades downward into main body of black, slope-forming shale. Thickness 

125–170 ft 

Wedington Sandstone Member—Brown to light-gray, well-indurated, 

calcite-cemented, very fine grained sandstone and siltstone; thin to thick 

bedded and has parallel laminations and locally developed low-angle 

crossbeds. Sandstone grades downward into siltstone beds that are ripple 

cross-laminated and bioturbated. Unit gradational with underlying main 

body and caps steep slopes of the main body to form a topographic bench. 

Thickness 25–50 ft 

Main body—Fissile black shale that locally contains thin beds of ripplemarked olive-brown siltstone near its top. Lower part of Fayetteville 

exposed along stream gullies and may contain medium- to light-gray, fetid 

septarian concretions as large as 2 ft in diameter. Unit is susceptible to 

landslides and is conformable with underlying Batesville Sandstone. 

Thickness 100–120 ft

Batesville Sandstone (Upper Mississippian, Chesterian)—Light- to mediumbrown, fine-grained to very fine grained, calcite-cemented sandstone with 

sparse interbedded limestone. Sandstone is thin to medium bedded with 

parallel laminations and occasional low-angle crossbeds in upper part of 

unit. Commonly contains burrows on bedding-plane surfaces and weathers 

to form thin flat blocks or tabular blocks. Fetid, fossiliferous limestone in 

discontinuous 1- to 3-ft-thick beds. Unit contains oxidized pyrite framboids 

0.1–0.5 in. in diameter; framboids weather to reddish-brown spheres. 

Batesville caps topographic flats where Fayetteville Shale is eroded and 

contains sinkholes resulting from collapse in underlying Boone Formation. 

Unconformable with underlying Boone Formation. Thickness 40–60 ft 

Boone Formation (Upper to Lower Mississippian)—Limestone and cherty 

limestone of main body that grade into basal St. Joe Limestone Member 

(Mbs). The Boone Formation is a common host of caves and sinkholes. 

Total thickness 365–375 ft

Main body (Upper to Lower Mississippian, Meramecian to Osagean)— 

Light- to medium-gray, coarsely crystalline, bioclastic limestone and 

interbedded chert; thin- to thick-bedded with parallel planar and wavy beds 

of limestone. Crinoid ossicles are common throughout and a 1- to 

3-ft-thick bed of oolitic limestone is common in upper part of unit. Chert 

content is highly variable both laterally and vertically; horizons with 

abundant chert are typically poorly exposed and only chert lag is observed. 

Brachiopod and crinoid ossicle molds are observed in chert in upper part of 

unit. Most chert is white but blue, orange, or reddish chert become more 

common approaching gradational contact with St. Joe Limestone Member 

(Mbs). Thickness 300–350 ft

St. Joe Limestone Member (Lower Mississippian, Osagean to 

Kinderhookian)—Limestone is red to pink on fresh surface due to 

hematite content in the matrix, but color varies and gray or white is not 

uncommon. Matrix varies from muddy to finely to coarsely crystalline 

supporting abundant crinoid fragments in thin to medium, parallel wavy 

beds. Chert-poor except in upper part where red to pink lenticular chert 

becomes more persistent as it grades upward into main body of Boone 

Formation (Mb). Middle and lower parts of unit contain greenish-gray, tan, 

and yellow interbedded shale. Base of St. Joe is a 1- to 10-ft-thick, 

fine-grained, moderately sorted sandstone containing phosphate pebbles; 

sandstone has discontinuous conglomerate beds with clasts from underlying 

units. Unit unconformable with underlying Silurian and Ordovician rocks, 

amount of missing section beneath unconformity increases to northwest. 

Thickness 30–60 ft

Silurian rocks, undivided—Includes parts of units discussed below. Cumulative 

thickness 0–95 ft although no more than 60 ft exposed in any one location

Lafferty Limestone (upper to middle Silurian, Ludlow)—Light-gray, 

purple, and red dense micrite that breaks with conchoidal fracture; white to 

light-gray on weathered surface. Medium bedded and forms rounded 

outcrop. Contact with St. Clair Limestone sharp and described as unconformable by Wise and Chaplin (1979) and Smart and Hutto (2008) but 

Craig and others (1984) and Craig (1993) interpreted as conformable. 

Thickness 0–5 ft

St. Clair Limestone (middle to lower Silurian, Ludlow to upper 

Llandovery)—Light-pink, tan, and light-gray fossiliferous limestone; 

contains crinoid and brachiopod fragments. Limestone is micritic to 

coarsely crystalline and massive bedded. Unit contains pyrite framboids 

and irregular vugs filled with white or colorless sparry calcite crystals. Basal 

contact with Brassfield Limestone is unconformable. Thickness 0–60 ft

Brassfield Limestone (lower Silurian, Llandovery)—Light-gray to 

light-pink, micritic to coarsely crystalline, thin- to massive-bedded limestone 

mottled red and gray. Contains crinoid ossicles, pyrite framboids, and 

irregular vugs filled with colorless to white sparry calcite; alteration around 

calcite-filled vugs produces red to maroon color that contributes to mottled 

appearance. Unit underlain unconformably by the Cason Shale (Oc). 

Thickness 0–30 ft

Cason Shale (Upper Ordovician)—Green, tan, black, and blue-green, poorly 

exposed, fissile shale and siltstone that is occasionally dolomitic. Contains 

phosphate-replaced fossils and abundant, polished phosphate nodules from 

sand to pebble size and oxidized pyrite framboids. At type section to the 

east near Batesville, Ark., Cason Shale extends into the Silurian (Craig and 

others, 1984; Craig, 1993). Unit unconformably overlies Fernvale 

Limestone (Of). Thickness 0–15 ft

Fernvale Limestone (Upper Ordovician)—Light-pink, red, and light-gray 

coarse-grained fossiliferous limestone; massive to thick bedded and 

crossbedded with distinctive stylolitic partings 2–3 in. thick that enhance 

dissolution giving the appearance of thinner bedding. Crinoid fragments 

are common including distinctive barrel-shaped crinoid ossicles and 

phosphate nodules are present. Unit unconformably overlies Plattin 

Limestone (Opl). Thickness 0–60 ft

Plattin Limestone (Middle Ordovician)—Light-gray to tan, medium- to 

thin-planar-bedded micrite with discontinuous calcarenite beds. Micrite is 

dense and breaks with conchoidal fracture and locally contains, 

fine-grained, well-rounded quartz grains. Calcarenite is tan, yellow, and 

light-brown, medium bedded, slightly fetid, and contains poikilitic calcite 

growth. Unit unconformably overlies St. Peter Sandstone (Osp). Thickness 0–120 ft 

St. Peter Sandstone (Middle Ordovician)—Tan, white, and lesser blue 

calcite-cemented quartz arenite with minor interbedded dolomite and 

blue-green shale and siltstone. Sandstone is medium to massive bedded, 

often crossbedded, with well-rounded, fine-grained quartz grains; friable 

where calcite cement has been leached out. Upper part of unit rarely 

preserved but as thick as 15 ft when present and forms a ledge above 

middle slope-forming part. Middle part of unit is poorly exposed slope 

former and consists of interbedded sandstone, dolomitic layers, and 

blue-green shale and siltstone. Basal part is best preserved and forms a 

5 to 30 ft ledge with an undulatory unconformable contact with the Everton 

Formation. Sandstone beds often bioturbated and characteristically contain 

cylindrical Skolithos burrows perpendicular to bedding. Thickness 

0–120 ft 

Everton Formation (Middle Ordovician)—Interbedded dolostone, dolomitic 

sandstone, and limestone, divided into upper and lower parts. Base not 

exposed in quadrangle. Total thickness 320 ft

Upper part—Jasper Member (Glick and Frezon, 1953) forms up to 80 ft of 

upper part of Everton Formation and is light-gray, finely crystalline to 

micritic, medium-bedded limestone and sandy limestone. Below Jasper 

Member, upper part of Everton Formation consists of dark- to light-gray, 

micritic to finely crystalline dolostone, limey dolostone, and carbonate 

cemented sandstone. Dolostone and limey dolostones are planar-laminated 

to medium-bedded and commonly contain rounded to well-rounded quartz 

grains. Sandstone is well-sorted, rounded to well-rounded, fine- to 

medium-grained quartz arenite that is dolomite or limey-dolomite cemented. 

Unit contains dolomitic stromatolite mounds. Farther west base of upper 

part of Everton Formation is marked by base of Newton Sandstone 

Member (McKnight, 1935) but is absent in this quadrangle; therefore, basal 

contact is placed above the first consistent limestone beds. Thickest 

exposed section is in northwestern part of quadrangle, 140–160 ft, where 

Jasper is mostly removed. Cumulative thickness 220–240 ft 

Lower part—Interbedded finely crystalline to micritic dark- to light-gray 

limestone, limey sandstone, and sandy limestone. Medium to thick bedded 

with planar to wavy laminations. Near upper contact stromatolite mounds 

are present. Upper beds also contain collapse breccia with clasts of 

overlying dolomitic rocks of upper part of Everton. Only about 60 ft 

exposed in quadrangle 

Lower Ordovician and Cambrian rocks, undivided—Sedimentary rocks 

shown on cross section only

STRATIGRAPHY

The 1200-ft-thick stratigraphic section of Paleozoic rocks (fig. 2) records deposition in a 

continental shelf environment during the Ordovician, Silurian, and Mississippian Periods. 

Provincial series terms determined for Mississippian and Silurian units are from McFarland 

(1988) and Craig (1993), respectively, and are based mostly on conodont biostratigraphy. 

The Buffalo River and its major tributaries have exposed the Paleozoic units and have 

recorded Quaternary deposition in the preserved terrace levels. 

Limestone in the lower part of the Everton Formation (Oel) is restricted to the northwest portion of the quadrangle where it has been exposed by erosion of a structural high. 

The limestones host a karst aquifer that discharges groundwater from an artesian spring 

along Water Creek. Dolomitic rocks in the upper part of the Everton Formation (Oeu) 

grade upward into the basal sandy limestone of the Jasper Member (Glick and Frezon, 

1953; Suhm, 1974), which reaches a maximum thickness of 80 ft on the eastern edge of 

the quadrangle. The Jasper Member thins and pinches out to the north and west in the 

quadrangle. The St. Peter Sandstone (Osp), Plattin Limestone (Opl), and Fernvale Limestone (Of) all reach maximum thicknesses in the southeast corner of the quadrangle but are 

mostly absent in the northwest part. We observed the Cason Shale (Oc) at three localities in 

the quadrangle, although McKnight (1935) documented additional exposures within the 

quadrangle. At the type-section east of the map area near Batesville, Ark., the upper part of 

the Cason Shale is Silurian because it overlies the Silurian Brassfield Limestone and contains 

Silurian fauna (Craig and others, 1984; Craig, 1993), but Craig (1975) demonstrated that in 

its western outcrops, including this quadrangle, only the Ordovician part of the Cason Shale 

is present. 

Silurian rocks (Su) are restricted to the southern half of the quadrangle and continue 

into the Marshall quadrangle to the south (McKnight, 1935; Maher and Lantz, 1953; Hutto 

and Smart, 2008). Silurian rocks are generally preserved in pre-Mississippian structural 

lows; their limited extent resulted from multiple episodes of erosion prior to deposition of 

the Boone Formation (Mb) (McKnight, 1935; Craig, 1993). Differentiation of Silurian rocks 

from Fernvale Limestone (Of) is difficult but Fernvale outcrops are typically moss covered, 

friable, lack micritic facies, and contain characteristic stylolitic partings. 

Although the Mississippian Boone Formation (Mb) overlies Silurian rocks (Su) in the 

southern part of the quadrangle, the major unconformity at the base of the Boone Formation progressively truncates underlying rocks north and west across the quadrangle, eventually placing basal St. Joe Limestone Member (Mbs) above the eroded upper part of the 

Middle Ordovician Everton Formation (Oeu) (cross section A–A’). The basal contact of the 

Boone Formation is often marked by the presence of phosphate nodules in the sandstone or 

shaley horizons. Horner and Craig (1984) suggest this sandstone was deposited as a 

transgressive lag during Late Devonian time. 

The Batesville Sandstone (Mbv) marks a change to dominantly clastic sedimentation 

from mostly carbonate sedimentation in the underlying Boone Formation (Mb). Sandstone 

blocks are commonly found in sinkholes developed from the karstification of the Boone 

Formation. Sandstone blocks found around some larger sinkholes and faults in the 

quadrangle are interpreted as remnant block deposits (Qbx) and not indicative of the basal 

contact. Thicknesses for the Boone Formation of 365 ft and 375 ft are documented in 

wells from the towns of St. Joe, Ark., to the west (well records from Arkansas Geological 

Survey, Little Rock, Ark.) and Marshall, Ark., to the southeast (Maher and Lantz, 1952; 

1953), respectively. In the areas mapped as Qbx however, numerous sandstone blocks are 

present that cannot be in situ without a greatly reduced thickness of the Boone Formation. 

We interpret the blocks to have been trapped in closed depressions created by sinkholes and 

as the underlying limestone was dissolved, reducing the total thickness of the Boone 

Formation, the erosion resistant sandstone blocks remain. The relation between remnant 

blocks and faults is unknown. Fayetteville Shale (Mf) overlies the Batesville Sandstone but is 

only preserved in the Tomahawk graben system. The Fayetteville Shale hosts the only 

mappable landslide deposit (Qls). 

Four levels of terrace deposits are preserved along the Buffalo River. Relative age is 

indicated by elevation above river level with the oldest at the highest elevation. Dating of 

archeological materials and analysis of soil characteristics by Guccione and Guendling (1988) 

suggest an age of Holocene and late Pleistocene for young terrace deposits (Qty) and medial 

terrace deposits (Qtm) are likely late Pleistocene. Old terrace deposits (Qto1) are Quaternary (< 2.6 Ma; Head and others, 2008; Walker and Geissman, 2009) but have not been 

studied in detail. Old terrace deposits correlate to similar terrace deposits about 80–120 ft 

above base-flow level of the Buffalo River on the Western Grove (Hudson and others, 2006), 

Hasty (Hudson and Murray, 2004), Jasper (Hudson and others, 2001) and Ponca 

quadrangles (Hudson and Murray, 2003) to the west (fig. 1). Very old terrace deposits 

(Qto2) are significantly higher than any other terrace deposit at 230–260 ft above base-flow 

level. These deposits are located on narrow point bars and are suspected to be correlative 

with a similar mapped terrace on the Western Grove quadrangle (Hudson and others, 2006) 

(fig. 1). 

STRUCTURAL GEOLOGY

Rocks within the map area were deformed by faults and folds, and structure contours 

on the base of the Boone Formation illustrate the location and relative offset of these 

structures. The structure contours conform to elevations at 565 control points located at 

both lower and upper contacts of the Boone Formation, as well as other information 

limiting maximum or minimum elevations of these contacts. A 370-ft average thickness for 

the Boone Formation (Mb), including the St. Joe Limestone Member (Mbs), was used to 

project the elevation of the basal contact from points on the upper contact. This average 

thickness is constrained by well data documenting approximately 375 ft of Boone Formation southeast in the town of Marshall (Maher and Lantz, 1952; 1953) and a well that 

penetrated about 365 ft in the town of St. Joe to the west (well records from the Arkansas 

Geological Survey, Little Rock, Ark.). The average thickness determined for the Boone 

Formation in this quadrangle is 20 ft less than a 390-ft average thickness determined from 

surface stratigraphic sections of the Boone Formation farther to the west in the Buffalo 

River watershed (Hudson, 1998) that was used in construction of structure contours for 

published geologic maps farther to the west (fig. 1).

Several regionally extensive faults and folds are present within the Maumee quadrangle. 

The Tomahawk, South Tomahawk, and Pilot Mountain faults correspond to faults previously 

named by McKnight (1935) in the western part of the quadrangle and the North Rocky 

Creek and South Rocky Creek in the southeastern part of the quadrangle. As a result of our 

new detailed geologic mapping, we have revised fault traces from those of McKnight (1935). 

We mapped several newly recognized faults, including the Ranch, McKinney Hollow, and 

Caney Hollow faults. 

Some structural features mapped as folds by McKnight (1935) are reinterpreted as 

combined fault and fold zones. A N 50° E-trending structural zone with a down-to-southeast 

throw of about 200 ft extends across the northwestern part of the quadrangle and was 

named the Water Creek monocline by McKnight (1935). This zone contains several 

left-stepping en echelon faults of N 55° E to N 68° E strike, the longest of which is the 

northeastern extension of the Davy Crockett fault from the adjacent St. Joe quadrangle 

(Hudson and Turner, 2009). In the center of the zone, the Davis Hollow fault elevated the 

lower part of the Ordovician Everton Formation, the lowest stratigraphic level in the 

quadrangle, to the surface in its footwall. At its southwestern end the Davis Hollow fault 

loses throw but is interpreted to continue across Water Creek on the basis of an abrupt start 

of a dolostone and sandstone cliff of upper part of Everton Formation (Oeu) to the south 

and a silicified zone holding up a bedrock knob southwest of the creek. However, dips as 

great as 25° southeast of this fault accommodate most of the throw and mark the limb of 

the Water Creek monocline. The Caney Hollow fault is a NE-striking fault and associated 

fold located at the intersection of Water Creek and White Oak Hollow in the east-central 

part of the quadrangle. This is named for exposures in the Caney Hollow drainage just to 

the east of the quadrangle boundary (S. Ausbrooks, Arkansas Geological Survey, oral 

commun., 2010). Beds dip as steeply as 40° SE adjacent to the fault, and folding contributes significantly to the overall down-to-southeast throw across the structure. A small dome 

southwest of the Caney Hollow fault (Sec. 3, T. 16 N., R. 16 W.) may have formed as a 

result of flexure related to termination of a right-lateral component of the Caney Hollow 

fault. 

The Tomahawk graben of McKnight (1935) is a system of west-northwest- to 

northwest-trending faults and associated folds that form a broad down-dropped zone across 

the southern part of the quadrangle (fig. 3). The northern margin of this zone is formed by 

the Tomahawk and North Rocky Creek faults. Although a portion of the North Rocky 

Creek fault is concealed beneath the Buffalo River and alluvium, we interpret it to be 

continuous from the Rocky Creek area, northwest to its intersection with the Tomahawk 

fault. The southern margin of the graben system is defined by down-to-north faults and 

monoclines. The South Rocky Creek fault dies into a monocline at its eastern end and is 

discontinuous with the McKinney Hollow fault that dies into the Baker Spring monocline at 

its western end. The graben system is internally deformed by the South Tomahawk, Pilot 

Mountain, and Ranch faults and several folds including the Copper Mine Hollow syncline 

marking the lowest structural axis.

Fault data collected at numerous sites within the quadrangle (fig. 3) indicate the typical 

orientations and slip senses for faults (fig. 4A) and give insight into the causative stresses 

responsible for deformation. Many of these faults are small displacement cataclastic faults, 

deformation bands (Aydin and Johnson, 1978), preferentially developed in well-sorted 

Ordovician sandstones of the St. Peter Sandstone (Osp). Frequency maxima demonstrate 

common orientations of faults that dip moderate to steeply either to the south to southsoutheast or to the north to northeast. A subset of faults whose slip senses could be 

determined are predominantly normal or strike slip (fig. 4B). Dips of normal faults vary 

from north to north-northeast or south to southwest. Among strike-slip faults, those with 

right-lateral sense mostly strike east-northeast and dip southeast, whereas those with 

left-lateral sense mostly strike southeast and dip northeast or southwest. Paleostress 

inversions for these normal and strike-slip faults, using the method of Angelier (1990), 

mostly fit stress regimes with a least principal stress axis oriented south-southwest and near 

horizontal, and with intermediate and maximum principal stress axes flipping between near 

vertical and east-southeast and near horizontal (fig. 4B). From these data we interpret that 

northeast-striking fault zones in the quadrangle have right-lateral slip as well as down-to-thesoutheast throw, whereas east-southeast to southeast-striking faults have dominantly normal 

slip but may also have components of left-lateral slip. Similar coordinated movements 

among normal and strike-slip faults have been documented elsewhere in the southern Ozark 

dome, and their dominantly north-south extension accommodated late Paleozoic flexure of 

the southern continental margin as it was loaded by the adjacent Ouachita orogenic belt 

(Hudson, 2001).

Whereas most of the faulting in the quadrangle is probably late Paleozoic in age, the 

outcrop distribution of pre-Mississippian rocks suggests effects of older deformation. The 

progressive truncation of Silurian rocks (Su), Upper Ordovician Fernvale Limestone (Of), 

and Middle Ordovician Plattin Limestone (Opl) and St. Peter Sandstone (Osp) beneath the 

Mississippian unconformity suggests the presence of a broad pre-Mississippian uplift 

centered northwest of the quadrangle. McKnight (1935) suggested that this progressive 

truncation might be linked to uplift across the Water Creek monoclinal zone, but detailed 

mapping in this and adjacent quadrangles (Hudson and others, 2006; Hudson and Turner, 

2009) demonstrates a more regionally extensive east-northeast trend of these stratigraphic 

truncations, distinct from the N 50° E Water Creek monoclinal zone. In a second example, 

the northern margin of the Tomahawk graben system probably was active before Mississippian deposition. Silurian rocks (Su) and Upper Ordovician Fernvale Limestone (Of) are 

thickest in the hanging wall of the North Rocky Creek fault but are thin to absent in footwall 

exposures (cross section B–B’), suggesting that this west-northwest-trending zone had 

pre-Mississippian activity (McKnight, 1935). Northeast of North Rocky Creek fault, 

thickening, thinning, and removal of the Plattin Limestone (Opl) indicate this paleohigh area 

was an irregular surface with localized domes and basins and one small steep-limbed syncline 

(SE 1⁄4, Sec. 15, T. 16 N., R. 16 W.) prior to being planed off during pre-Mississippian 

erosion.

Joints measured within the map area (918 total) are near vertical and distributed in 

several sets (fig. 4C). The dominant set strikes north. Less prominent joint sets strike 

west-northwest and northeast. Joint planes within limestone and dolostone formations, 

such as the Boone (Mb) and Everton Formations (Oeu and Oel), are commonly enlarged 

due to dissolution.

ACKNOWLEDGMENTS

This work was conducted in a cooperative project between the U.S. Geological Survey 

and the U.S. National Park Service. Helpful discussions with M.E. Berry of the U.S. 

Geological Survey, Denver, Colo. provided guidance and insight into classification of surficial 

deposits. Thoughtful reviews by W.R. Page of the U.S. Geological Survey and S. Ausbrooks 

of the Arkansas Geological Survey improved the map. Special thanks go to the many 

private owners who allowed access onto their land during this study. 

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Arkansas, in Hayward, O.T., ed., Centennial Field Trip Guide, v. 4: Geological Society 

of America, p. 207–210. 

McKnight, E.T., 1935, Zinc and lead deposits of northern Arkansas: U.S. Geological Survey 

Bulletin 853, 311 p. 

Purdue, A.H., and Miser, H.D., 1916, Descriptions of the Eureka Springs and Harrison 

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County, Arkansas: Arkansas Geological Survey Digital Geologic Quadrangle Map 

DGM-AR-00374, scale 1:24,000. 

Suhm, R.W., 1974, Stratigraphy of Everton Formation (Early Medial Ordovician), northern 

Arkansas: The American Association of Petroleum Geologists Bulletin, v. 58, p. 

685–707.

Walker, J.D., and Geissman, J.W., 2009, 2009 GSA geologic time scale: GSA Today, 

April/May 2009, p. 60–61.

Wise, O.A., and Chaplan, W.M., 1979, Silurian and Devonian rocks of northern Arkansas: 

Arkansas Geological Commission Information Circular 25, 14 p.

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Qty

Qls

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Qto1

Qbx

Qto2

Mfw

Mf

Mbv

Mb

Mbs

Su

Oc

Of

Opl

Osp

Oeu

Oel

Ou

Mfw

Mf

Mbv

Qls

Mb

Mbs

Su

Unconformity

Unconformity

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Of

Ou

Unconformity

Unconformity

Unconformity

Unconformity

Unconformity

Unconformity

Unconformity

Oeu

Opl

Osp

Oel

CORRELATION OF MAP UNITS

Oc

Qto2

QUATERNARY

MISSISSIPPIAN

SILURIAN

ORDOVICIAN

CAMBRIAN

Chesterian

Meramecian–Osagean

Osagean–Kinderhookian

Ludlow–Llandovery

Lower Ordovician

and

Cambrian

Middle Ordovician

Upper Ordovician

0

500

1,000

FEET

0

500

1,000

FEET

B B’ SOUTH ROCKY CREEK FAULT NORTH ROCKY CREEK FAULT Buffalo River Buffalo River

Mb Mbs Mb Mb

Mbs

Mbs Mbs

Opl Osp Oeu

Oel

Osp Oeu

Oel

Ou

Opl

Opl Osp Oeu

Oel

Su Of Su

Qty

VERTICAL EXAGGERATION 2X

Ou Ou

-500

500

0

1,000

1,500 

FEET

-500

500

0

1,000

1,500

FEET

A A’

Oel

Oeu Osp

Opl

Oc Of

Mbs

Mbs Mb

Su

Qal Opl

Oel

Oeu

Of

Mbv

Mbs

Osp Opl

Mbs Mbs Mb

Oel

Oeu

Oel

Oeu

Mbv Mf

Opl

Mb

Osp

Opl

Mb Mb Mbs

Mb Mb Mbs

Ou

RANCH FAULT

MCKINNEY HOLLOW FAULT

NORTH ROCKY CREEK FAULT

TOMAHAWK FAULT

DAVIS HOLLOW FAULT

BEND IN

SECTION

Water Creek

Dry Creek

Tomahawk Creek

VERTICAL EXAGGERATION 2X

Qal

Qal

Ou

Ou

Ou

U.S. DEPARTMENT OF THE INTERIOR

U.S. GEOLOGICAL SURVEY

SCIENTIFIC INVESTIGATIONS MAP 3134

Version 1.0

Prepared in cooperation with the

U.S. NATIONAL PARK SERVICE

Any use of trade names is for descriptive purposes only 

and does not imply endorsement by the U.S. Government

This map was produced on request, directly from 

digital files, on an electronic plotter

For sale by U.S. Geological Survey Information Services

Box 25286, Federal Center, Denver, CO 80225

1-888-ASK-USGS

ArcInfo coverages and a PDF for this map are available at 

http://pubs.usgs.gov/sim/3134/

Suggested citation:

Turner, K.J., and Hudson, M.R., 2010, Geologic map of the

Maumee quadrangle, Searcy and Marion Counties, Arkansas:

U.S. Geological Survey Scientific Investigations Map 3134,

scale 1:24,000.

GEOLOGIC MAP OF THE MAUMEE QUADRANGLE, SEARCY AND MARION COUNTIES, ARKANSAS

By

Kenzie J. Turner and Mark R. Hudson

2010

CONVERSION FACTORS

Multiply By To obtain

inches (in.)

feet (ft)

miles (mi)

2.54

0.3048

1.609

centimeters (cm)

meters (m)

kilometers (km)

1 .5 0 1 KILOMETER

SCALE 1:24 000

CONTOUR INTERVAL 20 FEET

NATIONAL GEODETIC VERTICAL DATUM OF 1929

1 1/ 2 0 1 MILE

MAGNETIC NORTH

6.5°

APPROXIMATE MEAN

DECLINATION, 1966 TRUE NORTH

QUADRANGLE LOCATION

ARKANSAS

Geology mapped by K.J. Turner and M.R. Hudson,

2007–2009

Digital map database prepared by Kenzie J. Turner

Editing and digital cartography by

Gayle M. Dumonceaux

Denver Publishing Service Center

Manuscript approved for publication

September 1, 2010

Base from U.S. Geological Survey, 1966

Projection and 10,000-foot grid ticks: Arkansas

coodinate system, north zone

1000-meter Universal Transverse Mercator grid ticks, zone 15

1927 North American Datum