Capitol Reef National Park 

Geologic Resource Evaluation Report 

Natural Resource Report NPS/NRPC/GRD/NRR—2006/005 

National Park Service 

U.S. Department of the Interior 

Natural Resource Program Center 

Capitol Reef National Park 

Geologic Resource Evaluation Report 

Natural Resource Report NPS/NRPC/GRD/NRR—2006/005 

Geologic Resources Division 

Natural Resource Program Center 

P.O. Box 25287 

Denver, Colorado 80225 

September 2006 

U.S. Department of the Interior 

Washington, D.C.
The Natural Resource Publication series addresses natural resource topics that are of interest 

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issues of management applicability. Examples of the diverse array of reports published in this 

series include vital signs monitoring plans; "how to" resource management papers; 

proceedings of resource management workshops or conferences; annual reports of resource 

programs or divisions of the Natural Resource Program Center; resource action plans; fact 

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Printed copies of reports in these series may be produced in a limited quantity and they are 

only available as long as the supply lasts. This report is also available from the Geologic 

Resource Evaluation Program website (http://www2.nature.nps.gov/geology/inventory/

gre_publications) on the internet, or by sending a request to the address on the back cover. 

Please cite this publication as: 

Graham, J. 2006 Capitol Reef National Park Geologic Resource Evaluation Report. Natural 

Resource Report NPS/NRPC/GRD/NRR—2006/005. National Park Service, Denver, 

Colorado. 

NPS D-224, September 2006 
 CARE Geologic Resource Evaluation Report iii

Table of Contents 

List of Figures .............................................................................................................. iv

Executive Summary ...................................................................................................... 1

Introduction ................................................................................................................... 2

Purpose of the Geologic Resource Evaluation Program ............................................................................................2

Park History................................................................................................................................................................2

Regional Geology.......................................................................................................................................................2

Geologic Issues............................................................................................................. 7

Geohazards................................................................................................................................................................7

Groundwater...............................................................................................................................................................8

Disturbed Lands .........................................................................................................................................................8

Paleontological Resources .........................................................................................................................................8

Mineral Occurences....................................................................................................................................................9

Seismicity .................................................................................................................................................................10

Geologic Features and Processes............................................................................. 13

Waterpocket Fold .....................................................................................................................................................13

Teasdale Anticline ....................................................................................................................................................13

Teasdale Fault..........................................................................................................................................................13

Thousand Lake Fault................................................................................................................................................13

Other Folds and Faults .............................................................................................................................................14

Joints ........................................................................................................................................................................14

Dikes and Sills..........................................................................................................................................................14

Quaternary Features ................................................................................................................................................14

Tour of Park Features...............................................................................................................................................15

Map Unit Properties .................................................................................................... 21

Map Unit Properties Table........................................................................................................................................22

Geologic History.......................................................................................................... 27

Paleozoic Era ...........................................................................................................................................................27

Mesozoic Era............................................................................................................................................................27

Cenozoic Era............................................................................................................................................................31

Glossary....................................................................................................................... 41

References................................................................................................................... 42

Appendix A: Geologic Map Graphic .......................................................................... 45

Appendix B: Scoping Summary................................................................................. 47

Appendix C: Geoindicators Report............................................................................ 50

Attachment 1: Geologic Resource Evaluation Products CD 
 NPS Geologic Resources Division iv 

List of Figures 

Figure 1. Location map of Capitol Reef National Park ...................................................................................................4

Figure 2. The Colorado Plateau physiographic province................................................................................................5

Figure 3. Major structural features in the Capitol Reef area...........................................................................................6

Figure 4. Mineral and abnormal-radioactivity map of the Capitol Reef area.................................................................11

Figure 5. Schematic diagrams of some common types of hydrocarbon traps..............................................................12

Figure 6. View to the south of Glass Mountain.............................................................................................................19

Figure 7. Upper Cathedral Valley.................................................................................................................................19

Figure 8. Photograph of “the Castle”............................................................................................................................20

Figure 9. Stone lace or Honeycomb weathering ..........................................................................................................20

Figure 10. Geologic time scale.....................................................................................................................................33

Figure 11. Lower Permian depositional environments in southeastern Utah ...............................................................34

Figure 12. Unconformities and depositional sequences in the Permian of the Colorado Plateau ................................34

Figure 13. Paleogeographic map of the Lower Triassic ...............................................................................................35

Figure 14. Paleogeographic map of the fluvial system in the Upper Triassic ...............................................................35

Figure 15. Lower Jurassic paleogeography .................................................................................................................36

Figure 16. Middle Jurassic paleogeography.................................................................................................................37

Figure 17. Upper Jurassic paleogeography .................................................................................................................38

Figure 18. Location of the Cretaceous Period, Western Interior Seaway.....................................................................39

Figure 19. Upper Cretaceous paleogeography ............................................................................................................40
 CARE Geologic Resource Evaluation Report 1

Executive Summary 

This report has been developed to accompany the digital geologic map produced by Geologic 

Resource Evaluation staff for Capitol Reef National Park in Utah. It contains information 

relevant to resource management and scientific research. 

Capitol Reef National Park is located within the 

Colorado Plateau Physiographic Province. The dominant 

geologic feature in the park is the north-south trending 

Waterpocket Fold, a nearly 160-km (100-mi) long steplike flexure called a monocline. West of the fold lies the 

flattop topography of the High Plateaus subprovince, to 

the east are the narrow, steep-sided gorges of the Utah 

Canyon Lands subprovince. 

Erosion has produced most of the unique geologic 

features in the park. Exposed within Capitol Reef 

National Park are monolithic structures reminiscent of 

cathedrals, as well as pinnacles, arches, bridges, slot 

canyons, landslides, and elongated valleys. Streams 

eroding downward through bedrock form sharp, incised 

meanders or “goosenecks.” 

The strata exposed in Capitol Reef represent a variety of 

depositional environments that span the last 275 million 

years. Geologic structures present in the park include 

large-scale folds, faults, and fractures. Igneous dikes and 

sills intrude into the softer sedimentary strata. 

A Geologic Resource Inventory (now Geologic Resource 

Evaluation) scoping meeting, convened in September 

1999, and a Geoindicators scoping meeting, held in June 

2002, served as a forum for discussing mapping and 

geologic issues relevant to the park. The following 

geologic issues were identified as important to park 

management: 

• Geohazards 

• Flash flooding and debris flows 

• Swelling clays 

• Uranium and radon contamination 

• Rockfalls and landslides 

• Groundwater 

• Disturbed lands 

• Paleontological resources 

• Mineral occurrences 

• Seismicity 

Groundwater quality and quantity are significant issues 

in the semi-arid climate of the Colorado Plateau. Steep, 

narrow canyons in semi-arid and arid climates are prone 

to flash flooding in response to intense rainfall events. 

Flash flooding may occur in the narrow, steep canyons 

cut into the Waterpocket Fold or along the Fremont 

River and its tributaries. Flash floods in arid 

environments carry a high sediment load and with 

enough rock fragments, soil, and mud can become debris 

flows as they travel downstream. Flash flooding related 

to stream channel morphology, erosion, streamflow, and 

debris flows are significant park management issues. 

Several Mesozoic formations in the park contain clays 

that swell with the addition of water and shrink upon 

drying. This shrink-swell characteristic causes unstable 

conditions with regard to roads, building construction, 

and infrastructure maintenance. 

Mesozoic rocks host deposits of uranium, vanadium and 

radium in Capitol Reef National Park. Uranium and 

radon contamination are indicated by elevated levels of 

radiation. The stratigraphic units at Capitol Reef that 

contain abnormal radioactivity include: the Moenkopi 

Formation, the Shinarump Member of the Chinle 

Formation, the middle and upper members of the Chinle 

Formation, and the Salt Wash Member of the Morrison 

Formation. 

Fractures in the massive, cross-bedded Mesozoic 

sandstones and the Permian limestone cliffs combined 

with physical and chemical weathering processes 

increase the potential for rockfalls in the park. Cliffs that 

are undercut by the erosion of less resistant strata below 

may collapse. 

Ten abandoned mine sites are known to exist in the park 

including 27 individual mine openings. Three sites have 

been mitigated: the Oyler, Terry, and Rainy Day. 

Paleontological resources are abundant in Capitol Reef. 

Marine invertebrate fossils are found in Permian strata 

and thick accumulations of Cretaceous oysters form the 

Oyster Reef exposed along the Notom-Bullfrog Road. 

Ancient marine and terrestrial vertebrates such as turtles, 

crocodiles, and dinosaurs are also preserved in Capitol 

Reef. Reptile and amphibian tracks are present in the 

Triassic Moenkopi Formation. Poaching and theft of 

fossils are resource management concerns. 

In addition to Uranium minerals identified in the park 

include gypsum, copper, and manganese. Oil and gas 

exploration and production occur outside but adjacent 

to the park boundary. The park is closed to mineral entry 

under the 1872 mining law and federal mineral and oil 

and gas leasing under federal statute. 

Mostly minor earthquake activity occurs on the 

Colorado Plateau. The potential for an earthquake with a 

magnitude more than 5.5 in the Capitol Reef area is 

considered low. 
 NPS Geologic Resources Division 2 

Introduction 

The following section briefly describes the regional geologic setting and the National 

Park Service Geologic Resource Evaluation program. 

Purpose of the Geologic Resource Evaluation Program 

Geologic features and processes serve as the foundation 

of park ecosystems and an understanding of geologic 

resources yields important information for park decision 

making. The National Park Service (NPS) Natural 

Resource Challenge, an action plan to advance the 

management and protection of park resources, has 

focused efforts to inventory the natural resources of 

parks. Ultimately, the inventory and monitoring of 

natural resources will become integral parts of park 

planning, operations and maintenance, visitor 

protection, and interpretation. 

The Geologic Resource Evaluation (GRE) Program, 

which the NPS Geologic Resources Division administers, 

carries out the geologic component of the inventory. 

Staff associated with other programs within the Geologic 

Resources Division (e.g., the abandoned mine land, cave, 

coastal, disturbed lands restoration, minerals 

management, and paleontology programs) provide 

expertise to the GRE effort. The goal of the GRE 

Program is to provide each of the identified 270 “natural 

area” parks with a digital geologic map, a geologic 

resource evaluation report, and a geologic bibliography. 

Each product is a tool to support the stewardship of park 

resources and is designed to be user friendly to nongeoscientists. 

GRE teams hold scoping meetings at parks to review 

available data on the geology of a particular park and to 

discuss specific geologic issues affecting the park. Park 

staff are afforded the opportunity to meet with park 

geology experts during these meetings. Scoping meetings 

are usually held for individual parks although some 

address an entire Vital Signs Monitoring Network. 

Bedrock and surficial geologic maps and information 

provide the foundation for studies of groundwater, 

geomorphology, soils, and environmental hazards. 

Geologic maps describe the underlying physical 

framework of many natural systems and are an integral 

component of the physical inventories stipulated by the 

NPS in its Natural Resources Inventory and Monitoring 

Guideline (NPS-75) and the 1997 NPS Strategic Plan. 

The NPS GRE is a cooperative implementation of a 

systematic, comprehensive inventory of the geologic 

resources in National Park System units by the Geologic 

Resources Division; the Inventory, Monitoring, and 

Evaluation Office of the Natural Resource Program 

Center; the U.S. Geological Survey; and state geologic 

surveys. 

For additional information regarding the content of this 

report, please refer to the Geologic Resources Division 

of the National Park Service, located in Denver, 

Colorado. Up-to-date contact information is available on 

the GRE website (http://www2.nature.nps.gov/ 

geology/inventory/). 

Park History 

The Fremont people, contemporaries of the Ancestral 

Puebloans, lived on the northern border of the Colorado 

Plateau from A.D. 500 to A.D. 1300. They grew crops in 

the rich soils on the floodplains of the Fremont River and 

other perennial rivers. Game was plentiful due to 

abundant water in the river valleys, water pockets, 

springs, and seeps. 

For several centuries following the disappearance of the 

Fremont culture, no significant human activity is known 

in the region. The first European explorers found Ute 

and Southern Paiute nomads in the area. After the Civil 

War, Mormon Church officials in Salt Lake City tried to 

establish missions in remote niches of the intermountain 

west. However, it wasn’t until Major John Wesley Powell 

and his team of surveyors entered the Capitol Reef 

country that the geomorphology and physiographic 

features of the area were systematically described. 

Early visitors to the area saw the numerous rounded 

“domes” of rock and were reminded of the impressive, 

white, rotundas in Washington, D.C. At the time of these 

first pioneers, the term “reef” referred to any rocky 

barrier or escarpment that hindered travel and the 

rugged spine of the Waterpocket Fold certainly qualified. 

Thus the area came to be known as “Capitol Reef” as a 

result of its geologic features. 

On August 2, 1937, President Roosevelt signed a 

proclamation setting aside 37,711 acres as Capitol Reef 

National Monument. President L B. Johnson placed an 

additional 215,056 acres under NPS control in 1968. A 

series of bills were introduced to change the status of the 

monument to a park. On December 18, 1971 the 241,904 

acres (378 square mi) of Capitol Reef National 

Monument became Capitol Reef National Park. 

Regional Geology 

Capitol Reef National Park has some of the most 

spectacular geology in the western United States. 

Because of the brilliantly colored canyon walls, the 

Navajo people called it the Land of the Sleeping 

Rainbow. Examples of the natural beauty of this desert 

landscape include: the rugged spine of the Waterpocket 

Fold, high-walled gorges cut through the fold, monoliths, 

ridges, buttes, and miles of colorful canyons. 

Located in southern Utah, Capitol Reef is part the 

Colorado Plateau Physiographic Province (figures 1 & 2). 

The Colorado Plateau is bordered on the east by the 

Southern Rocky Mountains, on the north by the Middle 

Rocky Mountains and the Wyoming Basin and on the 
 CARE Geologic Resource Evaluation Report 3

west and south by the extensional Basin and Range 

Physiographic Province (figure 2). 

Rocks at Capitol Reef National Park range in age from 

Permian to Tertiary and record 275 million years of the 

earth’s history. The strata represent a variety of ancient 

environments including open marine, nearshore, fluvial 

(river), lacustrine (lake), and desert. 

The highest point in the Capitol Reef area is Blue Bell 

Knoll, a low, rounded hill on top of Boulder Mountain at 

3,446 m (11,306 ft) in elevation. The irregular outline of 

Boulder Mountain has been deeply cut by several broad 

glaciated valleys. Thousand Lake Mountain is a smaller 

flat-topped feature located north of Boulder Mountain 

(figure 3). 

Folds and Faults 

Capitol Reef National Park is geologically defined by the 

escarpment of the Waterpocket Fold, a nearly 160-km 

long (100-mi) step-like flexure (monocline) in the 

sedimentary rock. Associated large-scale geologic 

structures include anticlinal and monoclinal folds, faults, 

and fractures. Other prominent structural features of the 

Capitol Reef region are the Teasdale Anticline, the 

Teasdale Fault, and the Thousand Lake Fault (figure 3), 

discussed in Geologic Features and Processes below. 

Most of the major faults lie west of the Waterpocket Fold 

(figure 3) (Smith et al. 1963; Billingsley et al. 1987). On 

the surface, the majority of the faults have been mapped 

as normal faults that follow the northwest-southeast 

trend of the anticlines and synclines (Billingsley et al. 

1987). While some normal faults are thought to have 

fractured rocks from the surface down through the 

Precambrian, most are interpreted as relatively shallow 

(Billingsley et al. 1987). However, interpretations of the 

faults at depth may be suspect because of limited 

subsurface geologic data. 

Reverse faults in the subsurface have been mapped as 

dipping 60o to the southwest (Billingsley et al. 1987). 

Billingsley and others (1987) mapped the reverse faults 

below Capitol Reef as blind thrust faults that disturb 

Precambrian through Mississippian rocks. Blind faults 

are buried faults that have no surface expression. 

Younger strata have been folded over the axis of the 

reverse faults beneath Capitol Reef but have not been 

offset, or fractured, by the underlying faults. 

While the Waterpocket Fold is the dominant geologic 

feature of Capitol Reef National Park, the park also 

contains classic elongated “strike” valleys, dikes and sills, 

intrusive gypsum domes, massive landslides, fossilized 

oyster reefs, petrified logs, dinosaur bones, bentonitic 

hills, and unusual soft-sediment deformational features. 
 NPS Geologic Resources Division 4 

Figure 1. Location map of Capitol Reef National Park. From Morris and others, 2000. 
 CARE Geologic Resource Evaluation Report 5

Figure 2. The Colorado Plateau physiographic province, showing some of the significant uplifts, basins, faults, volcanic centers, and 

rivers. High areas are shown in gray: AM, Abajo Mts.; AP, Aquarius Plateau; BC, Book Cliffs; CCU, Circle Cliffs Uplift; DU, Defiance 

Uplift; KU, Kaibab Uplift; LSM, La Sal Mts.; MU, Monument Upwarp; RC, Roan Cliffs; SRS, San Rafael Swell; UU, Uncompahgre Uplift. 

Basins: PB, Paradox Basin; UB, Uinta Basin. Capitol Reef National Park is located on the Waterpocket Fold. Leading edge of Sevier 

Thrust Belt is shown with sawteeth on upper, overriding thrust plate. Modified from Kiver and Harris, 1999. 
 NPS Geologic Resources Division 6 

Figure 3. Major structural features in the Capitol Reef area. Modified from Smith and others, 1963. 
 CARE Geologic Resource Evaluation Report 7

Geologic Issues 

A Geologic Resource Evaluation scoping session was held for Capitol Reef National Park 

on September 27-28, 1999, to discuss geologic resources, address the status of geologic 

mapping, and assess resource management issues and needs. The following section 

synthesizes the scoping results, in particular, those issues that may require attention 

from resource managers. 

In addition to the GRE scoping session in 1999 a 

geoindicators meeting was held in Moab, UT from June 

3-6, 2002 to discuss geologic issues for four NPS units in 

southeastern Utah. Discussions from this meeting and 

the GRE scoping meeting identified the following 

geologic issues as significant to park management. 

Geohazards 

Flash Flooding and Debris Flows 

Surface water issues relating to stream channel 

morphology, erosion, streamflow, surface water quality, 

and wetlands are also considered significant to park 

management (Appendix C). The Water Resources 

Division of the NPS may be contacted for additional 

information regarding many of these surface water issues 

at Capitol Reef. 

Capitol Reef lies within a semi-arid climatic zone that 

experiences intense thunderstorms of short duration. 

Flash flooding may result from rapid runoff of surface 

water into narrow, steep canyons that cut into the 

Waterpocket Fold. Intense storms may also lead to 

flooding in the Fremont River and its tributaries. Because 

vegetation is sparse, flash floods carry a high sediment 

load and can become debris flows transporting 

downstream large quantities of unsorted sediment 

ranging in size from clay to boulders. Flash floods and 

debris flows are a potential hazard to hikers in these 

canyons as well as to roads, trails, structures, and other 

infrastructure that intersect the canyons and streams. 

Swelling Clays 

Clays that shrink and swell are composed primarily of 

smectites, clay minerals formed by the chemical 

alteration of glassy volcanic ash (bentonite) or by 

alteration of other silicates in contact with water. Clay 

minerals are arranged in layers, much like the pages of a 

book. These clays expand with the addition of water 

between these layers and shrink upon drying (Moore 

and Reynolds 1989). This shrink and swell characteristic 

results in surface instability impacting roads, buildings, 

and infrastructure. Formations that contain expandable 

clays and which may pose a potential problem in Capitol 

Reef include: the Blue Gate Shale Member and Tununk 

Member of the Cretaceous Mancos Shale, the Brushy 

Basin Member of the Jurassic Morrison Formation, and 

the Petrified Forest Member and Monitor Butte Member 

of the Triassic Chinle Formation. The abundance of 

smectite in the Morrison Formation suggests that large 

quantities of volcanic ash fell over the region during its 

deposition (Morris et al. 2000). 

Uranium and Radon Contamination 

Uranium exploration was allowed in Capitol Reef from 

1953 to 1956. Uranium bearing rocks have been mapped 

throughout the park although economic concentrations 

of uranium have not been discovered (Smith et al. 1963; 

Doelling and Tooker 1983). The principal host rocks for 

the radium, vanadium, and uranium deposits are fluvial 

deposits in Mesozoic rocks. The stratigraphic units at 

Capitol Reef that contain abnormal radioactivity include: 

the Moenkopi Formation, the Shinarump Member of the 

Chinle Formation, the middle and upper members of the 

Chinle Formation, and the Salt Wash Member of the 

Morrison Formation. The volcanic rocks a few miles 

west of the mapped area of figure 4 also contain 

abnormal radioactivity although the volcanic rocks 

inside the park do not (Smith et al. 1963). 

Details of any uranium and radon contamination in the 

park were not discussed during the scoping workshop. 

However, the United States Environmental Protection 

Agency (EPA) joined the NPS and the Utah Abandoned 

Mineral LandsProgram to study radioactive 

contamination at the Rainy Day and Duchess Mine sites 

in September 2002. EPA has compiled the data but has 

yet to complete a report of findings. There does not 

appear to be an environmental problem except for 

radioactive contamination in the immediate area of the 

sites (alpha and gamma radiation). Park visitors should 

be advised not to camp on the spoil piles from the 

abandoned mines or to drink the nearby water, which 

possibly has additional contaminants such as arsenic 

(Burghardt, Geologic Resources Division, personal 

communication, 2006). 

Rockfall and Landslides 

Potential rockfall and landslide hazards exist in 

Paleozoic and Mesozoic strata that form steep slopes and 

cliffs. Rockfalls may also occur in the Permian Cutler 

Group and Kaibab Limestone, although these strata are 

exposed only in deeply incised canyons along the 

western margin of the park. 

Rockfall and cliff collapse are potential hazards in the 

massive, cross-bedded sandstones of the Mesozoic 

strata. These same hazards are associated with the Lower 

Jurassic Navajo Sandstone and Wingate Sandstone, the 

Middle Jurassic Entrada Sandstone and Page Sandstone, 

and the Upper Cretaceous Ferron Sandstone Member 

and Emery Member of the Mancos Shale, and the 

Mesaverde Formation. Minor rockfall potential is 

present in some of the steep outcrops of the Triassic 

Moenkopi Formation, the Middle Jurassic Curtis 
 NPS Geologic Resources Division 8 

Formation, and the Lower Cretaceous Dakota 

Sandstone. 

The Red Slide is a geologic feature that formed in the 

Moenkopi Formation during the wetter climate of the 

Pleistocene Epoch. Underlain by more resistant 

sandstone beds of the Torrey Member, red mudstones of 

the Moody Canyon Member became unstable when 

saturated with water. Intense rainfall of long duration 

combined with intense erosion and debris flows could 

result in similar landslides today. At risk are roads, trails, 

and any structures or infrastructure that may be in the 

path of major downslope movement. 

Groundwater 

A well drilled in the Fremont River Gorge in 1993, about 

0.8 km (0.5 mi) west of the campground, provides the 

public water supply for Capitol Reef (Martin 1998). The 

well produces water from a 1.5-meter (5 ft) thick quartz 

sandstone aquifer in the Moenkopi Formation. The well 

produced 15,000 gallons per day during peak demand in 

the summer of 1998 (Martin 1998). There are no other 

water wells in the area; hence, the hydraulic gradient, 

groundwater flow direction, and effective porosity 

cannot be calculated accurately. Groundwater flow is 

presumed to follow the general northeast dip of bedding. 

No contaminant sources were identified within 

protection zones of 250-day, 3-year, and 15-year 

groundwater travel times to the well. Initial water quality 

studies found no connection between the river and the 

well, no presence of cryptosporidium (a parasitic 

protozoan), giardia, or microscopic particulates (Martin 

1998). However, water samples collected in 1993 and 

1996, exceeded the maximum contaminant levels (MCL) 

for both sulfate and total dissolved solids (TDS). The 

MCLs for sulfate and TDS are 250 mg/l and 500 mg/l, 

respectively. The Capitol Reef well contained 320 mg/l 

sulfate and 720 mg/l TDS. Sulfate and TDS are secondary 

(recommended) drinking water standards that do not 

require system compliance. 

In 1993, water sample analyses using a detection limit of 

0.001 mg/l for thallium did not detect any thallium in the 

well (Martin 1998). However, results from the 1996 

analysis reported 0.008 mg/l of thallium (Martin 1998). 

This high level is thought to reflect a lab error. Thallium 

is a primary drinking water standard with a MCL of 

0.002 mg/l. Sources for thallium include ore-processing 

sites and discharge from electronics, glass and 

pharmaceutical companies (EPA website www.epa.gov/ 

safewater/mcl.html, access April 2005). As of this report, 

the Water Resources Division does not have any more 

recent water quality data on the well (Larry Martin, 

Water Resources Division, NPS, personal 

communication 2006). 

Disturbed Lands 

According to John Burghardt (GRD), ten abandoned 

mine sites are recorded in the park, entailing 27 

individual mine openings. The Oyler, Terry, and Rainy 

Day abandoned mineral landsites have been fully 

mitigated by closing 20 openings. Seven openings remain 

at the other 7 sites. Some low-grade coal can be found in 

the Carmel Formation just east of the intersection of 

Notom Road and State Highway 24. A few small borrow 

pits may be present along the Burr Trail. 

Cattle grazing has disturbed the area around Oak Creek 

and Pleasant Creek. A preliminary disturbed lands map 

GIS layer for roads that the park wants closed, cattle 

ponds, dams, tanks, and other features is available to 

management (Tom Clark, Capitol Reef National Park, 

Natural Resources 1999). 

Paleontological Resources 

The Permian White Rim Sandstone (Cutler Group) crops 

out locally within the park and contains marine trace 

fossils of Thalassinoides and Chondrites. The fossiliferous 

Kaibab Limestone interfingers with the White Rim 

Sandstone and contains fragments of marine 

invertebrates such as bryozoans, brachiopods, 

gastropods, bivalves, and crinoids (Koch and Santucci 

2002). 

Brachiopods, gastropods, bivalves, and ammonites are 

found in the Sinbad Limestone Member of the Triassic 

Moenkopi Formation. The Moenkopi also contains 

fossil vertebrate tracks of Rotodactylus and swimming 

traces of Chirotherium (Mickelson 2004). Invertebrate 

fossil traces of Palaeophycus, and Diplidnites are reported 

from the Torrey Member of the Moenkopi Formation 

(Santucci et al. 1998). 

The Shinarump Member of the Triassic Chinle 

Formation contains abundant paleobotanical fossils such 

as Zamites powelli, Palissya sp., Sphenozamites sp., 

abundant stems of the fossil horsetails, Equisetites, 

Phlebopteris, Cyneopteris, Cladophlebis, Pagiophyllum, 

and Araucarioxylon (Koch and Santucci 2002). Leaves of 

the palm-like plant Sanmiguelia cf. S lewisi have been 

found in the Owl Rock Member of the Chinle 

Formation. Other fossils from the Chinle include 

tetrapod remains, lungfish toothplates and burrows, 

coprolites, marine snails, and bivalves. 

Dinosaur and tritylodont tracks are reported from the 

Lower Jurassic Kayenta Formation (Santucci et al. 1998). 

The Lower Jurassic Navajo Sandstone, primarily an 

eolian deposit, also contains algal mounds formed in 

interdunal playa deposits in Capitol Reef NP (Koch and 

Santucci 2002). 

The Middle Jurassic Carmel Formation preserves a small 

marine assemblage including Ostrea sp., Trigonia sp., 

Camptonectes sp., and the star-shaped columnals of the 

crinoid Pentacrinus asteriscus. Upper Jurassic dinosaur 

bones and petrified logs have been found in the Salt 

Wash Member of the Morrison Formation in and near 

Capitol Reef National Park. 

Turtle and dinosaur remains have been discovered in the 

Lower Cretaceous Cedar Mountain Formation just north 

of the park. The Oyster Reef is a geologic feature 

exposed along the Notom-Bullfrog road where thick 

accumulations of oyster shells, principally Pycnodonte sp. 
 CARE Geologic Resource Evaluation Report 9

and Exogyra (Costagyra) olisiponensis, can be seen in the 

Upper Cretaceous Dakota Sandstone. Marine fossils, 

including bivalves, gastropods, ammonites, and shark’s 

teeth, are found in the Tununk Shale Member and Blue 

Gate Member of the Mancos Shale. Vertebrate remains 

of turtles, crocodiles, and ceratopsian dinosaurs have 

been found in the Masuk Member of the Mancos Shale. 

The Late Paleocene or Early Eocene age Flagstaff 

Limestone contains charophytes (green algae), 

ostracods, bivalves, and gastropods that indicate a 

freshwater origin for the carbonate unit. 

Although theft and vandalism of fossils do not present a 

problem, the abundance, variety, and accessibility of 

fossils in Capitol Reef, make fossil poaching and fossil 

preservation potential issues for resource management. 

Mineral Occurrences 

Capitol Reef National Park has been closed to mineral 

entry including oil and gas since it was established as a 

National Monument in 1937, with the exception of a 

period from 1953 to 1955 when uranium exploration was 

allowed (Smith et al. 1963). Mineral occurrences in the 

area include uranium, vanadium, copper, manganese, 

gypsum, minor coal, building stone, sand and gravel, and 

oil and gas (figure 4) (Smith et al. 1963; Doelling and 

Tooker 1983). 

Uranium 

The presence of uranium in the Capitol Reef area has 

been known for many years and the presence of ten 

abandoned mineral land sites related to uranium mining 

attest to development of these uranium deposits (figure 

4). The monument was again closed to mineral entry 

after May 1955. The Oyler mine, established on the north 

side of Grand Wash in Capitol Reef, was located in 1901 

and is the oldest uranium-radium prospect in the Capitol 

Reef area. 

Uranium minerals in the Moenkopi Formation are not 

widespread in the park. Perhaps the only significant 

locality is 2.4 km (1.5 mi) northwest of Torrey (figure 4). 

Found in a massive sandstone channel about 10 meters 

(32 ft) thick and 122 m (400 ft) below the top of the 

formation, the uranium mineral, metazeunerite, is a 

green mineral associated with a black substance that is 

layered parallel to bedding and also found as black spots 

within the sandstone (Smith et al. 1963). 

Throughout the Colorado Plateau, uraniferous deposits 

are found in Shinarump sandstones that fill channels cut 

into the underlying Moenkopi Formation. More 

uranium minerals are found in the Shinarump Member 

of the Chinle Formation than any other stratigraphic unit 

in the Capitol Reef area. East of the Waterpocket Fold, 

the Shinarump forms a discontinuous, uranium-bearing 

unit from about 4 km (2.5 mi) northwest of Fruita, Utah, 

southeastward along the Waterpocket Fold to Oak Creek 

and North and South Coleman Canyons (figure 4). West 

of the Waterpocket Fold, where the Shinarump forms a 

more continuous deposit, uranium-bearing rocks are less 

abundant and found in lower concentrations compared 

to the discontinuous Shinarump in the Capitol Reef area 

(Smith et al. 1963). Nearly all the uranium minerals and 

radioactive material, and most copper minerals present 

in the abandoned Oyler mine, are found in an almost 

continuous tan and yellow clay layer at the base of the 

Shinarump (Smith et al. 1963). 

Radioactive material also occurs in the middle and upper 

members of the Chinle, but no large concentrations have 

been found in the Capitol Reef area (Smith et al. 1963). 

Most of the abnormal radioactivity is found in widely 

scattered fossil logs in South Coleman Canyon, just north 

of Oak Creek, east of Sand Creek, and northwest of 

Teasdale, Utah (figure 4). 

Other than in the Shinarump, channel deposits in the Salt 

Wash Conglomerate Member of the Morrison 

Formation appear to be the most favorable locations for 

uranium minerals. These deposits are generally 0.6 to 2 

meters (2 to 6 ft) long, 0.6 to 1 meters (2 to 3 ft) wide, 

5 to 15 cm (2 to 6 in) thick, and contain abundant 

carbonized plant fragments (Smith et al. 1963). The 

primary uranium mineral found in the Salt Wash 

Conglomerate is carnotite. 

Other Minerals 

Several old copper prospects are located on Miners 

Mountain (figure 4). Workings from these prospects 

have collapsed and are mostly inaccessible (Smith et al. 

1963). In the early part of the 20th century, “a few 

hundred pounds of high-grade ore is reported to have 

been shipped” from the Capitol Reef area, but Smith and 

others found no evidence of any further copper 

production when they visited the area in 1954 (Smith et 

al. 1963). Samples of uranium ore from the Shinarump 

Member of the Chinle Formation in the Capitol Reef 

area showed abnormal amounts of copper, lead, zinc, 

molybdenum, and arsenic along with uranium. The 

quantities of these metals, however, were of little 

economic value (Smith et al. 1963). 

A manganese deposit is located north of Spring Gulch on 

the east side of Boulder Mountain (figure 4). The 

manganese mineral is pyrolusite (MnO2) which forms 

cylindrical, pipe-like masses as much as 5 cm (2 in) in 

diameter. The manganese oxide holds the sand grains 

together in parts of the Carmel Formation. Iron oxide is 

associated with manganese in the sandstone. 

Gypsum, Building Stone, and Sand and Gravel Resources 

Non-metallic mineral resources also exist within the 

boundaries of Capitol Reef National Park. Glass 

Mountain is composed largely of gypsum (CaSO4o 

2H2O). Gypsum beds, up to 24 meters (80 ft) thick, are 

exposed in the Carmel Formation, particularly in the 

area of Black Ridge west of Teasdale (Smith et al. 1963). 

On the east side of the Waterpocket Fold, a north-south 

trending area of gypsum and anhydrite has been mapped 

that extends to the north and south of the park (Doelling 

1983). 

The sandstone beds in the Moenkopi Formation have 

been quarried and used for buildings in the local 
 NPS Geologic Resources Division 10 

communities and for the Capitol Reef headquarters 

building near Fruita (Smith, et al. 1963). These finegrained sandstone beds split easily along bedding planes 

to make flat and relatively uniform building stone. 

Pediment gravels and terrace gravels along the Fremont 

River have been used for aggregate and general 

construction activities. 

Oil & Gas 

The potential for oil and gas reservoirs in both structural 

and stratigraphic traps in the Capitol Reef area is 

unknown. The Teasdale, Fruita, and Thousand Lake 

anticlines are structures with the potential to trap 

hydrocarbons (figure 5A) (Smith et al. 1963). 

The youngest formation to yield oil and gas in the area is 

the Moenkopi Formation, and Moenkopi traps may be 

present in both the Fruita and Thousand Lake anticlines. 

On the Teasdale anticline, however, erosion has exposed 

the beds of the Moenkopi to the surface so that any oil 

has been biodegraded and any gas has escaped to the 

atmosphere. All three structures have the potential for 

yielding oil and gas from older formations such as the 

Permian White Rim Sandstone or the Pennsylvanian 

Paradox Formation. 

As of 1963, only the Teasdale anticline had been tested 

for hydrocarbons (Smith et al. 1963). Three wells were 

drilled in the vicinity of the Teasdale anticline, but only 

one was located on the structure. The Pacific Western 

Oil Corp. Teasdale 1, drilled in 1949, reached a total 

depth of 1503 meters (4932 ft) in Cambrian-aged 

limestone. Oil-stained beds were found in the Permian 

Coconino Sandstone (called the Cedar Mesa Sandstone 

in other areas of the Colorado Plateau) and in the upper 

part of the Pennsylvanian Hermosa Limestone (Smith et 

al. 1963). In 1950, the Parry Oil Company Teasdale 1 was 

drilled to a depth of 159 m (523 ft). No hydrocarbons 

were discovered. Another dry hole was drilled by Smith 

and others (1963) during fieldwork in 1953-54, no 

information is available for this hole. 

By 1963, six wells had been drilled about 8 km (5 mi) 

northeast of the Capitol Reef area on an anticline having 

180 meters (600 ft) of trap closure. Gas was produced 

from five of these wells from the Sinbad Limestone 

Member of the Moenkopi Formation and from a 

sandstone bed above the Sinbad in the Torrey (?) 

Member of the Moenkopi (Smith et al. 1963). The daily 

gas production in four of the wells ranged from 1 million 

to 21 million cubic feet of gas per day. 

Increased interest in the exploration and development of 

oil and gas resources in the State of Utah has resulted in 

the Bureau of Land Management offering numerous oil 

and gas leases for competitive bid directly north and 

northeast of Capitol Reef National Park. The Bureau of 

Land Management has placed several protective 

stipulations on these leases to help protect the park’s air, 

water, visual, wildlife, vegetation, and soundscape 

resources. Although the various tracts were successfully 

bid upon, limited exploratory drilling has not resulted in 

any producing wells near the park. 

Capitol Reef National Park is closed to leasing, however, 

approximately one square mile of the park is 

encumbered by the Viking oil and gas lease. The Viking 

lease is a valid existing right that predates the park. The 

owner of the Viking lease continues to propose 

development of his lease holdings, but no action has 

taken place to date. 

In the early 1980’s and again in 2006, Utah’s tar sand 

resources were considered for federal leasing. While the 

park is closed to tar sand leasing, such leasing and 

development adjacent to the park could take place if the 

technological and economic conditions were right. Areas 

adjacent to the park considered for tar sand leasing will 

be identified by the 2006-2007 programmatic 

environmental impact statement that is currently being 

prepared by the Bureau of Land Management. 

Seismicity 

Seismicity on the Colorado Plateau is relatively low both 

in number and magnitude. Diffusely distributed 

earthquakes have small to moderate magnitudes 

(Humphrey and Wong 1983). From December 1978 to 

January 1980, a spatially and temporally isolated swarm 

of at least 38 earthquakes, with magnitudes ranging from 

1.0 to 3.6, occurred near Capitol Reef National Park. 

This was the highest level of natural seismicity 

historically observed within the interior of the Colorado 

Plateau (Humphrey and Wong 1983). 

The earthquakes occurred in a structurally complex area 

where the Waterpocket Fold meets the Caineville 

monocline just west of Henry Mountains. The location 

suggests a possible association with basement faults 

generated by the Cretaceous-Tertiary Laramide 

Orogeny, which controlled the development of both the 

fold and monocline. The earthquakes may represent an 

occurrence of Basin-and-Range extensional tectonism 

along a reactivated Laramide structure within the 

transition zone between the Basin-and-Range and 

Colorado Plateau physiographic provinces (Humphrey 

and Wong 1983). The potential for a major earthquake 

with a magnitude greater than 5.5 is considered very low 

in the Capitol Reef area. 
 CARE Geologic Resource Evaluation Report 11

Figure 4. Mineral and abnormal-radioactivity map of the Capitol Reef area. Modified from Smith and others (1963). 
 NPS Geologic Resources Division 12 

Figure 5. Schematic diagrams illustrating common types of hydrocarbon traps (gas is omitted except in “a”). 
 CARE Geologic Resource Evaluation Report 13

Geologic Features and Processes 

This section describes the most prominent and distinctive geologic features and processes 

in Capitol Reef National Park. 

Waterpocket Fold 

The Waterpocket Fold is one of the longest continuously 

exposed monoclines in the world and is the centerpiece 

geologic structure of Capitol Reef (figure 3) (Morris et al. 

2000). The Waterpocket Fold monocline stretches for 

almost 161 km (100 mi), from the Colorado River south 

of the Henry Mountains, along the east side of the Circle 

Cliffs, northward to the north end of Thousand Lake 

Mountain. The general trend of the Waterpocket Fold is 

northwest-southeast. Between Oak Creek and the 

Fremont River, the fold trends approximately N 25o W, 

but north of the Fremont River the fold trends more 

westward to N 50o W (figure 3). 

The rock layers on the western limb of the fold are more 

than 2,100 m (7,000 ft) higher than the rock layers on the 

east. From the crest of the fold, the High Plateaus Section 

of the Colorado Plateau extends westward. To the east 

lies the desolate beauty of the Canyon Lands Section. 

Water is a powerful erosive agent, especially in a desert 

environment with scarce vegetation. Over time, water 

has carved catchments for surface runoff in the uplifted 

and tilted sandstone layers of the Waterpocket Fold. 

These small basins, also known as water pockets, are 

common throughout the fold and give this feature its 

name. 

Within the park, the sedimentary beds on the western 

limb of the fold dip generally to the east and northeast 

about 10o to almost 35o (Smith et al. 1963; Billingsley et 

al. 1987). East of the near vertical fold of the monocline, 

the dips are gentler and appear to be more consistent, 

ranging from 4o - 7o (Billingsley et al. 1987). Local bends 

or kinks in the fold alter the northwest trend of the beds 

along the monocline. One prominent bend occurs just 

north of Fruita, Utah, and another is just north of Oak 

Creek (figure 3). Bends or kinks in the Waterpocket Fold 

may represent offset along a reverse fault within the 

subsurface Precambrian section of rocks. 

The geologic processes that form many of the 

exceptional landforms of the desert southwest are 

evident throughout Capitol Reef National Park. The 

features below can be seen along the Cathedral Valley 

Loop, Highway 24, the Notom-Bullfrog Road, and 

throughout the park. 

Teasdale Anticline 

The Teasdale anticline extends at an angle of 

approximately 20o - 30o from the Waterpocket Fold 

(figure 3). The general northwest trend of the Teasdale 

Anticline is N 55o W but changes to N 75o W north of 

Grover, Utah (near Torrey). If the surface expression of 

the Teasdale anticline is projected to the southeast, the 

fold will intersect the Waterpocket Fold at the Oak 

Creek bend. Both the northwestward and southeastward 

hinge line extensions of this anticline disappear, or 

plunge, below the surface, making the Teasdale anticline 

a doubly plunging anticline. The Teasdale anticline is an 

asymmetric anticline with dips ranging from 20o - 50o SW 

on the southwest limb and from 10o - 14o NE on the 

northeast limb (figure 3). Major uplifts on the Colorado 

Plateau such as the Circle Cliffs and the San Rafael Swell 

are also asymmetric, but unlike the Teasdale anticline, 

their steeper limbs are on the east side of the fold (Smith 

et al. 1963). 

Teasdale Fault 

The Teasdale fault lies southwest of the Teasdale 

anticline and follows a similar trend of N 60o W except 

south of Pleasant Creek where the trend is about N 70o 

W (figure 3). The southwest side of this high-angle to 

vertical normal fault has dropped as much as 335 m 

(1,100 ft) relative to northeast side (Smith et al. 1963). 

The Teasdale fault is a 40- km (25- mi) long fault zone 

composed of two dominant faults and many small 

branching faults and cross faults. The fault crosses the 

southeastern nose of the Teasdale anticline and splays 

into several eastward-trending faults at its southeastern 

end. These faults extend for about 6 km (3.7 mi) into the 

Waterpocket Fold (figure 3). The north sides of these 

shorter, normal faults have dropped down relative to 

their south sides. Several east-west trending faults also 

extend for about 5.6 km (3.5 mi) into the Waterpocket 

Fold from east of the Teasdale anticline (figure 3). These 

smaller faults also have their north sides downthrown. 

Maximum vertical displacement is about 30 m (100 ft). 

Sedimentary strata within or adjacent to the fault zone 

dip from 20o SW to vertical with some overturned beds 

dipping 75o NE (figure 3) (Smith et al. 1963). On the 

downthrown side near the Teasdale fault, beds 

consistently dip at high angles, flattening to almost 

horizontal less than 0.8 km (0.5 mi) from the fault. 

Thousand Lake Fault 

Dutton recognized and named the Thousand Lake fault 

in 1880. This normal fault zone west of the park 

boundary, begins east of Fremont, Utah, and trends 

southward for over 32 km (20 mi) becoming 

unrecognizable along the western edge of Boulder 

Mountain (figure 3) (Smith et al. 1963). The fault zone 

may continue to the northeast, north of the park 

boundary, as the Paradise fault. 

The western block of the Thousand Lake fault has 

dropped relative to the eastern block. Total displacement 

along the fault is about 762 m (2,500 ft) (Smith et al. 

1963). Displacement along the fault can be calculated by 

measuring the difference in elevation between volcanic 
 NPS Geologic Resources Division 14 

layers on Thousand Lake Mountain and the area west of 

the mountain. 

Other Folds and Faults 

Other folds in the region include the Fruita Anticline, the 

Circle Cliffs Upwarp, the Thousand Lake Anticline, and 

the Saleratus Creek Syncline (Smith et al. 1963; 

Billingsley et al. 1987; Morris et al. 2000). The 

asymmetric Fruita Anticline and the Saleratus Creek 

Syncline have geomorphic trends similar to the 

Waterpocket Fold (figure 3). The Circle Cliffs Upwarp 

and the Thousand Lake Anticline lie south and west of 

the park boundary, respectively, although the east limb 

of the Thousand Lake Anticline is part of the 

Waterpocket Fold. 

Beginning just north of Fruita, Utah, a zone of normal 

faults trends approximately N 70°-80o W and extends for 

about 24 km (15 mi) (figure 3)(Smith et al. 1963). Most of 

the faults are downthrown to the north. The maximum 

length of a single fault is only about 10 km (6 mi). Smith 

and others (1987) measured a maximum displacement 

along the faults of 110 m (360 ft), but found that most of 

the fault movement is less than 30 m (100 ft). 

Also present in the Capitol Reef area are faults that are 

not as concentrated or pronounced as those discussed 

above. Near Fremont, Utah, several high-angle normal 

faults trend chiefly northeastward with west sides 

downthrown. West of Boulder Mountain, northeasttrending high-angle normal faults cross an area of 

volcanic rocks (figure 3). The Y-shaped fault southwest 

of Fruita, Utah, is on the north side of Miners Mountain. 

The maximum displacement on this fault is 53 m (174 ft) 

measured near the split in its trace. Reverse faults cut the 

Moenkopi Formation on the flanks of the Teasdale 

anticline (Smith et al. 1963). These reverse faults have 

maximum displacements of 3 m (10 ft) and are too small 

to be shown on the geologic map. 

Joints 

Numerous vertical joints are also present in Capitol Reef 

NP. Joints, like faults, are semi-planar breaks in the rock, 

but unlike faults, there is relatively little displacement 

along a joint. The most prominent joints are along the 

Waterpocket Fold. South of latitude 38o 13’ N (near the 

border of Wayne and Garfield counties) the joints trend 

from about N 15o W to N20o W. North of this latitude, 

their trends change to N 15o E - N 15o W with many of 

these joints trending almost due north. 

Prominent cross joints trending N 50o - 80o W also cut 

through the Waterpocket Fold at three locations along 

warps in the fold. One is found in the synclinal trough 

along Oak Creek south of the southeast extension of the 

Teasdale anticline as it projects into the Waterpocket 

Fold. A second is in the synclinal trough north of Fruita 

and on the south side of the southeast extension of the 

Fruita anticline as it projects into the fold. The third area 

of cross joints is in the area of Deep Creek east of 

Thousand Lake Mountain (Smith et al. 1987). 

Dikes and Sills 

The dikes and sills in Capitol Reef NP have been 

interpreted as part of a larger basaltic dike complex that 

extends out of the park to the north and into the San 

Rafael Swell. Resistant dark gray igneous dikes intrude 

into Entrada sandstones just north of the Gypsum 

Sinkhole. Tabular sills parallel to sedimentary bedding 

can be found in Cathedral Valley and on the steep westfacing hillsides adjacent to the road just a few miles to the 

east of the Gypsum Sinkhole turnoff. These are some of 

the best exposed tabular sills in the world. A brecciafilled volcanic pipe (diatreme) is exposed at the Upper 

South Desert Overlook, emplaced into (generally) flatlying sedimentary rock by a gaseous explosion. 

Quaternary Features 

Pleistocene and Holocene features in the park include 

pediment deposits (deposits on a gently inclined surface 

eroded into bedrock), glacial till, outwash gravel, terrace 

gravel, colluvial deposits, landslide deposits, eolian 

deposits, and alluvium and alluvial fan deposits. 

Pediment deposits of volcanic boulders, cobbles, sand 

and gravel occur on gently sloping surfaces several 

hundred feet above adjacent streams and valleys as well 

as on some flat-topped hills and benches in Capitol Reef 

(Billingsley et al. 1987). The volcanic boulders are round 

to oblong and average 0.9 to 1.5 m (3 to 5 ft) in the long 

direction with some reaching more than 4.5 m (15 ft) in 

length. Lenticular beds of gravel are generally between 6 

to 15 m (20 to 50 ft) thick. Many of the exposed boulders 

have grooved or fluted top surfaces indicative of sand 

blasting caused by prevailing southwest winds. 

Boulder deposits, distinct from the boulders found in the 

pediment gravels, have been mapped near the mouths of 

Fish and Carcass Creeks and near Browns Reservoir and 

Tantalus Flats along Pleasant Creek (Smith et al. 1963; 

Billingsley et al. 1987). Caliche, a near surface crust of 

crystallized calcite commonly found in desert soils, coats 

many of the boulders. The thickness of the caliche varies 

with altitude. Caliche at 2,100 m (7,000 ft) averages 0.6 

cm (0.25 in) thick while caliche at 2,400 m (8,000 ft) is 

only a thin coating. The advanced dissection of the 

boulder deposits indicates that the boulders are 

erosional remnants of deposits whose original 

topographic forms have been destroyed. 

Glacial till, outwash gravel, terrace gravel, and landslide 

deposits near the west boundary of Capitol Reef are 

associated with an ice cap that formed on Boulder 

Mountain. Moraines composed of till and some outwash 

gravels form a landscape of ridges, irregular knobs, and 

kettles. Remnants of glacial moraines may be found 

along Donkey, Fish, Carcass, Pleasant, Oak, East 

Boulder, West Boulder, and Miller Creeks (Smith et al. 

1963). 

Terrace gravels and sands along the Fremont River and 

its tributaries rest on erosional surfaces cut in the 

bedrock that are elevated above the present floodplain. 

The distance from the terrace to the river increases 

downstream. At the mouth of Carcass Creek, west of 
 CARE Geologic Resource Evaluation Report 15

Fruita, for example, the terrace is about 46 m (150 ft) 

above the Fremont River while Johnson Mesa, a large 

terrace remnant at Fruita, is about 76 m (250 ft) above the 

river. The terrace deposits range in thickness from less 

than 6 to more than 12 m (20 to 40 ft) and contain a few 

rounded volcanic boulders and pebbles from Boulder 

Mountain, chert and quartzite from the Salt Wash 

Member of the Morrison Formation or from the 

Flagstaff Limestone, and limestone clasts probably from 

the Carmel Formation. 

Alluvial fan deposits form fan-shaped aprons of poorly 

sorted silt, sand, pebbles, cobbles, and boulders at the 

mouth of canyons. Alluvial fans are convex topographic 

features with a main stream channel providing sediment 

from the mouth of the canyon to the fan. The stream 

channel, however, is difficult to define across the fan as 

its channel morphology changes as in-channel sediment 

is deposited, choking the stream and modifying its slope 

so that the channel shifts to a new location on the fan. 

Grand Wash, Capitol Wash, Pleasant Creek, Sheets 

Gulch, and Oak Creek flow in precipitous gorges being 

eroded into the Waterpocket Fold. A dirt road 

connecting Fruita to Hanksville, Utah, extends through 

the narrow gorge of Capitol Wash, a gorge that is typical 

of all the gorges crossing the fold. Cliffs of Navajo 

Sandstone tower hundreds of feet above the road and at 

its narrowest point, Capitol Wash is only 7.6 m (25 ft) 

wide at road level. 

Tour of Park Features 

Cathedral Valley Loop 

Cathedrals and Monoliths of Cathedral Valley 

Accessible only by high clearance or four-wheel drive 

vehicles, Cathedral Valley is located in the northern 

portion of the park where bedrock dips about 3o- 5o to 

the northeast. Erosion of the red-orange mudstone, 

siltstone, and fine-grained sandstone of the Entrada 

Sandstone formed the valley and sculpted numerous 

freestanding masses of rock (monoliths) (Morris et al. 

2000). Temple of the Sun, Temple of the Moon (figure 6), 

and erosional features in the Upper Cathedral Valley 

(figure 7) are outstanding examples of monoliths that 

resemble cathedrals or temples rising from the valley 

floor. 

Occasionally, the more resistant gray-green sandstones 

of the Curtis Formation cap the monoliths in the park. 

Closely spaced rock towers, the precursors to monoliths, 

are found at a number of places along the southwest wall 

of the valley. Headward erosion by streams and rivers 

resulting in downcutting and slope retreat will, in time, 

strand these towers and create monoliths (Morris et al. 

2000). 

The Entrada and Curtis were once buried and when the 

overlying strata were removed by erosion, the release of 

the overlying pressure produced fractures and joints in 

the rock. Fractures and joints expose more surface area 

and accelerate weathering and erosion. Once water 

penetrates along the fractures, mechanical and chemical 

weathering begin to erode the fractured rock. The 

fractures expand, the rock crumbles, and the less 

fractured more resistant rock is left free-standing. Where 

the resistant Curtis Formation directly overlies the 

Entrada, it forms a resistant cap rock protecting the 

underlying strata from further erosion. 

Glass Mountain and Gypsum Sinkhole 

Fractures may be filled with evaporite (salt) deposits that 

may flow upward from underlying strata forming a salt 

diapir. A diapir is a dome or bulge that forms when 

plastic, lower density rock layers (as salt) are squeezed 

upward through denser, more resistant sedimentary 

rock. When seawater evaporated during Carmel 

Formation time, approximately 165 million years ago, a 

thick gypsum layer formed. At increased pressures and 

temperatures various salts as well as gypsum will flow as 

a viscous fluid under conditions in which other 

sedimentary rocks would deform in a brittle fashion. As 

sedimentation buried the gypsum, it began to plastically 

deform and to flow upward. Where the gypsum 

encountered areas of lower pressure, perhaps created by 

faults and fractures in the overlying rock column, the 

gypsum formed small domes or plugs in the overlying 

Entrada Sandstone. Glass Mountain is a surface 

expression of one of these plugs. Rising more than 3 m 

(10 ft) above the valley floor, Glass Mountain (figure 6) is 

composed of selenite, a clear, colorless variety of gypsum 

(Morris et al. 2000). 

Although gypsum is somewhat soluble, Glass Mountain 

remains exposed at the surface because of the dry 

climate. Gypsum Sinkhole, located approximately 11 km 

(7 mi) to the northwest of Glass Mountain, was likely 

created by the dissolution of another gypsum plug, 

possibly when the climate was wetter (Morris et al. 2000). 

Volcanic Features 

Igneous dikes exposed just north of the Gypsum 

Sinkhole are examples of differential erosion. Dikes are 

tabular igneous rock bodies that intrude at angles into 

sedimentary strata. The dark gray igneous dikes of 

Capitol Reef National Park are more resistant to erosion 

than the relatively soft red-orange sandstones of the 

Entrada. Dikes are often exposed above the surrounding 

sedimentary strata that have eroded around them. 

Dikes are often associated with igneous sills, tabular 

sheet-like bodies that intrude parallel to bedding planes. 

Capitol Reef contains exceptional exposures of sills on 

steep west-facing hillsides adjacent to the road just a few 

miles to the east of the Gypsum Sinkhole turnoff (Morris 

et al. 2000). 

A diatreme, a breccia-filled volcanic vent or pipe, is 

exposed adjacent to the walking path on a west-facing 

pillar of rock at the Upper South Desert Overlook. The 

diamond-bearing kimberlite pipes of South Africa are 

probably the most well-known diatremes in the world.
 NPS Geologic Resources Division 16 

Bentonite Hills 

To the east of North Blue Flats, just outside Capitol Reef, 

the Brushy Basin Member of the Morrison Formation 

has eroded into barren, color-banded, rounded hills or 

badlands. Vegetation is scarce in the area and the surface 

of the hills has a “popcorn” texture from the bentonitic 

clay. The hills are best viewed approximately 14 km (9 

mi) north of the River Ford (Fremont River crossing). 

Exposures of Morrison Formation in the park are 

located north of Highway 24. 

The Morrison Formation is world-renowned for its 

abundant and diverse Jurassic-age dinosaurs, and 

dinosaur bones in this formation can be seen in and 

around the park. At Bentonite Hills, a number of large 

petrified logs have also been found. The petrified logs 

and dinosaur bones indicate that a lush, humid, tropical 

climate probably existed in the Capitol Reef area during 

Morrison time. Research in the Morrison Formation at 

Dry Mesa Dinosaur Quarry, located 400 km (250 mi) east 

of Capitol Reef in western Colorado, suggests that major 

climate shifts occurred in the Jurassic so that the 

normally humid, wet conditions were interrupted by 

large-scale, cataclysmic drought (Richmond and Morris 

1998). The drought caused dinosaurs to gather at 

shrinking watering holes where they died, creating 

concentrated accumulations of bones such as those at 

Dry Mesa Dinosaur Quarry. 

Highway 24: west to east transect 

“The Goosenecks” at Sulfur Creek 

The Goosenecks of Sulfur Creek are classic examples of 

a superposed meandering stream (Morris et al. 2000). 

Rivers often follow the structural trend of a region, but at 

Capitol Reef, the rivers cut through (i.e., are superposed 

on) the structural features as if folding, faulting, and rock 

hardness did not influence the path of the river’s 

channel. 

The meandering river pattern at Capitol Reef originally 

developed on a relatively flat topographic surface during 

Paleocene-Eocene time, about 66 to 38 million years ago. 

About 20 million years ago, the Colorado Plateau began 

uplifting (Morris et al. 2000). The meandering rivers 

either cut into the underlying sediment and flat-lying 

rocks faster than the rocks were uplifted or the river had 

already entrenched its channel by the time uplift began. 

The river began cutting the channel vertically downward 

rather than laterally across its floodplain. Once the 

stream eroded through the flat-lying rocks, it cut into the 

underlying folded strata. In this way, the meandering 

pattern was superposed on the underlying folded rocks 

and today cuts across the structural trend rather than 

being influenced by the geologic structure. 

Permian age rocks that are part of the 250 to 290 millionyear-old Cutler Group, some of the oldest rocks at 

Capitol Reef, are exposed on the canyon floor at the 

Goosenecks. Massive exposures of the Permian Kaibab 

Limestone, as well as the Black Dragon Member, the 

Sinbad Limestone Member, the Torrey Member, and the 

Moody Canyon Member of the Triassic Moenkopi 

Formation overlie sandstones of the Cutler Group. 

Visitor Center: “The Castle” 

The “Castle” (figure 8), seen from the Visitor Center 

parking lot, is a geomorphic feature resulting from 

tectonism and erosion. The vertical fractures in the wellindurated eolian (wind blown), Jurassic-age Wingate 

Sandstone developed during uplift of the Colorado 

Plateau (Morris et al. 2000). The fractures on the walls of 

the “Castle” have been enlarged over the years due to ice 

wedging and dissolution. Ice wedging is the mechanical 

process wherein water trapped in a fracture (or pore 

space) freezes, expands, applying pressure on the 

surrounding matrix, and loosens the bonds holding 

grains together. When the water melts, the loosened 

grains are washed away. 

The Visitor Center and campground area lie on the 

contact between the Moenkopi and Chinle Formations. 

The area is relatively flat because of differential erosion 

between the two formations. The mudstone and siltstone 

beds of the Chinle erode more easily than the underlying 

siltstone and sandstone of the Moenkopi. Consequently, 

the variegated colored beds of the Chinle Formation 

retreated northwestward off the Moenkopi, creating a 

relatively flat surface. 

Arches and Bridges 

Arches National Park is best known for its extraordinary 

arches, but Capitol Reef National Park also has a number 

of natural arches and bridges. Hickman Bridge, Brimhall 

Double Bridge, and Saddle Arch (near Upper Muley 

Twist Canyon) are examples of these unique features. 

Differential erosion, fractures, and groundwater 

contribute to the formation of bridges and arches. 

Capitol Dome and Navajo Dome 

Capitol Dome and Navajo Dome, two of the more 

spectacular and easily observed domes in the park, were 

formed by a number of processes including headward 

erosion, downcutting, slope retreat, and weathering 

operating on cross-bedded sandstone. The two domes 

can be viewed from a number of places along Highway 

24 between the Hickman Bridge turnout (mile marker 

81.8) and Grand Wash (Morris et al. 2000). The 

numerous rounded “domes” of rock are typical of the 

weathering pattern of eolian, cross-bedded Navajo 

Sandstone. 

Cavernous Weathering 

A latticework of small pockets in the sandstone walls 

called stone lace or honeycomb weathering can be seen 

along the base of sandstone faces throughout the park 

and along Highway 24 (figure 9). The small pockets may 

enlarge to form larger caverns or alcoves. The pockets 

are irregularly oblong to hemispherical in shape with 

some individual pockets reaching depths as much as two 

to three times the opening diameter. The pockets may 

branch internally to form several chambers. 
 CARE Geologic Resource Evaluation Report 17

Caverns are the result of both chemical and mechanical 

weathering (Morris et al. 2000). Mineral grains are 

loosened due to hydration and dehydration enlarging the 

hollows and recesses (Mustoe 1983). In areas where the 

sandstone is not protected by a surface coating of desert 

varnish, this process accelerates formation of pockets 

and caverns. These areas are frequently found in dark 

slot canyons and at the bases of sandstone cliff faces 

where the sandstone can absorb salt from underlying 

formations, thus making the rock even more susceptible 

to cavernous weathering. These chemical and 

mechanical processes, however, are not evenly 

distributed in the rock and so some parts of the rocks 

erode, creating caverns, while others do not. 

Slot Canyons 

Most of the narrow, steep-walled slot canyons in Capitol 

Reef are cut into the thick Navajo Sandstone along the 

Waterpocket Fold. When the Waterpocket Fold was 

uplifted and the overlying flat-layered rocks eroded 

away, the dipping strata of the Waterpocket Fold allowed 

water to run off rapidly. The erosive energy of the water 

was focused along fractures that widened into a myriad 

of steep-walled canyons (Morris et al. 2000). Some wellknown slot canyons in the park include Spring Canyon, 

Grand Wash, Upper and Lower Muley Twist Canyons, 

and Halls Creek Narrows. 

Soft-Sediment Deformation 

Soft-sediment (or contemporaneous) deformation 

occurs in semi-consolidated sediment that is deformed 

prior to lithification. Outcrops of the Navajo Sandstone 

that contain soft-sediment deformation can be observed 

between mile marker 86.2 and 87 on Highway 24 (Morris 

et al. 2000). Often, soft-sediment deformation occurs in 

water saturated sediment due to changes in groundwater 

dynamics, or by seismic activity. 

Contorted or convolute bedding is a type of softsediment deformation in which highly contorted laminae 

are bounded above and below by parallel undisturbed 

layers. These contorted laminae may form recumbent 

folds (folds that roll over on themselves) or flower (also 

called “pop-up”) structures that look like a flower on a 

stem. Both of these features can be seen on the southeast 

vertical wall at mile marker 86.2 (figure 12 in Morris et al. 

2000). The structures suggest that semi-cohesive lamina 

sets moved downward and laterally along a depositional 

slope. There also appears to be a basal surface on which 

the contorted lamina sets detached and slid (Morris et al. 

2000). The detachment surface is largely composed of 

silt- and clay-sized particles that are finer-grained than 

the host sandstone. 

Approximately 2.4 km (1.5 mi) up the canyon from the 

confluence of Spring Canyon and the Fremont River is 

another example of large-scale soft-sediment 

deformation. About one third of the way up the west wall 

of the canyon is a distinctive curl within the Navajo 

Sandstone that Morris and others (2000) have termed 

“The Elf’s Toe” (figure 13 in Morris et al. 2000). 

Downslope movement (landslide-like movement) when 

the sand was cohesive, but not lithified, caused this 

feature. Closer to the canyon floor on the same wall is 

another soft-sediment feature termed the “Sea Lion” 

(Morris et al. 2000). 

Unconformities 

At Capitol Reef, numerous unconformities, representing 

substantial breaks or gaps in the geologic record, 

separate the sedimentary strata. Unconformities reflect 

periods of time when no sedimentation occurred and/or 

substantial erosion took place. If strata underlying the 

unconformity are tilted at an angle from the horizontal, 

then some tectonic event must have occurred to disturb 

the originally horizontal strata. Following tilting, erosion 

then leveled the plain to form an angular unconformity 

between the tilted strata and subsequent horizontally 

deposited sediments. 

A particularly striking angular unconformity is found at 

mile marker 87.5 along Highway 24 (figure 14 in Morris 

et al. 2000) where gently dipping beds of Quaternary 

deposits of basalt-rich alluvium (black cobble and gravel) 

overlie the more steeply dipping Carmel Formation and 

Entrada Sandstone (Morris et al. 2000). More than 100 

million years of Earth history is missing between the 

Mesozoic strata and the Quaternary deposits in this area. 

Notom-Bullfrog Road 

Oyster Reef 

As a sea inundated the Capitol Reef area during the Late 

Cretaceous, brackish marine environments supported an 

abundance of oysters (Morris et al. 2000). The shells of 

these oysters were concentrated in high-energy 

environments such as beaches preserved in the Dakota 

Sandstone. Thick accumulations of oyster shells can now 

be seen just a few yards east of the road approximately 39 

km (24 mi) from the Highway 24 turnoff. 

Strike Valleys 

When tilted sedimentary rocks differentially erode, the 

harder, more resistant strata develop into ridges, 

sometimes referred to as hogbacks, while the less 

resistant strata form valleys that parallel the strike 

orientation of bedding. The strike is the direction 

measured on a compass that is perpendicular to the dip 

of the inclined strata. Roads are often constructed in 

strike valleys, and the Notom-Bullfrog Road follows a 

strike valley of upper Jurassic and Cretaceous age rocks 

(figure 6 in Morris et al. 2000). The road trends northsouth and parallels the length of the Waterpocket Fold 

on its east side. The Strike Valley Overlook offers the 

best view of the park’s strike valleys. 

A number of geologic features can be observed at Halls 

Creek Overlook, located approximately 79 km (49 mi) 

from Highway 24 on the Notom-Bullfrog Road. Strike 

valleys offer a stunning view to the north. Brimhall 

Double Bridge lies to the west. The Circle Cliffs, a cross 

section of the Waterpocket Fold, can be seen to the 

southwest. Erosion of the Glen Canyon Group exposes 

variegated redbeds of the Moenkopi and Chinle at the 

crest of the fold (Morris et al. 2000). 
 NPS Geologic Resources Division 18 

Landslides 

The fine-grained redbeds of the Moenkopi Formation 

were unstable during the wetter climatic conditions 

earlier in the Quaternary. With increased precipitation, 

the mudstones and siltstones became saturated with 

water, reducing the friction between the layers of rock. 

The unstable red mudstones of the Moody Canyon 

Member of the Moenkopi slid down slope under the 

force of gravity. The more sand-rich beds of the 

underlying Torrey Member were more coherent than the 

Moody Canyon and thus acted as a detachment surface 

allowing downslope movement of the Moody Canyon 

(Morris et al. 2000). The mudflow spilled out of the 

higher ridges of the Waterpocket Fold into the Entrada 

strike valley forming the Red Slide that can be seen to the 

south (Morris et al. 2000). 
 CARE Geologic Resource Evaluation Report 19

Figure 6. View to the south of Glass Mountain (foreground), Temple of the Sun, and Temple of the Moon. Large selenite crystals pushed 

upward as a plug or diapir from the underlying Carmel Formation to form Glass Mountain. Temples of the Sun and Moon are monoliths 

within the Entrada Sandstone. Photograph from Morris and others (2000). 

Figure 7. Upper Cathedral Valley looking to the northwest. The Jurassic Curtis Formation (Jcs) forms the light gray caprock on the 

monoliths in the valley center (left edge of photo). Overlying the Curtis are the red mudstone, siltstone, and sandstone of the Jurassic 

Summerville Formation (Js). The light-colored sandstones of the Salt Wash Member of the Morrison Formation (Jms) are on the skyline, 

overlying the Summerville strata. Je: Entrada Sandstone. Photograph from Morris and others (2000). 
 NPS Geologic Resources Division 20 

Figure 8. The red rock at the lower part of this photograph of “the Castle” from the Visitors Center parking lot is the Moody Canyon Member 

of the Triassic Moenkopi Formation (Trm). The Shinarump Conglomerate that normally overlies the Moody Canyon is absent at this locality. 

Above the Moody Canyon are the gray and purple beds of the Monitor Butte Member of the Chinle, the slope-forming red siltstone and 

sandstone of the Petrified Forest Member with the resistant “Capitol Reef bed” capping this member (ledge in the middle f the slope). The 

Owl Creek Member of the Chinle Formation (Trc) comprises the upper slope of mudstone, siltstone, and fine sandstone. “The Castle” is 

fractured Jurassic Wingate Sandstone (Jw). The Jurassic Kayenta Formation (Jk) caps the Wingate on the skyline. Photograph from Morris 

and others (2000). 

Figure 9. Stone lace or Honeycomb weathering in large-scale, high-angle trough cross-stratified dune sets of the Jurassic Navajo Sandstone 

in Spring Canyon. View is to the south. Location is approximately 0.8 km (0.5 mi) up-canyon from the confluence of Spring Canyon and the 

Fremont River. Person for scale. Photograph from Morris and others (2000). 
 CARE Geologic Resource Evaluation Report 21

Map Unit Properties 

This section provides a description for and identifies many characteristics of the map 

units that appear on the digital geologic map of Capitol Reef National Park. The table is 

highly generalized and is provided for informational purposes only. Ground disturbing 

activities should not be permitted or denied on the basis of information contained in this 

table. More detailed unit descriptions can be found in the help files that accompany the 

digital geologic map or by contacting the NPS Geologic Resources Division. 

Exposed sedimentary rocks at Capitol Reef range in age 

from Permian in the west to Cretaceous in the east. The 

Permian Cedar Mesa Sandstone is the oldest sedimentary 

rock unit and the Cretaceous Mesaverde Formation is 

the youngest. The Flagstaff Limestone exposed 

northwest of the park boundary is the youngest 

sedimentary rock formation in the vicinity of the park 

(Smith et al. 1963). 

Tertiary-age, intrusive and extrusive igneous rocks have 

limited exposure in the park. The dikes and sills are 

remnants of a volcanic field that covered the northern 

quarter of Capitol Reef about 4.6 to 3.7 million years ago 

(Billingsley et al. 1987; Morris et al. 2000). About 145 and 

107 m (475 and 350 ft) of volcanic deposits cap 

Boulder and Thousand Lake Mountains, respectively 

(Smith et al. 1963). 

Erosion of the sandstones of the Lower Jurassic Glen 

Canyon Group has formed many of the distinctive 

arches, domes, and slot canyons of Capitol Reef National 

Park. Together, the three formations of the Glen Canyon 

Group (Wingate Sandstone, Kayenta Formation, and 

Navajo Sandstone) reach a thickness ranging from 460 to 

820 m (1,500 to 2, 700 ft) and form the backbone of the 

Waterpocket Fold. 

West of the Waterpocket Fold, the Permian Kaibab 

Limestone and Cutler Group are exposed in steep, 

relatively inaccessible canyons. On the east flank of the 

Waterpocket Fold, the Cretaceous Mancos Shale forms a 

series of parallel strike valleys and subdued hogbacks 

(Morris et al. 2000). 

Unconsolidated Quaternary deposits reflect Pleistocene 

glacial processes and more recent fluvial and eolian 

deposits. At an elevation of more than 3,400 m (11,000 

ft), the Aquarius Plateau, west of Capitol Reef, holds the 

distinction of being the only highland in Utah that was 

covered by an ice cap during Pleistocene glaciation 

(Fillmore 2000). The effects of this glaciation are seen in 

the Capitol Reef Quaternary deposits. 

The following Map Unit Properties Table presents a list 

of features for rock units mapped in Capitol Reef 

National Park. This table includes a description of the 

formation or map unit, its map symbol, significant 

sedimentary structures and paleontologic resources, 

topographic expression, resistance to erosion, hazard 

potential, mineral and cultural resources, and any global 

significance attached to the unit. 
Map Unit Properties Table 

Age Map Unit (symbol) Unit Description Topographic Expression Resistance to Erosion Paleontological Resources 

Alluvium 

(Qal) 

Heterogeneous mixture of clay, silt, sand, and gravel; local organic-rich layers (Tantalus Creek) of peat; coarse gravel forms lenses and channel fill with gently dipping cross-laminations; sandy alluvium forms thin, regular 

beds with steeply dipping cross-laminations; evenly bedded silty alluvium; thickness ranges from 3-12 m (10-40 ft) 

Flat lowlands bordering streams; alluvial fans (fanshaped aprons) at mouth of canyons 

Variable – silt more easily eroded than boulders 

Mammoth, goat, musk ox, sloth, fragile snail shells; skull of bighorn sheep, elk antler, deer jawbone 

Rock glacier 

deposits (Qmr) Boulder deposits near the summits of Boulder Mountain and Mt. Pennell Boulder slopes High None 

Eolian deposits 

(Qed) Windblown sand, fine to medium grained; limited aerial extent Small dunes Low None 

Colluvial deposits 

(Qms) 

Includes rockslides, slumps and talus slopes consisting of a mixture of 

boulders, gravel, sand, and silt; thickness ranges from 0-6 m (0-20 ft) Talus slopes High if disturbed None 

Quaternary 

(Holocene) 

Terrace gravel 

deposits 

(Qat) 

Boulders, gravel, sand, and silt; includes glacial outwash and pediment gravels; cross-laminations & horizontal bedding 

Form terraces above current streams Variable Unknown 

Glacial till 

(Qgt) 

Unstratified mixture of unsorted angular boulders, gravel and sand; boulders are o.3 to 1 m (1-3 ft) in length (one over 9 m, 30 ft, in length); locally up to at least 60 m (200 ft) thick; includes some glacial outwash deposits which overlie the till; probably deposited about 12,000 BP. 

Moraines along Donkey, Fish, Carcass, Pleasant, Oak, East Boulder, West Boulder, Miller Creeks; irregular knobs; kettle depressions 

Variable None 

Boulder deposits 

(Qnb) 

Diverse mixture of soil and boulders that generally mantle the upper slopes of Thousand Lake and Boulder mountains; includes undifferentiated glacial 

landslide and alluvial deposits 

Mouths of Fish and Carcass Creeks; near Browns Reservoir; Tantalus Flats along Pleasant Creek 

Quaternary High None 

(Pleistocene) 

Pediment gravels 

(Qap) 

Volcanic boulders, cobbles, sand, and gravel; round to oblong volcanic boulders are 0.9 to 1.5 m (3-5 ft) in the long direction (some more than 4.5 

m, 15 ft, in length); lenticular beds of gravel between 6 to 15 m (20-50 ft) thick; dissection of pediment surfaces suggest deposition at more than 75,000 years BP 

Cap flat-topped hills and benches in Capitol Reef; on gently sloping surfaces several hundred feet above adjacent streams and valleys 

Variable to low due to position in landscape 

None 

Regional Unconformity 

Volcanic rocks 

(Tv) 

Mostly lava flows of porphyritic andesite; black to dark gray; light-gray phenocrysts of plagioclase feldspar; individual flows may reach 30 m (100 ft) thick and can be traced for over a kilometer; about 145 m (475 ft) thick on Boulder Mountain and 107 m (350 ft) thick on Lake Mountain 

Lava flows High None 

Diorite porphyry 

intrusion (Tdp) 

Intrusions of diorite porphyry; includes some monzonite porphyry on Mt. Pennell Limited aerial extent High None 

Sedimentary and 

igneous rocks (Ts) 

Sedimentary and igneous rocks irregularly intruded by igneous materials; many dikes and sills Limited aerial extent Insignificant None 

Tertiary 

(Pliocene) 

Intrusive igneous 

rocks 

(Ti) 

Intrusive dikes, sills, and a few plug-like dikes with intrusive breccias, remnants of a volcanic field; mostly dark gray, fine-grained porphyritic basalts with vesicles filled with calcite and analcite (a zeolite mineral); pyroxene most prominent phenocryst; volcanic field dated as 4.6 to 3.7 Ma 

Dikes trend N 15o E, parallel 

to major joint trend High None 

Regional Unconformity 
Age Map Unit (symbol) Unit Description Topographic Expression Resistance to Erosion Paleontological Resources 

Tertiary 

(Paleocene-Eocene) Flagstaff Limestone (Tf) Limestone; light gray tuff, tuffaceous sandstone, to almost quartz sandstone, siltstone, claystone and conglomerate; tuff and tuffaceous beds are as abundant as limestone beds; limestone is yellowish-gray and grayish-orange and weathers to tints of cream pink; conglomerate is poorly sorted with well rounded pebbles and cobbles of white quartz, black chert, tan quartzite, and tan to gray silicified limestone; limestone beds are thin, 1.3 to 20 cm (0.5-8 in) thick; beds of tuff and tuffaceous sandstone range from 0.08 to 20 cm (0.03-8 in) thick; 150 m (500 ft); exposed NW of the park. Not exposed in Capitol Reef Variable – not exposed in Capitol Reef 

Pebbles contain Paleozoic corals, bryozoans, crinoid stems, brachiopods; freshwater ostracods (Metacypris sp. 

& Paracypris sp.); algae (Chlorellopsis coloniata); gastropods 

Regional Unconformity 

Mesaverde 

Formation (Kmv) 

Light brown, thick-bedded sandstone and thin interbedded dark gray shale; intertongues with Masuk mbr of the Mancos Shale; 90 to 120 m (300-400 ft) is exposed in extreme southeastern corner of Capitol Reef 

Cliff former High None 

Masuk mbr of 

Mancos Shale 

(Kmm) 

Yellowish-gray mudstone and minor bluish-gray to black mudstone with 

interbedded light gray sandstone; gradational contact with Emery mbr.; 200-

230 m (650-750 ft) thick 

Mudstones form slopes; sandstones form cliffs 

Mudstones have low resistance; sandstones relatively high resistance 

Gastropods, bivalves, turtles, crocodiles, ceratopsian dinosaurs 

Emery mbr (Muley 

Canyon mbr) of 

Mancos Shale 

(Kme) 

Light gray to yellow, medium-bedded sandstone containing interbedded carbonaceous shale and coal beds in the upper part; lower beds intertongue 

with the Blue Gate Shale mbr; about 90 to 120 m (300-400 ft) thick 

Cliff former 

Carbonaceous shales have low resistance; sandstone high 

Unknown 

Blue Gate Shale 

mbr of Mancos 

Shale 

(Kmb) 

Laminated blue-gray and black bentonitic shale with a few interbedded light yellow sandstone and limestone lenses; thickness ranges from 365 m (1,200 ft) in the south to 455 m (1,500 ft) in the north 

Weathers to gullied slopes similar to the slopes of the Tununk Shale 

Low 

Planktonic foraminifera (Clioscaphites vermiformis & 

Clioscaphites choteauensis) 

Ferron Sandstone 

mbr of Mancos 

Shale 

(Kmf) 

Fine-grained laminated brown sandstone and white cross-bedded sandstone containing interbedded carbonaceous shale and gray, impure coal in the upper part; intertongues with the Tununk Shale mbr; 60-120 m (205-385 ft) 

thick. 

Cliff and ledge former Relatively high 

Ophiomorpha trace fossil; marine bivalve, Inoceramus

Tununk mbr of 

Mancos Shale 

(Kmt) 

Bluish-gray and black bentonitic shale; interbedded mudstone, siltstone, and very fine-grained sandstone; locally fossiliferous; 165-220 m (540-720 ft) thick 

Slope former Low – erodes into gullied slopes Marine invertebrate shell fragments 

Dakota Sandstone 

(Kd) 

Yellowish-brown to gray quartz-rich sandstone and conglomerate with interbedded carbonaceous shale and thin coal beds; locally fossiliferous; deposited 92-96 Ma; 0 to 46 m (0-150 ft) thick 

Weathers to small cliffs and hogbacks Relatively high 

Marine bivalves Pycnodonte newberryi& Corbula sp. in upper 

part; petrified wood in lower section 

Regional Unconformity 

Cretaceous 

Cedar Mountain 

Formation (Kcm) 

Variegated mudstone including some white, gray and brown sandstone and conglomerate (the Buckhorn Conglomerate mbr); deposited 97.5 to 113 Ma; 0 to 50 m (0-166 ft) thick in the north 

Slope former; north of Capitol Reef, Buckhorn Conglomerate mbr forms a cliff at base of the formation. 

Low except for Buckhorn Conglomerate mbr. 

Freshwater mollusks & 

ostracods, fish scales, 

dinosaur bones, 

charophytes, pollen, and 

a Tempskya fern 
Age Map Unit (symbol) Unit Description Topographic Expression Resistance to Erosion Paleontological Resources 

Brushy Basin mbr 

of Morrison Fm. 

(Jmb) 

Variegated, bentonitic mudstone including some white, gray and brown sandstone and conglomerate containing abundant red and green chert pebbles; 

gradational contact with Salt Wash member; thickness averages 60 m (200 ft) 

in the south and 60-100 m (200-350 ft) in the north 

Slope former 

Low; bentonite weathers to a “popcorn” surface 

Contains many dinosaur quarries in UT & western CO 

Salt Wash mbr of 

Morrison Fm. 

(Jms) 

Thick-bedded light gray sandstone and chert-pebble conglomeratic sandstone interbedded with greenish to reddish mudstone; sandstones are fine- to medium-grained with moderate sorting; thickness varies from 30-60 m (100-200 ft) in the north to 150 m (500 ft) in the south 

Discontinuous lenses of sandstone and conglomerate form ledges and small cliffs; shale forms slopes 

Sandstone and conglomerate lenses more resistant than shales 

Fragments of dinosaur bones and teeth 

Upper Jurassic 

Tidwell mbr of 

Morrison Fm. 

(not mapped) 

Red, green, or gray mudstone; difficult to recognize from the underlying Summerville Formation; maybe 15 to 30 m (50-100 ft) thick in Capitol Reef Slope former Low Not differentiated in Capitol Reef 

Regional Unconformity 

Summerville 

Formation 

(San Rafael Gp) 

(Js) 

Thin beds of reddish-brown siltstone and mudstone and fine-grained sandstone; map unit includes interbedded red and gray mudstone, pink and white gypsum, gray limestone, and gray sandstone in the Tidwell mbr of the Morrison Fm; mudstone and siltstone beds are 2.5 to 15 cm (1-6 in) thick, sandstone beds are 

0.15 to 0.6 m (0.5 to 2 ft) thick; gypsum beds are 0.3 to 8.5 m (1-28 ft) thick; total about 15-75 m (50-250 ft) thick 

Reddish slopes in Cathedral Valley; Exposed in steep slopes or cliffs on northeast side of Waterpocket Fold 

Low None documented in Capitol Reef 

Regional Unconformity 

Curtis Fm 

(San Rafael Gp) 

(Jcu) 

Thin- to thick-bedded white, fine-grained calcareous sandstone and siltstone and minor sandy limestone; sandstones contain glauconite; gradational with the Summerville Fm; discontinuous to the south and increases to about 55 m (175 ft) in the north; 

Forms resistant caprock on some monoliths & cathedrals 

Sandstone high; siltstone low Unknown 

Regional Unconformity 

Entrada 

Sandstone 

(San Rafael Gp) 

(Je) 

Thin- to thick-bedded reddish brown sandstone and siltstone (upper and lower part of formation); siltstone (middle part of formation); subangular to subrounded, fine-grained to very fine-grained quartz sandstone; calcareously cemented; Crossbedded units may reach 12 m (40 ft) thick; sandstone and siltstone in the north, siltstone in the south; ranges from 120 to 275 m (400-900 ft) thick 

Cliff former in the north; slope former in the south 

Erodes into knobby pinnacles (hoodoos), monoliths, and cathedrals 

None documented 

Carmel Fm 

(San Rafael Gp) 

(Jc) 

Very fine-grained thin-bedded orange-red sandstone and siltstone; calcareous mudstone common in the lower half; pink gypsiferous siltstone & gray limestone beds in upper part; beds generally only a few inches thick but may 

reach 1.2 m (4 ft) thick; gypsum as veinlets and beds 0.3 to 0.6 m (1-2 ft) thick (beds 24 m, 80 ft, thick reported on black Ridge); gypsum is white, massive, finely crystalline or granular but may be greenish gray or green; banded appearance produced by alternation layers of whitish-gray limestone and gypsum with reddish-brown siltstone and sandstones; formation ranges from 60 m (200 ft) in the south to 305 m (1,000 ft) in the north 

Reddish to red-brown flatirons (triangular-shaped spurs) form eastern rampart of Waterpocket Fold; ledge and slope former 

Sandstone is resistant; siltstone and gypsum is not as resistant to erosion 

None documented 

Middle Jurassic 

Page Sandstone 

(not mapped) 

Light reddish-brown, fine-grained large-scale cross-bedded sandstone; divided 

into Harris Wash, Judd Hollow, and Thousand Pocket members; red cliff above falls of Fremont River at mile marker 86.5 is Judd Hollow mbr; sandstone 

above cliff is Thousand Pockets mbr; ranges from 0 to 30 m (0-100 ft) thick in Capitol Reef 

Red cliff above falls of Fremont River High None documented 

Regional Unconformity 
Age Map Unit (symbol) Unit Description Topographic Expression Resistance to Erosion Paleontological Resources 

Navajo 

Sandstone 

(Glen Canyon 

Group) 

(Jn) 

White, yellow, and light reddish-brown, large-scale (60 ft) crossbedded finegrained sandstone; well-rounded, frosted quartz sandstone; contact with Kayenta is gradational; thickness ranges from 240 m (800 ft) to 335 m (1,100 ft) along Waterpocket Fold 

Forms massive white to reddish-brown cliffs, monoliths & domes (Capitol & Navajo) 

High None documented 

Kayenta Fm. 

(Glen Canyon 

Group) 

(Jk) 

Divided into three units based on weathering features; lower ledge and middle cliff units are very fine-grained sandstone; upper unit contains abundant siltstone; clay-pebble conglomerate and traces of interbedded mudstone and limestone throughout the formation; horizontal and small-scale lenticular and tabular cross-beds; cross-beds are small (few ft thick); gradational contact with Wingate; 107 m (350 ft) thick 

Lower ledge forming unit; middle cliff forming unit; upper slope forming unit 

Lower and middle units are more resistant than upper unit 

Theropod dinosaur 

tracks 

Lower Jurassic 

Wingate 

Sandstone 

(Glen Canyon 

Group) 

(Jw) 

Reddish-brown, thin- to thick-bedded, fine-grained quartz sandstone; massive and crossbedded; well-rounded quartz grains; large-scale, low- to high-angle 

trough cross-sets; iron oxide cement produces reddish, salmon color; 107 m (350 ft) thick, thins slightly from east to west 

Cliff former; caps the western escarpment of Waterpocket Fold; forms features like Castle & Fruita Cliffs 

High except where undercut and then litters slopes of Owl Rock mbr of Chinle Fm 

None documented 

Regional Unconformity 

Owl Rock mbr: orange and purple mudstones, siltstones, and fine-grained sandstones with characteristic 0.3 to 3 m (1-10 ft) thick interbeds of mottled pink to green limestone; not bentonitic; micritic limestones have a knobby texture from coalescence of carbonate nodules; mudcracks filled with Wingate Sandstone; 46 to 61 m (150-200 ft) thick 

Slopes below Wingate Sandstone cliffs 

Low, but protected by cliffs 

Large cylindrical burrows & ostracodes 

Petrified Forest mbr: reddish-orange bentonitic siltstones and clayey quartz sandstone; lower 46 to 61 m (150-200 ft) forms slopes capped by a regionally persistent, crossbedded sandstone known as the “Capitol Reef bed” that forms a prominent cliff or ledge 

Lower slopes capped by sandstone ledge or cliff of “Capitol Reef bed” 

Low; bentonitic mudstones 

Tetrapod remains, lungfish toothplates, coprolites, marine gastropods & mollusks, vertebrate fossils, petrified wood, crocodilian and amphibian teeth 

Monitor Butte mbr: light purplish-gray, bentonitic claystones and clayey sandstones with interbeds and lenses of crossbedded sandstone and carbonate nodules; distinct color makes it readily traceable along the lower to middle slopes of the Waterpocket escarpment; most heterogeneous member of Chinle Fm 

Slope former Low; bentonitic mudstones Lung fish burrows (5 in dia; 5 ft long); petrified plants 

Upper Triassic Chinle Formation (TRc) 

Shinarump mbr: yellowish-gray, fine- to coarse-grained, friable sandstone with lenses and interbeds of conglomerate and conglomeratic sandstone; pebbles comprised of quartz, quartzite, and chert; near west entrance, fills broad channels eroded into top of Moenkopi Fm; discontinuous, where absent, Monitor Butte rests on Moenkopi; up to 27 m (90 ft) thick 

Prominent white cliff; forms caprock for Twin Rocks, Egyptian Temple, & Chimney Rock 

More resistant than mudstones, but sandstones are friable 

None documented 

Regional Unconformity 
Age Map Unit (symbol) Unit Description Topographic Expression Resistance to Erosion Paleontological Resources 

Moody Canyon mbr: lower unit of horizontally laminated reddish-brown siltstones and upper unit of ripple laminated reddish-orange siltstones; lower unit is 61 to 91 m (200-300 ft) thick; upper unit is well exposed in lower part of the Egyptian Temple and at Chimney Rock and forms reddish-orange cliffs at base of Waterpocket escarpment 

Lower unit forms slopes; Upper unit forms cliffs 

Rippled siltstones are relatively resistant 

None documented 

Torrey mbr: reddish-brown to chocolate colored siltstone and fine-grained sandstone with rare interbeds of mud-pebble conglomerate, sandy dolomite, dolomitic limestone, and claystone; sandstones have horizontal bedding & low angle cross-bedding; ripple marks & mudcracks in finer grained beds; halite crystal casts in upper part; about 76 to 98 m (250-320 ft) thick 

Ledge former Relatively resistant Well known for large reptile and amphibian trackways 

Sinbad mbr: yellowish fossiliferous to muddy limestone and dolomite with subordinate amounts of siltstone and sandstone; oolitic layers (composed of tiny carbonate spheres) are characteristic of lower part; yellowish color and carbonate lithology distinguishes Sinbad from other Moenkopi members; carbonates are thin-bedded to laminated with some small-scale trough crossbedding; about 21 to 43 m (70-140 ft) thick 

Ledge former Relatively resistant 

Inarticulate brachiopod,

Lingula; ammonite cephalopod,Meekoceras

Lower Triassic Moenkopi Formation (TRm) 

Black Dragon mbr: reddish conglomerate, siltstone, and sandstone; abundant 

angular chert in basal conglomerates from underlying Kaibab Ls.; interbeds of dolomite and limestone with sparse marine fossils in upper part; 15 to 34 m (50-

110 ft) thick 

Slope former 

Less resistant than bordering formations 

Sparse marine fossils in carbonates 

Regional Unconformity 

Kaibab Limestone 

(PNk) 

Light gray to white, cherty dolomite interbedded with thin calcareous sandstone 

and siltstone layers; limestone especially in lower half; exposed only in the 

deeply incised canyons along the western margin of Capitol Reef; middle and upper parts contain silcretes (siliceous paleosols) and calcretes (calcitic 

paleosols); channels reaching 30 m (100 ft) deep were scoured into the Kaibab when its surface was exposed during Middle Permian time; averages 61 m (200 ft) thick 

Relatively inaccessible cliffs Highly resistant 

Brachiopods, Neospirifer pseudocamer-atus, Dictyoclostus bassi; pelecypods, gastropods, crinoids, bryozoans 

Permian 

Cutler Group 

(PNc) 

White Rim Sandstone and Cedar Mesa Sandstone: light-yellow to gray, crossbedded quartz sandstones; well-rounded, moderately well-sorted with grains ranging in size from very fine- to medium grained; White Rim Sandstone cannot be distinguished from older Cedar Mesa Sandstone because the Organ Rock Shale that usually separates the two formations pinches out east of Capitol Reef; exposed only in the deeply incised canyons along the western margin of Capitol Reef; Cutler sandstones reach a thickness of 244 m (800 ft) 

Relatively inaccessible cliffs Highly resistant Marine trace fossils, shark teeth 
 CARE Geologic Resource Evaluation Report 27

Geologic History 

This section highlights the map units (i.e., rocks and unconsolidated deposits) that occur 

in Capitol Reef National Park and puts them in a geologic context in terms of the 

environment in which they were deposited and the timing of geologic events that created 

the present landscape. 

Figure 10 summarizes the significant life forms, major 

extinctions, and tectonic events in North America from 

the Precambrian to the Quaternary. The geologic history 

exposed at Capitol Reef begins in the Permian Period, 

approximately 275 million years ago. 

Paleozoic Era 

Permian Period 

During the Permian, most of Utah was located near 10o 

north latitude (Morris et al. 2000). A dry, high 

atmospheric pressure climatic belt, analogous to that of 

the Sahara Desert today, prevailed in this region and 

resulted in restricted marine evaporitic conditions over 

much of the cratonic shelf seaway (Peterson 1980). Large 

dune fields or ergs migrated across southeastern Utah as 

the climate became more arid (figure 11). These eolian 

deposits became the Cedar Mesa Sandstone and White 

Rim Sandstone (Loope 1984; Huntoon et al. 1994; Dubiel 

et al. 1996; Morris et al. 2000). Sand and sand-sized 

marine fossil fragments blew inland from a coastline 

located to the northwest and formed the dunes 

(Huntoon et al. 2000). Capitol Reef is located near the 

northern border of this dune field (figure 11) where the 

eolian dune complex may have been subjected to 

periodic marine flooding (Morris et al. 2000). 

Trending northwest-southeast, the peaks of the 

Uncompahgre Mountains were rising in western 

Colorado. The coarse grained, arkosic clastic rocks 

(sedimentary rocks high in feldspar) eroded from the 

rising Uncompahgre Mountains represent a complex 

depositional system of eolian-fluvial-alluvial fan 

sediments that affected the Capitol Reef region 

(Campbell 1980; Cole et al. 1996). 

Oolitic dolomite, fine-grained sandstone, and 

fossiliferous limestone are formed in normal to marginal 

marine environments. Limestone deposition 

transgressed over the ergs, preserved as the Kaibab 

Limestone, and recorded the last in a long series of 

shallow seas that covered Capitol Reef and the Colorado 

Plateau throughout the Paleozoic Era (Morris et al. 

2000). 

The interfingering of the Kaibab with the White Rim 

Sandstone suggests that the marine facies of the Kaibab 

migrated eastward (transgressed) in response to a 

relative sea-level rise (Dubiel et al. 1996). At times, the 

area was subaerially exposed and eolian sand with large 

sweeping cross-beds covered the area. Cross-beds such 

as these can be found along Pleasant Creek in a 

sandstone unit that forms a prominent ledge and cliff 

above dolomite and dolomitic limestone (Smith et al. 

1963). During the Permian, episodic transgressions and 

regressions occurred across the area, and with each sea 

level regression, erosion created a regional unconformity 

(figure 12) (Smith et al. 1963; Blakey 1996). 

With the final Permian regression of the sea, the 

limestone was exposed to erosion (Morris et al. 2000). 

Dissolution of the Kaibab created karst topography and 

channels, reaching 30 m (100 ft) in depth, scoured into 

the limestone surface (Morris et al. 2000). Rubbly 

silcretes and calcretes are found in the middle and upper 

portions of the Kaibab (Morris et al. 2000). Silcretes and 

calcretes are paleosols rich in silica and calcite, 

respectively. Paleosols are significant paleoenvironmental indicators because, like soils today, they 

developed during episodes of subaerial exposure and 

represent unconformities between depositional regimes. 

On the western margin of the continent in the Permian, 

in the vicinity of central Nevada, continental shelf and 

slope rocks were being compressed against the 

continental margin as the Sonoma Orogeny advanced 

eastward (Silberling and Roberts 1962). Subduction of 

the encroaching lithospheric plate from the west beneath 

the continental crust of North America caused melting of 

the oceanic plate and would eventually form a volcanic 

island chain on the western margin of the continent (in 

the area of western Nevada) during the Triassic. 

The third, and most severe, major mass extinction of 

geologic time occurred at the close of the Permian. 

Although not as famous as the extinction event that 

exterminated the dinosaurs at the end of the Mesozoic, 

the Permian extinction was much more extensive. As 

much as 96% of all species were eliminated at the end of 

the Permian (Raup 1991). Thousands of species of 

insects, reptiles, and amphibians died on land while in 

the oceans, species of coral, snails, urchins, sea lilies, 

some fish, and the once-prolific trilobites vanished. 

Mesozoic Era 

Triassic Period 

Prior to the Mesozoic, all the continents had come 

together to form a single landmass (supercontinent) 

called Pangaea which was located symmetrically about 

the equator (Dubiel 1994). During the Triassic (250 to 

206 million years ago), Pangaea reached its greatest size. 

To the west, explosive volcanoes formed a north-south 

trending arc of islands along the border of present-day 

California and Nevada (Christiansen et al. 1994; Dubiel 

1994; Lawton 1994). Clastic sediments continued to be 
 NPS Geologic Resources Division 28 

shed from the Uncompahgre Highlands in Colorado. As 

sea level fell, the shoreline of the shallow sea that 

extended into eastern Utah in the Early Triassic moved 

far to the west and off the continent. 

The terrestrial red beds of the Lower Triassic Moenkopi 

Formation were deposited in fluvial, mudflat, sabkha, 

and shallow marine environments (figure 13) (Stewart et 

al. 1972A; Christiansen et al. 1994; Doelling 2000; 

Huntoon et al. 2000). Fluvial systems drained uplifted 

areas throughout central and southeastern Utah 

(Huntoon et al. 2000). Ripple marks, mudcracks, thin 

interbeds of dolomite and limestone with sparse marine 

fossils are common on bedding planes in the upper part 

of the Black Dragon Member of the Moenkopi, 

indicating deposition in coastal plain and tidal flat 

environments. 

Brachiopod and ammonite fossils in the overlying Sinbad 

Limestone Member of the Moenkopi record a relatively 

short-lived incursion of the ocean into eastern Utah 

(Stewart et al. 1959). When the Sinbad Sea retreated to 

the west, tidal flat conditions returned to Capitol Reef, 

depositing redbeds of the Torrey and Moody Canyon 

members of the Moenkopi. The fossilized plants and 

animals in the Moenkopi are evidence of a climate shift 

to warm tropical conditions that may have experienced 

monsoonal, wet-dry periods (Stewart et al. 1972A; 

Huntoon et al. 2000; Morris et al. 2000). 

The Middle Triassic remains a mystery. No rocks that 

span this time ranging from 235-400 Ma have been 

preserved in Utah, resulting in a regional unconformity. 

The Upper Triassic Chinle Formation represents a 

complex assemblage of alluvial (Shinarump 

Conglomerate Member, Monitor Butte Member, 

Petrified Forest Member) marsh, lacustrine (Owl Rock 

Member), playa, and eolian deposits (Stewart et al. 

1972B; Dubiel 1987). Throughout the region, layers of 

smectite clays are interlayered with the clastic sediments. 

The clay layers indicate a period of renewed volcanism to 

the west caused by active lithospheric plate subduction 

(Christiansen et al. 1994). 

In the lower part of the Chinle, paleovalleys eroded into 

the underlying Moenkopi Formation forming a dendritic 

pattern that fed a northwest-trending, paleovalley trunk 

system (figure 14). Choked with sediment, braided 

streams (Shinarump Member) tended to occupy these 

paleovalley systems. Channel-fill deposits may reach a 

thickness of 27 m (90 ft). Weathering of the Shinarump 

has formed a prominent white cliff and cap rock for such 

features as the Egyptian Temple, Twin Rocks, and 

Chimney Rock (Smith et al. 1963; Morris et al. 2000). 

Fluvial processes formed the cross-bedded sandstones in 

both the Shinarump and Petrified Forest members of the 

Chinle. The cross-bedded sandstones of the Petrified 

Forest Member were formed in meandering (high 

sinuosity) river channels. The persistent, cross-bedded 

sandstone known as the Capitol Reef bed forms a 

prominent cliff or ledge in Capitol Reef National Park. 

During the final phases of Chinle deposition, lower water 

table conditions existed. Lacustrine mudflat siltstones 

and mudstones, ephemeral fluvial-channel sandstones, 

and eolian sand-sheets and dunes were deposited during 

extended dry periods (Dubiel 1994). The monsoonal 

precipitation that characterized the Early Triassic 

depositional systems was disappearing in the Late 

Triassic. As Pangaea began to break apart in the latest 

Triassic and earliest Jurassic, the monsoonal climate 

changed. The Western Interior of North America was 

slowly rotating into a position farther north of the 

equator. Soon, the jungle on the Colorado Plateau was to 

become a desert. 

Lower Jurassic Period 

The Jurassic western margin of North America was 

associated with an Andean-type margin where the 

eastward subduction of the seafloor gave rise to 

volcanism similar to that found in the Andes of South 

America today. Volcanoes formed an arcuate northsouth chain of mountains off the coast of western 

Pangaea in what is now central Nevada The Ancestral 

Rocky Mountains and the Monument Upwarp remained 

topographically high during the Jurassic. 

The Jurassic of Western North America was a time of 

extensive eolian (ergs or sand sheets) deposition. Vast 

sand deposits are preserved in the Wingate and Navajo 

sandstones, which represent an environment similar to 

the Sahara and Sahel deserts today. The region was 

located about 18o north latitude at the beginning of the 

Jurassic (about 208 Ma) and moved to 30o - 35o north 

latitude by the end of the Jurassic (about 144 Ma) 

(Kocurek and Dott 1983; Peterson 1994). This is the 

latitude of the present day northeast trade wind belt 

where most modern hot deserts occur. 

The Jurassic deserts that occupied the Colorado Plateau 

for roughly 40 million years (not counting the time 

represented by erosion) contained sand dunes that may 

be the largest recorded in the history of the earth 

(Kocurek and Dott 1983). Like today’s Sahara Desert, the 

Jurassic ergs formed on a coastal and inland dune field. 

Sand dunes were deposited in the present areas of 

southern Montana, eastern Utah, westernmost 

Colorado, southwest Colorado, northeastern Arizona, 

and northwestern New Mexico (Kocurek and Dott 1983; 

Peterson 1994). 

Erosion of Triassic and Upper Paleozoic sandstones 

exposed from as far north as Montana and Alberta 

provided abundant quantities of sand to be transported 

by wind to the Colorado Plateau (Kocurek and Dott 

1983). The volcanic arc to the west acted as a barrier to 

block the wind and channel it to the south (figure 15) 

(Kocurek and Dott 1983). The perpetually arid climate 

may have lowered the ground water table, which would 

have kept the surface sediments dry and available for 

movement by the wind. These eolian deposits are found 

today in the massive Wingate Sandstone that forms such 

features as the Castle and Fruita Cliffs. 
 CARE Geologic Resource Evaluation Report 29

A change from eolian to fluvial deposition is recorded in 

the sandstones of the Jurassic Kayenta Formation. In 

contrast to the sweeping eolian cross-beds of the 

Wingate and Navajo sandstones, the cross-beds in the 

Kayenta are only a few feet in thickness. Interbedded 

sandstone, basal conglomerates, siltstones, and 

mudstones are typical channel and floodplain deposits. 

Paleocurrent studies show that rivers flowed in a general 

westward to southwestward direction during Kayenta 

time (Morris et al. 2000). The large natural bridge near 

Fruita is carved out of the Kayenta Formation. 

The Navajo Sandstone records a return to arid 

conditions and the development of extensive ergs on the 

Colorado Plateau. Sand dune deposits reaching 240 to 

340 m (800 to 1,100 ft) in thickness gradually overtook 

the fluvial systems of the Kayenta (Morris et al. 2000). 

Differential weathering of the Navajo cross-beds has 

produced the massive white to reddish-brown cliffs, 

monoliths, and domes such as Capitol and Navajo 

Domes. 

Middle Jurassic Period 

As plate tectonic activity increased in the Middle 

Jurassic, the sea transgressed onto the continent from the 

north. Middle Jurassic strata on the Colorado Plateau 

represent a complex interfingering of marine and 

nonmarine sediments. Broad tidal flats formed along the 

margin of the shallow sea that lay to the west of Capitol 

Reef (Wright et al. 1962). 

The Page Sandstone is separated from the underlying 

Navajo Sandstone by a regional unconformity. Above the 

unconformity, eolian deposits (Harris Wash Member) 

are overlain by a sabkha environment (Judd Hollow 

Member) followed by a series of two eolian episodes 

separated by a marine incursion into the area (Thousand 

Pocket Member) (Blakey 1994; Morris et al. 2000). 

Restricted marine and marginal marine environments 

(Carmel Formation) similar to those in the Page 

Sandstone record a period of intermittent marine 

flooding and evaporation in the Capitol Reef area prior 

to development of the next aerially extensive erg 

(Entrada Sandstone) (Morris et al. 2000). 

The cross-stratified Entrada Sandstone covers the entire 

Colorado Plateau and is the most widespread of the 

preserved late Paleozoic and Mesozoic eolian deposits 

on the Colorado Plateau. In the southern part of Capitol 

Reef, the Entrada consists predominantly of tidal flat 

deposits (figure 16) (Doelling 2000; Morris et al. 2000). 

Marine conditions had retreated to the north by this time 

and as the groundwater table dropped, the wind moved 

the sand into huge dune fields south of Capitol Reef 

(Kocurek and Dott 1983; Hintze 1988). When 

groundwater levels rose, the sand grains were held 

together by water and became unavailable to wind 

transport. 

In the Curtis Formation, glauconite, a green iron- and 

potassium-bearing (usually marine) clay, indicates a 

major transgression of marine environments into the 

area from the north. Transgression of the sea destroyed 

the vast dune fields and coincided with the onset of the 

Sevier Orogeny (about 157.1 Ma) (Kocurek and Dott 

1983). 

Regression of this shallow sea left mudcracks, ripple 

marks, and inch-scale cross-bedding in tidal flat 

siltstones and mudstones (Summerville Formation) 

(Morris et al. 2000). 

Upper Jurassic Period 

Eventually, the sea receded from the western continental 

United States followed by the deposition of the extensive 

Upper Jurassic, Morrison Formation (figure 17). The 

Morrison at Capitol Reef represents hypersaline lagoon 

deposits (Tidwell Member), a meandering stream system 

with associated channel and floodplain deposits (Salt 

Wash Member), and a fluvial-deltaic depositional system 

(Brushy Basin Member) (Haynes et al. 1972; Petersen 

and Roylance 1982; Morris et al. 2000). The thicker, 

continuous sandstone deposits of the Salt Wash Member 

contain small and large uranium deposits eroded from 

the adjacent highlands and transported into the area 

(Haynes et al. 1972). 

Compared to the Salt Wash Member, the Brushy Basin 

Member contains only minor amounts of conglomerate 

and sandstone deposited in river channels. The more 

abundant siltstone and mudstone are interpreted as 

flood-plain deposits. Some of the most complete 

dinosaur skeletons ever found have been discovered in 

the lake-floor and floodplain deposits of the Morrison 

Formation. Deposits of disarticulated bones in channel 

sandstones are oriented so that their long axes are 

parallel to the paleo-current direction. 

The character of the shale slopes also is distinct between 

the Salt Wash and the Brushy Basin because of the 

bentonite in the Brushy Basin Member. These swelling 

clays expand when wet and dry to a crumbly “popcorn” 

surface that characterizes the Brushy Basin slopes. 

Cretaceous Period 

Accelerated lithospheric plate collision during the 

Cretaceous caused mountains to form along the western 

margin of North America. The Sevier Orogeny formed a 

roughly north-south trending thrust belt that is well 

defined in present-day southern Nevada, central Utah, 

and western Montana (figure 10). As the mountains rose 

in the west, the Gulf of Mexico separating North and 

South America continued to rift open in the south, and 

seawater extended northward into an expanding 

depression called the Western Interior Basin (or, 

Western Interior Seaway). Marine water also began to 

transgress southward from the Arctic region. 

In the Lower Cretaceous, continental fluvial conditions 

prevailed in the Capitol Reef region with the low-energy 

floodplain, fluvial, and interfluvial lacustrine deposits of 

the Cedar Mountain Formation (97.5 to 113 Ma) (Fouch 

et al. 1983; Elder and Kirkland 1994; Morris et al. 2000; 

Doelling 2000). Paleocurrent directions show that Cedar 

Mountain sediments came from rivers originating in 
 NPS Geologic Resources Division 30 

central Utah where an unconformity between the Cedar 

Mountain strata and the underlying Morrison Formation 

is marked by a calcrete, a layer that forms in semi-arid 

climates. 

As the shoreline continued to advance into eastern Utah 

and western Colorado, a heterogeneous mixture of 

terrestrial and shallow marine environments prevailed 

(Dakota Sandstone). Strata in the lower Dakota 

Sandstone contain petrified wood and are dominated by 

fluvial, lagoonal, and marsh environments (Morris et al. 

2000). As the Cretaceous interior seaway widened, 

however, the fluvial-dominated system changed to a 

coastal plain depositional system with deposition in 

coastal swamps, lagoons, and beaches (Condon 1991). 

Marine bivalves, especially the chunky clam shells of 

Gryphaea and Exogyra, make some of the beds look 

conglomeratic (Smith et al. 2000). 

Gradually, as sea level rose, the sparsely fossiliferous, 

dark-gray muds of the Mancos Shale were deposited in 

the deepening Western Interior Seaway above the 

Dakota Sandstone. The paleobathymetry over eastern 

Utah was approximately 100-200 m (328-656 ft) at this 

time (Sageman and Arthur 1994). 

The seas advanced and retreated many times during the 

Cretaceous until the most extensive interior seaway ever 

recorded drowned much of western North America 

(figure 18). The Western Interior Seaway was an elongate 

basin that extended from today’s Gulf of Mexico to the 

Arctic Ocean, a distance of about 4,827 km (3,000 mi) 

(Kauffman 1977). During periods of maximum 

transgression, the width of the basin was 1,600 km (1,000 

mi) from western Utah to western Iowa. The basin was 

relatively unrestricted at either terminus (Kauffman 

1977). The western margin of the seaway coincided with 

the active Cretaceous Sevier Orogenic belt so that 

sedimentation into the basin from the rising mountains 

was rapid. Rapid sedimentation led to further sediment 

loading and downwarping along the western margin. 

The calcareous marine mudstones that comprise the 

lower part of the Tununk Member were deposited 

during a transgression that flooded the Dakota 

Sandstone environments (Gardner and Cross 1994). The 

lower Tununk shales represent the maximum extent of 

the Cretaceous Interior Sea (figure 19) (Elder and 

Kirkland 1994). The bluish shales of the Tununk are 

responsible for the scenery at Blue Desert just southeast 

of Cathedral Valley (Morris et al. 2000). 

At Capitol Reef, the hummocky to low-angle crossstratification, ball-and-pillow structures, the 

Ophiomorpha trace fossils and the marine bivalve 

Inoceramus indicate deposition in the middle to lower 

shoreface, marine environment and signal a regressive 

episode (Ferron Sandstone Member) (Peterson et al. 

1980; Morris et al. 2000). Hummocky cross-stratification 

forms undulating cross-bed sets of both swales 

(depressions) and hummocks (mounds). Today, 

hummocky cross-stratification is commonly produced 

by large storm waves in near-shore marine 

environments. Ball-and-pillow structures are contorted 

features found in sandstone beds that overlie shale beds. 

Liquefaction of the mud layers causes water to escape 

upward, deforming and breaking up the semiconsolidated sand into hemispherical masses that 

resemble balls or pillows. 

Another transgression produced the fossiliferous, marine 

mudstones of the Blue Gate Member, and like the 

Tununk, the mudstones represent deposition under 

open marine conditions (Morris et al. 2000). Bentonite in 

the clays records continued volcanic activity to the west. 

Subsequent regression brought about a succession of 

facies from fine-grained sandstones to carbonaceous 

shales and coal, reflecting a transition from a marine 

shoreline to a continental coastal plain (Muley Canyon 

Member) (Morris et. al. 2000). Gastropods, bivalves, 

turtles, crocodiles and ceratopsian dinosaurs are present 

in the cross-bedded and ripple laminated sandstone of 

the Masuk Member, indicating continued regression of 

the Cretaceous Seaway (Peterson et al. 1980; Morris et al. 

2000). 

For roughly ten million years, clay, silt, sand, and shell 

debris were deposited in the Mancos Sea. As sea level 

continued to fall, barrier beaches and deltas of the 

Mesaverde Formation were deposited in the region 

(Morris et al. 2000). The Mesaverde Formation is 

conformable with the underlying Masuk Member of the 

Mancos Shale. 

Cretaceous – Tertiary Laramide Tectonics 

The regional folds in Capitol Reef are products of the 

Laramide Orogeny (about 75-35 Ma), which resulted 

when the North American lithospheric plate, moving 

westward, collided with the Farallon lithospheric plate, 

moving relatively eastward. The oceanic crust of the 

Farallon plate was subducted beneath the less dense 

continental crust of the North American plate. The 

sedimentary rocks at Capitol Reef responded to the 

collision mostly by folding in a plastic fashion and 

although some faulting occurred, no major faults cut the 

sedimentary rocks at the surface. 

The Waterpocket Fold monocline resulted from a 

reverse fault at depth (Billingsley et al. 1987; Morris et al. 

2000). When the Waterpocket Fold monocline formed, 

brittle Precambrian rocks at depth ruptured due to westsouthwest compressional forces and the Precambrian 

section detached and moved eastward along a reverse 

fault or a series of reverse faults. The overlying 

sedimentary strata, being more ductile than the 

Precambrian rocks, draped over the fault forming the 

monocline. 

The asymmetry of the folds in Capitol Reef and the 

coincident northwest trends suggest that these folds 

formed at about the same time, probably due to the same 

northeast directed compressive stress that generated the 

thrust fault at depth. Like a throw rug on a wooden floor, 

the surface strata deformed into a series of folds as the 

deeply buried Precambrian basement rocks were 

displaced by the thrust. 
 CARE Geologic Resource Evaluation Report 31

Cenozoic Era 

Tertiary Period 

Near the end of the Laramide Orogeny, about 26-35 

million years ago, in early mid-Tertiary time, volcanic 

activity again erupted across the Colorado Plateau. A 

volcanic field covered the northern quarter of Capitol 

Reef from approximately 4.6 to 3.7 million years ago. The 

igneous dikes and sills mapped in Capitol Reef served as 

a feeder system to a large volcanic field that has 

subsequently eroded away (Gartner 1986; Delaney and 

Gartner 1997; Morris et al. 2000). 

The laccoliths that formed the Sleeping Ute Mountain, 

La Plata Mountains, Henry Mountains, La Sal 

Mountains, and Abajo Mountains were emplaced by 

mid-Tertiary volcanism (figure 2) (Baars 2000: Fillmore 

2000). The Henry Mountains laccolith is part of the vista 

seen from both Canyonlands National Park and Capitol 

Reef National Park. 

A vast outpouring of lava spread over southern Utah 

from about 6.5 to 3.4 Ma (Fillmore 2000). Rather than 

erupting from volcanoes, the lava flowed from numerous 

fissures in the landscape. The lava formed thin, basalt 

layers that resisted erosion and today cap many of the 

plateaus and mesas on the Colorado Plateau including 

the Aquarius and Thousand Lakes Plateaus. Basalts 

constitute the bulk of the igneous rocks that cover about 

259 square km (100 square mi) of the Capitol Reef area, 

west of the park boundary (Smith et al. 1963). 

The Flagstaff Limestone (about 58 to 35 Ma), exposed 

northwest of the park boundary, is the only record of 

Tertiary sedimentary deposition in the Capitol Reef 

region. The Flagstaff is a lacustrine limestone that 

formed in Lake Uinta from 58 to 35 million years ago 

(Morris et al. 2000). The locally abundant tuffaceous 

beds are the result of extensive volcanic ash fall. 

Uplift of the Colorado Plateau 

Late Cretaceous marine shoreline sediments were 

deposited near sea level. Today, these shoreline deposits 

are found on the Colorado Plateau at several thousand 

feet in elevation. Since the end of the Cretaceous Period 

66 million years ago, the Colorado Plateau has risen 

about 3,660 m (12,000 ft) (Fillmore 2000). Erosion began 

to strip away the highlands, exposing the structure of the 

Waterpocket Fold and creating the domes, cathedrals, 

and other spectacular desert landforms for which 

Capitol Reef is famous. 

Some of this uplift occurred quite rapidly in geologic 

time. As the rate of uplift increased, so did the rate of 

erosion. The Colorado River, for example, carved its 

present course within the last 6 million years. 

The Colorado Plateau has been subjected to repeated 

minor uplifts since the end of the last ice age. Today, the 

climate is drier than during the Pleistocene ice ages yet 

the intermittent streams in the canyons are still in a 

period of active downcutting, only more slowly than in 

the past. Like other parts of the Canyonlands section of 

the Colorado Plateau, the geologic units that form the 

cliffs, slopes, benches, domes, natural bridges, and other 

physiographic features reflect their varying susceptibility 

to erosion. 

Quaternary Period 

During the Pleistocene epoch (1.6 to 0.01 Ma), extensive 

deposits of pediment gravels, boulder deposits, glacial 

till, outwash, and landslide material accumulated in the 

Capitol Reef region (Smith et al. 1963). Pediment gravels 

that cap many of the flat-topped hills and benches in the 

Capitol Reef area are believed to have been deposited 

more than 75,000 years B.P. (Smith et al. 1963). 

Like the pediment gravels, the boulder deposits were 

probably once covered by a deep soil that has largely 

been removed, leaving only the caliche or carbonate-rich 

lower layer. The advanced dissection of the boulder 

deposits indicates a period of erosion that destroyed the 

original topographic forms associated with the boulders. 

The glacial drift on and around the Aquarius Plateau has 

not been directly dated, but geologists speculate that the 

deposits range in age from 70,000 years to about 12,000 

years B.P. (Fillmore 2000). As the climate cooled during 

the Wisconsin glacial stage and precipitation increased, a 

large icecap formed on top of Boulder Mountain. Long 

tongues of ice moved down several valleys carving into 

the mountain rim. Glacial moraines formed with each 

advance and retreat of the glaciers. In places, up to 60 m 

(200 ft) of till was deposited. A broad ice tongue 

extended into the lowlands near Grover, southwest of 

Fruita, Utah, to an altitude of about 2,100 m (7,000 ft) 

(Smith et al. 1963). 

The top of Boulder Mountain was scoured by Wisconsin 

glacial ice. Unweathered volcanic rock is exposed as bare 

rock knolls and roche moutonneés. Volcanic rock also 

underlies shallow basins and is thinly veneered with drift 

throughout the area. Volcanic flow surfaces have been 

abraded and grooved by glacial ice. The alignment of the 

grooves and of linear topographic depressions revealed 

on aerial photographs, records the radial direction of ice 

movement from the top of Boulder Mountain (Smith et 

al. 1963). 

Melt water flowed from these valleys and spread 

outwash gravels along the drainage routes. Outwash 

sediments carried by meltwater streams subsequently 

formed a deltaic fan in the Fremont River Valley. The fan 

dammed the river to form a glacial lake in which sandy 

lake sediments were deposited. 

Rain-saturated slopes collapsed in areas not covered by 

ice and formed landslide deposits on the flanks of 

Boulder and Thousand Lake Mountains. Most mass 

movements in the Capitol Reef area probably took place 

during or shortly after Wisconsin glaciation when 

precipitation was high and the ground was saturated 

(Smith et al. 1963). 

Terrace gravels and sands along the Fremont River and 

its tributaries may hold the key to the age of glaciation in 
 NPS Geologic Resources Division 32 

the Capitol Reef area. Recent isotope analyses of 

beryllium-10 and aluminum-26 from three widely 

preserved terraces revealed ages of about 60,000 years, 

102,000 years, and 151,000 years B.P. (Fillmore 2000). 

These ages, however, are quite a bit older than the 

previous interpretations of 12,000 B.P. If the age dates 

hold up to repeated testing, then glacial and interglacial 

activity occurred over a much longer time frame than 

was previously thought. 

Following the Wisconsin glacial stage, a warming trend 

melted the glacial ice completely from the region and 

deposits of alluvium, colluvium, alluvial fan, and rock 

glaciers became the dominant sediments. 

The most recent erosional history involves dissection of 

the alluvial deposits and continued downcutting. Streams 

have entrenched about 8 m (26 ft) along Bullberry Creek 

just east of Teasdale and about 3 m (10 ft) along lower 

Donkey Creek. Some of the best agricultural land is being 

destroyed by erosion of the alluvium. Livestock grazing 

accelerates stream bank erosion by trampling and 

denuding vegetation destabilizing the fluvial regime. 

Both climate and grazing have played a part in the rate of 

erosion and entrenchment of the alluvium (Smith et al. 

1963). Streams also continue to erode the gorges that 

have been carved into the Waterpocket Fold.
 CARE Geologic Resource Evaluation Report 33

Figure 10. Geologic time scale; adapted from the U.S. Geological Survey and International Commission on Stratigraphy. Red lines indicate 

major unconformities between eras. Included are major events in life history and tectonic events occurring on the North American continent. 

Absolute ages shown are in millions of years. 
 NPS Geologic Resources Division 34 

Figure 11. Lower Permian depositional environments in southeastern Utah during deposition of the Cedar Mesa Sandstone. CARE: Capitol 

Reef National Park. Modified from Huntoon and others (2000). 

Figure 12. Unconformities and depositional sequences in the Permian of the Colorado Plateau. Shaded areas indicate gaps in time between 

depositional episodes. Yellow shading indicates rocks exposed at Capitol Reef National Park. Modified from Blakey (1996). 
 CARE Geologic Resource Evaluation Report 35

Figure 13. Paleogeographic map of the Lower Triassic, Moenkopi Formation during the second transgressive episode of the Early Triassic 

(Black Dragon and Sinbad Limestone members). CARE: Capitol Reef National Park. Modified from Dubiel (1994). 

Figure 14. Paleogeographic map of the fluvial system in the Upper Triassic. CARE: Capitol Reef National Park. UN: Uncompahgre uplift; SL: 

San Luis uplift; FR: Front Range uplift. Highlands are shaded a solid gray. Modified from Dubiel (1994). 
 NPS Geologic Resources Division 36 

Figure 15. Lower Jurassic paleogeography. Thick arrows indicate eolian transport of sand. Thin arrows on Mogollon Slope indicate fluvial 

transport of sediments. Gray shading shows the location of the volcanic arc. Saw teeth indicate the location of the subduction zone with the 

teeth on the overriding, upper lithospheric plate. CARE: Capitol Reef National Park. Modified from Lawton (1994). 
 CARE Geologic Resource Evaluation Report 37

Figure 16. Middle Jurassic paleogeography during deposition of the Entrada Sandstone. Note that the northern marine environments have 

eliminated the sand source to the north (compare with Figure 18), yet Entrada ergs are widespread. CARE: Capitol Reef National Park. 

Modified from Peterson (1994). 
 NPS Geologic Resources Division 38 

Figure 17. Upper Jurassic paleogeography. Thin arrows indicate fluvial dispersal. Thick arrows indicate wind directions. Saw teeth indicate 

the location of the subduction zone with the teeth on the overriding, upper lithospheric plate. Note the possible marine environment to the 

east where continental environments were previously established. The alluvial plain expanded to the east with time. CARE: Capitol Reef 

National Park. Modified from Lawton (1994). 
 CARE Geologic Resource Evaluation Report 39

Figure 18. Location of the Cretaceous Period, Western Interior Seaway. Shaded areas indicate land above sea level. North indicates the 

Cretaceous north. Modified from Rice and Shurr (1983). 
 NPS Geologic Resources Division 40 

Figure 19. Upper Cretaceous paleogeography at the time of deposition of the Tununk Shale Member of the Mancos Shale. Saw teeth mark 

the leading edge of thrust faulting with the teeth on the overriding plate. Modified from Elder and Kirkland (1994). 
 CARE Geologic Resource Evaluation Report 41

Glossary 

This glossary contains brief definitions of technical geologic terms used in this report. Not all 

geologic terms used are referenced. For more detailed definitions or to find terms not listed 

here please visit: http://wrgis.wr.usgs.gov/docs/parks/misc/glossarya.html. 

alluvial fan. A fan-shaped deposit of sediment that 

accumulates where a high gradient stream flows out of 

a mountain front into an area of lesser gradient such as 

a valley. 

angular unconformity. An unconformity where the strata 

above and below are oriented differently; generally 

caused by structural deformation and erosion prior to 

deposition of the upper bed. 

basement. The undifferentiated rocks, commonly 

igneous and metamorphic, that underlie the rocks of 

interest. 

braided stream. A stream, clogged with sediment that 

forms multiple channels that divide and rejoin. 

breccia. A coarse-grained, generally unsorted, 

sedimentary rock consisting of cemented angular 

clasts. 

carbonaceous. A rock or sediment with considerable 

carbon, esp. organics, hydrocarbons, or coal. 

continental crust. The type of crustal rocks underlying 

the continents and continental shelves; having a 

thickness of 25-60 km (16-37 mi) and a density of 

approximately 2.7 grams per cubic centimeter. 

continental shelf. The shallowly-submerged portion of a 

continental margin extending from the shoreline to the 

continental slope with water depths of less than 200 m 

(656 ft). 

craton. The relatively old and geologically stable interior 

of a continent (also see continental shield). 

cross-bedding. Uniform to highly-varied sets of inclined 

sedimentary beds deposited by wind or water that 

indicate distinctive flow conditions. 

crust. The outermost compositional shell of Earth, 10-40 

km (6-25 mi) thick, consisting predominantly of 

relatively low-density silicate minerals (also see 

oceanic crust and continental crust). 

debris flow. A rapid and often sudden flow or slide of 

rock and soil material involving a wide range of types 

and sizes. 

dike. A tabular, discordant igneous intrusion. 

dip. The angle between a structural surface and a 

horizontal reference plane measured normal to their 

line of intersection. 

eolian. Formed, eroded, or deposited by or related to the 

action of the wind. 

facies (sedimentary). The depositional or environmental 

conditions reflected in the sedimentary structures, 

textures, mineralogy, fossils, etc. of a sedimentary 

rock. 

fold axis. A line connecting the points of maximum 

curvature of the bedding in a fold (hinge line). 

karst topography. Topography characterized by 

abundant sinkholes and caverns formed by the 

dissolution of calcareous rocks. 

kettle. A bowl-shaped depression in glacial drift formed 

by the melting of a large block of ice left by a glacier; 

often contain a lake or swamp. 

laccolith. A concordant igneous intrusion with a domed 

or convex-up roof and flat floor. 

lithosphere. The relatively rigid outmost shell of Earth’s 

structure, 50 to 100 km (31 to 62 mi) thick, that 

encompasses the crust and uppermost mantle. 

monocline. A one-limbed flexure in strata, which are 

usually flat-lying except in the flexure itself. 

normal fault. A dip-slip fault in which the hanging wall 

moves down relative to the footwall. 

orogeny. A mountain-building event, particularly a wellrecognized event in the geologic past (e.g. the 

Laramide orogeny). 

paleosol. A soil formed in the past with distinctive 

characteristics resulting from a soil- forming 

environment that no longer exists. 

pediment. A gently sloping, erosional bedrock surface at 

the foot of mountains or plateau escarpments. 

red beds. Sedimentary strata composed largely of 

sandstone, siltstone, and shale that are predominantly 

red due to the presence of ferric oxide (hematite) 

coating individual grains. 

regression. A long-term seaward retreat of the shoreline 

or relative fall of sea level. 

reverse fault. A contractional, high angle (>45o), dip-slip 

fault in which the hanging wall moves up relative to the 

footwall (also see thrust fault). 

roche moutonneé. A small (usually a few meters) 

elongate knob of bedrock sculpted by a large glacier 

oriented in the direction of ice movement. 

sabkha. A coastal environment in an arid climate where 

evaporation rates are high. 

sill. A tabular, igneous intrusion that is concordant with 

the country rock. 

strike. The compass direction of the line of intersection 

that an inclined surface makes with a horizontal plane. 

subduction zone. A convergent plate boundary where 

oceanic lithosphere descends beneath a continental or 

oceanic plate and is carried down into the mantle. 

tectonic. Relating to large-scale movement and 

deformation of Earth’s crust. 

till. Unsorted, unstratified, unconsolidated mixture of 

clay, silt, sand, gravel and boulders left by a glacier. 

trace (fault). The exposed intersection of a fault with 

Earth’s surface. 

transgression. Landward migration of the sea due to a 

relative rise in sea level. 

unconformity. A surface within sedimentary strata that 

marks a prolonged period of nondeposition or 

erosion. 
 NPS Geologic Resources Division 42 

References 

This section provides a listing of references cited in this report. A more complete geologic 

bibliography is available and can be obtained through the NPS Geologic Resources Division. 

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Billingsley, G. H., Huntoon, P. W., and Breed, W. J., 1987, 

Geologic Map of Capitol Reef National Park and 

Vicinity, Utah: Utah Geological and Mineral Survey, 

Map 87, scale 1;62,000, 4 plates. 

Blakey, R. C., 1994, Paleogeographic and tectonic 

controls on some Lower and Middle Jurassic erg 

deposits, Colorado Plateau, in Mario V. Caputo, James 

A. Peterson, and Karen J. Franczyk, eds., Mesozoic 

Systems of the Rocky Mountain Region, USA: Rocky 

Mountain Section, SEPM (Society for Sedimentary 

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Blakey, R.C., 1996, Permian eolian deposits, sequences, 

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Longman and M.D. Sonnenfeld, eds., Paleozoic 

Systems of the Rocky Mountain Region: Rocky 

Mountain Section, SEPM (Society for Sedimentary 

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Brown, K. W. and Ritzma, H. R., 1982, Oil and gas fields 

and pipelines of Utah: Utah Geological and Mineral 

Survey, Map 61, Scale 1:750,000. 

Campbell, J.A., 1980, Lower Permian depositional 

systems and Wolfcampian paleogeography, 

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Mineralogists (SEPM), Rocky Mountain Section, p. 

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Campbell, J. A. and Bacon, R. S., 1976, Penetration chart 

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Christiansen, E. II, Kowallis, B. J., and Barton, M. D., 

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Cole, R.D., Moore, G.E., Trevena, A.S., Armin, R.A., and 

Morton, M.P., 1996, Lithofacies definition in Cutler 

and Honaker Trail Formations, Northeastern Paradox 

Basin, by sedimentologic observations and spectral 

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Paradox Basin: Utah Geological Association 

Guidebook 25, p. 169-178. 

Condon, S. M., 1991, Geologic and structure contour 

map of the Ute Mountain Ute Indian Reservation and 

adjacent areas, southwest Colorado and northwest 

New Mexico: USGS Map I-2083, Scale: 1:100,000. 

Delaney, P.T., and Gartner, A.E., 1997, Physical 

processes of shallow mafic dike emplacement near the 

San Rafael Swell, Utah: Geological Society of America 

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Doelling, H. H., 1983, Non-metallic mineral resources of 

Utah: Utah Geological and Mineral Survey, Map 71, 

Scale 1:750,000. 

Doelling, H. H., 2000, Geology of Arches National Park, 

Grand County, Utah, in D.A. Sprinkel, T.C. Chidsey, 

Jr., and P.B. Anderson, eds., Geology of Utah’s Parks 

and Monuments: Utah Geological Association 

Publication 28, p. 11-36. 

Doelling, H. H. and Tooker, E. W., 1983, Utah mining 

district areas and principal metal occurrences: Utah 

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1:750,000. 

Dubiel, R.F., 1987, Sedimentology of the Upper Triassic 

Chinle Formation, Southeastern, Utah: Boulder, 

Colorado, University of Colorado, Ph.D. dissertation, 

132 p. 

Dubiel, R. F., 1994, Triassic deposystems, 

paleogeography, and paleoclimate of the Western 

Interior, in M. V. Caputo, J. A. Peterson, and K. J. 

Franczyk, eds., Mesozoic Systems of the Rocky 

Mountain Region, USA: Rocky Mountain Section, 

SEPM (Society for Sedimentary Geology), Denver, 

CO., p. 133-168. 

Dubiel, R. F., Huntoon, J. E., Condon, S. M., Stanesco, J. 

D., 1996, Permian deposystems, paleogeography, and 

paleoclimate of the Paradox Basin and vicinity, in 

M.W. Longman and M.D. Sonnenfeld, eds., Paleozoic 

Systems of the Rocky Mountain Region: Rocky 

Mountain Section, SEPM (Society for Sedimentary 

Geology), p. 427-444. 
 CARE Geologic Resource Evaluation Report 43

Dutton, C.E., 1880, Geology of the High Plateaus of 

Utah: U.S. Geographical and Geological Survey of the 

Rocky Mountain Region. 

Elder, W. P. and Kirkland, J. I., 1994, Cretaceous 

paleogeography of the southern Western Interior 

Region, in M. V. Caputo, J. A. Peterson, and K. J. 

Franczyk, eds., Mesozoic Systems of the Rocky 

Mountain Region, USA: Rocky Mountain Section, 

SEPM (Society for Sedimentary Geology), Denver, 

CO., p. 415-440. 

Fillmore, R., 2000, The Geology of the Parks, 

Monuments and Wildlands of Southern Utah: The 

University of Utah Press, 268 p. 

Fouch, T.D., Lawton, T.F., Nichols, D.J., Cashion, W.B., 

and Cobban, W.A., 1983, Patterns and timing of 

synorogenic sedimentation in Upper Cretaceous rocks 

of Central and Northeast Utah, in M. W. Reynolds and 

E. D. Dolly, eds., Mesozoic Paleogeography of the 

West-Central United States: Rocky Mountain 

Paleogeography Symposium 2, Rocky Mountain 

Section, Society of Economic Paleontologists and 

Mineralogists (SEPM), p. 305-336. 

Fouret, K. L., 1996, Depositional and diagenetic 

environments of the Mississippian Leadville 

Limestone at Lisbon Field, Utah, in A.C. Huffman, Jr., 

W.R. Lund, and L.H. Godwin, eds., Geology and 

Resources of the Paradox Basin: Utah Geological 

Association Guidebook 25, p. 133-138. 

Gardner, M. H. and Cross, T. A., 1994, Middle 

Cretaceous paleogeography of Utah, in M. V. Caputo, 

J. A. Peterson, and K. J. Franczyk, eds., Mesozoic 

Systems of the Rocky Mountain Region, USA: Rocky 

Mountain Section, SEPM (Society for Sedimentary 

Geology), Denver, CO., p. 1471-502. 

Gartner, A.E., 1986, Geometry, emplacement history, 

petrography, and chemistry of a basaltic intrusive 

complex, San Rafael and Capitol Reef areas, Utah: 

U.S.G.S. Open-Rile Report 86-61, 112 p. 

Harr, C. L., 1996, Paradox oil and gas potential of the Ute 

Mountain Ute Indian Reservation, in A.C. Huffman, 

Jr., W.R. Lund, and L.H. Godwin, eds., Geology and 

Resources of the Paradox Basin: Utah Geological 

Association Guidebook 25, p. 13-28. 

Haynes, D. D., Vogel, J. D., and Wyant, D G., 1972, 

Geology, structure, and uranium deposits of the 

Cortez Quadrangle, Colorado and Utah: USGS Map I629, Scale 1:250,000. 

Hintze, L.F., 1988, 1993, Geologic history of Utah: 

Brigham Young University Studies Special Publication 

7, 202 p. 

Huntoon, J. E., Dolson, J. C., and Henry, B. M., 1994, 

Seals and migration pathways in paleogeomorphically 

trapped petroleum occurrences: Permian White Rim 

Sandstone, Tar-Sand Triangle area, Utah: in J. C. 

Dolson, M. L. Hendricks, and W. A. Wescott, eds., 

Unconformity-Related Hydrocarbons in Sedimentary 

Sequences: Rocky Mountain Association of 

Geologists, p. 99-118. 

Huntoon, J. E., Stanesco, J. D., Dubiel, R. F., and Dougan, 

J., 2000, Geology of Natural Bridges National 

Monument, Utah, in D.A. Sprinkel, T.C. Chidsey, Jr., 

and P.B. Anderson, eds., Geology of Utah’s Parks and 

Monuments: Utah Geological Association Publication 

28, p. 233-250. 

Kauffman, E. G., 1977, Geological and biological 

overview: Western Interior Cretaceous Basin: 

Mountain Geologist, v. 14, p. 75-99. 

Kiver, E.P., and Harris, D.V., 1999, Geology of U.S. 

Parklands: John Wiley & Sons, Inc., New York, p. 466-

478. 

Koch, Alison L., and Santucci, Vincent L., 2002, 

Paleontological Resource Inventory and Monitoring 

Northern Colorado Plateau Network: National Park 

Sercice, TIC #D-206, p. 18-21. 

Kocurek, G. and Dott, R. H. Jr., 1983, Jurassic 

paleogeography and paleoclimate of the central and 

southern Rocky Mountain region, in M. W. Reynolds 

and E. D. Dolly, eds., Mesozoic Paleogeography of the 

West-Central United States: Rocky Mountain Section, 

SEPM (Society for Sedimentary Geology), Denver, 

CO., p. 101-118. 

Lawton, T. F., 1994, Tectonic setting of Mesozoic 

sedimentary basins, Rocky Mountain region, United 

States, in M. V. Caputo, J. A. Peterson, and K. J. 

Franczyk, eds., Mesozoic Systems of the Rocky 

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SEPM (Society for Sedimentary Geology), Denver, 

CO., p. 1-26. 

Loope, D.B., 1984, Eolian origin of Upper Paleozoic 

sandstones, southeastern Utah: Journal of Sedimentary 

Petrology, v. 54, no. 2, p. 563-580. 

Martin, L., 1998, Capitol Reef National Park drinking 

water source protection plan Fremont River Gorge 

well: Water Resources Division, NPS, 22 p. and 

appendices. 

Mickelson, D.L., 2004, The diversity and stratigraphic 

distribution of pre-dinosaurian communities from the 

Triassic Moenkopi Formation, Capitol Reef National 

Park and Glen Canyon National Recreation Area, 

Utah: Park Paleontology, v. 8, no. 1, p. 1-4. 

Moore, D. M. and Reynolds, R. C., Jr., 1989, X-ray 

Diffraction and the Identification and Analysis of Clay 

Minerals: Oxford University Press, New York, 332 p. 
 NPS Geologic Resources Division 44 

Morris, T., H., Manning, V. W., and Ritter, S. M., 2000, 

Geology of Capitol Reef National Park, Utah: in D.A. 

Sprinkel, T.C. Chidsey, Jr., and P.B. Anderson, eds., 

Geology of Utah’s Parks and Monuments: Utah 

Geological Association Publication 28, p. 85-106. 

Mustoe, G.E., 1983, Cavernous weathering in the Capitol 

Reef Desert, Utah: Earth Surface Processes and 

Landforms, John Wiley and Sons Ltd., New York, v. 8. 

Nuccio, V. F. and Condon, S. M., 1996, Burial and 

thermal history of the Paradox Basin, Utah and 

Colorado, and petroleum potential of the Middle 

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57-76. 

Petersen, L.M., and Roylance, M.M., 1982, Stratigraphy 

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Brigham Young University Geology Studies, v. 29, pt. 

2, p. 1-12. 

Peterson, F., 1994, Sand dunes, sabkhas, stream, and 

shallow seas: Jurassic paleogeography in the southern 

part of the Western Interior Basin, in M. V. Caputo, J. 

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Peterson, F., Ryder, F.T., and Law, B.E., 1980, 

Stratigraphy, sedimentology, and regional 

relationships of the Cretaceous System in the Henry 

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Rice, D. D. and Shurr, G. W., 1983, Patterns of 

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northern Great Plains, in M. W. Reynolds and E. D. 

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Quarry, Mesa Country, Colorado, in K. Carpenter, 

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Sageman, B. B. and Arthur, M. A., 1994, Early Turonian 

paleogeographic/paleobathymetric map, Western 

Interior, U.S., in M. V. Caputo, J. A. Peterson, and K. J. 

Franczyk, eds., Mesozoic Systems of the Rocky 

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SEPM (Society for Sedimentary Geology), Denver, 

CO., p. 457-470. 

Santucci, V.L., Hunt, A.P., and Lockley, M.G., 1998, 

Fossil Vertebrate Tracks in National Park Service 

Areas: Dakoterra Volume 5, p. 108-110. 

Silberling, N. J. and Roberts, R. J., 1962, Pre-Tertiary 

stratigraphy and structure of northwestern Nevada: 

GSA Special Paper 72, 58 p. 

Smith, F.J, Jr., Huff, L.C., Hinrichs, E.N., and Luedke, 

R.G., 1963, Geology of the Capitol Reef Area, Wayne 

and Garfield Counties, Utah: U.S.G.S. Professional 

Paper 102, p. 1-98. 

Stewart, J.H., Poole, F.G., and Wilson, R. F., 1972A, 

Stratigraphy and origin of the Triassic Moenkopi 

formation and related strata in the Colorado Plateau 

region with a section on sedimentary petrology by R.A. 

Cadigan: USGS Prof Paper 691, 195 p. 

Stewart, J.H., Poole, F.G., and Wilson, R. F., 1972B, 

Stratigraphy and origin of the Chinle Formation and 

related Upper Triassic strata in the Colorado Plateau 

region with a section on sedimentary petrology by R.A. 

Cadigan and on conglomerate studies by W. 

Thordarson, H.F. Albee, and J.H. Stewart: USGS Prof 

Paper 690, 336 p. 

Stewart, J.H., Williams, G.A., Albee, H.F., and Raup, O.B., 

1959, Stratigraphy of Triassic and associated 

formations in part of the Colorado Plateau region: 

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Definition of members of Jurassic Entrada Sandstone 

in east-central Utah and west-central Colorado: 

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Bulletin, v. 46, no. 11, p. 2057-2070. 
 CARE Geologic Resource Evaluation Report 45

Appendix A: Geologic Map Graphic 

The following page provides a preview or “snapshot” of the geologic map for Capitol 

Reef National Park. For a poster size PDF of this map or for digital geologic map data, 

please see the included CD or visit the GRE publications webpage: http://www2.nature. 

nps.gov/geology/inventory/gre_publications.cfm 

 CARE Geologic Resource Evaluation Report 47

Appendix B: Scoping Summary 

The following excerpts are from the GRI (now GRE) scoping summary for Capitol Reef 

National Park. The scoping meeting occurred September 27-28, 1999; therefore, the 

contact information and Web addresses referred to herein may be outdated. Please 

contact the Geologic Resources Division for current information. 

Joe Gregson (NPS-NRID) presented an overview of the 

NPS I&M Program, the status of the natural resource 

inventories, and the GRI. Geologists familiar with GIS 

methods were quite impressed with the method of 

displaying geologic maps digitally, which Joe and NRID 

have developed. 

Bruce Heise (NPS-GRD) followed with an overview of 

the GRD and GRI and outlined the following main goals 

of the program: to assemble a bibliography of associated 

geological resources for NPS units with significant 

natural resources, to compile and evaluate a list of 

existing geologic maps for each unit, to develop digital 

geologic map products, and to complete a geological 

report that synthesizes much of the existing geologic 

knowledge about each park. 

Heise emphasized that the inventory is not to routinely 

initiate new geologic mapping projects, but to aggregate 

existing information and identify where serious geologic 

data needs and issues exist in the NPS. 

Interpretation 

The GRI also aims to help promote geologic resource 

interpretation within the parks. GRD has staff and 

technology to assist in preparation of useful materials 

including developing site bulletins and resource 

management proposal (RMP) statements appropriate to 

promoting geology. 

UGA Guidebook of Utah’s National and State Park Areas 

In 1999, Doug Sprinkel (UGA) announced the 

compilation of a guidebook that would treat the geology 

of Utah’s national and state parks and monuments. This 

guidebook was published in 2000, and while some of the 

guidebook may be too technical for non-geologists, the 

publication should be a part of every Utah park’s library. 

The reference is: 

• D.A. Sprinkel, T.C. Chidsey, Jr., and P.B. Anderson, 

eds., Geology of Utah’s Parks and Monuments: Utah 

Geological Association Publication 28. 

Soils Mapping Status 

Pete Biggam (GRD) oversees the soil mapping program, 

and he handed out an overview of the current status of 

soils maps for Capitol Reef National Park (CARE). 

Questions regarding soil mapping or interpretation 

should be directed to Pete. 

Paleontological and other natural resources 

Vince Santucci (NPS) presented an overview of 

paleontological resources for CARE. Paleontology is not 

currently part of the first level of the I&M program. 

Tom Clark (CARE-natural resources) is interested in 

having a paleontological survey conducted for CARE 

similar to the studies completed for Zion, Yellowstone, 

and Death Valley. Surveys of this type often uncover 

valuable, new information on previously unrecognized 

resources. Participants suggested that if additional 

significant findings occur, paleontological resource 

management plans should be produced for CARE 

involving some inventory and monitoring to identify 

human and natural threats to these resources. 

Collections taken from CARE and that now reside in 

outside repositories should be identified for inventory 

purposes. Special concern was noted for the protection 

of paleontological resources because of the “black 

market” fossil trade that has become quite lucrative and 

often results in illegal collecting from federal lands. 

In 1999, significant paleontological resources for CARE 

included the following: 

• Both invertebrate and vertebrate traces from the 

Moenkopi and Chinle formations 

• Vertebrate tracks in the Kayenta Formation 

• Dinosaur bones in the Morrison Formation 

• Petrified trees in Salt Wash Member of the Morrison 

Formation outside the park boundary; some also near 

the Terry mines 

• Cretaceous suite of marine invertebrates in Tununk 

Shale (Griffia movaria, Exogyra); oyster shell reef in 

Dakota Sandstone 

• Pack-rat middens 

• Ammonite zone in the Moenkopi Formation 

• Pentacrinus zones in Sinbad Member of the Carmel 

Formation 

Also mentioned were the current cases involving mineral 

and fossil poaching from CARE. Rock hounds have 

targeted the numerous “sunset” agate concretions in the 

Tidwell Member of the Morrison Formation, and 

gypsum crystals are also in high demand. Phil Cloues 

(GRD Mineral Economist) may be contacted for 

additional information. 
 NPS Geologic Resources Division 48 

Geologic Mapping 

The following digital geologic map product that was 

projected for completion by December, 1999, has been 

completed and is now available: 

• Billingsley, G. H., Huntoon, P. W., and Breed, W. J., 

1987, Geologic Map of Capitol Reef National Park and 

Vicinity, Utah: Utah Geological and Mineral Survey, 

Map 87, scale 1:62,500, 4 plates. 

At the workshop, additional improvements to the 

current coverage were noted that might be desirable for 

certain resource issues such as roads, campgrounds, 

vegetation, soil, and wastewater. 

The following mapping improvements at a 1:24,000 scale 

were suggested. Contact Tim Connors (GRD) as to the 

status of these improvements. 

• More detailed mapping of surficial units along the 

Fremont River 

• Identification and placement of new map units not on 

existing 62,500 scale map. 

• Mapping of gravel terraces that tell an important 

geologic story about CARE 

• Mapping mountain top boulder deposits since they 

have an important role in groundwater recharge and 

geologic hazard identification 

• Joint systems need to be incorporated onto the 

existing map and are important to the groundwater 

story 

• Delineating range management and endangered 

species areas 

• Waterpocket Fold 

• Burr Trail (for hazard assessments); Wagon box Mesa, 

The Post, and Bitter Creek Divide were all mentioned 

by name along this route 

• Heavy use areas (“threshold zone/backcountry”) such 

as the Fruita-Scenic Drive (Twin Rocks, Fruita, and 

Golden Throne 24,000 scale quadrangles). 

Other Sources of Natural Resources Data 

• Participants noted that the UGS has a significant 

quadrangle database that they have furnished to NRID 

for the entire state of Utah. Contact Tim Connors for 

details. 

• NRID has compiled a geologic bibliography for 

numerous parks and monuments including Capitol 

Reef NP. The website has undergone some changes 

since 1999. Contact Wendy Schumacher (NRID) 

(Wendy_Schumacher@nps.gov, 970-225-3548) for the 

current user id and password. 

• Abandoned Mineral Land (AML) database by John 

Burghardt (GRD). Noted at the workshop were 

several reports from GRD on the Oyler, Terry and 

Rainy Day mine closures that existed in addition to 

inventories for several other sites within CARE. Three 

of ten sites were mitigated. At the time, there were 27 

openings at 10 sites inventoried. All of the sites were 

uranium mines. Contact John Burghardt (GRD) for 

updated information (John_Burghardt@nps.gov). 

• Smith, J.F. Jr., Huff, L.C., Hinrichs, E.N., and Luedke, 

R.G., 1963, Geology of Capitol Reef Area, Wayne and 

Garfield Counties, Utah: USGS Professional Paper 

363. 

• Davis, G., 1999?, Structural Geology of the Colorado 

Plateau Region of Southern Utah with Special 

Emphasis on Deformation Bands: Geological Society 

of America Special Paper 342, (specifically thanks 

CARE staff for their cooperation). 

• Allyson Mathis has maintained a database on CARE 

geologic features that was mentioned at the meeting, 

but needs still to be obtained by GRD (as of 

workshop). 

• Engelmanns GPS locations from Morrison Ecosystem 

study 

• Previously mentioned digital geologic map from 

Billingsley and others, 1987, map with fault layers 

• UGS paper and digital 1:100,000 scale coverages of the 

Escalante and Hites Crossing sheets 

• Soils data from NRCS 

Geologic Hazards 

The following were recognized as geologic hazards at the 

1999 workshop: 

• Rockfalls 

• Floods 

• Debris flows 

• Uranium/radon 

• Expansive clays 

• Old adits from AML sites 

• Faults: closest active fault is on the west side of plateau 

according to Grant Willis (UGS). Allyson Mathys 

(NPS) thinks there is an active fault somewhere next to 

Needles with a report on it (source unknown). Tom 

(Clark?) says a 3.8 earthquake shook the area in the 

Spring, 1999, up Fremont River\ 

• Water quality issues for the Water Resources Division 

(WRD) 

Potential Research Topics for Capitol Reef NP 

Participants at the workshop listed the following as 

potential research topics: 

• Paleo current directions in Kayenta time 

• Black boulder debris flows 

• Track studies by Kirby and McAllister 

• Possible new tracksite in Moenkopi (from Jackie 

Huntoon) 

• Study playa deposits in Cottonwood Wash in Navajo 

Sandstone for flood events 

• Joint systems/fracture study for entire park for water 

quality issues 
 CARE Geologic Resource Evaluation Report 49

• Study selenite deposits and structure of gypsum 

sinkhole 

• Terrace deposits (rework late Cenozoic history of 

park); hasn’t been done well to this point in time 

(1999). 

• Study origin of honeycomb weathering patterns 

• Soft sediment deformation in Navajo and Entrada 

Formations 

• Conduct full Paleontological survey 

• Study depositional environments of earthy Entrada 

facies, Curtis, Summerville, Morrison Formations, etc. 

• Chinle Ecosystem study (for Russ Dubiel, then at 

USGS)\ 

• Dike/sill emplacement history, petrology, depth of 

source and emplacement and relate to uplift and 

erosion story of Colorado Plateau 

• Study structure of Waterpocket Fold at depth 

• Tie soil chemistry to rare plants; overall soil 

characterization 

• Tie CARE story to adjacent areas for interpreters to 

present to public 

• Inventory commercially valuable minerals for 

collecting 

• Study entrenched meanders along Fremont River, 

Halls Creek drainage, Sulfur Creek 

Disturbed Lands 

Disturbed lands/abandoned mineral lands issues at 

CARE include the following: 

• There are AML summaries from GRD that are in GIS 

layer already; according to John Burghardt (GRD) 3 of 

10 sites mitigated (Oyler, Terry, Rainy Day). There are 

27 openings at the 10 sites 

• Preliminary (in 1999) disturbed lands map GIS layer 

exists according to Tom Clark for roads they want 

closed, cattle ponds, dams, tanks, etc. 

• Some small borrow pits may be along the Burr Trail; 

also Notom Road has some low-grade coal near 

Highway 24 East in Carmel 

• Oak Creek cattle grazing has hammered the area there, 

some disturbance along Pleasant Creek 

Unique Geologic Features 

• Type Sections: Torrey Member of Moenkopi 

Formation, Capitol Reef bed in Chinle Formation 

(member unknown, likely Petrified Forest Member). 

Moody Canyon Member (near Escalante, likely 

outside park) of Moenkopi Formation. San Raphael 

area has a few (San Raphael Group, Bluegate Member 

of Mancos Shale Formation, Tunnock Member in 

Mancos Shale, Muley Canyon, Tarantula Mesa 

Sandstone). 

• Sills/dikes in north district 

• Selenite crystals (Glass Mountain area) 

• Cathedrals in Cathedral Valley 

• Waterpocket Fold 

• Black boulder deposits 

• Geomorphology in general, specifically the slot 

canyons (Halls Creek narrows). 

• Gypsum sinkholes 

• Strike valley 

• Soft sediment deformation 

• Capitol Dome 

• Sapping features – alcoves in Halls Creek area (cutoff 

meanders) 

• Red Slide down by Halls Creek 

• Hoodoos, demoiselles geomorphic features 

GRI Workshop Participants, CARE, September 27-28, 1999 

NAME AFFILIATION PHONE E-MAIL 

Biggam, Pete NPS, NRID 303-987-6948 Pete_Biggam@nps.gov 

Billingsley, Pete USGS-Flagstaff, AZ 520-556-7198 Gbillingsley@usgs.gov 

Clark, Tom NPS-CARE, Resources 435-425-3791,ext 144 Tom_O_Clark@nps.gov 

Connors, Tim NPS, GRD 303-969-2093 Tim_Connors@nps.gov 

Gregson, Joe NPS, NRID 970-225-3559 Joe_Gregson@nps.gov 

Heise, Bruce NPS, GRD 303-969-2017 Bruce_Heise@nps.gov 

Hendricks, Al NPS-CARE, 

Superintendent 435-425-3791,ext 100 Al_Hendricks@nps.gov 

Mathis, Allyson NPS-GRCA 505-278-2201,ext 231 Allyson_Mathis@nps.gov 

Morris, Tom Brigham Young Un. 801-378-3761 Tom_Morris@byu.edu 

Peterson, Pete USGS-Denver, CO 303-236-1546 Fpeterson@usgs.gov 

Santucci, Vince NPS-FOBU 307-877-4455 Vincent_Santucci@nps.gov 

Sprinkel, Doug Utah Geol. Association 801-782-3398 Sprinkel@vii.com 

Willis, Grant Utah Geological Survey 801-537-3355 Nrugs.gwillis@state.ut.us 

Wood, Vicky Brigham Young Un. 801-798-3882 Vaw3@byuemail.edu 

Worthington,Dave NPS-CARE, Biologist 435-425-3791,ext 145 Dave_Worthington@nps.gov 
 NPS Geologic Resources Division 50 

Appendix C: Geoindicators Report 

The following excerpts are modified from the Geoindicators Report for Capitol Reef 

National Park. This report was completed June 3-6, 2002; therefore, the contact 

information and Web addresses referred to herein may be outdated. Please contact to 

the Geologic Resources Division for current information. 

From June 3-5, 2002, staff of the National Park Service, 

Utah Geological Survey, U.S. Geological Survey, Bureau 

of Land Management, Northern Arizona University, and 

Brigham Young University participated in a 

geoindicators scoping meeting in Moab, Utah for four 

National Park Service units in southeastern Utah. The 

four parks were Arches National Park (ARCH), 

Canyonlands National Park (CANY), Capitol Reef 

National Park (CARE), and Natural Bridges National 

Monument (NABR). 

Purpose of meeting 

The purpose of the meeting was to bring together park 

staff, geoscientists, and other resource specialists to 

address the issue of human influences on geologic 

processes in the four park areas. The group used 

collective knowledge of the four parks’ geology and 

natural resources to identify the geologic processes active 

in the parks, to identify the human activities affecting 

those processes, and to develop recommendations for 

long-term monitoring of geoindicators in conjunction 

with park Vital Signs monitoring. 

In addition, the Northern Colorado Vital Signs Network 

is coming on-line in fiscal year 2002 and will be receiving 

its first funding for Vital Signs monitoring. The scoping 

meeting was timed so the Network could use the 

information gained during the meeting in the Vital Signs 

selection process. 

This report summarizes the group’s discussions and 

provides recommendations for studies to support 

resource management decisions, inventory and 

monitoring projects, and research needed to fill data 

gaps. 

Park Settings 

All four parks are located in the high desert of 

southeastern Utah. The climate is one of very hot 

summers, cold winters, and very little rainfall. On a daily 

basis, temperatures may fluctuate as much as 50 degrees 

Fahrenheit. Afternoon thunderstorms occur frequently 

from about mid-July through late summer. Snow 

occasionally falls in winter, especially at the higher 

elevations of the parks. 

Capitol Reef National Park 

Capitol Reef is a long, linear park that follows the mostly 

north-south trending Waterpocket Fold, a spectacular 

100-mile long fold in Earth’s crust known as a 

monocline. Elevations range from 4,200 feet to 9,800 feet. 

The lowest elevations are on the east side of the park—

the downdropped side of the monocline, and the highest 

are on the west side of the park—the uplifted side of the 

monocline. 

The park has several distinct regions. In the northern 

part of the park is Cathedral Valley. Rock layers in 

Cathedral Valley have a gentle inclination of 3 to 5 

degrees to the east and appear nearly horizontal. Deep 

erosion has carved Cathedral Valley's free-standing 

monoliths, or temples, out of the soft reddish-orange 

Entrada Sandstone. South of Cathedral Valley, the 

Fremont River bisects the park east to west. South of the 

river is the park's scenic drive, which travels into an area 

of narrow gorges, towering cliffs, and large sandstone 

domes. The name Capitol Reef is partially derived from 

these large, white domes of Navajo Sandstone: "capitol" 

for the white domes that resemble capitol building 

rotundas, and "reef" for the rocky cliffs which are a 

barrier to travel, like a coral reef. The long, narrow 

southern region of the park includes many canyons, most 

notably the Halls Creek Narrows. 

Topographic relief created a variety of habitats, such as 

perennial streams, water- pockets, hanging gardens, and 

dry washes, which are home to a diversity of flora and 

fauna in the park. "Waterpockets" are basins that form in 

many of the sandstone layers as they are eroded by water. 

These basins are common throughout the fold, thus 

giving it the name "Waterpocket Fold." 

Early human occupation of the park was by the Fremont 

people, from about AD 700 to AD 1300. The culture was 

named for the Fremont River and its valley in which 

many of the first Fremont sites were discovered. Several 

types of artifacts left by the Fremont people have been 

identified, including baskets, smooth and corrugated 

gray pottery, and moccasins made from the hides of large 

animals. The most unique artifacts are clay figurines of 

unknown significance to the Fremont people. Also, a 

variety of pictographs and petroglyphs are scattered 

throughout parts of the park. 

The pioneer community of Fruita, about one mile from 

the visitor center, was settled in 1880 by Mormon 

pioneers. The National Park Service now manages the 

historic orchards, which contain about 2,700 trees 

(mostly cherry, apricot, peach, pear, and apple), as part of 

Rural Historic Landscape. 

The park was first designated a national monument in 

1937, and was later expanded and re-designated a 

national park in 1971. 
 CARE Geologic Resource Evaluation Report 51

Park Geologic Setting 

All four parks are located on the Colorado Plateau, a 

geologic province encompassing most of southern Utah 

and northern Arizona, northwest New Mexico, and 

western Colorado. The Plateau is characterized by 

relatively horizontal sedimentary rock layers that have 

been uplifted as much as 10,000 feet with relatively little 

deformation, with the exception of a number mostly 

north-south trending folds known as monoclines. 

Waterpocket Fold in Capitol Reef is a classic example of 

one of the monoclines. 

For hundreds of millions of years, material was deposited 

in what is now southeast Utah. As movements in Earth’s 

crust altered surface features and the North American 

continent migrated north from the equator, the local 

environment changed dramatically. Over time, southeast 

Utah was flooded by oceans, crisscrossed by rivers, 

covered by mudflats, and buried by sand. The strata 

records changes in climate and biota spanning from the 

Pennsylvanian through Tertiary periods. 

Until about 15 million years ago, most of the area was 

near sea level. Local uplifts and volcanic activity had 

created features like Capitol Reef's Waterpocket Fold 

and the La Sal Mountains near Moab, but then 

movements in Earth's crust caused the whole area to rise. 

Today, the average elevation is over 5,000 feet above sea 

level. 

The following is a stratigraphic column of rock units in 

or near the four parks: 

Capitol Reef National Park 

Nearly 10,000 feet of sedimentary strata are found in the 

Capitol Reef area. These rocks range in age from the 

Permian White Rim Sandstone (as old as 270 million 

years old) to the Cretaceous Mancos Shale (as young as 

80 million years old.). The Waterpocket Fold has tilted 

the geologic layers such that the layers on the west side of 

the Fold have been lifted more than 7,000 feet higher 

than the layers on the east. Therefore, the older rocks are 

found in the western part of the park, and the younger 

rocks are found near the east boundary. 

Layer-upon-layer of sedimentary rocks records nearly 

200 million years of geologic history. Rock layers in 

Capitol Reef reveal ancient climates as varied as rivers 

and swamps (Chinle Formation), Sahara-like deserts 

(Navajo Sandstone), and shallow ocean (Mancos Shale). 

Waterpocket Fold formed between 50 and 70 million 

years ago when a major mountain-building event in 

western North America, the Laramide Orogeny, 

reactivated an ancient buried fault. When the fault 

moved, the overlying rock layers were draped above the 

fault and formed a monocline. 
 NPS Geologic Resources Division 52 

The following table was generated by scoping participants during the 2002 meeting: 

Geoindicators Table 

Geoindicators Identified in the Ecosystem 

Importance to 

park 

ecosystem 

Human impact 

Significance to 

park 

management 

ARID AND SEMIARID 

 1. Desert surface crusts (bio and phys/chem) and 

pavements 5 5 5 

 2. Dune formation and reactivation 3 3 4 

 3. Dust storm magnitude, duration and frequency 1 5 / 3* 3 

 4. Wind erosion and deposition (ecosystem inputs 

and outputs) 5 5 / 3* 5 

SURFACE WATER 

 5. Stream channel morphology 5 5 5 

 6 Stream sediment erosion, storage and load 5 5 5 

 7. Streamflow 5 5 5 

 8. Surface water quality 5 5 5 

 9. Wetlands extent, structure, hydrology 5 5 5 

GROUNDWATER 

10. Groundwater quality 5 4 3 

11. Groundwater level and discharge 5 5 5 

SOILS 

12. Soil quality (the capacity to function within 

“natural” range of variability—as reflected by 

dynamic soil properties that change in relation to 

management or climate—see SQIS definition) 

5 1 / 5* 5 

13. Soil and sediment erosion and deposition by 

water (upland environments) 5 3 / 5* 5 

14. Sediment sequence and composition 1 5 3 

HAZARDS 

15. Slope failure (landslides, rockfalls and debris 

flows) 3 1 2 

16. Seismicity 1 0 1 

17. Surface displacement (including salt dissolution 

features) 2 0 1 

OTHER 

18. Fire Occurrence (e.g. spatial distribution and 

frequency may vary in relation to geophysical 

features/processes and can affect processes) 

1 5 1 

19. Atmospheric deposition (N, SO4) 1 3 1 

20. Paleontological resources 1 3 3 

21. Climate 5 1 5 

0 - Not Applicable (N/A) 

1 - LOW or no substantial influence on, or utility for 

3 - MODERATELY influenced by, or has some utility for 

5 - HIGHLY influenced by, or with important utility for 

UNK - Unknown; may require study to determine applicability 

* Out of park/Inside park activity 
The Department of the Interior protects and manages the nation’s natural resources and cultural heritage; provides scientific and other 

information about those resources; and honors its special responsibilities to American Indians, Alaska Natives, and affiliated Island 

Communities. 

Capitol Reef National Park 

Geologic Resource Evaluation Report 

Natural Resource Report NPS/NRPC/GRD/NRR—2006/005 

NPS D-224, September 2006 

National Park Service 

Director • Fran P. Mainella 

Natural Resource Stewardship and Science 

Associate Director • Michael A. Soukup 

Natural Resource Program Center 

The Natural Resource Program Center (NRPC) is the core of the NPS Natural Resource Stewardship and 

Science Directorate. The Center Director is located in Fort Collins, with staff located principally in 

Lakewood and Fort Collins, Colorado and in Washington, D.C. The NRPC has five divisions: Air 

Resources Division, Biological Resource Management Division, Environmental Quality Division, Geologic 

Resources Division, and Water Resources Division. NRPC also includes three offices: The Office of 

Education and Outreach, the Office of Inventory, Monitoring and Evaluation, and the Office of Natural 

Resource Information Systems. In addition, Natural Resource Web Management and Partnership 

Coordination are cross-cutting disciplines under the Center Director. The multidisciplinary staff of NRPC 

is dedicated to resolving park resource management challenges originating in and outside units of the 

national park system. 

Geologic Resources Division 

Chief • David B. Shaver 

Planning Evaluation and Permits Branch Chief • Carol McCoy 

Credits 

Author • Dr. John Graham

Editing • Sid Covington and Lisa Norby 

Digital Map Production • Stephanie O’Meara, Jerome Walker, and Jenny Adams 

Map Layout Design • Melanie Ransmeier
Geologic Resources Division 

Natural Resource Program Center 

P.O. Box 25287 

Denver, CO 80225 

http://www.nature.nps.gov/geology/inventory/ 

(303) 969-2090 

EXPERIENCE YOUR AMERICATM 

National Park Service 

U.S. Department of the Interior