Qmsy Kst Qmt Qmt Qmsy Qmt Kd Kd Kd Kd Kd Kd Kd Qmt Qmt Qmt Qmt Qat 2 Kt Kt Kt Qmsh Kt Kt Kt Qmsy Qmsy Ksu Kst Ta Qco Ksu Ksu Qc Kst Kd Kd Qmt Qmt Qmsy Qmt Qmt Qmt Kst Kst Kd Kd Qmsy Ksu Kst Qes/Qbhp Qbhp Qbhp Qmsy Qmsy Qac Kd Kd Kd Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Qac Kst Kst Qmt Qmt Qmsy Qmsy Qmsy Qc Qc Qac Qmsy Qc Kst Kd Qmso(Kd) Qmsy Qmsh Kd Kt Kt Kt Kt Kt Kt Kt Kst Kst Kst Kst Kst Kst Kst Kst Kst Qmt Qmt Qmt Qmt Qmt Qmt Qmsy Qmsy Qmsy Qmso Kd Kd Kd Qmsy Qac Qac Qac Qmt Qmt Qmt Kd Kd Qmso Jcw Qat 2 Qat 2 Qat 2 Qat 2 Qat 2 Qat 2 Jcw Jcw Kcm Qaf 2 Qmsy Qmt Qmt Jcw Jcp Jcp Jcw Jcx Jcx Jcp Jcx Jcx Qaf 1 Qmsy Qmsy Jcw Kcm Kcm Kcm Qmsh Jccu Jcp Ksu Ksu Ksu Ksu Ksu Ksu Qmt Qmt Qmt Qmt Qmt Qmt Qmt Qmt Qmt Qmsy? Qmsy Qmt Qbhk Qbhk Kd Kd Kd Kd Kd Kd Kst Kst Kst Ksu Ksu Ksu Ksu Ksu Ksu Ksu Kst Kst Kst Kst Kst Kst Kd Kd Kd Kd Kd Kd Kcm Kcm Kcm Qmsy Qmsy Qmso Jcw Jcw Jcw Jcw Jcw Jcw Kcm Qmsy Qaf 1 Qmsh Qat 2 Qat 2 Qat 2 Qaf 1 Qaf 1 Qaf 1 Jcw Kt Kt Kt Qaf 1 Qac Qac Qac Kt Qaco Qat 2 Qao Qal 1 Jcp Qaf 1 Qal 1 Qmso Qmsh Jcp Jcx Qmso Qmt Qmt Qmso Qc Qc Qaf 1 Jcx Jcp Qaf 1 Jcx Qao Jcx Qmt Qbvk Qaf 1 Jccu Jccu Jccl Qmt Qac Qaf 1 Jcp Jcx Jccu Qaf 1 Qaf 1 Qaf 1 Qal 1 Qal 1 Qbvkc Qbvk Qea Qac Jcw Qbvk Qbvk Qbvk Qaf 2 Qaf 2 Jccu Jcx Jccu Jccl Jccu Jcx Jccu Jcx Jcp Jcw Jcw Qc Qc Qbhp Qbhp Qmt Kcmc Kcmc Kcmc Qmsh Jcw Jcp Jcx Jcw Kd Kd Qmsy Qmsy Qmsy Kd Kd Qc Qf Kcmc Qc Jcw Jcx Jcp Jccu Qmt Kcmc Kcmc Jcw Jcp Jcp Jcx Jccu Jccu Qmt Qac Qmsy Jccl Jtw Jtw Jccl Jccl Jtw Jccl Qmsy Jcw Jcp Jcx Qmso Qmt Jts Jts Jn Jtw Jccl Qmsy Jccl Qmsy Jtw Jts Qmt Qac Qac Jts Jts Jtw Jcx Jcx Jcx Qbvf Qbvf Qbvfc Qmt Qac Qaco Qac Qbvf Qmsy Qmsy Jccu Jccl Jtw Qac Qmsy Qmt Jccl Jccu Jtw Jts Jts Qmt Jccl Jccu Jtw Jn Qmt Qmt Qmsy Qac Jccl Jccu Jccu Jccl Jtw Jts Qmsy Jtw Jts Qac Jccl Jccl Jccu Jccu Qmsy Qmsy Jtw Jtw Qac Jccl Jccl Jccu Qmsy Jtw Jtw Qac Qmt Jn Jtw Qac Jccu Qmsy Jcx Jts Jccl Jccl Qac Qbvf Jccl Qac Qac Qaco Qac Qaf 1 Qaf 1 Qaf 1 Jccu Jccu Jccu Qac Qc Jccl Jccl Jccl Qbhp Qbvk Qbvk Qmt Qmt Qmt Qmt Qmsy Qmsy Qmsy Qmt Qbhk Qbhk Qmsy Qms Qmsy Qmsy Kcm Kcm Kcm Kcm Qmt Qbvk Qbvk Jccl Jccl Qmt Qmt Qac Qac Qmt Qac Jccu Jcx Jcx Jcp Jcp Qac Jcw Qaf 1 Qaf 1 Qaf 1 Qmt Qmt Jcp Jcx Jccu Qao? Qao? Qae Jcw Jcp Jcw Jcx Jccu Jccl Jccu Qbvk Jtw Jtw Jtw Jtw Jccl Qae Qae Qbvk Qbvk Qbvk Qbvk Qmt Jn Qc Qes Qea Qea Qmt Qmt Jtw Qbhk Qao Qao Jtw Jccl Qc Qc Qc Qmt Qmsy Qmsy Jtw Qmt Qmt Qmt Qmt Qbvk Qal 1 Qal 1 Qal 1 Qal 1 Qal 1 Jts Jts Jts Jccu Jccl Jccl Jccu Qre Qmt Qmt Qmt Qmt Qre Qre Jccl Jccl Jtw Jtw Jn Jtw Qac Qac Jcx Qc Qc Qmso Qmsy Qmsy Qmsy Jcp Jcp Jcp Jcp Jcp Jcw Jcw Jcw Kcm Kcm Kcm Kcm Kcm Qmt Qmt Kcm Qmt Jcw Qc Kcm Jccu Qmsy Qc Jccu Jccl Jccu Jcp Jcp Jcp Qmso Jcw Jcp Jccu Qc Qc Qre Jcx Jcx Qmsy Qc Kcm Kcm Kd Kd Kd Kd Qf Jcx Jcp Qmso Jcx Jcx Jccl Qmt Qms Qaco Qc Qc Qc Qc Kd Qmso(Kd) Qmsy Qc Qc Qc Qmt Qmt Kt Kt Kt Kt Qmt Qmso?(Kd) Qmt Kst Kst Kst Kst Kst Ksu Ksu Ksu Ksu Ksu Ksu Kst Kst Kst Kst Ksu Qac Qaco Qac Qac Qac Qac Qac Qac Qc Ksu Qmsh Kt Qac Qac Qac Qac Qac Qmsy Qmsh Qmsh Qac Qbhkc Qbhkc Qbhk Qbhk Qbhkc Qac Qac Kd Kt Kd Qc Kt Kt Kt Qmsy Kd Kd Kd Kd Kd Kt Qbtc Qbtc Qmt Qac Kst Kst Qmt Qac Qac Qac Qmsy Qmsy Kd Kt Qac Qc Jcw Jccu Kd Qac Kst Qmsy Ksu Ksu Kd Qmsy Qc Qmsy Qmt Qmsy Qmsh Kt Qmsh Qmsh Qmsy Qmsh Kd Kd Qbhk Qac Qac Qac Kcm Qat 2 Qat 2 Kt? Qao Qac Kt Qmsy Qmsh Jcx Jcp Jcw Jcx Jccu Qmt Jccu Qmt Qaf 1 Qat 2 Jtw Jtw Jcx Jcx Jn Jn Jn Jts Jts Qmt Jtw Jccu Jcp Qmt Qac Qao Jts Qmt Jtw Jcx Jts Jtw Jts Jn Jts Qmsy Qmt Kst Qmt Kd Qmt Jccl Jcx Qaf 1 Jccu Qmt Qmt Jccu Jccu Jccl Kd Kd Kd Kst Qbhk Qmt Kd Ksu Jcp Kcm Kcm Kcm Jcw Kst Kst Qmt Jccu Jccu Qmt Jts Jccl Qal 1 Qal 1 Qmt Qal 1 Qal 1 Qbvk Qal 1 Kt Kt Kcm Qal 1 Qaf 2 Qat 2 Jccu Qal 1 Kst UTAH GEOLOGICAL SURVEY a divison of Utah Department of Natural Resources in cooperation with National Park Service 1 0.5 0 1 0.5 0 1 KILOMETER 1 MILE SCALE 1:24,000 CONTOUR INTERVAL 40 FEET NATIONAL GEODETIC VERTICAL DATUM OF 1929 0 1000 1000 2000 3000 4000 5000 6000 7000 FEET GEOLOGIC MAP OF THE COGSWELL POINT QUADRANGLE, WASHINGTON, KANE, AND IRON COUNTIES, UTAH by Robert F. Biek and Michael D. Hylland 2007 Fieldwork by authors in 2000-01 Project Manager: Grant C. Willis GIS Analyst: Kent D. Brown Cartographer: James W. Parker ISBN 1-55791-740-X Base from U.S. Geological Survey, Cogswell Point 7.5' quadrangle, 1980 Shaded topography generated from digital elevation data Plate 1 Utah Geological Survey Map 221 Geologic Map of the Cogswell Point Quadrangle UTAH QUADRANGLE LOCATION A A' APPROXIMATE MEAN DECLINATION, 2007 MAGNETIC NORTH TRUE NORTH 12°24' This geologic map was funded by the Utah Geological Survey and the U.S. Department of the Interior, National Park Service. The views and conclusions contained in this document are those of the authors and should not be interpreted as necessarily representing the official policies, either expressed or implied, of the U.S. Government. Although this product represents the work of professional scientists, the Utah Department of Natural Resources, Utah Geological Survey, makes no warranty, expressed or implied, regarding its suitability for a particular use. The Utah Department of Natural Resources, Utah Geological Survey, shall not be liable under any circumstances for any direct, indirect, special, incidental, or consequential damages with respect to claims by users of this product. For use at 1:24,000 scale only. The UGS does not guarantee accuracy or completeness of data. Utah Geological Survey, 1594 W. North Temple, P.O. Box 146100, Salt Lake City, Utah 84114-6100. Phone: 801-537-3300; fax 801-537-3400; www.geology.utah.gov 3 3 2 2 2 2 2 2 1 2 2 2 2 2 2 2 2 2 2 2 2 2 2 2 2 2 2 2 1 1 3 2 2 2 2 CP62001-1 CP62001-2 CP10700-6 CP10700-7 CP71900-5 CP71900-6 CP719001-7 CP10700-3 CP10700-8 CP10700-1 CP71900-1 CP10700-5 CP83100-3 CP83100-2 CP83100-1 CP90100-1 CPF61901-1 CP62001-3 CP61901-1 CP10700-2 CP71900-3 6500 6400 6300 6200 6100 6000 5900 5800 5700 5500 5600 5400 5300 8000 7900 7800 7900 7800 7900 7800 7800 7700 7700 7600 7700 7800 7600 7900 8000 8100 8200 8300 8400 8500 8600 8700 8800 7900 8900 7800 6600 See plate 2 references for geologic map list
Transcript
Qmsy
Kst
Qmt
Qmt
Qmsy
Qmt
Kd
Kd
Kd
Kd
Kd
Kd
Kd
Qmt
Qmt
Qmt
QmtQat2
Kt
Kt
Kt
Qmsh
Kt
Kt
Kt
Qmsy
Qmsy
Ksu
Kst
Ta
Qco
Ksu
Ksu
Qc
Kst
Kd
KdQmt
Qmt
QmsyQmt
Qmt
Qmt
Kst
Kst
Kd
Kd
QmsyKsu
Kst
Qes/Qbhp
Qbhp
Qbhp
Qmsy
Qmsy
Qac
Kd
Kd
Kd
Qac
Qac
Qac
Qac
QacQac
QacQac
Qac Qac
Qac
QacQac
Qac
Qac
QacQac
Qac
Qac
Qac
Qac
Qac
Qac
Kst
Kst
Qmt
Qmt Qmsy
Qmsy
Qmsy
Qc
Qc
Qac
Qmsy
Qc
Kst
Kd
Qmso(Kd)
QmsyQmsh
Kd
Kt
Kt
Kt
Kt
Kt
Kt
Kt
Kst
Kst
Kst
Kst
KstKst
Kst
Kst
Kst
Qmt
Qmt
Qmt
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QmtQmsy
Qmsy
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Qmt
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Kd
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Jcw
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Qat2
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Kd
Kd
Kd
Kd
Kd
Kd
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Kst
Kst
Ksu
Ksu
Ksu
Ksu
Ksu
Ksu
Ksu
Kst
Kst
Kst
Kst
Kst
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Kd
Kd
Kd
Kd
Kd
Kcm
Kcm
Kcm
Qmsy
Qmsy
Qmso
Jcw
Jcw
Jcw
JcwJcw
Jcw
Kcm
Qmsy
Qaf1
Qmsh
Qat2
Qat2
Qat2
Qaf1
Qaf1
Qaf1
Jcw
Kt
Kt
Kt
Qaf1
Qac
Qac
Qac
Kt
Qaco
Qat2
Qao
Qal1
Jcp
Qaf1 Qal1
Qmso
Qmsh
Jcp
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Qmt
QmtQmso
Qc
Qc
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Jcx
Jcp
Qaf1
Jcx
Qao
Jcx
Qmt
QbvkQaf1
Jccu
JccuJccl
QmtQac
Qaf1
Jcp
Jcx
Jccu
Qaf1
Qaf1Qaf1
Qal1
Qal1
Qbvkc
Qbvk
Qea
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QbvkQbvk
Qbvk
Qaf2Qaf2
JccuJcx
Jccu
Jccl
Jccu
Jcx
JccuJcx
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JcwQc
QcQbhp
Qbhp
Qmt
Kcmc
Kcmc
Kcmc
Qmsh
Jcw
Jcp
Jcx
Jcw
Kd
Kd
Qmsy
Qmsy
Qmsy
KdKd
Qc
Qf
Kcmc
Qc
Jcw
Jcx
Jcp
Jccu
Qmt
Kcmc
KcmcJcw
JcpJcp
Jcx
Jccu
Jccu
Qmt
Qac
Qmsy
Jccl
JtwJtw
Jccl
Jccl
Jtw
Jccl
Qmsy
Jcw Jcp
Jcx
Qmso
Qmt
Jts
Jts
Jn
Jtw
Jccl
Qmsy
JcclQmsy
Jtw
JtsQmt
Qac
Qac
Jts
Jts
Jtw
Jcx
Jcx
Jcx
Qbvf
Qbvf
Qbvfc
Qmt
Qac
Qaco
Qac Qbvf
Qmsy
Qmsy
Jccu
Jccl
JtwQac
Qmsy
Qmt
Jccl
Jccu
JtwJts
Jts
Qmt
Jccl
Jccu
JtwJn
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QmsyQac
Jccl JccuJccu
JcclJtw Jts
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Jccl
Jccl
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Jccl
Jccl
Qac
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Qac
Qaf1
Qaf1
Qaf1
Jccu
Jccu
Jccu
Qac
Qc
Jccl
Jccl
Jccl
Qbhp
Qbvk
Qbvk
Qmt
Qmt
Qmt
Qmt
Qmsy
Qmsy
QmsyQmt
Qbhk
Qbhk
Qmsy
Qms
Qmsy
QmsyKcm
Kcm
Kcm
Kcm
Qmt
Qbvk
Qbvk
Jccl
Jccl
Qmt
Qmt
Qac
Qac
QmtQac
Jccu
Jcx
Jcx
Jcp
Jcp
Qac
Jcw
Qaf1
Qaf1
Qaf1Qmt
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Jcx
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Qae
Jcw
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Jccl
Jccu
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Jtw
Jtw
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Qmt
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Qc
Qc
Qc
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Qmsy
Qmsy
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Qmt
Qmt
Qmt
Qmt
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Qal1
Qal1
Qal1
Qal1
Qal1
Jts
Jts
Jts
Jccu
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Jccu
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Qmt
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Jccl
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Qac
Qac
Jcx
Qc
Qc
Qmso
Qmsy
Qmsy
Qmsy
Jcp
JcpJcp
Jcp
JcpJcw
JcwJcw
Kcm
KcmKcm
Kcm
KcmQmt
Qmt
KcmQmt
JcwQc
Kcm
Jccu
Qmsy
Qc
Jccu
Jccl
Jccu
Jcp
Jcp
Jcp
Qmso
Jcw
Jcp
Jccu
Qc
Qc
Qre
Jcx
Jcx
Qmsy
QcKcm
Kcm
Kd
Kd
Kd
Kd
Qf
JcxJcp
Qmso
Jcx
Jcx
Jccl
Qmt
QmsQaco
QcQc
Qc
Qc
KdQmso(Kd)
Qmsy
Qc
Qc
Qc
Qmt
Qmt
Kt
Kt
Kt
Kt
Qmt
Qmso?(Kd)
Qmt
Kst
Kst
Kst
Kst
Kst
Ksu
Ksu
Ksu
Ksu
Ksu
Ksu
Kst
Kst
Kst
KstKsu
Qac
Qaco
Qac
Qac
Qac
Qac
QacQac
Qc
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Kt
Qac
Qac
Qac
Qac
Qac
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Qmsh
Qmsh
Qac
Qbhkc
Qbhkc
Qbhk
Qbhk
Qbhkc
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Qac
Kd
Kt
Kd
Qc
Kt
Kt
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Kd
Kd
Kd
Kd
Kd
Kt
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Qbtc
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Qac
Kst
Kst
Qmt
Qac
Qac
Qac
Qmsy
Qmsy
Kd
Kt
Qac
Qc Jcw
Jccu
Kd
Qac
Kst
Qmsy
Ksu
Ksu
Kd
Qmsy
Qc
Qmsy
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Qmsy
Qmsh
Kt
Qmsh
Qmsh
Qmsy
QmshKd
KdQbhk
Qac
QacQac
Kcm
Qat2
Qat2
Kt?
Qao
Qac
Kt
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Qmsh
Jcx
JcpJcw
Jcx
Jccu
Qmt
Jccu
Qmt
Qaf1
Qat2
Jtw
Jtw
JcxJcx
Jn
Jn
Jn
Jts
Jts
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Jccu
JcpQmtQac
Qao
Jts
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Jts
Jtw Jts
JnJts
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Qmt
Kst
QmtKd
Qmt
Jccl
Jcx
Qaf1
Jccu
Qmt
QmtJccu
Jccu
Jccl
Kd
KdKd
Kst
Qbhk
Qmt
Kd
Ksu
Jcp
KcmKcm
Kcm
Jcw
Kst
Kst
Qmt
Jccu
Jccu
Qmt
Jts Jccl
Qal1
Qal1
Qmt
Qal1
Qal1
Qbvk
Qal1
Kt
Kt
Kcm
Qal1
Qaf2
Qat2
Jccu
Qal1
Kst
UTAH GEOLOGICAL SURVEYa divison ofUtah Department of Natural Resourcesin cooperation withNational Park Service
1 0.5 0
1 0.5 0 1 KILOMETER
1 MILESCALE 1:24,000
CONTOUR INTERVAL 40 FEETNATIONAL GEODETIC VERTICAL DATUM OF 1929
01000 1000 2000 3000 4000 5000 6000 7000 FEET
GEOLOGIC MAP OF THE COGSWELL POINT QUADRANGLE,WASHINGTON, KANE, AND IRON COUNTIES, UTAH
byRobert F. Biek and Michael D. Hylland
2007
Fieldwork by authors in 2000-01Project Manager: Grant C. Willis
GIS Analyst: Kent D. BrownCartographer: James W. Parker
ISBN 1-55791-740-X
Base from U.S. Geological Survey,Cogswell Point 7.5' quadrangle, 1980Shaded topography generated from digital elevation data
Plate 1Utah Geological Survey Map 221
Geologic Map of the Cogswell Point Quadrangle
UTAH
QUADRANGLE LOCATION
A
A'
APPROXIMATE MEANDECLINATION, 2007
MA
GN
ETI
C N
OR
TH
TRU
E N
OR
TH
12°24'
This geologic map was funded by the Utah Geological Survey and the U.S. Department of the Interior, National Park Service. The views and conclusions contained in this document are those of the authors and should not be interpreted as necessarily representing the official policies, either expressed or implied, of the U.S. Government.
Although this product represents the work of professional scientists, the Utah Department of Natural Resources, Utah Geological Survey, makes no warranty, expressed or implied, regarding its suitability for a particular use. The Utah Department of Natural Resources, Utah Geological Survey, shall not be liable under any circumstances for any direct, indirect, special, incidental, or consequential damages with respect to claims by users of this product.
For use at 1:24,000 scale only. The UGS does not guarantee accuracy or completeness of data.
Utah Geological Survey, 1594 W. North Temple, P.O. Box 146100, Salt Lake City, Utah 84114-6100. Phone: 801-537-3300; fax 801-537-3400; www.geology.utah.gov
3
3
2
2
2
22
2
1
2
2
2
2
2
2
2
2
2
2
2
2
2
2
2
2
2
2
2
1
1
3
2
2
2
2
CP62001-1
CP62001-2
CP10700-6
CP10700-7
CP71900-5
CP71900-6
CP719001-7
CP10700-3
CP10700-8CP10700-1
CP71900-1
CP10700-5
CP83100-3
CP83100-2
CP83100-1
CP90100-1
CPF61901-1
CP62001-3CP61901-1
CP10700-2
CP71900-3
6500 6400
6300
6200
6100
6000
5900
5800
5700
55005600
5400
5300
8000
7900
7800
7900
7800
7900
7800
7800
7700
7700
7600
77007800
7600
7900
8000
8100
8200
8300
8400
8500
8600
8700
8800
7900
8900
7800
6600
See plate 2 references for geologic map list
150-200(45-60)
Jcw
Qbvf,QbvfcVirgin Flats flow and cinder cone
CedarMountainFormationundivided
Crystal CreekMember
Co-opCreek
LimestoneMember
old boulder gravel deposits
Temple CapFormation
Shown on crosssection only
700-1000(210-300)
100-150(30-45)
120-160(37-50)
SpringdaleSandstone Member
upper unitKayenta
Formation
200-240(60-73)
80-120(24-37)
conglomeratemember
Winsor Member
40-110 (12-35)Paria River Member
Kcmc
Kd
Kcm 0-100 (0-30)
10-180 (3-55)
Jcp
Jcx
Jccu
Jccl
upper
lower
200-240(60-73)
Dakota Formation 700-900(210-275)
JnNavajo Sandstone 2100-2200(640-670)
Kt 3?-200 (1?-60)Tropic Shale
KstTibbet CanyonMember
450-550(135-170)
StraightCliffs
Formation
600+ (180+)upper unit Ksu
0-90 (0-27)Ta
Horse Knoll flow and cinder cones 0-300 (0-90)Qbhk,Qbhkc
Utah Geological Surveya division ofUtah Department of Natural Resourcesin cooperation withNational Park Service
CORRELATION OF MAP UNITS LITHOLOGIC COLUMNDESCRIPTION OF MAP UNITS
Averitt, Paul, 1962, Geology and coal resources of the Cedar Mountain quadrangle,Iron County, Utah: U.S. Geological Survey Professional Paper 389, 72 p.
—1967, Geologic map of the Kanarraville quadrangle, Iron County, Utah: U.S.Geological Survey Geologic Quadrangle Map GQ-694, 1 plate, scale 1:24,000.
Best, M.G., McKee, E.H., and Damon, P.E., 1980, Space-time-composition patternsof late Cenozoic mafic volcanism, southwestern Utah and adjoining areas: AmericanJournal of Science, v. 280, p. 1035-1050.
Biek, R.F., 2007a, Geologic map of the Kolob Reservoir quadrangle, Washington andIron Counties, Utah: Utah Geological Survey Map 220, 2 plates, scale 1:24,000.
—2007b, Geologic map of the Kolob Arch quadrangle and part of the Kanarravillequadrangle, Washington and Iron Counties, Utah: Utah Geological Survey Map217, 3 plates, scale 1:24,000.
Blakey, R.C., 1994, Paleogeographic and tectonic controls on some Lower and MiddleJurassic erg deposits, Colorado Plateau, in Caputo, M.V., Peterson, J.A., andFranczyk, K.J., editors, Mesozoic systems of the Rocky Mountain region, USA:Denver, Colorado, Rocky Mountain Section of the Society for Sedimentary Geology,p. 273-298.
Blakey, R.C., Peterson, Fred, Caputo, M.V., Geesman, R.C., and Voorhees, B.J., 1983,Paleogeography of Middle Jurassic continental, shoreline, and shallow marinesedimentation, southern Utah, in Reynolds, M.W., and Dolley, E.D., editors, Mesozoicpaleogeography of west-central United States: Rocky Mountain Section of Societyof Economic Paleontologists and Mineralogists, p. 77-100.
Cashion, W.B., 1961, Geology and fuels resources of the Orderville-Glendale area,Kane County, Utah: U.S. Geological Survey Coal Investigations Map C-49, scale1:62,500.
—1967, Geologic map of the south flank of the Markagunt Plateau, northwest KaneCounty, Utah: U.S. Geological Survey Miscellaneous Geologic Investigations MapI-494, 1 plate, scale 1:24,000.
Doelling, H.H., 2002, Interim geologic map of the Temple of Sinawava quadrangle,Washington and Kane Counties, Utah: Utah Geological Survey Open-File Report396, 16 p., 1 plate, scale 1:24,000.
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Doelling, H.H., Willis, G.C., Solomon, B.J., Sable, E.G., Hamilton, W.L., and Naylor,L.P., II, 2002, Interim geologic map of the Springdale East quadrangle, WashingtonCounty, Utah: Utah Geological Survey Open-File Report 393, 20 p., 1 plate, scale1:24,000.
Eaton, J.G., Laurin, Jiri, Kirkland, J.I., Tibert, N.E., Leckie, R.M., Sageman, B.B.,Goldstrand, P.M., Moore, D.W., Straub, A.W., Cobban, W.A., and Dalebout, J.D.,2001, Cretaceous and early Tertiary geology of Cedar and Parowan Canyons, westernMarkagunt Plateau, Utah, in Erskine, M.C., editor and Faulds, J.E., Bartley, J.M.,and Rowley, P.D., co-editors, The geologic transition, High Plateaus to Great Basin– a symposium and field guide, The Mackin Volume: Utah Geological AssociationPublication 30 and Pacific Section American Association of Petroleum GeologistsPublication GB 78, p. 337-363.
Gustason, E.R., 1989, Stratigraphy and sedimentology of the middle Cretaceous (Albian-Cenomanian) Dakota Formation, southwestern Utah: Boulder, University ofColorado, Ph.D. dissertation, 376 p.
Hamilton, W.L., 1978 (revised 1987), Geological map of Zion National Park, Utah:Zion Natural History Association, scale 1:31,680.
Hayden, J.M., 2004, Geologic map of the Little Creek Mountain quadrangle, WashingtonCounty, Utah: Utah Geological Survey Map 204, 2 plates, scale 1:24,000.
—in preparation, Geologic map of the Virgin quadrangle, Washington County, Utah:Utah Geological Survey Map, 2 plates, scale 1:24,000.
Hylland, M.D., 2000, Interim geologic map of the Clear Creek Mountain quadrangle,Kane County, Utah: Utah Geological Survey Open-File Report 371, 12 p., 2 plates,scale 1:24,000.
Imlay, R.W., 1980, Jurassic paleobiogeography of the conterminous United States inits continental setting: U.S. Geological Survey Professional Paper 1062, 134 p.
Kirkland, J.I., Britt, Brooks, Burge, D.L., Carpenter, Ken, Cifelli, Richard, Decourten,Frank, Eaton, Jeffrey, Hasiotis, Steve, and Lawton, Tim, 1997, Lower to middleCretaceous dinosaur faunas of the central Colorado Plateau – a key to understanding35 million years of tectonics, sedimentology, evolution and biogeography, in Link,P.K., and Kowallis, B.J., editors, Mesozoic to recent geology of Utah: BrighamYoung University Geology Studies, v. 42, part 2, p. 69-103.
Laurin, Jiri, and Sageman, B.B., 2001, Tectono-sedimentary evolution of the westernmargin of the Colorado Plateau during the latest Cenomanian and early Turonian,in Erskine, M.C., editor and Faulds, J.E., Bartley, J.M., and Rowley, P.D., co-editors,The geologic transition, High Plateaus to Great Basin – a symposium and fieldguide, The Mackin Volume: Utah Geological Association Publication 30 and PacificSection American Association of Petroleum Geologists Publication GB 78, p. 57-74.
LeBas, M.J., LeMaitre, R.W., Streckeisen, A., and Zanettin, B., 1986, A chemicalclassification of volcanic rocks based on the total alkali-silica diagram: Journal ofPetrology, v. 27, p. 745-750.
Lucas, S.G., and Heckert, A.B., 2001, Theropod dinosaurs and the Early Jurassic ageof the Moenave Formation, Arizona-Utah, USA: Neves Jahrbuch fur Geologic andPaläontologie Mh., Stuttgart, Germany, v. 7, p. 435-448.
Lucas, S.G., Tanner, L.H., Heckert, A.B., and Hunt, A.P., 2005, Tetrapod biostratigraphyacross the Triassic-Jurassic boundary on the southern Colorado Plateau, USA, inTracking dinosaur origins, the Triassic/Jurassic terrestrial transition, abstracts volume,a conference held at Dixie State College, St. George, Utah, March 14-16, 2005, p.16.
Marzolf, J.E., 1994, Reconstruction of the early Mesozoic Cordilleran cratonal marginadjacent to the Colorado Plateau, in Caputo, M.V., Peterson, J.A., and Franczyk,K.J., editors, Mesozoic systems of the Rocky Mountain region, USA: Denver,Colorado, Rocky Mountain Section of the Society for Sedimentary Geology, p. 181-216.
Molina-Garza, R.S., Geissman, J.W., and Lucas, S.G., 2003, Paleomagnetism andmagnetostratigraphy of the lower Glen Canyon and upper Chinle Groups, Jurassic-Triassic of northern Arizona and northeast Utah: Journal of Geophysical Research,v. 108, no. B4, 2181, doi: 10.1029/2002JB001909.
Moore, D.W., Nealey, L.D., Rowley, P.D., Hatfield, S.C., Maxwell, D.J., and Mitchell,Eric, 2004, Geologic map of the Navajo Lake quadrangle, Kane and Iron Counties,Utah: Utah Geological Survey Map 199, 2 plates, scale 1:24,000.
Moore, D.W., and Sable, E.G., 2001, Geologic map of the Smithsonian Butte quadrangle,Washington County, Utah and Mohave County, Arizona: Utah Geological SurveyMiscellaneous Publication MP-01-1, 30 p., 2 plates, scale 1:24,000.
Nichols, D.J., 1995, Palynology and ages of some Upper Cretaceous formations in theMarkagunt and northwestern Kaiparowits Plateaus, southwestern Utah, in Maldonado,Florian, and Nealey, L.D., editors, Geologic studies in the Basin and Range–ColoradoPlateau transition in southeastern Nevada, southwestern Utah, and northwesternArizona, 1995: U.S. Geological Survey Bulletin 2153-E, p. 81-95.
Peterson, Fred, 1994, Sand dunes, sabkhas, streams, and shallow seas – Jurassicpaleogeography in the southern part of the Western Interior Basin, in Caputo, M.V.,Peterson, J.A., and Franczyk, K.J., editors, Mesozoic systems of the Rocky Mountainregion, USA: Denver, Colorado, Rocky Mountain Section of the Society forSedimentary Geology, p. 233-272.
Sable, E.G., 1995, Geologic map of the Hildale quadrangle, Washington and KaneCounties, Utah and Mohave County, Arizona: Utah Geological Survey Map 167,14 p., 2 plates, scale 1:24,000.
Sable, E.G., Biek, R.F., and Willis, G.C., in preparation, Geologic map of the SmithMesa quadrangle, Washington County, Utah: Utah Geological Survey Map, 2 plates,scale 1:24,000.
Sable, E.G., and Doelling, H.H., 1993, Geologic map of The Barracks quadrangle,Kane County, Utah: Utah Geological Survey Map 147, 11 p., 2 plates, scale 1:24,000.
—1990, Geologic map of the Elephant Butte quadrangle, Kane County, Utah andMohave County, Arizona: Utah Geological and Mineral Survey Map 126, 10 p.,2 plates, scale 1:24,000.
Sable, E.G., and Hereford, Richard, 2004, Geologic map of the Kanab 30'x60' quadrangle,Utah and Arizona: U.S. Geological Survey Geologic Investigations Series Map I-2655, 1 plate, scale 1:100,000.
Steiner, M.B., 2005, Correlation of Triassic/Jurassic boundary strata of North Americathrough paleomagnetic characteristics, in Tracking dinosaur origins, the Trias-sic/Jurassic terrestrial transition, abstracts volume, a conference held at Dixie StateCollege, St. George, Utah, March 14-16, 2005, p. 24.
Tibert, N.E., Leckie, R.M., Eaton, J.G., Kirkland, J.I., Colin, Jean-Paul, Leithold, E.L.,and McCormic, M.E., 2003, Recognition of relative sea-level change in UpperCretaceous coal-bearing strata – a paleoecological approach using agglutinatedforaminifera and ostracods to detect key stratigraphic surfaces, in Olsen, H.C., andLeckie, R.M., editors, Micropaleontologic proxies for sea-level change and strati-graphic discontinuities: Society for Sedimentary Geology Special Publication no.75, p. 263-299.
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QUATERNARY
Alluvial deposits
Stream deposits (Holocene) – Stratified, moderately to well-sorted sand,silt, clay, and pebble to boulder gravel in river channels and floodplains; locally includes small alluvial-fan and colluvial deposits, andminor terraces as much as 10 feet (3 m) above current stream level;generally 0 to 20 feet (0-6 m) thick.
Stream-terrace deposits (Holocene and upper Pleistocene) – Stratified,moderately to well-sorted sand, silt, and pebble to boulder gravel thatforms level to gently sloping terraces about 10 to 30 feet (3-9 m)above Deep Creek and Crystal Creek; because incision rates differalong the length of these streams throughout and beyond the quadrangle,age equivalency of Qat2 deposits throughout the Zion National Parkarea is not known; deposited in river-channel and flood-plain envi-ronments; locally includes colluvial and alluvial-fan deposits toosmall to map separately; 0 to 30 feet (0-9 m) thick.
Old stream deposits (middle to lower Pleistocene) – Yellowish-brown,moderately sorted sand, silt, and pebble to boulder gravel that formsisolated deposits as much as 1000 feet (300 m) above Deep Creek;prominent clasts include subrounded cobbles and boulders of Creta-ceous fossiliferous sandstone, recycled, rounded pebbles and smallcobbles of Precambrian and Cambrian quartzite, subrounded cobblesand boulders of basalt, uncommon, subrounded cobbles and bouldersof early Tertiary Claron Formation limestone, and, locally, cobblesof Carmel Formation limestone; query indicates uncertain designationdue to poor exposures and remote location; deposited in stream-channel environment; 0 to about 60 feet (0-20 m) thick.
Alluvial-fan deposits (Holocene to upper Pleistocene) – Poorly tomoderately sorted, poorly stratified, boulder- to clay-size sedimentdeposited as small alluvial fans along major drainages; level 1 depositsform active depositional surfaces, although locally the fan’s masterstream is deeply entrenched; level 2 deposits form deeply incisedinactive surfaces as much as 50 feet (15 m) above active drainages;typically overlies and includes stream deposits (Qal1) at the toe ofthe fans, and locally includes minor slope wash and talus along theupslope margins of the fans; generally 0 to 40 feet (0-12 m) thick.
Artificial-fill deposits
Artificial-fill deposits (historical) – Fill used to create a small stockpond in the west-central part of the quadrangle and a landing strip atBurnt Flat; as much as 25 feet (8 m) thick.
Colluvial deposits
Colluvial deposits (Holocene to upper Pleistocene) – Poorly sorted,angular, clay- to boulder-size, locally derived sediment depositedprincipally by slope wash and soil creep; gradational with talus depositsand mixed alluvial and colluvial deposits; locally includes talus onslopes where colluvium and talus form a thin mantle that grades fromone deposit to another; older colluvial deposits are mapped only atthe south end of Miners Peak and consist of reworked old bouldergravel deposits; generally less than 20 feet (6 m) thick.
Eolian deposits
Eolian sand deposits (Holocene) – Well- to very well sorted, fine- tomedium-grained, well-rounded, frosted quartz sand derived from theNavajo Sandstone; mapped only on top of the Volcano Knoll lavaflow near Virgin Flats; 0 to 6 feet (0-2 m) thick.
Mass-movement deposits
Landslide deposits, undivided (Holocene to middle[?] Pleistocene) –Mass-movement complexes similar to both younger (Qmsy) and older(Qmso) mass-movement deposits, but not readily distinguishable; 0to 200 feet (0-60+ m) or more thick.
Landslide deposits (Historical to middle[?] Pleistocene) – Very poorlysorted, clay- to boulder-size, locally derived material deposited byrotational and translational landslide movement; characterized byhummocky topography, numerous internal scarps, and chaotic beddingattitudes; basal slip surfaces most commonly form in the lower unitof the Co-op Creek Limestone Member of the Carmel Formation, theCedar Mountain Formation, the Dakota Formation, and the upper unitof the Straight Cliffs Formation, and the slides incorporate these andoverlying map units; the Dakota Formation especially forms verylarge, complex mass movements; Qmsh denotes slides having historicalmovement; younger landslides (Qmsy) may have historical movement,but typically are characterized by slightly more subdued landslidefeatures indicative of early Holocene to late Pleistocene age; olderlandslides (Qmso) are deeply incised and their main scarps andhummocky topography have been extensively modified by erosion,suggestive of late to possibly middle(?) Pleistocene age, but they toomay be locally active; query indicates uncertain designation; Qmso(Kd) denotes large, relatively coherent bedrock blocks of the DakotaFormation as much as 200 feet (60 m) thick that slumped downslopeunder the influence of gravity and that are likely late to possiblymiddle(?) Pleistocene age.
Talus deposits (Holocene to upper Pleistocene) – Very poorly sorted,angular boulders and finer grained interstitial sediment depositedprincipally by rock fall on and at the base of steep slopes; typicallygrades downslope into colluvial deposits and may include colluvialdeposits where impractical to differentiate the two; includes a thin,unmapped ribbon of alluvial deposits in the upper reaches of DeepCreek and West Fork; generally less than 30 feet (9 m) thick.
Mixed-environment deposits
Alluvial and colluvial deposits (Holocene to upper Pleistocene) – Poorlyto moderately sorted, generally poorly stratified, clay- to boulder-size, locally derived sediments deposited principally in swales, smalldrainages, and the upper reaches of large streams by fluvial, slope-wash, and creep processes; gradational with both alluvial and colluvialdeposits; Qac deposits form active depositional surfaces and aregenerally less than 20 feet (6 m) thick; Qaco deposits are deeplyincised and of similar thickness.
Alluvial and eolian deposits (Holocene to Pleistocene) – Locally derived,fine- to coarse-grained sand and silt with subangular to subroundedgravel; deposited in topographic depressions by slope wash and wind;includes small alluvial fans and colluvium along margins of deposits;locally conceals the Virgin Flats and Volcano Knoll flows; 0 to 20feet (0-6 m) thick.
Eolian and alluvial deposits (Holocene to Pleistocene) – Locally derived,fine- to medium-grained sand and silt with minor coarse sand andsubangular to subrounded gravel; deposited in topographic depressionsby wind and slope wash; includes small alluvial fans and colluviumalong margins of deposits; locally conceals the Volcano Knoll flow;0 to 20 feet (0-6 m) thick.
Residual and eolian deposits (Holocene to Pleistocene) – Reddish-orange to pale-yellowish-gray, residual silt and fine sand with scatteredresidual, subangular gravel; forms discontinuous mantle over the Co-op Creek Limestone; locally reworked by eolian processes; generally0 to 10 feet (0-3 m) thick.
Stacked-unit deposits
Hornet Point lava flow and eolian sand deposits (Holocene to Pleis-tocene) – Hornet Point lava flow that is partly covered by a mantleof eolian sand and silt; eolian deposits are generally 0 to 10 feet (0-3 m) thick.
Volcanic rocks
Major- and trace-element geochemistry and 40Ar/39Ar raw data areavailable on the Utah Geological Survey Web site (http://geology.utah.gov/online/analytical_data.htm); rock names are after LeBas andothers (1986).
Three Creeks lava flow (middle Pleistocene) – Medium to dark-gray,fine-grained olivine basalt lava flow; not dated, but probably less than300,000 years old based on amount of incision adjacent to flow;erupted from one or more vents in the adjacent Webster Flat andNavajo Lake quadrangles; as much as 35 feet (11 m) thick.
Volcano Knoll lava flow and cinder cone (middle Pleistocene) –Medium- to dark-gray, fine-grained olivine basalt lava flow; sampleCP71900-6 yielded 40Ar/39Ar plateau age of 0.34 ± 0.03 Ma; consistsof as many as seven cooling units that total as much as 300 feet (90m) thick where it blocked the ancestral Deep Creek channel; eruptedfrom vent at Volcano Knoll cinder cone (Qbvkc).
Virgin Flats lava flow and cinder cone (middle Pleistocene) – Medium- to dark-gray, fine-grained olivine basalt lava flow; sample CP71900-1 yielded 40Ar/39Ar plateau age of 0.37 ± 0.02 Ma; erupted from ventat unnamed cinder cone (Qbvfc) at the common border of sections16 and 17, T. 39 S., R. 10 W.; maximum exposed thickness is about100 feet (30 m).
Hornet Point lava flow (middle Pleistocene) – Medium- to dark-gray,medium- to coarse-grained olivine basalt to trachybasalt lava flow;contains abundant pyroxene phenocrysts; locally deeply weatheredto gruss-like soils and boulders typically have concentric weatheringrinds; sample CP83100-3 yielded 40Ar/39Ar isochron age of 0.74 ±0.05 Ma; erupted from vent at deeply weathered cinder cone at HornetPoint in the Kolob Reservoir quadrangle (Biek, 2007a); as much as200 feet (60 m) thick in this quadrangle.
Horse Knoll lava flow and cinder cones (lower Pleistocene) – Medium- to dark-gray, fine-grained olivine basaltic trachyandesite to trachybasaltlava flow; yielded a K-Ar age of 0.81 ± 0.05 Ma (Best and others,1980); locally consists of at least eight cooling units that total about300 feet (90 m) thick; erupted from vents at Horse Knoll and PineKnoll in the adjacent Straight Canyon quadrangle and at least twosmaller vents marked by cinder cones (Qbhkc) in this quadrangle.
unconformity
TERTIARY
Old boulder gravel deposits (Miocene) – Unconsolidated, very poorlysorted, clay- to very large boulder-size sediment characterized byvery large quartz monzonite boulders; quartz monzonite boulders asmuch as about 30 feet (10 m) in diameter constitute about 90% of thedeposits; clasts also include large boulders of Claron Formationlimestone to 18 feet (6 m) long, recycled, rounded pebbles and smallcobbles of Precambrian and Cambrian quartzite, lesser Cretaceoussandstone boulders, and rare cobbles and boulders of pebbly sandstoneof uncertain origin; except for the quartzite, most clasts are subangularto subrounded; caps Miners Peak in the northwest part of the quad-rangle; probably deposited by debris flows originating in the ancestralPine Valley Mountains (see Biek, 2007a, b, and references therein fora discussion of the provenance and age of these unusual deposits); 0-90 feet (0-27 m) thick.
unconformity
CRETACEOUS
Straight Cliffs Formation
Upper unit (Upper Cretaceous, Santonian to Turonian) – Slope-forming, grayish-orange to yellowish-brown, thin- to thick-bedded,fine-grained subarkosic sandstone and gray mudstone and shale;contains a few thin coal beds, common carbonaceous shale, andseveral thin bivalve coquina beds; forms broad, rounded hillstypically mantled with unmapped colluvium; east of Deep Creek,the ground surface is locally covered with a residual pebble lagpresumably derived from a weathered conglomerate bed in thelower part of the unit; believed to be equivalent to the SmokyHollow Member and possibly John Henry Member of the StraightCliffs Formation of the Kaiparowits Plateau (see, for example,Eaton and others, 2001); deposited in fluvial, flood-plain, andlagoonal environments of a coastal plain (Eaton and others, 2001);at least 600 feet (180 m) thick in the quadrangle, but upper contactnot preserved.
Tibbet Canyon Member (Upper Cretaceous, Turonian) – Grayish-orange to yellowish-brown, generally medium- to thick-bedded,planar-bedded, fine- to medium-grained quartzose sandstone andlesser interbedded, grayish-orange to gray mudstone and siltstone;locally contains pelecypods, gastropods, and thin to thick beds ofoyster coquina; typically forms bold cliffs; upper contact correspondsto a break in slope and is placed at the top of a coquinoid oyster
bed that caps the member; deposited in shoreface, lagoonal, estuarine,and flood-plain environments of a coastal plain (Laurin and Sageman,2001; Tibert and others, 2003); about 450 to 550 feet (135-170 m)thick.
Tropic Shale (Upper Cretaceous, Turonian to Cenomanian) – Yellowish-brown and gray, slope-forming mudstone, fine-grained sandstone,and silty sandstone; basal mudstone locally characterized by a lag ofseptarian nodules; locally contains Inoceramus sp. fossils indicativeof open shallow-marine environment (see, for example, Eaton andothers, 2001); very poorly exposed, but forms subtle, vegetated slopeat the base of the Straight Cliffs Formation and above the prominent“sugarledge sandstone” (Cashion, 1961) at the top of the DakotaFormation; upper contact placed at the base of the cliff-forming,planar beds of the Straight Cliffs Formation; deposited in shallow-marine environment dominated by fine-grained clastic sediment (Tibertand others, 2003); thins westward across the quadrangle, from about200 feet (60 m) thick near Cogswell Point to about 40 feet (12 m)thick south of Miners Peak; query indicates uncertain designation atThorley Point where Tropic strata, if present, may be a few feet thick.
Dakota Formation (Upper Cretaceous, Cenomanian) – Interbedded,slope- and ledge-forming sandstone, siltstone, mudstone, claystone,carbonaceous shale, coal, and marl; sandstone is yellowish brown orlocally white, thin to very thick bedded, fine to medium grained;includes two prominent cliff-forming sandstone beds each severaltens of feet thick in the upper part of the formation, the upper one ofwhich may correspond to the “sugarledge sandstone” of Cashion(1961); mudstone and claystone are gray to yellowish brown andcommonly smectitic; oyster coquina beds, clams, and gastropods,including large Craginia sp., are common, especially in the upperpart of the section; thin marl beds above the “sugarledge sandstone”locally contain small, distinctive gastropods with beaded edge Adme-topsis n. sp. indicative of a latest Cenomanian brackish environment(Eaton and others, 2001) (for example, sample CPF61901-1 in section35, T. 38 S., R. 10 W.); Dakota strata are typically poorly exposedand involved in large landslides; large blocks involved in rotationallandslides are labeled Qmso(Kd); upper contact placed at the top ofthe thin marl beds overlying the “sugarledge sandstone”; depositedin a variety of flood-plain, estuarine, lagoonal, and swamp environments(Gustason, 1989; Laurin and Sageman, 2001; Tibert and others, 2003);invertebrate and palynomorph fossil assemblages indicate shallow-marine, brackish, and fresh-water deposits of Cenomanian age (Nichols,1995); about 700 to 900 feet (210-275 m) thick.
unconformity
Cedar Mountain Formation
Cedar Mountain Formation, undivided (Cretaceous, Cenomanianto Albian) – Gray to variegated smectitic mudstone with minorlight-gray to yellowish-gray fine-grained sandstone; near the baseof this predominantly mudstone interval there is a distinctive, 1- to4-foot-thick (0.3-1.2 m), locally ledge-forming, pale-olive to greenish-gray, thin- to medium-bedded, fine- to medium-grained sandstonecontaining subangular, reddish-brown chert granules; east of CrystalCreek and Deep Creek, includes the basal conglomerate member(Kcmc), a 10-to 15-foot-thick (3-5 m), ledge-forming conglomeratethat is generally too thin to depict separately in this area; except forthin conglomerate ledge at base, weathers to generally poorlyexposed slopes covered with debris from the overlying DakotaFormation; upper contact is poorly exposed and corresponds to acolor and lithologic change, from comparatively brightly coloredsmectitic mudstone below to gray and light-yellowish-brownmudstone and fine-grained sandstone above; regionally, the CedarMountain Formation is unconformably overlain by the DakotaFormation (see, for example, Kirkland and others, 1997); we obtaineda single-crystal 40Ar/39Ar age of 97.9 ± 0.5 Ma on sanidine froma volcanic ash in Cedar Mountain mudstones in the Straight Canyonquadrangle to the east; recent pollen analyses indicate an Albian orolder age for these beds (Doelling and Davis, 1989; Hylland, 2000);deposited in flood-plain environment of a broad coastal plain(Tschudy and others, 1984; Kirkland and others, 1997); previouslymapped as the lower part of the Dakota Formation, but the lithology,age, and stratigraphic position of these beds suggest correlation tothe Cedar Mountain Formation; 0 to 100 feet (0-30 m) thick.
Conglomerate member (Cretaceous, Cenomanian to Albian) – Thick- to very thick bedded, yellowish-brown, channel-form conglomerate,pebbly sandstone, and pebbly gritstone; clasts are subrounded torounded, pebble- to small-cobble-size quartzite, chert, limestone,and rare, reworked petrified wood; locally stained reddish-brownto dark-yellowish-brown; west of Volcano Knoll consists of a basal,ledge-forming pebbly conglomerate 10 to 15 feet (3-5 m) thick thatgrades upward to a grayish-orange to very pale-orange, non-calcareous, fine- to medium-grained quartzose sandstone and pebblysandstone that has a “sugary” texture; this generally poorly cementedsandstone is characterized by low-angle cross-stratification withpebbles concentrated along cross-bed surfaces, and it contains afew thin, poorly exposed mudstone and siltstone intervals near thetop of the unit; west of Crystal Creek and Deep Creek upper contactis poorly exposed and upper Cedar Mountain mudstone unit maybe missing, but marks a change from yellowish-brown pebblyconglomerate or very pale-orange pebbly sandstone below (Kcmc)to yellowish-brown to gray mudstone and fine-grained sandstoneabove (Kd); east of these creeks, the contact between the thin lowerconglomerate unit (Kcmc) and the upper mudstone unit (Kcm) issharp, but this contact is not mapped due to problems of scale;deposited in river-channel environment on broad coastal plain(Tschudy and others, 1984; Kirkland and others, 1997); about 10to 180 feet (3-55 m) thick.
unconformity (K)
JURASSIC
Carmel Formation
Winsor Member (Middle Jurassic) – Light-reddish-brown, very fineto medium-grained sandstone and siltstone; uppermost beds typicallybleached white; poorly cemented and so weathers to denselyvegetated slopes, or, locally, badland topography; upper contact isthe basal Cretaceous unconformity and in this quadrangle Winsorstrata are everywhere overlain by pebbly conglomerate; depositedon a broad, sandy mudflat (Imlay, 1980; Blakey and others, 1983);about 200 to 240 feet (60-73 m) thick.
Paria River Member (Middle Jurassic) – Laminated to very thinbedded, light-gray argillaceous limestone and micritic limestone,and, locally, a basal, thick, white, alabaster gypsum bed; limestoneweathers to small chips and plates, forms steep, ledgy slopes, andlocally contains small pelecypod fossils; upper contact is sharp andplanar; deposited in shallow-marine and coastal-sabkha environments(Imlay, 1980; Blakey and others, 1983); about 40 to 110 feet (12-35 m) thick.
Crystal Creek Member (Middle Jurassic) – Thin- to medium-bedded,reddish-brown, gypsiferous siltstone, mudstone, and very fine tomedium-grained sandstone; typically friable and weakly cementedwith gypsum; forms vegetated, poorly exposed slopes; upper contactis sharp and broadly wavy and corresponds to the base of a thickParia River gypsum bed or argillaceous limestone interval; depositedin coastal-sabkha and tidal-flat environments (Imlay, 1980; Blakeyand others, 1983); about 150 to 200 feet (45-60 m) thick.
Co-op Creek Limestone Member (Middle Jurassic) – Thin- tomedium-bedded, light-gray micritic limestone and calcareous shale;locally contains Isocrinus sp. columnals, pelecypods, and gastropods;deposited in a shallow-marine environment (Imlay, 1980; Blakeyand others, 1983).
Upper unit – Thin- to medium-bedded, light-gray micritic limestone;locally oolitic and sandy; forms sparsely vegetated, ledgy slopesand cliffs; upper contact is sharp and planar; about 80 to 120 feet(24-37 m) thick.
Lower unit – Mostly thinly laminated to thin-bedded, light-graycalcareous shale and platy limestone; forms steep, vegetatedslopes; contact with upper unit is gradational and corresponds toa subtle break in slope and vegetation patterns; about 200 to 240feet (60-73 m) thick.
unconformity (J-2)
Temple Cap Formation
White Throne Member (Middle Jurassic) – Very thick bedded,yellowish-gray to pale-orange, well-sorted, fine-grained quartzsandstone with large high-angle cross-beds; similar to the NavajoSandstone; upper contact is sharp and planar and corresponds tothe J-2 unconformity; deposited in coastal dune field (Blakey, 1994;Peterson, 1994); about 120 to 160 feet (37-50 m) thick.
Sinawava Member (Middle Jurassic) – Interbedded, slope-forming,moderate-reddish-brown mudstone, siltstone, and very fine grainedsilty sandstone; forms narrow, but prominent, deep-reddish-brown,vegetated slope at the top of the Navajo Sandstone; upper contactis gradational and interfingering with the White Throne Member;deposited in coastal-sabkha and tidal-flat environments (Blakey,1994; Peterson, 1994); about 40 feet (12 m) thick.
unconformity (J-1)
Navajo Sandstone (Lower Jurassic) – Massively cross-bedded, poorlyto moderately well-cemented sandstone that consists of well-rounded,fine- to medium-grained, frosted quartz; typically very light gray orwhite because of alteration and remobilization of limonitic andhematitic cement; locally moderate-reddish-orange to moderate-orange-pink; contains rare planar interdune deposits; forms spectacular,sheer cliffs and is locally prominently jointed; upper, unconformablecontact is sharp and planar and corresponds to a prominent break inslope, with cliff-forming, cross-bedded sandstone below and reddish-brown mudstone above; generally equivalent to the “white Navajo”as mapped in the Temple of Sinawava quadrangle (Doelling, 2002);deposited in a vast coastal and inland dune field with prevailing windsprincipally from the north (Blakey, 1994; Peterson, 1994); only theupper 840 feet (255 m) is exposed in the quadrangle, but the formationis about 2100 to 2200 feet (640-670 m) thick in the Zion NationalPark area.
Kayenta Formation
Marzolf (1994) and Blakey (1994) presented evidence to restrict theMoenave Formation to the Dinosaur Canyon and Whitmore PointMembers, with a major regional unconformity at the base of theSpringdale Sandstone. Further work supports this evidence, indicatingthat the Springdale Sandstone is more closely related to the KayentaFormation and should be made its basal member (see, for example,Lucas and Heckert, 2001; Molina-Garza and others, 2003; Steiner,2005). We anticipate that this change will be formalized, and so hereinformally reassign the Springdale Sandstone as the basal member ofthe Kayenta Formation.
Upper unit (Lower Jurassic) – Shown on cross section only; about700 to 1000 feet (210-300 m) thick (Doelling, 2002; Willis andHylland, 2002; Biek, 2007b).
Springdale Sandstone Member (Lower Jurassic) – Shown on crosssection only; about 100 to 150 feet (30-45 m) thick (Willis andHylland, 2002; Biek, 2007b).
unconformity
JURASSIC AND TRIASSIC
Moenave Formation, undivided (Lower Jurassic to Upper Triassic) –Shown on cross section only; age from Lucas and others (2005); about200 to 350 feet (60-105 m) thick (Willis and Hylland, 2002; Biek,2007b).
J-0 unconformity
TRIASSIC
Chinle Formation, undivided (Upper Triassic) – Shown on cross sectiononly; about 450 to 650 feet (135-200 m) thick (Willis and Hylland,2002; Biek, 2007b).
TR-3 unconformity
Moenkopi Formation, undivided (Middle to Lower Triassic) – Shownon cross section only; about 1700 to 1800 feet (520-550 m) thick(Willis and Hylland, 2002; Biek, 2007b).
View east across the Crystal Creek and Deep Creek drainages from below Thorley Point. The Tropic Shale (Kt) forms a westward-thinning, heavily vegetated slope at the base of theTibbet Canyon Member of the Straight Cliffs Formation (Kst). The Dakota Formation (Kd) is locally exposed at the base of the cliffs, but typically forms large landslide complexes thatcover most of the lowlands below. Sample CPF61901-1 from a thin marl bed at the top of the Dakota Formation yielded small, distinctive gastropods with a beaded edge (Admetopsisn. sp.) indicative of a latest Cenomanian brackish environment. The 800,000-year-old Horse Knoll basaltic lava flow (Qbhk) forms a classic inverted valley east of Deep Creek. Theupper unit of the Straight Cliffs Formation (Ksu) is also shown. On the skyline northeast of the Cogswell Point quadrangle, the Tertiary Claron Formation forms the Pink Cliffs of theMarkagunt Plateau.
View north-northeast to the Winsor Member of the Carmel Formation (Jcw) and newly identified Cedar Mountain Formation(Kcmc and Kcm) along Crystal Creek in the south-central part of section 2, T. 39 S., R. 10 W. The poorly cemented Winsor Memberlocally weathers to badland topography and its uppermost part is typically bleached white to light gray. The Cedar MountainFormation includes a thin basal pebbly conglomerate member (Kcmc) with rounded quartzite and chert clasts that is overlain bygray to variegated smectitic mudstone (Kcm). The heavily vegetated Dakota Formation (Kd) unconformably overlies CedarMountain strata and typically forms large complex landslides. The Tibbet Canyon Member of the Straights Cliffs Formation formsthe bold cliffs on the skyline.
Close-up of Cedar Mountain conglomerate mem-ber (Kcmc) showing pebbly conglomerate, gritstone,and thin sandstone interbeds that collectively totalabout 15 feet (5 m) thick. Underlying Winsor strata(Jcw) and overlying Cedar Mountain mudstone(Kcm) are also shown.
Contact
Normal fault, dashed where approximately located, dottedwhere concealed; bar and ball on downthrown side
Structure contour on top of Navajo Sandstone (near southborder) and on top of Tibbet Canyon Member (northand central parts of map); short dash where projected,long dash where control is poor; interval 100 feet
Landslide or slump scarp, hachures on down-dropped side
Approximate strike and dip of inclined bedding determinedphotogrammetrically
Pit - sand and gravel (no letter), cinders (c)
Spring
Volcanic vent
Sample location and number
Qal1
Qat2
Qao
Qf
Qes
Qms
Qmt
Qae
Qea
Qre
Qes/Qbhp
Qbtc
Qbhp
Ta
Ksu
Kt
Kd
Kcm
Kcmc
Jcw
Jcp
Jcx
Jccu
Jccl
Jtw
Jts
Jn
Jku
Jks
JTRm
TRc
TRm
Qbvk
Qbvf
Qbhk
Qbvkc
Qbvfc
Qbhkc
2
CP719001-7
MAP SYMBOLS
REFERENCES
Selected geologic maps available for the Zion National Park areaIn addition to the 1:24,000-scale geologic quadrangle maps listed below, Hamilton(1978) provided a 1:31,680-scale geologic map of Zion National Park. See indexmap on plate 1 for quadrangle locations.
Cedar Mountain Averitt (1962)Clear Creek Mountain Hylland (2000)Elephant Butte Sable and Doelling (1990)Hildale Sable (1995)Kanarraville Averitt (1967)Kolob Reservoir Biek (2007a)Navajo Lake Moore and others (2004)Kolob Arch Biek (2007b)Little Creek Mountain Hayden (2004)Smith Mesa Sable and others (in preparation)Smithsonian Butte Moore and Sable (2001)Springdale East Doelling and others (2002)Springdale West Willis and others (2002)Straight Canyon Cashion (1967)Temple of Sinawava Doelling (2002)The Barracks Sable and Doelling (1993)The Guardian Angels Willis and Hylland (2002)Virgin Hayden (in preparation)Webster Flat Doelling and Graham (1972)
Acknowledgments
We appreciate the assistance of Dave Sharrow, National Park Service, who helped coordinate this mapping project. PeteRowley, Geologic Mapping Inc., and Grant Willis, Utah Geological Survey (UGS), provided constructive reviews of thismap. Gary Christenson, Sandy Eldredge, Hugh Hurlow, and Dave Tabet, each with the UGS, also reviewed parts of this map.Thanks to Jim Kirkland for identifying Cretaceous gastropods and for sharing his knowledge of the Cretaceous strata ofsouthwest Utah. Photogrammetric model setup and GIS digital cartography was by Kent Brown (UGS). Bill McIntosh andhis colleagues at the New Mexico Geochronology Research Laboratory provided 40Ar/39Ar analyses on basalt flows. AlanDeino, Berkeley Geochronology Center, provided the 40Ar/39Ar age for volcanic ash from the Cedar Mountain Formation.
