UGA-Geosite-Biek-Sevier-Fault.indd Utah Geosites 2019 Utah Geological Association Publication 48 M. Milligan, R.F. Biek, P. Inkenbrandt, and P. Nielsen, editors Robert F. Biek Utah Geological Survey, P.O. Box 146100, Salt Lake City, UT 84114-6100 bobbiek@utah.gov Cover Image: View north-northeast across Utah Highway 12 to the Sevier fault and Black Mountain at the entrance to Red Canyon. Sevier Fault at Red Canyon 2 M. Milligan, R.F. Biek, P. Inkenbrandt, and P. Nielsen, editors 2019 Utah Geological Association Publication 48 Utah Geosites 2019 Utah Geological Association Publication 48 M. Milligan, R.F. Biek, P. Inkenbrandt, and P. Nielsen, editors Utah Geosites showcases some of Utah’s spectacular geology, both little-known localities and sites seen by visitors to Utah’s many national and state parks and monuments. Th e geosites refl ect the interests of the many volunteers who wrote to share some of their favorite geologic sites. Th e list is eclectic and far from complete, and we hope that additional geosites will be added in the coming years. Th e Utah Geological Survey also maintains a list of geosites https://geology.utah.gov/apps/geosights/index.htm. We thank the many authors for their geosite contributions, Utah Geological Association members who make annual UGA publications possible, and the American Association of Petroleum Geologists—Rocky Mountain Section Foundation for a generous grant for desktop publishing of these geosite papers. Design and desktop publishing by Jenny Erickson, Graphic Designer, dutchiedesign.com, Salt Lake City, Utah. Th is is an open-access article in which the Utah Geological Association permits unrestricted use, distribution, and reproduction of text and fi gures that are not noted as copyrighted, provided the original author and source are credited. See the Utah Geological Association website, www.utahgeology.org, and Creative Commons https://creativecommons.org/licenses/by/4.0/ for details. Suggested citation for this geosite: Biek, R.F., 2019, Sevier fault at Red Canyon, in Milligan, M., Biek, R.F., Inkenbrandt, P., and Nielsen, P., editors, Utah Geosites: Utah Geological Association Publication 48, 6 p., https://doi.org/10.31711/geosites.v1i1.53. Presidents Message I have had the pleasure of working with many diff erent geologists from all around the world. As I have traveled around Utah for work and pleasure, many times I have observed vehicles parked alongside the road with many people climbing around an outcrop or walking up a trail in a canyon. Whether these people are from Utah or from another state or country, they all are quick to mention to me how wonderful our geology is here in Utah. Utah is at the junction of several diff erent geological provinces. We have the Basin and Range to the west and the Central Utah Hingeline and Th rust Belt down the middle. Th e Uinta Mountains have outcrops of some of the oldest sedimentary rock in Utah. Utah also has its share of young cinder cones and basaltic lava fl ows, and ancient laccoliths, stratovolcanoes, and plutonic rocks. Th e general public comes to Utah to experience our wonderful scenic geology throughout our state and national parks. Driving between our national and state parks is a breathtaking experience. Th e “Utah Geosites” has been a great undertaking by many people. I wanted to involve as many people as we could in preparing this guidebook. We have had great response from authors that visit or work here in the state. Several authors have more than one site that they consider unique and want to share with the rest of us. I wanted to make the guidebook usable by geologists wanting to see outcrops and to the informed general public. Th e articles are well written and the editorial work on this guidebook has been top quality. I would like to personally thank Mark Milligan, Bob Biek, and Paul Inkenbrandt for their editorial work on this guidebook. Th is guidebook could not have happened without their support. I would like to thank Jenny Erickson for doing the great desktop publishing and the many authors and reviewers that helped prepare the articles. Your work has been outstanding and will certainly showcase the many great places and geology of Utah. Last, but not least, Th ank you to the American Association of Petroleum Geologists, Rocky Mountain Section Foundation for their fi nancial support for this publication. Guidebook 48 will hopefully be a dynamic document with the potential to add additional “geosites” in the future. I hope more authors will volunteer articles on their favorite sites. I would like to fi ll the map with locations so that a person or family looking at the map or articles will see a great location to read about and visit. Enjoy Guidebook 48 and enjoy the geology of Utah. Peter J. Nielsen 2019 UGA President R.F. Biek Sevier Fault at Red Canyon 3 INTRODUCTION The Sevier fault is spectacularly displayed on the north side of Utah Highway 12 at the entrance to Red Canyon, where it offsets a 500,000-year-old basaltic lava flow. The fault is one of several active, major faults that break apart the western margin of the Col- orado Plateau in southwestern Utah. The Sevier fault is a “normal” fault, a type of fault that forms during extension of the earth’s crust, where one side of the fault moves down relative to the other side. In this case, the down-dropped side (the hanging wall) is west of the fault; the upthrown side (the footwall) lies to the east. The contrasting colors of rocks across the fault make the fault stand out in vivid detail (figure 1). Immediately south of Red Canyon, the 5-million-year-old Rock Canyon lava flow, which erupted on the eastern slope of the Mark- agunt Plateau, flowed eastward and crossed the fault (which at the time juxtaposed non-resistant fan alluvium against coarse-grained volcaniclastic deposits) (figure 2) (Biek and others, 2015). The flow is now offset 775 to 1130 feet (235-345 m) along the main strand of the fault, yielding an anomalously low vertical slip rate of about 0.05 mm/yr (Lund and others, 2008). However, this eastern branch of the Sevier fault accounts for only part of the total dis- placement on the fault zone. A concealed, down-to-the-west fault is present west of coarse-grained volcaniclastic strata at the base of the Claron cliffs. Seismic reflection data indicate that the total displacement on the fault zone in this area is about 3000 feet (900 m) (Lundin, 1987, 1989; Davis, 1999). LOCATION Park at the scenic overlook and rest stop 2.6 miles (4.2 km) east of the junction of Utah Highway 12 and U.S. Highway 89. Coordi- nates are 37° 44' 38", 112° 19' 46". Picnic tables and pit toilets are available. Figures 3 and 4 show a geologic map and cross section of this area. Several scenic pullouts and a paved bicycle trail make Red Canyon a popular spot for visitors on their way to nearby Bryce Canyon National Park. A U.S. Forest Service visitor center with restroom facilities is about one mile (1.6 km) east up Red Canyon. Figure 1. View north-northeast across Utah Highway 12 to the Sevier fault and Black Mountain at the entrance to Red Canyon. The 500,000-year-old Red Canyon lava flow (Qbrc) on the north side of the canyon erupted from vents on the down-dropped side of the Sevier fault (red line, D = down, U = up) and flowed eastward across the fault, which then did not form a significant topographic barrier as it does today (at the time the lava flow erupted, the fault juxtaposed tilted, non-re- sistant late Tertiary basin-fill deposits in the hanging wall against non-resistant, basal Brian Head strata in the footwall). The lava flow has since been displaced about 650 feet (200 m), yielding a vertical slip rate of 0.4 mm/yr (Lund and others, 2008). The trace of the fault is largely concealed by talus and landslides. Tvf, late Tertiary basin-fill deposits; Tbhv, basal Brian Head strata; Tbm, conglomerate at Boat Mesa; Tcwl, lower unit of the white member of the Claron Formation; Tcp, pink member of the Claron Formation. Figure 2. View south along the Sevier fault zone just south of Red Canyon. 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Qmtc Tbrc Qms Tm(Ti) Qc Qc Ksd Qc Kk Kst Qms Kw Qgtp Qms Qacf Qaly Qalo Tbrc QaoTm Qc Kgc Qac Tql QacQap Qms QmsTbh Qacfo Qms Tcp Kw Qafo Qaly Qacf Qc Qmtc Qms Qacf Qca Qmt Qms Ksj Tql Qmsc Qms Tcw? Tm Qc Qalo Qc Qac Tm(Tdm) Qc Kw Tcp Qap Ti? QTap Qacf Tm(Ti) Qaf2Tm(Tbh) Thma Qms Kk Tbhm Qafy Qmtc Qat Tm(Ti) Kw Qc Tbh Kwcs Qaf2 QalyQmtc Qacf Qc/Tcp Qms Qac Qafo Tcp? Qac Thm Ksd Qafy Ksd QTap Tbh Qacf Qacfo Tbh Tbh Qap Tm(Ti) Qmtc Qalo Qms Qacf Tm Qaly Qms Qc Tm(Td) Qaly Qacf Tm(Ta) Qmtc Qac Tm(Td) Tcp Qafo Tql Qc Tbh Qafo Tm(Ta) Tbrc Qacf Tm(Td) Tm(Ti) Tm? Qalo Qac Qaly Tbh Tvg QafoQms Qacf Qaly Qaly Tm Qacf Qacf Qmtc Qms Taf Qaly Qc Qafo Qaly QafoTm Qc QTap Taf Qat Thm Qaly Qms Qac Qaf2 Tbh Tbrc?Qc Qmtc Tvf Tcp Taf Qmsc Qmtc Qafy Ti Qacf QmtcQafy Qms Tcp Kw Qac Qacf QTap Tm(Tbv) Tcp Qap Tm(Ti) Qaf2 Qc/Tcp Qmtc Ti Qacf Qms Ksj Qc Tm(Td) Qaco Kw Kgc Qacfo Tm(Tbh) Qc Tcwl Qc Qac Qc Ti Qat Qafo Qmt Thm Qms Qc Qms Tbh Ksj Qaco Qafo Tm(Ta) Tm(Ti) Tm(Tbh) Qafy Qmt Qc Tm Qmtc QafyTbh Ksd Qacf Qco Qacf Qms? Qms? Qacfo Ti Qaly Qalo Qc Qc Qaly Qac Qafy Qaly Qms? Tcwl QTap Qms Qac Qap Tcp Qms? Taf Tcwm Tm(Tqcb) Kw Qco Tbh Qmtc Tm Qaly Qacf Qc Qmtc Qac QTap Qap Tm(Tbv) Qac Qafo Qac Qc Qaf2 Tm Tm Tcw Tm(Ti) Ksd Qbrc Qc Qc Qmtc Qafy Qc QTap Qc Qc Tcw Tvf Qafo Qmt Tcp Tcw Qap Qafy Tm Qap Qc Kwcs Qalo Tcwl Qafo Qms Qap Qms Qms Qaly Qafy Kk Qaf2 Qaf2 Kgc Tm Qc Qce Kw Qms(Ti) Qafo Qmtc Kw Tcwl Qbrc Qafy Tm(Ti) Qaf2 Qafo Tcw Qaco Qaly Qac Qac Ti Tmf QTap Qms Qac Kwcs Qmtc Tm(Td) Qms QTapKsj Qac Tbhv Tm Qaly Qmtc Ksd Qc Tm Qc Ti Qco Qafo Qafo Qc Tbrc? Qco QTap Kw Tm(Ti) Qafo QalyTbmQaf1 Qmtc Tm(Ti) Tm Ksjs Tcw Tm(Td) Ksj Taf Qc Qafo Qac Tm Tcw Qc Tm Tcp Qacf Qms? Tcwl Tql Tm? Taf Qms?QTap Tbdh Qms? Thm Qac Tm(Tbv) Kst Tcwl Tbm Kw Ksjs Qaly Tm Qac Tm(Ti) Tm QTap Qaf2 Qaly QTap Qms Tm(Td) Tcw Tm(Ti) QcQap Tbrc? Qafy Ti Tm Qafo Qmtc Qat Tm(Tbv) Qms Qacf Tcw Tm Ta Qac Qms Qap Qc Tcp Tcw Qac Qmtc Tm(Ti) Qafy Qaco Qmtc Qalo Taf QhdQacQms Qmsc Qmtc Tbdh Tcp? QacQat Ksd Qacf Ti Qbrc Tm(Ti) Qac Qac Qacf Qc Ksj Ti Tm Tcwm Qaly Kw Kst Qac Qaly Qac Qacf Qafo QcTbm Tm Qms Kw Kwcs Qms Qc Kgc Tm(Td) Qacfo Tcp Tbm Tbrc? QTap Qafo Tqcb Ti Qbe Td Qacf Qaf1 Qac TcpQacf Tm(Ti) Qmtc Qms Qac Qacf QTapTbh Qalo Qc Tm(Ti) QTap Tqh Tbhv Qc Tcp Taf Tql Tcwm Tbm QTap Tql Kgc Qaf2 Tcwu Qc Qc Qmt Qc Qms Qacfo Tm(Tbv) Qacf Td Tbm Qmt Qc Qc Tm Qms Qms Tbhv Qaly KsdQms Qaf2 Taf Qaly Qac Qat Qms Ti Tbhv Qc Qmtc Qap Kwcs Qmt Tcw Qafy Tm(Ti) Qacf Qc Qacf Qac Tm(Ti) Ti Tbrc? Ksd Tm(Tbv) Tql Tm(Tdbv) Qmt Tvf Qmtc Tcp Qaf2 Qaf2 Tqcb Kgc Qaf2 Tm(Ti) Ksd Qc Qafy Tmf(Td) Tcw QTap Tbh Qms Kwcs Tbh Qms Qafy Qbe Qc Ti QacTcp Qmtc Thm Qc Taf Qc Qc Qafy Ksj Qacf Qaly Qacf Qc Tm(Td) Qac Tql Ti Td Qbc Qbs Tbhv Qc Qaly Qmtc Ksd Ti Qac Qms Tbm Tm Qafo Qap Qmtc Tql? QTlf Qacf Tqh Qc Tm(Tbv) Qafy Qac Qbsc Tm(Ti) Tbhv Qc Qmt Qac Qafo Tbh? Qaly Qmtc Qacfo Tm Ksd QacQac Qac Qac QmtcQat Qms? Qacfo Ksd Tm(Ti) Qaly Qc Tcp Qac Qms? Taf Qmtc Qaf2 Qc Ksj Qacf Tm Qaf2 Tbh1 QTaf Qalo Tm Qap QTap Kwcs Thm Tqcb Tbhv Qms Qms Qbs Thm Qat Tbfr Qaf2 Qat Qacf Tcwm Qac Qac Ksj Tm Qafo Tcp Qms Qc Qc Qmtc Qc Qal Qafo2 Ti Tql TbhvTvf Qc Qc Qc Qms Qac Kgc Qaf2 Qafy Qac Tcwu Tbfr Taf Qac Thma Qms Tcw Tbh Tm(Td)Qc Tbhv Qc Qmtc Tm Kw Qac Qafo Qms? Qap Qc Tcwm Qaly Qap Qac Qc/Tbh Qc Qms Tm Qc TbdhcTm(Ti) Tcwl Qap Qmtc Kwcs Qap Ksj Qac Qacfo Tbhv Qc Ksd Tbm Qc Ksj Ksd Ti Tm(Td) Tm(Ti) Ksjs Qap Ksj Qaf1 Tcwm Qms Qc Tcwl Qacf KwcsQaf2 Qac Qafo Qaf2 Tbh Tm(Tbv) Ksd Qc Ti Qat Kgc Tm(Tbv)Qaly Qmtc Qacf Qafy Tm Qc Qms Qco Qmtc Ti Qafy Tcwm Qmtc Tbh Qafo Tqcb Qmtc Tm(Ti) Td Qaly Qmtco Qac TcwQap Tm Tcwu Qap Tbhv Ksj Tcw Tbm Qat Qaly Tbm? Qacf Tcp Tbhv Tm Qaf1 Qms QacQc Qmtc Tm(Tbv) Ti Tbdh Tcp Qacf Ti Qbs Qc Tm(Tbv) Tbhv Qafy Qc Qacf Qaly Tbfr Tcwu Kwcs Qc Qms Tql Tm(Ti) Qac Qc Qc Qc QTap Qms? Qaly Tbh Qms Tm Qafy Qmtco Tm(Ti) Qc Qafo Kwcs Qc Qms Taf Tcp Qc Qco Tcp Qalo Qacf Tcp Qc Qac Tbh Qc Tbm Tm Qafo Tbdh Qms? Qc Tm(Tdbv) Tm(Td) Tbh Qc Taf TcwQTap Qms Tm(Tbh)Tbdh Qca Qaf2 Ti Kgc Tbh Tm Tql Qaf2 Kwcs Tm(Td) Qap Tcw Qafy Tbm Tbh Tm(Ti) Ksd Qbs Qacf Qaly Qaly Ti? Tm(Tbv) Tm(Td) Qac Qmtc Qac Ti Qms Qac Tm(Tbv) Qacf Taf Qaly Qmtc Qc Qmtco Qco Qmt Qmtco TbvKwcs Qaly Tbhv Ksjs Qap Qaly Tbhv Tcp Tm(Tdbv) Qafy Tm(Td) Qmtc Qaf1 Ti Qca Qmt Ti Qafy Tm(Tbv) Taf Tcp Tbh Qms Qafo? Qacf Qc Tbm Ksj Kgc Tcwu? Qmtc QTaf Tcp Qacf Ti Qmtco Qac Tcwm? Qac KwQc Tcw Tm(Tql) Tm(Tbv) Tm(Td) Tcp Tvf Qmt Qac Tm(Ti) Tbh Qc/TbhKwcs Qap Qco Tbhv Tcwt? Ksd Qmt Qafy Qaco Tm(Td) Tcwl Qac QTap Qc Qaf2 Ti? QbsQmt Qaf2 Qc/Tbh Qafo Thm Qms Ksd Qc Ksd Tm(Tbv) Qc Tbh Qms? Ksd Qc Qmtc Qap Tm(Td) Qc Qac Tm(Tbv) Qafo Kw Qac Qacf Qmtc Td Tbh1 Qat Qaly Qc/Tbh Ti Qms? Qmtc Ksd Kwcs Qmtc Tm Qaco Tcp Taf Tm(Td) Thma Tbh1 Kgc Qmtc Qc Qacf Qmtc Tbh2 Ti Kwcs Qap Qap Qac Qms Qafo Tcwu? Tbh Qafo Qmtc Ksj Taf Qat Qafo Tm Qafy Qap QTaf Tm(Tbv) Ti Qaly Qafo Tcw Tbhv Taf Tbh Qms Qco Tcwl Qap Qacf Qc Tcwm? Ti Thm Qac Qac Qms Tm Td Qc Qaf2 Tcwm QTap Ksj Kgc Qat Tcwl Tbh Tcp Qac Tbh Qacf Tcp Qac Qc/Tbh QafoQaly Qc/TcpQc/Tcp Qla Qc/Tbh Tcwl? Qc Tbh Qms Qafy Qafy Ti Qac Ti Tcw Qaf2 Tm(Tbh2) Tcw QTaf Tm(Tbv) Tm(Td) Qaf2 Qc Qafo Tbh1 Qms Qac Qc/Tbh Td Ti Tm(Tdbv) Tcwu Qms? Qmtc Qc TafTm Tm(Ti) Tm(Tbv) Qms Tbfr Tbh Qaly Tcw Qmtc Ti Qac Qmtc Qac Qaco Qc Tm(Td) Tm(Ti) Qaf2 Qap Tm(Tbh3)Ti Qac Qafo Tbh Qafo TvfQmtc Ti Qac Qms Qms Tbhv Qms Ksj Qaco Qc Qc Qc Kgc Tbh1 Qafo Qms Tm(Ti) Qmt Tm(Td) Qms Qac Tbh Qacf Qafy Taf Tm(Tnw) Qafo Ksd Taf Qal Tm(Td) Tm(Tdbv) Ti Qbrh Tbml Qc Qafo Tcp Thm Tbm Qac QacTm(Td) Qafo Taf Td Qaly Tcwm Qc Qms? Qc/Kws Tbh Qaly Qaco Qacf Qmtc Qaly Qaf1 Qmtc Tm(Ti) Qco Qce Qafo Qac Qaly Tcp Kwcs Qacf Tcp Qac Tcw Qmtc Tcwm Tm(Ti) Qacf Tm(Tnw) Tbfr Qmtc Tm(Td) Qaco Qacf Tcwl Tbh3 Tbh1 Tm(Ta) Qc Qmtc Qmtc Qms Tcwl Qafy Qms? Tcwl Ti Qafo Tm(Ti) Qmtc Qbwc Qc Qc Qc Qac Qap Ksj Qac Qc/Tbh Qap Qafo Kil Qacf TbhTaf Qmtc Tbh Tbm Qaly Tm(Td) Tbh2 QmtcTcw Qco Qat Qafy Tm(Tdbv) Qc Tbhb Ti Tcp Qmtc Qafo Qap Qal Tbfr Qat Qacf Tm(Ti) Qafo Tm(Tbv) Tm(Ta) Qms Ti Kgc Qacf Qafo Ti Qmtc Tm(Ti) Qms Qc Qmtc Qaly Tm(Td) Qaf1Qac Tbh Qc Qac Taf Qc Tbh Tm(Ti)Qms(Ti) Qms Tbm Tdk? QTap Qmtc Tm(Td) Kiu Ti Qac Qac Tm(Td) Tbh Qacf Qc Qms? Qaly Qmtc Qaly Thm Qms Qmtc Tm(Td) Tm(Tbv) Qmtc Qmtc Qafo QacoTm(Tbv) Tbh Tbhv Qmtc Qc Qaf2 Qacf QTap Qms Qc Qac Tbh Kgc Tm(Tbv) Qac Tm(Ti) Qms?Ti Qafy Qea Qmsc Qmtc Qaly Qms Tcw Qac Qafo Tcp Ksj Qc Ksd Tm(Tbv) Tm Tm Ksj Qafy Ksd Tm(Tbv) Qap Qms Qc Qaly Taf Qacf Qms? Tm(Tbh) Qms Tbh1 Tbh2 Qafy Tm(Tdbv) Tm Tm(Ti) Tm Qms? Qac Qac QacfTm(Tn) Qap Qafo2 Tbm Tcp Qc Tcp Tm(Td) Qc Qafo Kgc QmsTm(Tnw) Qc Qafy Tm(Tnw) Tbh3 Qac Qaco Qap Qc Qms? Qms Tm(Ti) Qafo Qaf2 Qacf Qac Qms Kwcs Tcw Qc Tbv Tbm Tm(Tbv) Kiu Qalo Tm(Td) Qc Tm(Ti) Qc Tbh Tm(Td) QcQc Tbh? Tbh QmscQaf2 Tm(Ti) Qacf Tcwm Tcwl Qms Qafo Qap Qc Qafy Qat Qafo Tm(Td) Qac Tm(Ti) Qc Qbw Qbrhc Tbh Tm Tm(Td) Tm Qc Tm(Tnw) Qaly Qap Qms? Qms Tm Qc Qacf Tbml Qc/Tbh? Tbml Qac Tm(Td) Tm(Tbv) Qaf2 Qafo Tbh3 Tm(Ti) TmTcp Qat Kwcs Tbh2 Tcw Ksd Kgc Qafo Qms Qms Tm(Tbv) Qafo Qacf Kwcs Qalo Qms Tbml Qac Qaf1 Ksj Qac Tm Qafo Tm(Ti) Tbm Qaly Qafo Tm(Tbv) Qmsc Tbm Tm Qac Qac Tm(Tbv) Qafy Qafy Qac Qco QcQms Qc Tm(Tbh1) Qmsh Qmsco Qacf Tbh3 QTaf Tbh1 Tbh Qms Qms Tbh1 Tm Qc Qaf2 Tbm Qaly Qap Qaly Qafy Qmtc Qaly Qc Qafo Tm Tm Qaly Qbw Tm(Td) Qafo Kil Tcw Tcw Tm(Tbv) Qafo Tbh Qafy Tbml Qafo2 Tbm Tbh1 Tbh2 Tm Qap Qae Tm(Td) Tbh Tm(Td) Qmt Tbh Tm(Ti)Kgc Tm(Td) QcTbh1 Qafo Qms? Qaf2 Kiu Tbh1 Tbh Qmsc Tbh3 Tbh2 Qafc Tm(Ti) Qap Kil Qms Qafo Qc Tm(Td) Qc Tm Qac Tm(Tbb) Tbh1 Tbh Qafy Qafo Tbh2 Qac Tm(Tbv) Tbh1 Qafo Qco Qmtc Qc Tm(Ti) Qlm Qafo Qafo Qat Qc Tm(Ti) Tbh1 Qaly Kwcsd Tm(Ti) Qaly Qc Qafo Qc Tm(Td) Qms Qaly Tm(Tn) Qafo Qce Qmsc Qaly Qafy Tbh Qap Tm(Tbv) Kgc Tm(Tbv) Tm(Ti) Qaly Qafo Tm(Td) Qmsc Tm(Tbv) Qbrh Qmsc Tbh3 Qms Tbh Qms Qms Tnw Kgc Td Qmt Tcp Qacf Qc Qafy Tm(Tn) Taf QTh Qc Tbh Qaly Kiu Qat Qaf2 Tm(Ti) Tm(Tbb) Tm(Tbv) Qms Qac Tbh Qc Qafo Qafy Tm(Tn) Kgc Qc Qat Qms? Qafo Qms Qafo Qms Kgc TbhTm Tm(Tnw) Qaf2 Qms? Tbh Tcp Tm(Td) Qmtc Qacfo Kiu Tm(Tbb) Ku Tbh3 Tm(Ti) Td Qac Qc Qlm Qc Kil Ksj Qc Qafo Qac Qaly Qac Qafy Qaf2Ku Qafc Qafy Qacf Tm(Td) Qc Qc Ksj Ku Tm(Tbvv) Tbh3 Tbh Tdk Tm(Tbv) Tm(Ti) Tm(Tn) Qc Ksj Qaly Qmsco Qacf Qaf2 Tbh3 Qc Tbh3 Qap Tm(Td) Qmsc Kiu Qaly Qaly Qes Tm(Tbv) Qafo Jcn Tm(Td) Qafo Qafo Qal Qc Tbh3Qap Qafo Tm(Tbv) Qc Qc Tm(Td) Jn Qmt Qaf2 Qafo Tbh3 Qac Qap Tm(Td) Jc Tbh Qafo Tbh Qaf2 Qaf2 Tm(Ti) Tm(Td) Qafo Tm(Ti) Qac Qc Qaf2 Qaf2 Tm(Tbv) Qc Tm(Td) Kgc Qaf2 Qc Tm Qms Qaf2 Qafo Qmtc Tbh3 QcQc Qmsc Tm(Td) Qap Qms Tm(Ti) Qms Qafo Qc/Tbh Qmsc Qacf Tm(Tbv) Qes Qac Qms Kgc Qms Qafo Qacf Qmsc Tm(Tn) Tm(Td) Tbh Tbh3 Qafo Qlm Qac Tbh Ksj Qms Tbh3 Qmtc Qap Jn? Qaf2 Tm(Tbh) Tm(Ti) Tm(Tnw) Tbh Qafo Qms Tdk Qafo Ti Tip Kwcsd Qms Qafo Qes Qafo Qmtc Tm(Td)Qac Qafy Qac Tm(Tbv?) Tm(Ti) Tm(Tbv?) Qafy Qc Qmsc Tdk Qms Qc Tbh Qaly Qac Qmtc Qac Tbh Tm(Tbh) Qms Qmsc Tm(Tnw) Qafy Qms? Qafo Qc Qafo Qms Qms? Tbh Qap QTaf Qaf2 Tdk Tbh Qc Tm(Td) Qat Qafo QTh Tbh3 Qc Qms Tm(Tn) Tnw Tbt Qmsc Qaf2 Qap Qc/Tbh Qc/Tbh Ti Tm(Tbvb)Tnl Tnl Tdk Tbh Qafo Tbhu1 Qafy Qafo Tbt Qaf2 Tm(Tbb) Qms Tnw Qaf2 Qc Qmt Qac Qac Tdk Qms Qaf1 Qms Qafo Qms Tm(Tbh) Ti Tnw Tbh Tnl Qaf2 Qap Tm(Td) Tm(Ti) Tm(Td)Tm(Td) Qafo Tbh3 Qat Tm(Tn) Qc Tnw Qaly QalyQc Qac Tnw Qac Qaly Qaly Ti Qafo Qaf2 Qes Qac Qlm Tbh Tbh3 Qacf Qafo Tm(Tbb) Qaly Qafy Qaly Qafy Qes Qafy Qaly Tnw Qac Tm(Td) Qaco Qms Qaco Qmt Tdk Qaly Qaf2 Taf Qat Qacfo Qc Qacf Qafo Tbh Qlm QTaf Tm(Tn) Ti QafoTm(Td) Tnw Qlp Tn Qafo Tbh Tbh Tn Qac Ti Tbh Qms Tbh Tnw QcTbh QTh Tnw Tm(Tbv) Ti Qc Tm(Tbv) Tql Tm(Ti) Tbt Qc QapQc Tm(Ti) Tcpl Tm(Tnw) Qat Ti Qmsc Tbh Tm(Td) Qac Ti Qc TcpTm(Tbh) Qes Tm(Tnw) Tcp Qms? Tn Qc Qafo Tdk Ti Qafy Qafy Ti Tm(Tbv) Tnl Qms Qafo Qms Qafo Qaly Qap Tbh Tm(Td) Tn Tm(Tbh)Qaf2 Tnl Tbh Tm(Ti) Tbt Qc Tm(Ti) Tm(Tn) Tm(Tbv) Ti Tm(Tbhu1) Tm(Tnw) Tm(Ti) Tm(Tnw) Tm(Ti) Tm(Tn) Tm(Tbhu2) Tbh Td Tnl Qaf2 Qac Tm(Tbb) Qmtc Tnw Tbh Qlm Qafo Qac Tm(Tbhu2) Ti Tn Tm(Td) Tm(Tbv) Qaly Qes Qafy Ti Qafo Qap Qms Tm(Tn) Qat Tm(Tbhu2) Ti Tm(Ti) Tm(Ti) Tm(Ti) Qac Qaf2 Tm(Tbv) Qap Qaly Tm(Tbb) Tm(Tbv) Qat Qc Qafo Tm(Tnw) Tnw QTaf Qafo Tdk Tnl Qat Qafo Qac Qmtc Tm(Td) Tcp Qafy Qaf2 Tm(Ti) Tm(Tqcb) Tm(Tbv)Tm(Td) Tdk Qafy Qac Tnw Tm(Td) Tnw Tm(Tbb) Qaly Tm(Ti) Tql Qafo Ti Td Tm(Tdli) Tbh Tm(Tbv) Qms Qafo Qms Tm(Tbvb) Tbt Tm(Tql) Tnl Tdk Tdbrp Ti Qac Tnw Qat Qc Qc Tdk Qafo Tm(Tbv) Qmtc Tm(Td) Qafo Tm(Td) Qac Qaf2 TqlTcp Tbrp Qms Qafo Qafo Qc Tm(Td) Qaly Qafy Qms? Tbt Td Taf Qac Tdk Qaf1 Qafo Qafo Tdbrp Tdk Qaco Tm(Tbb) Tbrp Tm(Td) Qap QTaf Qaly Qc Tm(Ti) Qafo Tm(Ti) Tql Tm(Tbv) Tm(Tql) Qaf2 Qafo Qap Tm(Tbv) Qaly Qc Tbh Qat Tm(Td) Qms? Tm(Td) Qafy Tm(Tbv) Qac Qafo Tnl TiQafy QTaf Qafo Tdk Tm(Tbv) Tm(Tbv) Qac Tm(Tbv) Tcp Qaly Ti QafoTm(Tn) Qafy Tm(Td) Tbv Qafo Tbv Tm(Tcp) Tm(Tbb) Qmtc Qms Td Qaly Qap Tm(Tbb) Tm(Tn) Tbv Ti Tm(Tbb) Tm(Tn) Tm(Td) Qaly Tm(Tbv) Tbht Tql Qafo Qafo Tm(Td) Tm(Ti) Td Qacf Tql Td Qms Qafo QafoTm(Td) Tm(Td) Tm(Tbrp) Tm(Td)Tm(Tbrp) Qafy Qap Tm(Tn) Qat Tbh Taf Tm(Td) Qafy Qap Tm(Td) Tm(Tbb) Tm(Ti) Tm(Td) Qmtc Tm(Tds) Tm(Td) Tm(Tds) Qafy Tm(Td) Tm(Td) Tm(Tbb) Qafo Qaly Qms Qafo Tm(Td) Qafo Tm(Tbv) Tm(Tbb) Qap Tm(Td) Qac Qap Qap Qaly Qap Qaly Qap Qat Tnw Qafy Tm(Tbv) Qafy Qafy Tbv Qafy Qafc Tm(Td) Tnl Qafy Qafc Qafo2 Tql Qafo Qaly Qafy Tql Ti Tbv Ti Tqin Qafo Tm Qafy Tm(Ti) Qms? Tm(Td) QTh Qaly Qafo Qaly Qms? Kil Tm Qms(Tql) Qaf1 Qaly Qc Qal Qal Qafy Qaf1 Tm(Tbv) Tm Tm(Tbv) Tm(Tcp) Tm(Tbv) Tm(Tql) Kgc Qafo Tnl Tm(Ti) Kil Kgc Kgc Tcp Tcp Jct Tbh Jn Tm(Tn) Qafo Qaf2 Ti Tcp Tm(Tbvb) Tm(Tbvb) Tbh Tm(Td) Tbh Tm(Td) Qms Qaly Tm(Tnw) Tm(Tbv) Tm(Ti) Tbh Tcp Tm(Td) Tm(Td) Tm(Td) Tm(Tnw) Tm(Tbv) Tm(Tbvb) Tm(Tbb) Tm(Td) Tm(Td) Tm(Td) Tm(Td) Tm(Tbv) Tm(Tbv) Tm(Td) Tm(Td) Tm(Tbv) Tm(Tbv) Tm(Tbv) Tm(Tbv) Tm(Ti) Tm Tm(Tbv) Tm(Tbv) Tm(Tbv) Tm(Tbv) Tm(Tbv) Tm(Tbv) Tm(Ti) Tm(Tbb) Tm(Td) Tm(Tbb) Tm(Tbv) Tm(Ti) Tm(Tn) Tm(Tbv) Tm(Ti) Tm(Ti) Tm(Tbv) Tm(Tn) Tm(Tbv) Qac Tm(Td) Tm(Td) Tm(Tbv) Tm(Tbv) Tm(Tbv) Tm(Tbv) Tm(Tbv) Tm(Td) Tm(Tbv) Qafy Tm(Tbhu1) Tm(Tbh) Tm(Tbhu2) Tm(Tbb) Qafy Tm(Td) Tm(Tbh) Qafo Tcw Td Td Tbhu1 Td Qac Qac Kw Tdk Tbt Tbt Tdk Tnw Tcw Tmf(Tbh)Tcw Qap Tcp Tcp Tcp Kw Qacf Qaly TcpTcwTbm Tbh Qac Qac Tcw Tbm Tcp Tcp Ksj Qaly Ksj Qap Qap Qap Qap Tbm Tbhv Tbh Qap Qap Ksj Tbh1 Qbrc Tbh Tbm Tbh Tm(Td) Tm(Td) Taf Tcwu Tvf Qal Tbrc Qacf Tvg Tbrc Tbrc Kwcg Qafo2 Qafo Qal QafoTbdh Tbrc?Taf Tbdh Tbrc?Tbdh Taf Qat Qafy Tbrc Qal QTap Tbh Qal Taf Tbfr Taf Tm(Td) Thm Tm(Ti) Qac Thm Tbh Taf Tm(Ti) Tm(Ta) Tm(Tbh) Ta Ta Tm(Ti) Tm(Ti) Tm(Td) Tm(Tbv) Tbh Qacf Tbh QTbx Ti Qms Ti Tm Tm(Tdbv) Tm Tm(Tdbv) Tm(Tdbv) Tm(Tdbv) Tm(Tdbv) Thm Tm(Tbv) Tm(Tdbv) Tm Tm(Tbvf) Tm(Tbv) Ti Tm Tm Tm Ti Ti? Tbh Tm(Ti) Qms(Ti) Qms Tm Tcp Tcp Tm(Ti) Qacfo Km Tm(Tbh) Kw Tcp Qms Tm Tm Qbe Tm Qbs Qafc Qbs Qafo Ti Tql Ti Qafy Tcp Tqcb Tqh Tm(Ti) Ksj Tcp Tbh Tcp Ti Kcm Ksd Qbwk Qacfo Kw Ksd Qalo Kw Ksd Ksjs Kw Ksd Qacfo Ksd Qat Ksd Kgc Qafo Calico bed? Qbal Calico bed? Kgc Tcwl Tcp Kgc Qbef QTbx Tcp Qalo Qacf Qbmk2 QTap Taf Tbh Qc Tbh Qbhk Qac Tcwu Tcwl Tbm Tbm Tbm Tcwu Tcwu Tbm Tcwu Qap Kw Qafo2 Qal Tcp Kkl Kwcs Tcwl Kkl Tcp Qc Tcw Tcwl Tcwl Tbm Kw Ksst Kw Kw Ksd Jcw Tbt Qaly Tm(Ti) Kil Tm(Tql) Tql Tm(Tn) Tm(Tbv) Tm(Ta) Tbh Tm(Ti) Tm Ti Ti Ti Td Kgc Kgc Ti Tbh Tbh Ta Tbh QTbx Tbm Tcwu Tl Kw Qafy Qms(Ktd) Tcwl Tcwm Kgc Kgc Kgc 25 11 15 3 8 4 20 9 22 20 18 18 15 6 45 4 11 3 3 1 2 2 2 2 25 7 5 5 8 70 12 9 4 6 2 27 3 5 3 3 2 2 12 5 4 3 3 2 2 2 2 3 2 2 30 35 7 6 8 6 30 7 4 12 13 8 22 17 2 3 3 45 25 12 45 7 9 20 18 42 34 22 5 15 3 5 5 10 9 12 8 14 30 10 20 10 8 11 10 4 45 40 40 2 40 35 21 5 30 40 30 50 35 35 30 18 10 35 10 30 15 10 55 12 10 8 10 15 30 27 15 22 25 65 35 35 35 10 32 30 5 4 30 45 7 25 80 2 14 4 28 33 15 7 30 2025 25 5 5 7 5 10 5 14 15 45 25 15 20 35 3 2 35 22 12 8 2 1 7 6 6 5 10 5 10 15 5 55 5 25 25 20 5 9 9 5 20 5 18 8 22 8 17 2218 15 32 5 30 25 32 20 15 25 10 5 10 8 12 6 4 12 4 11 20 35 10 35 70 15 15 80 35 10 8 17 8 14 20 12 5 11 6 24 15 7 10 18 22 15 15 25 25 15 20 15 13 9 10 15 85 40 40 20 35 12 55 8 4 4 3 4 6 5 65 52 80 34 65 10 4 12 3 7 12 6 10 5 16 30 5 12 7 20 2 3 5 11 14 14 25 12 4 5 8 11 30 25 2 5 10 6 2 8 6 10 5 1 2 15 2 1 4 1 1 3 5 2 35 10 40 40 15 26 30 20 15 13 15 25 20 5 4 5 2 10 20 50 75 10 25 10 70 3 5 45 40 30 12 46 15 35 14 20 3 2 3 4 2 2 1 10 2 1 2 3 2 3 3 2 2 2 2 2 2 10 10 5 7 3 20 60 63 55 58 37 78 80 72 85 10 2 2 2 2 7 5 2 8 12 10 40 14 50 30 25 15 33 15 4 12 4 26 25 12 70 60 75 41 6 2 30 80 2217 15 85 65 45 16 17 15 14 13 12 11 10 9 7 8 5 6 4 3 2 1 18 1 2 3 5 6 7 8 9 10 11 12 13 14 15 16 18 20 1 2 3 4 5 6 7 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60 61 62 63 64 65 66 67 68 69 70 71 72 73 74 75 76 77 78 79 80 81 82 83 84 85 86 87 88 89 90 91 92 93 94 95 96 97 98 15 100 101 102 103 104 105 106 107 110 114 115 116 118 119 120 121 122 123 126 127 128 129 130 131 132 133 134 135 136 137 138 139 140 141 142 143 144 145 146 147 148 149 150 151 152 153 154 155 156 157 158 159 160 161 162 163 164 165 166 167 168 169 170 171 172 173 174 175 176 177 178 179 180 181 182 183 184 185 186 189 190 191 194 195 196 197 198 199 200 201 202 203 204 205 206 207 208 209 210 211 212 213 214 215 216 218 219 220 221 223 224 225 226 227 228 229 230 231 232 233 234 235 236 237 238 239 240 241 242 243 245 1 2 3 4 5 6 7 9 10 11 12 13 14 99 16 17 18 19 20 21 22 23 24 26 27 29 30 31 32 33 3435 38 40 41 4243 44 222 46 48 49 50 246 247 248 249 250 251 252 253 254 255 256 4 17 29 108 109 111 112 113 117 124 125 187 188 192 193 217 244 8 25 28 37 39 47 15 SYNCLINE PANGUITCH AN TI CLI NE C AN YO N BR YC E SY N C LI N E CA NY O N BRYCE ANTICLINE BENCH JOHNSON ZO N E FA U LT PAUNSAUGUNT ZO NE FA ULT PA U N SA U G U N T FAULT THRUSTINN RUBYS FAULT THRUST HILLS PINE FA ULT THRUST VALLEY JOHNS FA ULT TH RU ST CREEK HUNTZO N E FA U LT SE V IE R ZO NE FA U LT SE VI ER FA U LT PA S S SA N D ZO N E FA U LT S E V IE R FA UL T PA N G U IT C H FA ULT VALLEY BE AR EA ST FAULT VA LL EY BEAR W EST FA UL T EA ST PEAK IR O N FA U LT W E ST PE AK IR ON FA ULT LEDGE BLACK FA U LT KN O LL W O O D FA UL T CANYON RA TT LE SN AK E FA UL T R ID G E NA VA JO FAULT ZO NE FAULT PAROWAN FA U LT TH R U ST SP R IN G S MOUNTA IN SU G AR LO AF FA U LT M O UN TA IN SU M M IT FA U LT H IL L JO N ES FA U LT R ID G E M ID DL E ZO N E FA UL T PA R AG O N AH ZO N E FAULT H IL LS RE D IR O N ZO N E FA U LT H U R R IC AN E F' F E' E D' D A' A B' B C' C 2 1 2 14 25 53 58 14 86 55 5947 20 3636 45 19 21 ? ? 1 0 1 2 3 40.5 MILES 1 0 1 2 3 4 5 60.5 KILOMETERS 1:62,500SCALE CONTOUR INTERVAL 50 METERS Disclaimer 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, and does not guarantee accuracy or completeness of the data. 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 1:62,500 scale only. This geologic map was funded by the Utah Geological Survey and the U.S. Geological Survey, National Cooperative Geologic Mapping Program through USGS STATEMAP award numbers 08HQAG0096, G09AC00152, G10AC00386, and G11AC20249. 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. Plate 1 Utah Geological Survey Map 270DM Geologic Map of the Panguitch 30' x 60' Quadrangle GEOLOGIC MAP OF THE PANGUITCH 30' X 60' QUADRANGLE, GARFIELD, IRON, AND KANE COUNTIES, UTAH 2015 by Robert F. Biek1, Peter D. Rowley2, John J. Anderson3, Florian Maldonado4, David W. Moore4, David B. Hacker5, Jeffrey G. Eaton6, Richard Hereford4, Harry Filkorn7, and Basia Matyjasik1 1 Utah Geological Survey, P.O. Box 146100, Salt Lake City, UT 84114-6100 2 Geologic Mapping Inc., P.O. Box 651, New Harmony, UT 84757 3 Kent State University, retired 4 U.S. Geological Survey, retired 5Department of Geology, Kent State University Trumbull Campus, Warren, OH 44483-1998 6Department of Geosciences, Weber State University, Ogden, UT 84408-2507 7Department of Physics and Planetary Science, Pierce College, Woodland Hills, CA 91371 APPROXIMATE MEAN DECLINATION, 2014 TR U E N O R TH M AG N ET IC N O R TH 111/2° Base from USGS Panguitch 30' x 60’ Quadrangle (1980) Projection: UTM Zone 12 Datum: NAD 1927 Spheroid: Clarke 1866 Project Manager: Douglas A. Sprinkel GIS and Cartography: Jay C. Hill, and Basia Matyjasik Utah Geological Survey 1594 West North Temple, Suite 3110 P.O. Box 146100, Salt Lake City, UT 84114-6100 (801) 537-3300 geology.utah.gov QUADRANGLE LOCATION U T A H UTAH GEOLOGICAL SURVEY a division of Utah Department of Natural Resources in cooperation with U.S. Geological Survey Sevier fault Sevier fault Black Mountain A A’ Parking area 12 89 UTAH ¹ 1 Mile 1 Kilometer 0 0 Tcp Taf Figure 3. Geologic map of the Red Canyon area, showing parking area to view the Sevier fault zone. Note numerous vent areas (stars) on Rock Canyon lava flow. Q = various surficial deposits; Qbrc = Red Canyon lava flow; Tbrc = Rock Canyon lava flow; Taf = old allu- vial-fan deposits; Tvg = coarse-grained volcaniclastic deposits; Tvf = fine-grained volcanic deposits; Tbh = Brian Head Formation; Tcp = pink member of the Claron Formation. Modified from Biek and others (2015). Figure 4. Schematic cross section showing displacement across the Sevier fault near Red Canyon. Basin-fill sediments (QTa) were stripped off the upthrown side of the fault prior to deposition of the Red Canyon lava flow (Qbrc). See figure 3 for cross section loca- tion and rock unit names. A A’ Sevier valley West East Black Mountain Paunsaugunt Plateau Qbrc QTaQTa QTa Tbh TbhTbh Tbh Tc Ku KuKu Tc Tc TcTcTc TbhQbrc 89 R.F. Biek Sevier Fault at Red Canyon 5 SEVIER FAULT Th e Sevier fault extends from south of the Grand Canyon north- ward to the southern part of the Marysvale volcanic fi eld, a dis- tance of at least 150 miles (250 km); it is known as the Toroweap fault in Arizona (fi gure 5) (Lund and others, 2008). Th e fault lies at the western base of the southern Sevier Plateau and Paunsau- gunt Plateau. Northward, fault-bounded basins in the heart of the Marysvale volcanic fi eld, including the Circleville, Marysvale, and Monroe areas, are on structural trend with the Sevier fault zone, indicating that the fault bisects the volcanic fi eld and links up with down-to-the-west normal faults in southern Sevier Valley south of Richfi eld (Hintze and others, 2003; Rowley and others, 2005). Like most long normal faults, the Sevier fault is composed of discrete parts that tend to rupture independently (Lund and others, 2008). Although Lund and others (2008) suggested that Hillsdale Canyon, about 3 miles (5 km) south of Red Canyon, may mark a segment boundary on the fault zone, Biek and others (2015) sug- gested a diff erent boundary farther north, east of Panguitch. Th ere, a complexly faulted bedrock high and associated graben in the hanging wall separate the Hatch part of the valley on the south from the Panguitch part of the valley on the north. In this area, numerous scarps are present on old alluvial fans where they collectively form a northeast-trending graben. Th is area also corresponds to the south end of the Sevier Plateau, which is of higher elevation and relief than the Paunsaugunt Plateau. Th is northern, “Panguitch” section of the fault zone appears to terminate several miles north of the junc- tion of Utah Highway 20 and U.S. Highway 89, where it devolves into an anastomosing series of down-to-the-west and down-to-the- east normal faults before linking up with the eastern bounding fault of Circleville Valley (fi gure 5) (Rowley and others, 2005). Displacement on the Sevier fault generally increases south to north along its length; it is about 3000 feet (900 m) at Red Canyon (Lundin, 1987, 1989; Davis, 1999; Lund and others, 2008). Apart from scarps in the hanging wall near Panguitch, no scarps on unconsolidated surfi cial deposits are present along the main trace of the Sevier fault in Utah. Th e inception of faulting on the Sevier fault zone is poorly known but widely cited as middle Miocene, 12 to 15 million years ago (see, for example, Davis, 1999). CLARON FORMATION Many people get their fi rst glimpse of the spectacularly colored, hoodoo-forming Claron Formation not at Bryce Canyon Nation- al Park or Cedar Breaks National Monument, but here in Red Canyon. Wide pullouts along the road attest to the area’s popular- ity, a stark contrast from the sage-covered, high-elevation basin and tree-covered plateau to the west. Apart from the bright pink, orange, and red rocks themselves (fi gure 6), what attracts most people are the fantastic variety of fi ns, spires, and hoodoos that the Claron Formation naturally erodes into. Hoodoos form by relatively rapid erosion of alternating resistant and less-resistant beds in combination with pervasive jointing, high precipitation rates, and some 200 freeze-thaw cycles per year. Freeze-thaw cycles loosen rock, whereas summer thunder- storms work to wash it away. Importantly however, new research shows that the local stress fi eld is a key factor that gives rise to the hoodoos; erosional processes act within that stress fi eld to create these fantastic forms (Bruthans and others, 2014). Th e vertical stress imparted by the weight of a resistant caprock holds grains together; as erosion removes some grains, the stress between the remaining grains increases, holding them more tightly together Red Canyon geosite Red Canyon geosite Circleville Marysvale Panguitch Section Figure 5. Th e Sevier-Toroweap, Hurricane, and Paunsaugunt faults in the Basin and Range-Colorado Plateau transition zone. Arrows indicate fault section boundaries. Each section likely has a diff erent rupture history and rate of long- term slip. Modifi ed from Lund and others (2008). 6 M. Milligan, R.F. Biek, P. Inkenbrandt, and P. Nielsen, editors 2019 Utah Geological Association Publication 48 and making it harder to erode the sides of the hoodoos. Erosion is thus slowed and the hoodoos tend to grow taller over time as in- tervening slopes erode. In addition, in the dry climate of southern Utah, much of the precipitation that falls on the hoodoos quickly evaporates, leaving behind any cement that the water started to dissolve and thus making the rind of the hoodoos more resistant. ACKNOWLEDGMENTS My knowledge of southwestern Utah geology comes from years of geologic mapping supported largely by the Utah Geological Sur- vey and U.S. Geological Survey. As the acknowledgments of those many published geologic maps attest, I am indebted to a great many people for their help over the years. Th anks to Grant Willis and Mike Hylland (UGS) and Kimm Harty (UGS retired) for their insightful reviews and to Jon Good (UGS) for draft ing the fi gures. REFERENCES Biek, R.F., Rowley, P.D., Anderson, J.J., Maldonado, F., Moore, D.W., Hacker, D.B., Eaton, J.G., Hereford, R., Filkorn, H.F., and Matyjasik, B., 2015, Geologic map of the Panguitch 30' x 60' quadrangle, Garfi eld, Iron, and Kane Counties, Utah: Utah Geological Survey Map 270DM, 162 p., 3 plates, scale 1:62,500. Bruthans, J., Soukup, J., Vaculikova, J., Filippi, M., Schweigstillova, J., Mayo, A.L., Masin, D., Kletetschka, G., and Rihosek, J., 2014, Sandstone landforms shaped by negative feedback be- tween stress and erosion: Nature Geoscience, v. 7, p. 597–601, published online, 20 July 2014 | DOI: 10.1038/NGEO2209. Davis, G.H., 1999, Structural geology of the Colorado Plateau region of southern Utah, with special emphasis on deforma- tion bands: Geological Society of America Special Paper 342, 157 p. Hintze, L.F., Davis, F.D., Rowley, P.D., Cunningham, C.G., Steven, T.A., and Willis, G.C., 2003, Geologic map of the Richfi eld 30' x 60' quadrangle, southeast Millard County and parts of Bea- ver, Piute, and Sevier Counties, Utah: Utah Geological Survey Map 195, 2 plates, scale 1:62,500. Lund, W.R., Knudsen, T.R., and Vice, G.S., 2008, Paleoseismic re- connaissance of the Sevier fault, Kane and Garfi eld Counties, Utah: Utah Geological Survey Special Study 122, Paleoseis- mology of Utah, volume 16, 31 p. Lundin, E.R., 1987, Th rusting of the Claron Formation, the Bryce Canyon region, Utah: Tucson, University of Arizona, M.S. thesis, 51 p. Lundin, E.R., 1989, Th rusting of the Claron Formation, the Bryce Canyon region, Utah: Geological Society of America Bulletin, v. 101, p. 1038–1050. Rowley, P.D., Vice, G.S., McDonald, R.E., Anderson, J.J., Machette, M.N., Maxwell, D.J., Ekren, E.B., Cunningham, C.G., Steven, T.A., and Wardlaw, B.R., 2005, Interim geologic map of the Beaver 30' x 60' quadrangle, Beaver, Piute, Iron, and Garfi eld Counties, Utah: Utah Geological Survey Open-File Report 454, 27 p., 1 plate, scale 1:100,000. Figure 6. Brightly colored Claron Formation at the entrance to Red Canyon. Yel- lowish-brown caprocks are pebbly conglomerate, evidence that these sedimentary rocks were deposited in stream and fl oodplain settings.