Interim Geologic Map of the Durst Mountain Quadrangle, Morgan and Weber Counties, Utah

Utah Geological Survey, a division of Open-File Report 498 Utah Department of Natural Resources Interim Geologic Map of the in cooperation with U.S. Geological Survey Durst Mountain 7.5' Quadrangle T

Cou S 85 Qc 68 51 23 37 Keh Qmc

70 U Keh Qc Qmc Zi Keh Qms Qms Tw Qms Qal R Qac Qac Qmc Cm Qdlb Qmc Keh Qmc Qmc Qms Qms Qmc H Zkc 48 26 Keh Qmc Tw 78 Cm T Zm 2 Qmc

Qac Zcc Keh Keh Tw Qmc Qmc

Qms 66 D Qmc 40 44 37 Keh Qac R Qmc Qms 88 Qms(TK) Qms Qat2 Cm A Tw Qa2? Tw L Keh Qmc Qmc Qmc L 42 6 Tw B I 7 Tw Qmc Qms?(Tw) Qa Qafo Cn Zkc Keh Qafy

Qmc W Qmc Qmc Qmc Tw Qmc Qal Qdlb 70 10 Qao Cn Qac Qc Qms Qal Qmc Cn Qms Qac 39 Qms Qal2 Qlg? Qmc Qmc Qmc Qmc Qmc Qms Qla/Qms Keh Qmc Qmc Qc Qms Qmc Ql Qc 15 Qms Qlg 15 27 Qmc Qms Qal Qac Qac Qms Qmc Qmc Qmc Ql/Qms Qms Keh Tw Qmc Qmc Qac Qaf Qmc Keh 12 Tw Keh 54 Tw Tw Qms Qms Qms Qac Qao Qafy Qc Qms Qmc Qa Qms?(Tw) Qay Ql Qms Qmc 7 Qmc Qal2 Qmc Tw Qafy Qla Qmso?(Tw) Qmc Tcg Ql Qms Qmc Qla 5 Tw Qmc Qay Qay Keh Qmc Tw Qmc Qmc Qmc Tw Keh Tw Ql/Tcg Qmc Qmc 4 Qc Ql/Tcg 5 Qmc Qafy Qla Ql Keh Qmc Qac Qms Qafy Qmc Qmc Qac Qafy 5 Qac Tcg Keh 34 Tw 5 4 Qac Ql/Tcg Ql Qla Tw Qms Qmc Qmdf Qms Qh Qmc 5 Keh 2 Qmc Qmc Qms Qafy Keh Qmc Tw Qac Qms Ql Ql 2 Qa2 Qmc Qc Qa2? Qac Qmc Qms Qmc Ql/Tcg B 4 Tw Tw Ql/Tcg Keh Qmc Keh Qmc Tcg Ql Qafy Qmc 84 Qmc Qmc 10 7 Qmdf Qc B Tcg Qla Jn Qmc Keh Qmc Tcg Qlg? 11 Keh 21 Tw Tw Qms? B X B Jn Keh 2 Tw Keh? Qa Qc Qms Qmc Qms?(Tcg) Qc 64 Qms Qla Ql Qmc Keh Qmc Tw Qmdf Qac Keh? Qac Qac 28 Keh B Keh? Qmc Qc Qmc Qms Tcg Qdlb Jn 25 Qac Qmc Qc Qmc Qmc Qab? Qms Qac Qafp? B 12 Qay Keh Qms Qla 53 16 Keh Qc Qng Qms Qmc Qmc Keh Qap? Tw Qc Qmc Qmc X Jn Keh Qms Qc Qcg 8 Qmc/Qa 2 2 Qmc Ql? Jn Qfdb Keh? Qmc Tw Qc 31 34 Qc Qafp? Qc Qmc Qc Qmc B 22 Qmc Qac Ql/Thv Keh Qap? 2 Qmc Tw Qms Qdlb Qcg Qa Qac Qc Qms(Tcg) Qdlb? Keh? Qmc Qmc Qmso Qms Keh Tw Qms 3 Qc Qc Qafy Thv Qap? Qms Qc Qla? Qmc Qmc Qc Qms Qac B Keh Qmc Qmc Qc Qmc Qms Qac TRt 46 Qmc 15 Qms Tcg Jn 78 Qmc Qcg Tcg Tcg Qms Keh Qmc/Qap Qac Qac Qmc Qmc Qmc Qms Qc Qac 4 Tw Qms Qal Qmc Qmso Qafy Qac TRa Qms?(Tw) Qc Qfdb Qaf Thv Qmso Qmc Qms Qms?(Tcg) Qms?(Tcg) Qms Qcg Qap Qmc Qmc Qmc B Qmc Qc Qms?(Tcw?) B Qa 22 Qms Qac Qmc Qms 42 Qcg Qmc Qmc Keh Qap Qcg Qc 2 Qmc TRt Qaf Qmc Qc Qmc Qmc Qms 17 Qmc 1 Qmc Qms Thv 16 6 Tcg Qms Qfdb Qmc Qac Qmc 46 Keh 0.5 Qms B Qmc 3 Qmc 14 13 Qaf TRt Keh 16 Qmc 3 Qmc Qc 29 Qc Qa Qac Tcg Qms Thv Qap Keh Qms Qmc TRt Qmc Qmc Qc Qay 3 Qafo Qmc 2 Qmc Qmc 23 Thv Qms BENNETT CREEK THRUST Qap Qaf Qmc 2 Pp Qms Qac Qac Qmc 2 Tcg 19 Tcg Qmc Tcg Qmc Qab? Qmc Qcg Qac 4 18 Qms Qms?(Ts) Qms Qmc 41 Qms Qcg Qac Qmc 6 Qms Thv Mhu Qms Qms Qmc 3 Tcg Qms Tcw Qmdf Qmc Qac Qmc Thv Qmc Qms Qmc 46 10 Qms 4 Qms 43 35 Qms 59 Keh Keh 11 Tw 15 Qms Keh Keh Qmc Qmc Keh Qc Qac Qmc Tcg Qc Qc Thv 21 Mhl Mdl Qac Qmc Qac Qc Qms Qms?(Tcg) Qac Qms Qc Qmc Mde Mdu Qmso Mdl Qmc Qmc Qmc Qmc Qmc Qac Qms Qmc 27 Qmc Qc Qc Qc Qmc Qmc Qms Qms Qng Keh 26 8 Qmc Tcw Qmdf 26 20 44 Qc Qao 31 Qc Qay Qms?(Tcg) 22 Mdl Keh 2 Qmc Qmc Mhu Qmc Tcg 12 Qmc Qms Qmc Qab Qab? Qmc Tcw 35 25 Qc Qmc Qms Qmc Tcg Thv Mde Qmc Qao Qmc Qmc Qc Qc Qmc Qmc 36 55 Tw? Qa Qms Qmso Tcg Thv 11 Qmc Qmc Qap Tw? Qms 1 Qmc Qac Qafb? 25 Keh Qms Qcg Mdu Qc Qmc Qafb? Ml Qc Qa Qap Qmc Cm Qms Qmc Qmc Cn Mde 36 37 Qmc Qmc Tcw 26 Qms 19 Qa/Tw? Qmc 25 26 Qmc Mdl Keh Qc 22 Qmc Cm 40 Ml 20 9 Tw Tw Tcg Tcg Qms?(Tcg) 46 Mhl Qafy Qa/Tw? Tw Qms Qmc 44 Thv Qay? Qmc Qmc 70 Qafy 55 70 Qa Qmc Tw Qmc Qmc Qmc Qms?(Tcg) Qms Qms Mde Qap Qmc/Qa Qc Tw Qmc Qms 50 Qms/Qafb? Qms 35 Qa 29 Qmc Qms Qmc Qmc/Qa Qms?(Tcg) Qmc Qms 28 Qal Qmc Tcg Qmc Ml Qmc Qms Qmc/Qafo? 3 Qmc Qmc 29 Qac Qms Qmdf Qms Qmc Qab? Cm 45 Qap Qac Tcg Cn Qms 35 Qmc Tcw Qmc Qmc 2 Tw Tw Qms Qmc Qmc 12 Qa Qa Qmc Tcg Qmc 18 Cm Dwc 14 Qac Qac Qmc Qms Keh Keh? Qms?(Tcg) Qmc Ml Qmc Tw? Qac 29 Qmc wm Tcw Tcw Qms Dh Qmc Tcg Qmc 33 Mhu Qay Qmc Qms Tw Qmso? Thv? 42 Qms Qac 6 Qmc Qc Qms?(Tcg) Qms 12 Qaf Mdl? 11 Qmc Tw Qmc (Tcg) Qms 29 Qms Qmc Tcw 3 19 Qc Mhl 55 31 Qap Qaf 1 pimple mounds Tw Qmc Tcy? 10 Qmc Mde Qmc 2 Qmc 3 86 3 Qmc Qms?(Tcg) 7 Qc Keh Qmc Qc Qaf Qa 35 Qmc Qmc Qmc Tcy? Ml Qafy Qmc Qms Qmc Tcw Qaf Qmc 8 Qmc Qmc Qc Qc 30 Qap Qms Qms Qa 10 Thv Ml Qa Qafp 2 Qms Dh Qap Qmc Qc Qms Qms Qmc Qms?(Keh) Tcg Tcg 24 Qms Thv Db Tw Tn Thv Qmc 3 Qmc 21 37 Qaf Qng Qay Qac Qms?(Tcg) Qac Qms Thv? Qay Qafy Qc Keh pimple mounds Qa Qmc Qc Qms Qmc Qmdf Qmc Qc Qac Dh Ml Qmc Tn Qmc 33 Qms Tw Qmc Qc Tcg 26 Qac Qms Qaf Qms Qafp Tw Qms Dwc Qms 21 Qac Qmc Qms Dh Qms Qay Qc Qac Qms?(Tcg) Qms Qms Qa Ts Ml Qc 28 Tcg Qaf Qmc Tw Qmc Tcw TRd TRw 21 Qmc Ts 44 37 Ppm Qms Tw Qc 34 Qac PIPwl Qmc 8 Qms?(Tw) pimple mounds Qc stone stripes? 36 Qmc Db Qmc 42 Qac 10 9 Qms Keh Tw Tcw Ml Qa2 42 Qms Qms Ppf Qmc Qms Thv Ts/Ml 70 Keh Qmc Qc Tcg Qmc QaQao? 4 Tw Qmc Qcg Pwu 32 43 Qms TRd Qms 12 Ts 74 Qc Qmc 24 Qms Ppg Qc Qao Qc Qc Tn Qmc Tcy? Qms Qay 9 Tcg Qmc Dh PIPwl Ppm 33 Qmc 30 29 Qaf Keh Qac Qmc Tcg Qmso 54 Qmc Qmc pimple mounds Qmc 25 36 Qmc 3 41 N 35 66 Qms?(Pp) Qmc Qmc stone stripes? O Dh Tcg Tcw R 9 18 Qa Qmc Qafo? Tn wm? M Qc Keh Qmc Qc Qc Qac A Ts 37 Qms Tw Qmc Qms?(Tcw) L TRd Qmc F Qms A Db 14 Qms 29 U Qc 2 Qac Qmc L Qaf Qc Qms Tn Qcg T 38 Tn Qms Qmc Qc ? Qac Ml 44 Qms Qaf Pwu 25 22 Qms Ppf 19 Qms Tcg Qmc Ppg Tw Tn Tcg Qms?(Tcw) Ppm 23 Qms Dh Db Ppm Keh 30 Qafo PIPwl 13 21 Qmc Qms Qms Ppg 4 Qcg Dwc 20 Tw Qmc 24 Qmc Qms Pwu Qac Tn Qc Qmc Qmc Qms?(Tcg) Qms Dh Ml Qms Qmc Qmc Qac Qmc 32 Qmc Dh Qa Pwu Keh Tcg Dwc? Dh Db Qmc Dh Qmc Qap? Qmc 33 Qms Db Db Qmc Qmc Tcg Dwc? Dwc Db 62 Qms Qmc Qms Tw 23 Qmc Qmdf Ct 28 48 Qac Qac Db Qac Qac Tca Ts Db Qac Qms Qmc Qap? Tcg 26 33 Tca 75 63 Dh Tcg Tcw? Qms 7 Qmc Qac 31 Qmc Ts Dh 63 Cn Dh Keh Qms Qac Qmso Qmc Qmso Tcw Qms?(Tcw) 27 58 35 75 Ml Keh Qmc Dh Mhl Keh C Tn Cn 2 O Qmc Tca? Ts Dwc N wm? Qmc Cm 54 Cn 2 C Qms?(Tcg) Tcy? 13 Db E Qms?(Ts) Ts 32 25 Cm 57 64 Qms A Qac Tn Qmc Qmc 39 68 Qms LE Qmc Qmc Qmc Qms?(Tct) 14 18 Dh D Qmc Qms Cou 49 56 Cn TK? Qmc W Tcg Qms Qmc 19 Qmso Qmc Tcg Ml 23 Mde Tw IL LA 24 Qmc Qms Qmc 30 Com Cm Keh R Tn Qmc Qms Tcw D Qac Qmso Qc Qms Qac Col 44 T Qms 26 Tca? 17 37 55 41 H Qmc 37 45 42 60 R 28 Tca Tct Qms Col Db Qac Mdd U Qac Tcg 23 Com Cou S Qmc 21 Tcw Tcy? 52 72 T Qmc Ct 58 Db Qmc Tw Tcg Qc Tcg Tcg Tct Qmc 52 Ml Qac 5 Qmso Tcg Tcg Qng 44 71 Qac 26 Qms Qmc Qmso?(Tcg) Qmc Tct Qa 52 Col 62 Mhl Tcg Qmc Qms Qc Qac Qmc Tcg 34 Qms 59 Qms Qac Tcg Tca Qmc Ct 62 Qmc Qmc Qmc 7 73 Tcg 19 Tcw? Qmc 53 Tct Col Qms 57 28 11 Qmc Qac 18 Tcg Tcg 26 Tct 87 Qmc 66 Qc Tcg Qmc Qmdf Ct 86 Mhl Qc 20 30 Qng Qafy Qmc 85 Qmc Qc Tcg Qmc Ct Qa Tw Tcg Tcg 20 Qmc Qng 88 62 Qms Qms Qc Qmc Tcg Qc 57 Keh Qmc Qmc 50 53 63 26 Qmc 54 Db 21 28 Tcg Tct Tct 14 54 Mhl Qmc/Qatp Tn Tcg 30 Tct Qms Col Mde Qafo Qac Tn Tn Qms Qmc 11Qmc Ct 55 37 Qmc 30 25 Qmc Tca 23 Qmc Qmc/Qatp Tcg Tcg Tcg Qms?(Tcg) Qc 37 64 Qaf1 63 Qms?(Tcw) Qms Qmc Tct 8 Tct Cou Db Ml 24 Qms Qc Tn 33 Xf? 45 3 Keh Qms Qac 23 Qmc 18 Qafoe Qatp Qmc 21 Qac 31 Tcy? Qms 49 Mde Qmc Ct 21 Tct Qmc 67 Keh Tcg Tcg Tcw 26 18 22 55 Qms 25 Qal Qafy Qafo Qms Qmc Qafo Tn Tn 36 Qms 70 52 Dh 7 Keh Keh Qc Qac Qafo Tct Qmc Keh Qaf1 Keh Qab Tn Tcw Qmc Qms(Tct) Qng Qmc Db Ml Qmc Qaf1 Qmc Qatp Tw? Qac Tcw Xf 54 70 Keh Tcw 6 81 Dwc Qac Qmc Qac Tn Qms?(Tcg?) 7 Qms Mde Qc Qmc 24 Xf 72 Qac 4 Tw Qmso Qc Xf Cn Dh Db Qaf1 Qat2 Tw Tw Qc 27 Tcw Qac Qmc Tct 47 Qmc Qmc Tn Tct 41 69 75 Qmc Qmc Qms Tw Qms Qmc Qafo 21 40 Qms Cm Qmc Qmc Keh Qms Tw Qmso Qac Qms Tcw Qms(Xf) 81 Qaf1 Keh Tct Cou Dh Db Tw 12 29 Tcw 53 Qmc Ml Qms?(Tn) Qms?(Tn) 43 Qms(Xf) Qms Qmc Qaf1 Qms Tn Tw Xf Dwc Qa? 26 Tw Qmc Qmc Tcw Qms?(Xf) Xf Com Qat2 Qmc Qmso?(Tn) Tn Qc Tw? Qmc Col Cm Dh Qmc Qal Qafo Qms Qms Tct Keh Qa Qmc Qmc Qac Qafoe? Qmc Qms Qmso Qmt Cn 72 Qc Qac Tcg? Qmc Qc Qafo Qato Qmc 20 Xf Ct Cm Dwc Keh Qc/QTao/ Qmc Qms Tcg? 79 Qac Qmso 43 Qms?(Tw?) Xf Xf Qac 3 QTay? Tw Qafo Com Cn 29 Tw Qmc 28 Tw Qaf Qmc Qms 12 15 Tw? Qms Ct Cou Cm Qmc Qafy Qms Qms Tw Qmc Xf Qal2 Keh Qmso?(Tn) Tw Qaoe? Col QTay? Tn Qc Qng/Xf Tw Qmc Qao Qaf1 Qmso Tn 45 Qms?(Tw) 85 Qafy Qac 7 Qmc Xf Qafy Qms Qac Qafo 50 Qms Qms Qc Qmt Ct Xf Qmc Qac Qac 44 51 79 Qmc Qms?(Keh) Tn 45 24 42 Qms Qmc 84 Qmc Qac Qmc Qaoe 55 Qao Qms Ct Qmt Tw Qaoe Ct Qafb Qafy Qao? Db Qmc Qms Qms Ct Qa Qaf 88 Qmc Qab Qmso Qac Cou Qac Qms Qac 35 88 Qmc/Qaoe Keh Qms Qac 77 34 Qafy Qatp Xf Qmc Qms Com Qafo Qafy Qmc Qa Qao? 64 Qmc/QTa Qac Qab Qal Cm or Com Qms Qmc 79 Qms Keh Tw Qaf Qms 7 Qmc Qms Qafy Qafy Qaf Qafy Ct 87 Col Qmc Qap? 8 Qc Qmc Xf Qms Xfpg 60 Qmdf 72 Ml Qms Tw Qafo Qmc Xf 73 Qmc/Qap? Qmc Qafy QmXsf Xf Qms Qms Qmsy Qafy Qms Qaf 88 Qmc/Qat Qmc 81 Qmc Qms1 Qafy Qmc 26 Qms 38 Qmc Qms?(Tn) Qaoe? Qmsy Qms Xf Dh Db O Qms Qms Xf Qms Qms G Qmc Xf Qms?(Xf) Com 71 Qafb? Qat2 D 10 83 43 70 74 Dwc E Qms Qms Keh Qac Qms N Qms Xf Xf QTay? 71 Cn Qab Qal Qms Qms 81 23 Qat Qmc 75 Qmc Qdlb 43 Qms 40 Cou Qmc Qmc Qafy Xf Qac Qmc Cm Qmc Qdlb Tcg? Qmc Tcg 41 Qms Qms(Xf) Qmrf Col QTay Tw Qab Qmc Qmc 26 Qmc Tw Qms RO 60 Cm? 52 Tcg O Qms Qmc Qmc Ct 68 62 Qmc Tcg Qms F Qac 60 86T Xf 68 Qms(Xf) Qms Qafy 6 Qmc Xf H Qms Qms?(Xf) Xf Qmc Qms RU Qms 10 S Qms Qms?(Xf) Qms Qmc Qms 83 65 34 55 Qc 7 Qms T 42 75 Qfdb Tcy? Xf Qmc Qmc Qms Tcg Qmc Qms Col Cou Qmc Ct Tcg? Xf 80 32 Qms Xf 53 50 Qmc/QTay? Qafy Qmc Tcy? Qms Xf 82 2 Tw Xf Xf Qms 61 Qdlb Qms Qms Qms 69 80 50 14 Qmc Qac Xf Qms Qms Col Qms?(Ts) 6 76 Qmc 77 Ct Keh Qmc Tcg 5 Qms?(Xf) Qms(Xf) Qms 59 Tcg? Ct Qac Cm 75 Keh 12 Tw 57 Qms Qms?(Xf) 73 Qmdf Qmc Qao 13 82 40 Qms Qms 60 Qmc Tcy? Qms Ct 64 77 Qms Qmc Xf 72 55 73 46 89 Qaf1 Thv Qms Qms 78 45 Col 70 Keh Qmc 40 Qms Qms Qmso(Xf) 36 Qmc 76 Qms Qms Qms 75 Qmc QTay? 2 Thv Qms Qms Qmc Xf 70 45 Col 70 Qms?(Keh) Qms Qmc Qmc Tcg 8 58 54 Cm 69 78 59 Mde Keh Qms Qms Ct 73 Tcg Qc Qms?(Ts) Thv? Qmc Qms Cn Tw Tcg Thv Qac Thv Qmc Cou Qafy Tcy? 59 82 Qmc Tw Qafy Ct Tcg? Thv Dh Ml Mde 7 Qmc Qmc 88 52 Qls Thv Xf Qmc 83 46 Cn Qmc Qafy Qc 1 Qms Thv? Qc 89 Qmt Qmc Tw Qac 34 Qms Qc Qms 74 Keh Tcg Thv Xf Thv Qmc 22 Cm 41 Db 3 Qmc 9 Qac Thv Qms Ct Qms Qmc Qmc Qms QTaf Qms Thv Cou 70 66 Qao Tcy? Qa SPRING FAULT Qmc 35 Qms 33 Qap? Qcg/Qmso Qmc Qms 55 75 70 Mde 88 Qmso(Tcg) Qcg Qmc BRANCH Xf? Ct Ml 8 Qms?(Thv) Db 53 Qmc Qac Keh Qmc 9 Qms Thv Qms Cm 57 Mde? 23 Tcy? Qms Qms Qac Ct Col 85 Dh Qmc Qmc Qc Qcg Qms?(Ct) Qms Xf? 35 15 42 Qms?(Thv) Qms?(Thv) Qc 34 7 Qms 35 34 Qmc/Qga PIPw Qaoe Qmc 64 80 51 0.5 Qmc Qms?(Thv) Qng Dwc Dh 89 76 61 14 Qafy Qmc Qmso(Ts) Qcg/Qmso 7 Qc Qms Xf t? 30 33 12 Qmc Qmc s Qms Qcg Qms Ct 46 60 ru 79 75 Qac Qmdf Keh Qmc Qms Qms th 32 47 Qga Db 64 Qmc Qa Mde Qc Qc Qms(Thv) Qms?(Thv) Cn 56 30 Mhu Tcg 20 Qmc Thv 40 22 Cou 89 61 IPr Qac Qmc Qms Ct Cm 67 Ml 80 Thv Xf 39 44 Qga Tcy? Thv Qms Qms Qa 50 71 Ml 79 36 Qmdf? Qc Tw Qcg Qmc 65 Mdl Db Qaoe Qcg Qay Qms 65 73 Qac Tcy? Qmc Qac Qc Xf Mdl 77 PIPw 10 Qmc Qms Thv Qmrf Qms Keh Qmc Qms?(Ct) Qms Qms 76 56 Col Col 88 76 Mdu Qac Qmc Qcg 20 Qms?(Xf) Qms 7 Thv 16 Qms(Xf) Qac 63 Db 75 Mhu Qc Cm? 15 88 86 Qms 54 Ml 47 Ct Qms 74 Tw Qc Qac Qcg Qms? Qms? 78 31 88 48 PIPw 76 Qmc Ct 50 Xf 45 PIPw Thv (Xfpg) Xf Qms 65 80 1 Qc 27 45 44 Mhl 48 Qcg/Qms Thv Thv 20 Cn 61 Ct Qms Qms Ct 46 Cou 50 Qmc Qmso 9 36 Qms 55 34 57 Ml Qms Qmc 39 Qmc Qmc Xfpg 55 88 Qac 73 55 Qmc 10 32 74 80 Ct Qms Thv 86 79 58 Qmc Thv Thv Qc Thv Qms? Dh 56 Keh Qms?(Tw) Tcg 29 Thv Qmc Qmc Qg? Mdl 37 PIPw Tw Tcy? 35 31 Cn Dh 35 Cm Xf 46 59 Qmc Tw Qmc Cn Qms Ct Cm Dwc Qgm 65 35 Tcy Qc Qc Qcg 12 17 Ct 44 20 Col 70 36 57 83 Qac Qms Qms Qac 65 Mhu PIPwls Qac Thv Cn Thv 75 Tw? 57 Keh Qa stone stripes? Qcg Cm Qmc Qmc 65 44 60 58 Cn IPm? PIPw Qafoe 10 Qmc Ct 30 23 23 45 Qms Qmc Tcy? Cm Qmc 76 57 Mdl IPr Qms Qmc Qc Com 50 IPr S 30 Cm Ct Qmc Y Qac 12 Cn 37 37 ? Qac 14 Qg? 57 N Thv Qms t Db Qmc QTao Tcy Qc Cn us Ml Qms Qcg C Thv Qmc Qmc Qaf 78 hr Mdu Qmc L 9 37 Qac 49 Qmt t Qg IPwl 23 I Qmc Qms 27 25 69 60 Qg 43 Qc N Qms Qmc 82 78 50 Qg Tw? Qms Tcg Qac E Cou 18 50 89 Mde Qg Keh Keh Tw Thv 45 73 Mhl Qmdf Tcg A 73 Qmc X 27 42 41 88 Qms Thv Ct 10 Mdl IS 49 69 50 Qmg 44 1 45 82 IPr Qmc O Qcg Qms Mhu Tw? Qac 46 57 Cou Dwc IPwl R Thv Cm 72 83 19 65 Qms Qcg Tcg 16 38 73 Tw N Thv 81 44 62 Qmc Qmc Qmc Qms O Cm Qms Qgm PIPw? Qmc Qms 40 68 58 12 36 45 14 R 88 54 M Thv 77 Cm Dh Cou 34 38 Qms1 34 Qmc Qmc 10 A 27 64 86 68 Qg 55 IPr Qms Tw L Qc 15 60 70 Qcg 13 20 Mdl Qgm Tcy Thv F Qmc 24 48 60 11 A stone stripes? 58 59 47 75 Tcg U Tw? 57 38 Ct 11 22 Qc 50 Qmc Keh L 50 45 Tw? 18 T Thv 57 Qaf 12 35 Keh Qmc Qms Thv 64 IPm? Qmc Qms?(Thv) 20 22 Db Dh Db 26 Mhu Qmg 15 PIPw? Qac Tcg 26 Qcg 15 Thv 15 Col Qac Qms 89 38 57 85 89 Qac Qac Qmc 32 19 Thv Thv 27 IPr Mdu Qms 40 21 Qmc Thv Cou Com 26 Qc 52 27 41 ? 71 Qmc QTao Qms Qmc 32 Com Cn Qac t 50 19 Thv 78 19 s Qmc 70 Tcy Thv Cn u 71 65 32 Qmc Ct Ct Col r 59 Qms Thv Qmc 42 h 44 Ct 30 Ct Qmc t 65 31 40 Qcg Qms Col 28 37 60 78 26 Cm IPwl Tcg Qcg Thv 28 42 Qc 34 77 31 17 47 Qac Tcy Qc 52 Mdd 49 O IPm Thv Qac Qms 23 50 Db? 83 Mdu 16 G Qmc 62 Qmc 40 60 IPm? 8 Thv 19 31 D Qmc Mdl Qmc 36 Qms Qcg Qmc 33 26 E 43 Cou 60 22 Qms N Qmso 71 48 Qcg Qcg Cm 51 Ct Col R 52 59 23 O Qms Qac Col 82 IPr Tcy Qng Qms 34 Qmc 32 Qms O 79 Dh 72 IPm 37 12 Qmc 35 51 74 F 77 70 Qmc Qmc Qmc Qac 36 Tcg Qac Qng 20 Qms Com T Qmc/Ct 60 89 48 Qms Qms 74 H Ct Cn 12 Qmc R 69 67 55 Qms Tcy 20 58 24 48 40 73 Qc Qc Ct Ct 40 Cou Qac U 56 PIPwu Thv S 31 71 30 67 80 13 Qmc T Cm Qmc 65 IPwl Tcg Qms Col 61 Dwc 5 Tcy Thv Qac Qmc Col IPm Qms Qmc Qms 40 Tcy Qcg Com Qmc 75 83 87 74 Qac Qcg Qcg Tcg Qms 25 Qac 62 79 20 Tcg Thv Qmt 35 Qmso 80 40 Qac 10 8 Tcy Qac 24 Col Qmc Col Db 52 Mdd Qmc PIPw 6 Tcy Qmc Qac 18 Qms?(Ts) Tcy Qmc Qmc Ct Ct 30 40 72 57 56 Qms Qms Cou 67 Ml Mde 58 Mhu Mdl Qac Qaf Ct Ct Mhl 57 24 IPwl 52 Qms PIPw Basemap produced by U.S. Geological Survey This open-file release makes information available to the public that may not conform to UGS standards; the map may be incomplete and possible inconsistencies, errors, and omissions have not been resolved. Therefore it may be premature for an individual or group to take action based on its contents. 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. INTERIM GEOLOGIC MAP OF THE This geologic map was funded by the Utah Geological Survey and the U.S. Geological Survey, National Cooperative Geologic Mapping Program through U.S. Geological Survey STATEMAP award number 04HQAG0040. The views DURST MOUNTAIN QUADRANGLE, and conclusions contained in this document are those of the author and should not be interpreted as necessarily representing the official policies, either MORGAN AND WEBER COUNTIES, UTAH expressed or implied, of the U.S. Government. by JAMES C. COOGAN AND JON K. KING 2006 Interim Geologic Map of the Durst Mountain Quadrangle, Morgan and Weber Counties, Utah

by James C. Coogan1 and Jon K. King2

1now at Western State College, Gunnison, Colorado 2Utah Geological Survey, Salt Lake City, Utah

This open-file release makes information available to the public that may not conform to UGS standards; the report may be incomplete and possible inconsistencies, errors, and omissions have not been resolved. Therefore it may be premature for an individual or group to take action based on its contents. 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. This geologic map was funded by the Utah Geological Survey and U.S. Geological Survey, National Cooperative Geologic Mapping Program through U.S. Geological Survey STATEMAP award number 04HQAG0040. 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.

OPEN-FILE REPORT 498 UTAH GEOLOGICAL SURVEY a division of Utah Department of Natural Resources 2006 SUMMARY

The Durst Mountain quadrangle is located east of Ogden, Utah (figure 1). The major geographic features in and near the quadrangle are Ogden and Morgan Valleys, the northern Wasatch Range to the west, the Ogden River and its forks in Ogden Valley, the Weber River in Morgan Valley, and Cottonwood Canyon, cut by Cottonwood Creek, separating Elk Mountain from Durst Mountain. Ogden and Morgan Valleys formed due to Cenozoic extensional faulting along at least one margin of each valley, and the valleys are filled with probable Oligocene Norwood Formation tuffaceous, lacustrine, and fluvial sedimentary rocks. The Precambrian (lower Proterozoic) Farmington Canyon crystalline rock complex and unconformably overlying Paleozoic (Cambrian through Permian) marine sedimentary strata are exposed on Durst and Elk Mountains. Mesozoic (Triassic and Jurassic) rocks are exposed northeast of Elk Mountain. A southern edge of the Willard thrust sheet, a Cretaceous structural feature containing late Proterozoic meta-sedimentary and Paleozoic sedimentary strata, is exposed in the northern part of the quadrangle and to the west in the Wasatch Range. The thrust sheet is likely buried under several thousand feet of Cenozoic valley fill in the northeast part of the quadrangle. The Cretaceous Ogden roof thrust is exposed to the west in the Wasatch Range and on Durst Mountain; its trace between exposures is likely present beneath the Cenozoic valley fill in the quadrangle. This roof thrust is east-directed and, due to rotation of the Durst-Elk Mountain block, is now east dipping. The Paleozoic and Mesozoic strata are in an east-dipping homocline that is locally complicated by Cretaceous folding, east- and west-directed thrusts and other faults, and is cut by Cenozoic extensional faulting. On the east flank of the Durst-Elk Mountain block, the latest Cretaceous Evanston Formation unconformably overlies the Precambrian, Paleozoic, and Mesozoic rocks, and these rocks and the Cretaceous thrust sheets are unconformably overlain by the Cenozoic (Eocene) Wasatch Formation. The Norwood Formation overlies the Wasatch Formation to the south in Morgan Valley and is overlain by and intertongues with unnamed conglomeratic strata on the west sides of Durst Mountain and Elk Mountain. These conglomeratic strata are unconformably overlain by still younger conglomeratic rocks of Miocene and/or Pliocene age. Remnants of Pliocene and/or Pleistocene alluvial deposits are present on both sides of Morgan Valley and along Cottonwood Creek. Quaternary (upper and possibly middle Pleistocene) glacial deposits cover bedrock locally east of Durst Mountain, and Quaternary (uppermost Pleistocene) lacustrine, deltaic, and alluvial deposits related to Lake Bonneville are present in Ogden and Morgan Valleys. Possible Quaternary fault scarps in this quadrangle are on mass movements of uncertain age on the west side of Durst Mountain, and on middle or lower Pleistocene alluvial deposits (>730 ka) north of Cottonwood Creek. Extensions of the fault in alluvium do not cut younger deposits, though changes in slope are present in Tertiary bedrock. All these scarps are part of the 10-mile (16-km) long fault system that bounds the west side of the Durst-Elk Mountain block, extending south to Morgan. South of the quadrangle near Morgan, Quaternary deposits are likely cut by extensional faults along the west side of Durst Mountain, but no scarps are visible.

1 Coogan mapped pre-Cenozoic rocks in the quadrangle, mostly on Elk and Durst Mountains. King is responsible for the Cenozoic rocks and deposits to the east and west of the mountains. Due to land access constraints, most of the map east of the Elk Mountain-Durst Mountain block is from interpretation of aerial photographs.

MAP UNIT DESCRIPTIONS

QUATERNARY Qa, Qa2, Qay, Qap, Qab, Qao Alluvium, undivided (Holocene and Pleistocene) - Sand, silt, clay, and gravel in stream and alluvial-fan deposits; composition depends on source area; distinguished from terraces (Qat) based on upper surface sloping toward adjacent drainage like an alluvial fan; relative ages are indicated by number and letter suffixes; Qa with no suffix used where age uncertain or age divisions of alluvium cannot be shown at map scale; generally 0 to 20 feet (0-6 m) thick, but Qap up to 50 feet (15 m) thick. Near latest Pleistocene Lake Bonneville, alluvium labeled y and 2 is younger than Lake Bonneville, mostly Holocene in age. Alluvium labeled Qap and Qab are graded to the Provo (and slightly lower) and Bonneville shorelines of Lake Bonneville (at ~ 4820 feet [1470 m] and 5180 feet [1580 m] in area), respectively; here letter o suffix means alluvium is older than Lake Bonneville. Elsewhere relative ages may only apply to local drainages. In the Durst Mountain quadrangle, ages of alluvium, including terraces and fans, are in part based on heights above present drainages (table 1); here Qay is at to slightly above, Qa2 is about 15 feet (5 m) above, Qap is 15 to 40 feet (5-12 m) above, Qab is 40 to 80 feet (12-24 m) above, and Qao is 70 to 120 feet (20-37 m) above present drainages. A prominent surface (“bench”) is present on Qap at about 4900 feet (1495 m) in Morgan Valley (Snow Basin, Durst Mountain, Morgan, and Peterson quadrangles), and is about 25 to 40 feet (8-12 m) above the Weber River.

Qaoe Pleistocene alluvium (middle and lower Pleistocene) - Eroded alluvium located above the Bonneville shoreline and apparently above and older than pre-Lake Bonneville older alluvium (Qao and Qafo); mapped on benches about 80 to 100 feet (24-30 m) above Cottonwood Creek (higher than adjacent Qafo, but with height above drainage similar to Qao and Qafo) (table 1), and might be slightly older generation of older alluvium; also mapped on benches about 120 to 215 feet (35-65 m) above the Weber River in Morgan Valley at an elevation of about 5300 to 5350 feet (1615-1630 m); contains mostly sand, silt, and gravel in stream and alluvial-fan deposits; about 10 feet (3 m) thick; west of the Weber River in the Morgan quadrangle, dated by Sullivan and others (1988) as older than 730 ka, based on reversed paleomagnetism.

Qal, Qal2 Stream alluvium and flood-plain deposits (Holocene) - Sand, silt, clay, and gravel in

2 channels, flood plains, and terraces less than 10 feet (3 m) above stream level; locally includes muddy, organic overbank and oxbow lake deposits; composition depends on source area; 0 to 20 feet (0-6 m) thick; suffix 2 indicates slightly older deposits in Ogden Valley and near head of Cottonwood Canyon, with Qal2 including low terraces and being slightly (5 to 10 feet [1-3 m]) higher stream alluvium.

Qat, Qat2, Qatp, Qato Stream-terrace deposits (Holocene and Pleistocene) - Sand, silt, clay, and gravel in terraces above flood plains, mostly along the Weber and South Fork of Ogden Rivers and Cottonwood Creek; number and letter suffixes indicate relative ages, with 2 being the youngest terraces; Qat with no suffix used where age uncertain or age divisions of terraces cannot be shown at map scale; 0 to at least 20 feet (0-6+ m) thick. Near latest Pleistocene Lake Bonneville, deposits with suffix 2 are younger than Lake Bonneville, and mostly Holocene in age, and deposits with o suffix are older than Lake Bonneville; elsewhere relative-age numbers and letters may only apply to local drainages. Terraces labeled Qatp are graded to the Provo and slightly lower shorelines of Lake Bonneville (at and < ~ 4820 feet [1470 m] in area), and with Qap form a “bench” at about 4900 feet (1494 m) along the Weber River in Morgan Valley. In the Durst Mountain quadrangle, terrace ages are partly based on heights above present drainages, with Qat2 about 20 feet (6 m) above, Qatp 25 to 30 feet (8-9 m) above, and Qato about 100 feet (30 m) above present drainages.

Qaf Alluvial-fan deposits, undivided (Holocene and Pleistocene) - Mostly sand, silt, and gravel that is poorly bedded and poorly sorted; includes debris flows, particularly in drainages and at drainage mouths (fan heads); generally less than 60 feet (18 m) thick. Mapped where fan age uncertain or for composite fans where portions of fans with multiple ages cannot be shown at map scale.

Qaf1, Qafy, Younger alluvial-fan deposits (Holocene and uppermost Pleistocene) - Mostly sand, silt, and gravel that is poorly bedded and poorly sorted; includes debris flows, particularly in drainages and at drainage mouths (fan heads); generally less than 40 feet (12 m) thick. Near latest Pleistocene Lake Bonneville, deposits with suffixes 1 and y are younger than Lake Bonneville (mostly Holocene). Qaf1 are active and are on Qat2 terraces along east Cottonwood Creek in the Durst Mountains quadrangle; Qafy fans are active, impinge on present-day drainages and may be partly older than Qaf1 fans.

Qafp, Qafb, Qafo Older alluvial-fan deposits (upper and middle(?) Pleistocene) - Incised fans of mostly sand, silt, and gravel that is poorly bedded and poorly sorted; includes debris flows, particularly in drainages and at drainage mouths (fan heads); generally less than 60 feet (18 m) thick. Fans labeled Qafp and Qafb are graded to the Provo (and slightly lower) and Bonneville shorelines of latest Pleistocene Lake Bonneville, respectively. Near Lake

3 Bonneville, unit Qafo is older than (above and apparently cut by) the Bonneville shoreline; upstream unit Qafo is above fans graded to the Bonneville shoreline. Elsewhere relative-age numbers and letters may only apply to local drainages. Like Qa and Qat suffixes, ages in the Durst Mountain quadrangle are partly based on heights above present drainages, in this case at drainage-eroded edge of fan, with Qafp about 40 to 45 feet (12-14 m) above, Qafb more than about 40 feet (>12 m) above, and Qafo about 70 to 110 feet (20-35 m) above present drainages. Dates presented in Sullivan and Nelson (1992) imply Qafo north of Morgan considerably predates Lake Bonneville and is middle Pleistocene in age (300-600 ka); however, the Bonneville shoreline is obscure on this fan.

Qafoe Eroded old alluvial-fan deposits (middle and lower Pleistocene) - Eroded fans located above and apparently older than pre-Lake Bonneville older alluvial-fan deposits (Qafo) along Cottonwood Creek; upper surface is about 160 feet (50 m) above eastern Cottonwood Creek and about 120 to 200 feet (35-60 m) above present streams in Morgan Valley; contains mostly sand, silt, and gravel that is poorly bedded and poorly sorted; less bouldery and lower relative to QTay, QTao, and QTaf; 0 to 60 feet or more (0-18+ m) thick; likely same age as Qaoe (>730 ka).

Qac Alluvium and colluvium (Holocene and Pleistocene) - Includes stream and fan alluvium, colluvium, and, locally, mass-movement deposits; 0 to 20 feet (0-6 m) thick.

Qc Colluvium (Holocene and Pleistocene) - Includes material moved by slopewash and soil creep; composition depends on local sources; generally 6 to 20 feet (2-6 m) thick; not mapped where less than 6 feet (2 m) thick.

Qcg Gravelly colluvial deposits (Holocene and Pleistocene) - Present downslope from gravel- rich deposits of various ages (for example, units Keh, Thv, QTaf, QTay/QTao, Qafoe/Qaoe, Qafo/Qao) but mostly mapped downslope from Thv on west side of Durst and Elk Mountains; typically differentiated from colluvium and residual gravel (Qc, Qng) by prominent stripes trending downhill on aerial photographs; stripes are concentrations of gravel up to boulder size; generally 6 to 20 feet (2-6 m) thick; some deposits previously included in Huntsville fanglomerate (see Thv).

Qng Colluvial and residual gravel deposits (Holocene and Pleistocene) - Gravel of uncertain origin, but probably mostly colluvium and residuum; poorly sorted pebble to boulder gravel in a matrix of silt and sand; typically dark colored, but this may be function of Thv source; mostly gravel-armored, nearly flat surfaces on bedrock but also includes steep area north of Cottonwood Canyon in Durst Mountain quadrangle; generally 6 to 20 feet (2-6 m) thick; previously included in Huntsville fanglomerate (see Thv) and mostly present on unit Thv.

Qmc Mass-movement and colluvial deposits, undivided (Holocene and Pleistocene) - Mapped

4 where landslides and slumps are difficult to distinguish from colluvium (slopewash and soil creep) and where mapping separate, small, intermingled areas of mass-movement and colluvial deposits is not possible at map scale; locally includes talus and debris flows; typically mapped where landslides and slumps are thin (“shallow”); also mapped where the blocky or rumpled morphology of the older (likely Pleistocene) mass movements has been diminished (“smoothed”) by slopewash and soil creep; composition depends on local sources; 0 to 40 feet (0-12 m) thick.

Qms, Qms1, Qmsy, Qmso Landslide and slump deposits (Holocene and Pleistocene) - Poorly sorted clay- to boulder-sized material; locally includes flow deposits; generally characterized by hummocky topography, main and internal scarps, and chaotic bedding in displaced blocks; composition depends on local sources; morphology becomes more subdued with time; thickness highly variable. Qms without suffix is mapped where age uncertain (though likely Holocene and/or upper Pleistocene), where portions of slide/slump complexes of different ages cannot be shown separately at map scale, or where boundaries between slides/slumps of different ages are not distinct. Qms may be in contact with Qms when two different slide/slumps abut. Locally, unit involved in slide/slump is shown in parentheses where a nearly intact block is visible. Near latest Pleistocene Lake Bonneville, estimated time of emplacement indicated by relative-age number and letter suffixes, with: (1) emplaced in the last 80 to 150 years, historical; (y) post- Lake Bonneville in age, and mostly pre-historic; and (o) likely emplaced before Lake Bonneville transgression. On west margin of quadrangle, Qmso(Ts) block was emplaced before Qao, making it middle Pleistocene (see table 1). Suffixes y (as well as 1) and o indicate probable Holocene and Pleistocene ages, respectively. Contacts are present between separate slides/slumps/flows. Qms and Qmso queried where bedrock block may be in place. Qmso mapped where rumpled morphology typical of mass movements has been diminished and/or younger surficial deposits cover or cut Qmso.

Qmdf Debris-flow deposits (Holocene and upper Pleistocene) - Mostly sand, silt, clay, gravel, and cobbles in debris flows; deposits have lobate debris accumulations and others are in narrow drainages; some lack vegetation cover; 0 to 40 feet (0-12 m) thick

Qmrf Rock fall (Holocene and Pleistocene) - Angular, boulder-sized, Tintic Quartzite debris at base of cliffs south of Cottonwood Canyon (section 13, T. 5N., R. 2E.) (likely Holocene) and up Brushy Canyon (section 26, T. 5N., R. 2E.) (likely Pleistocene) in Durst Mountain quadrangle; estimate 0 to 20 feet (0-6 m) thick.

Qmt Talus (Holocene and Pleistocene) - Angular debris at the base of and on steep slopes; only larger debris fields can be shown at map scale, and include colluvium locally; mapped on southwest border of quadrangle and on Durst and Elk Mountains; likely less than 20 feet (6 m) thick.

5 Qmg Mass-movement and glacial deposits, undivided (Holocene and Pleistocene) - Deposits with hummocky topography in two cirques on Durst Mountain; southern landslide began in shaley bedrock and continued downslope involving glacial deposits; up to about 30 feet thick (<9 m); younger than Pinedale age (<15,000 yrs old).

Qg, Qgm, Qga Glacial till and outwash (upper and middle? Pleistocene) - Qg is undivided glacial deposits; till is the material in a moraine (Qgm) and is non-stratified, poorly sorted clay, silt, sand and gravel, to boulder size; outwash (Qga) is better sorted and bedded due to alluvial reworking, is directly downslope from other glacial deposits, and is thick enough to obscure older deposits and bedrock; locally include mass-movements too small to show at map scale; 0 to about 100 feet (0-30 m) thick; likely Pinedale-age (~15,000 to 30,000 yrs old) deposits with poorly developed soil and moderate to sharp moraine morphology. Unlike in the Wasatch Mountains to the west, no sign of younger glacial deposits upslope, either as recessional deposits (about 13,000 to 14,000 years old) or in either cirque (about 8,000 to 10,000 years old) (see Madsen and Currey, 1979). Queried glacial deposits (Qg?) may be older (likely Bull Lake age, ~130,000 to 150,000 years old), and have well-developed soil; deposits on the northeast flank of Durst Mountain have subdued moraine morphology; in contrast queried deposits on northwest flank of Durst Mountain lack moraine morphology, but also lack an alluvial or mass movement source. Other possible glacial features are pimple mounds on Herd Mountain on the east margin of the quadrangle and possible stone stripes (solifluction) in unit Qcg.

Qla Lake Bonneville and post- and pre-Lake Bonneville alluvial deposits, undivided (Holocene and uppermost Pleistocene) - Mostly poorly sorted and poorly bedded sand, silt, and clay with some gravel; mapped near Bonneville shoreline (~5180 feet [1580 m] in area); stream alluvium has been deposited on lacustrine deposits in Ogden Valley rather than thin lacustrine deposits over alluvium; thickness uncertain.

Ql Lake Bonneville deposits, undivided (uppermost Pleistocene) - Includes cobbly gravel, sand, silt, and clay in Ogden Valley in Durst Mountain quadrangle; mapped where grain size is mixed or indistinct and deposits are not exposed in scarps or construction cuts; thickness uncertain.

Qls Lake Bonneville sand (uppermost Pleistocene) - Mostly sand with some silt and gravel deposited nearshore; typically less than 20 feet (6 m) thick where exposed to west near Mountain Green in Morgan Valley.

Qlg Lake Bonneville gravel (uppermost Pleistocene) - Mostly interbedded gravel and sand deposited along beaches and slightly offshore as the lake was near and at the Bonneville shoreline in Ogden Valley; likely less than 20 feet (6 m) thick.

Qdlb Lake Bonneville delta and lacustrine deposits, undivided (uppermost Pleistocene) -

6 Mostly sand, silty sand, gravelly sand, and cobbles deposited near shore as the lake transgressed to and was at the Bonneville shoreline; mapped where poor exposures preclude separation; mapped near the Bonneville shoreline in Ogden Valley (South Fork Ogden River and Bally Watts Creek) and along Cottonwood Creek; zero to at least 40 feet (0-12+ m) thick.

Qfdb Lake Bonneville alluvial-fan and delta deposits, undivided - Cobbly gravel, sand, silt, and clay deposited above (subaerially) and in Lake Bonneville (subaqueous) as lake transgressed to and was at the Bonneville shoreline; mapped where Bonneville shoreline obscure so that line cannot be drawn between delta and fan; typically should be better sorted delta and lake deposits over poorly sorted alluvial-fan deposits; 0 to at least 40 feet (0-12+ m) thick. Prominent along Bally Watts Creek; also present in Quarry Hollow and along Cottonwood Creek upstream from Qdlb.

Qh Human disturbance (Historical) - Obscures original deposits by cover or removal; borrow pit on farm in Ogden Valley. Also possibly near spring in Qac on south side of Bennett Creek in Durst Mountain quadrangle (SW1/4 SE1/4 section 26, T. 6N., R. 2E.).

QUATERNARY AND TERTIARY QTa, QTay, QTao High-level alluvium (lower Pleistocene and/or Pliocene) - Gravel, sand, silt, and clay above other stream-terrace and alluvial-fan deposits; typically more bouldery than lower alluvium (including units Qafoe and Qaoe); at least locally gravel-armored and poorly sorted; divided into younger (y) and older (o) based on relative height of adjacent deposits (see table 1); present about 160 to 300+ feet (50-90+ m) above Cottonwood Creek; as much as 800 feet (240 m) above the Weber River in Morgan Valley; located above Qaoe, so older than 730 ka; estimate 30 to 70 feet (9-20 m) thick, based on thicknesses in Morgan Valley (Durst Mountain, Snow Basin, Morgan, and Peterson quadrangles).

QTaf High-level alluvial-fan deposits (lower Pleistocene and/or Pliocene) - Gravel, sand, silt, and clay above other stream-terrace and alluvial-fan deposits (including QTa); typically more bouldery than alluvium lower than QTay and QTao (including units Qafoe and Qaoe); at least locally gravel-armored and poorly sorted; located above QTao and in this quadrangle about 1000 feet (300 m) above Cottonwood Creek; estimate 30 to 100 feet (9- 30 m) thick. Upper surfaces of these high-level deposits (with QTao) in the Durst Mountain, Peterson, and Snow Basin quadrangles appear to be the Weber Valley surface of Eardley (1944); however, high-level alluvial fans (QTaf) extend to mountain front at elevations of about 6800 to 7200 feet (2070-2195 m), rather than to the mountain ridgelines as suggested by Eardley (1944).

TERTIARY Ts Tertiary strata, undivided - Used where multiple Tertiary map units are in landslide blocks, Qms(Ts), and for mostly concealed outcrops with characteristics of Tcg, Tcw,

7 Tca, and Thv west of Elk Mountain block.

Thv Fanglomerate of Huntsville (Pliocene? and Miocene) - Typically dark-weathering, poorly to moderately consolidated, pebble to boulder gravel in brown to reddish-brown silt and sand that typically erodes to gravel-covered slopes with stone stripes; gravel and matrix reflects source of Wasatch Formation as well as Paleozoic and Precambrian rocks exposed in Durst-Elk Mountain block; in contrast, where fanglomerate is next to Tintic Quartzite (Ct) exposures on west flank of mountain block and in graben, clasts are angular to subangular Tintic, with less red matrix; unconformably overlies conglomeratic strata, Tcy south of Cottonwood Canyon with slight angular discordance and Tcy? near Bally Watts Creek (south of Sheep Herd Creek and north of Elk Mountain) with angular unconformity and change to larger clast quartzite conglomerate; overlies Tcw north of Sheep Herd Creek (north end of Elk Mountains block) with no recognizable change in dip and vague change to more Wasatch-Formation-looking clasts and matrix; may include Tcy or Tct equivalent strata in graben in Durst Mountain but lack of exposures precludes identification; estimate 40 to 1000 feet (12-300 m) thick on west flank of Durst Mountain and up to about 500 feet (150 m) thick on sides of Elk Mountain; thickness on Durst Mountain not known but several hundred feet of reddish strata exposed in graben; may be only up to about 500 feet (150 m) thick on west flank of Durst Mountain if repeated by fault or folded into syncline (see lineament on map); queried where identification uncertain; locally includes landslides, slumps, and flows that are too small to show at map scale, especially on Durst Mountain block. May be unit east of lineament up Bally Watts Creek or could be Tcy, Tcw, Tca, and/or Tcg, so Ts used on map. In Durst Mountain quadrangle west of Durst Mountain block, fanglomerate typically dips about 10o to 15o east into mountain and underlies prominent gently (<3o) northwest- dipping QTaf; to south in Morgan quadrangle folded into syncline with Tcy just west of faults bounding Durst Mountain, with typically flat-lying to gently (<5o) dipping beds on both limbs and locally steeper dips (~10-30o) on east limb of syncline. Named Huntsville fanglomerate but not mapped by Eardley (1955) and his Huntsville unit likely equal to QTc unit of Mullens and Laraway (1973); previously reported to be 0 to 400 or 1000 feet (0-120 or 300 m) thick (Lofgren, 1955; Schick, 1955; Mullens and Laraway, 1973); Mullens and Laraway (1973) descriptions of quartzite clasts are misleading; deposits included in Schick (1955) and Coody (1957) Huntsville fanglomerate and unit QTc of Mullens and Laraway (1973) have several ages and origins, so are here divided into units Qcg, Qng, Thv, and Tcy, as well as Tcw, Tct, Tca, and Tcg, and the fanglomerate of Huntsville is here redefined and restricted.

Tcy Younger unnamed Tertiary conglomeratic rocks (Miocene?) - Rounded, pebble- to boulder-sized, quartzite-clast conglomerate with gray, tan, or reddish matrix and some mudstone, siltstone, and sandstone; since lithologically like unit Tcg, Tcy-Tcg contact based on change in dip across angular unconformity (5-10o vs >10o in Morgan quadrangle) and more regular bedding in Tcy; locally erodes to gravel-covered slopes with stone stripes; Tcy-Tcg contact is easily visible angular unconformity at Durst

8 Mountain-Morgan quadrangle boundary but becomes less distinct to north (Tcy queried on map); in Morgan quadrangle, Tcy has gentle bedding dips to the east with syncline axis visible, though east limb is concealed (folded with Thv); estimate 200 to 400 feet (60-120 m) thick in Durst Mountain quadrangle; locally includes landslides, slumps, and flows that are too small to show at map scale. In Durst Mountain quadrangle, Tcy is not present north of Sheep Herd Creek (Thv “rests” on Tcw), while just south of Sheep Herd Creek, lower dips indicate Tcy might be present below Thv (queried on map); to the south Tcy-equivalent strata (above Tcy marker beds on map) might be present west of Bally Watts Creek in Tcw (based on marker bed that connects across lineament to Tcy? lower contact) and west of Elk Mountain in Tca and Tct (based on marker bed at possible angular unconformity); might be same age as Salt Lake Formation (Pliocene and upper Miocene); previously included in Huntsville fanglomerate (see Thv); mapped Tcy-Thv contact (lithologic change and unconformity) is more distinct than Tcy-Tcg contact (unconformity with no consistent lithologic change).

Tcg, Tcw, Tct, Tca Unnamed Tertiary conglomeratic rocks (Oligocene?) - Characterized by rounded, cobble- to boulder-sized, quartzite-clast conglomerate with pebbles and less than 10 to more than 50 percent gray, tan, or reddish matrix; interbedded with tan, gray, and reddish-brown pebble-bearing mudstone to sandstone and some claystone (altered tuff); most beds poorly indurated and poorly exposed; some non-conglomeratic beds in Tcg look like the gray upper Norwood Formation (Tn) and are locally tuffaceous (note white marker bed on map just below Tcw); mudstone likely constitutes the matrix of the conglomeratic beds; some Tcg pebble beds have carbonate and chert (like Norwood) and lesser quartzite clasts; Tcg conglomerates include rare altered tuff clasts from Norwood Formation (Tn); locally erodes to gravel-covered slopes with stone stripes; locally includes landslides, slumps, and flows that are too small to show at map scale. Subdivided into Tct, Tca, and Tcw lithosomes near Elk Mountain, based on clast characteristics (t=Tintic, a=angular, and w=Wasatch). These conglomeratic strata (Tcg, Tcw, Tct, Tca) are an estimated 500 feet (150 m) thick in aggregate and thicken northward in Durst Mountain quadrangle to possibly 3000 feet (900 m) thick, though faulting may make this estimate too large; previously included in Huntsville fanglomerate (see Thv). Subunit Tcw has mostly recycled Wasatch Formation clasts (quartzite and carbonate) with a distinct reddish patina; it looks like the fanglomerate of Huntsville (Thv), but typically Tcw matrix is less red than Thv and lacks red sandstone/siltstone clasts of Thv. Tcw overlies Tcg near Bally Watts Creek and appears to grade laterally into Tcg just north of Cottonwood Canyon. Subunits Tct and Tca appear restricted to a graben on the west side of Elk Mountain near exposures of Tintic Quartzite. Tct has mostly angular clasts of Tintic Quartzite and the clasts were likely derived from nearby faulted Tintic. Tct is mapped as two tongues, the lower in Tcw, and the upper above and likely into Tca (see correlation chart). Tca is cemented and has angular and rounded carbonate and angular Tintic clasts; it overlies Tcw and it appears to be the more distal (less angular quartzite) equivalent of Tct.

9 In Durst Mountain quadrangle, north of Cottonwood Creek, Tcg contact with Norwood Formation (Tn) based on resistant quartzite cobble/boulder conglomerate bed at least 30 feet (9 m) thick; this resistant bed is overlain by thinner non-resistant quartzite-clast beds and a relatively thick interval that looks like interbedded upper Norwood Formation (Tn) and reddish-brown strata. Because this resistant bed and overlying quartzite-clast beds grade northward into Norwood sandstone and pebble beds, the contact is also placed at the bottom of the lowest quartzite cobble bed at least 6 feet (2 m) thick and is partly based on regular bedding and reddish-brown strata in Tcg; the lack of angular unconformity at any of these quartzite-clast beds means the Norwood and this unit (Tcg) are interbedded; with the exception of the resistant (lowest) bed, cobble/boulder beds become thicker and clasts becoming bigger higher in Tcg; quartzite clasts are recycled Wasatch Formation clasts; Tcg is present on west side of Durst Mountain block and is faulted or, with Thv, folded into syncline (lineament on map); north of Cottonwood Canyon Tcg is overlain by Tcw, Tct, and Tca lithosomes with no apparent unconformity (unconformity may be within these lithosomes) and Tcy with angular unconformity.

Tn Norwood Formation (lower Oligocene and upper Eocene) - Typically light-gray to light- brown, altered tuff (claystone), tuffaceous siltstone, sandstone, and conglomerate; locally colored light shades of red and green; variably calcareous cement and zeolitization, but less common than to northwest in Snow Basin quadrangle; lacks extensive unaltered tuff present to south in Morgan quadrangle; upper Norwood Formation, as exposed on west margin of Durst Mountain quadrangle, and in northern Morgan quadrangle, is gray, granule to small pebble conglomerate, with chert and carbonate clasts, as well as claystone and fine- to coarse-grained sandstone; near Wasatch Formation (Tw) knob on Snow Basin-Durst Mountain quadrangle boundary there is much quartzite gravel in Norwood that disappears just north of the knob; also upper Norwood contains tuffaceous beds interbedded with pebble and quartzite-clast conglomerate on west margin of Durst Mountain quadrangle; these variations make it difficult to map Tcg-Tn contact (see also Tcg); from outcrop pattern, dip, and topography, Norwood is at least 7000 feet (2100 m) thick to west in Snow Basin quadrangle; thins to the south so about 5000 feet (1500 m) thick north of Morgan; about 1500-foot (460 m) thickness exposed east of East Canyon Creek in type area in Porterville quadrangle (not 800+ m inferred by Bryant and others (1989, p. K6); locally includes landslides, slumps, and flows that are too small to show at map scale. Norwood Formation generally considered younger than the Fowkes Formation, but not well dated due to alteration. Corrected Norwood K-Ar ages are 38.4 Ma (sanidine) from Norwood type area (Evernden and others, 1964) and 39.3 Ma (biotite) from farther south in East Canyon (Mann, 1974), while Fowkes 40Ar/39Ar ages are 40.41 Ma and 38.78 Ma on biotite and hornblende, respectively, from the Castle Rock quadrangle to east near Wyoming (King, unpublished); basal part of similar unit to north in western Cache Valley (“resting” on Wasatch and less than 600 feet thick) dated at 44.2 + 1.7 Ma and 48.6 + 1.3 Ma K-Ar on hornblende and biotite, respectively, with the latter date suspect (Smith, 1997; King, unpublished).

10 Unit referred to as Norwood Formation rather than using Norwood Tuff name of previous workers (see Eardley, 1944), because lithologies vary away from type area and the type area includes only part of formation; in southern Morgan quadrangle near type area, has much unaltered tuff, cut-and-fill structures (fluvial), volcanic-clast conglomerate, and local limestone and silica-cemented rocks.

Tw Wasatch Formation (Eocene and uppermost Paleocene) - Typically red to reddish-brown sandstone, siltstone, mudstone, and conglomerate; clasts typically rounded and from Precambrian and Paleozoic sedimentary rocks; lighter shades of red, yellow/tan, and light gray more common in uppermost Wasatch on east margin of Durst Mountain quadrangle and near Morgan; basal conglomerate contains locally derived clasts where contact with underlying rocks is exposed and is less likely to be red; Wasatch knobs north of Cottonwood Creek are reddish to light-gray to brownish-gray, variably cemented conglomeratic rocks; queried Wasatch is reddish strata that might be uneroded remnants on the southeast part of Durst Mountain, and in the southwest part of the quadrangle might be an exotic block in Thv or Wasatch subcrop like that north of Cottonwood Creek; Mullens (1971, p. 18) reported scattered beds up to 15 feet (5 m) thick of pale-red silty and gray algal limestone south of Morgan and similar beds may be present in eastern Durst Mountain quadrangle where field examinations were limited; about 1000 foot (300 m) exposed thickness in northeast Durst Mountain quadrangle; thickness varies locally due to considerable relief on basal erosional surface; total thickness increases up to about 4500 feet (1370 m) to south in Porterville quadrangle (Mann, 1974) and east near Henefer (Coogan, 2004b); locally includes landslides, slumps, and flows that are too small to show at map scale. North of Cottonwood Creek on west margin of map area (mostly to the west in the Snow Basin quadrangle), Wasatch, possibly along with Norwood strata, is apparently draped over a knob of highly fractured Cambrian Tintic Quartzite. This knob is either an exotic block emplaced before or during Wasatch deposition or the knob is fault zone rocks. The knob may be an exposure of the Cretaceous Ogden thrust fault zone or, more likely, the Tertiary (post-Wasatch) normal fault zone on the west flank of Durst Mountain, about 2 to 3 miles (3-5 km) to the southeast.

TERTIARY AND CRETACEOUS TK Wasatch Formation and/or Hams Fork Member of Evanston Formation - Only used where both map units are in landslide blocks, Qms(TK), and for an isolated, small, thin exposure of conglomeratic strata on northeast flank of Elk Mountain.

CRETACEOUS Keh Hams Fork Member of Evanston Formation (Upper Cretaceous- Maastrichtian/Campanian) - Light-gray, brownish-gray, and tan sandstone, conglomeratic sandstone, and quartzite- and chert-pebble conglomerate, and variegated gray, greenish- gray, and red mudstone; lacks carbonaceous shale and coal that is present in upper part in Lost Creek area (see Coogan, 2004b); member coarsens downward to gray and brownish-

11 gray, cobble conglomerate containing distinctive Proterozoic quartzite clasts; estimated thickness in this quadrangle 0 to 1000 feet (0-300 m); unconformably overlies Mesozoic and Paleozoic rocks; to east, this unit thickens from 300 feet (90 m) at Echo Canyon to 1200 feet (365 m) to north near Lost Creek Dam (Coogan, 2004b) and then thins to north to less than 450 (140 m) in Horse Ridge quadrangle (Coogan, 2006).

JURASSIC Jn Nugget Sandstone (Lower Jurassic) - Pale-grayish-orange, pinkish, and locally white, well-cemented, cross-bedded, quartz sandstone; incompletely exposed near Quarry Hollow; about 1100 to 1500 feet (335-460 m) thick to east and southeast at Toone Canyon, Lost Creek Dam quadrangle (Madsen, 1959; Coogan, 2004b) and near Devils Slide (Eardley, 1944); thickness near Devils Slide (estimated by King from outcrop pattern, dip, and topography) as about 1250 to 1360 feet (380-415 m).

TRIASSIC (Thickness estimates in Devils Slide quadrangle are by King from outcrop pattern, dip, and topography) TRa Ankareh Formation, Higham Grit, and Thaynes Formation, undivided (Triassic) - Upper Ankareh member (or Wood Shale Tongue) is bright-orange-red shale, siltstone, and sandstone and is exposed near Quarry Hollow; lower units (Higham Grit, two members of Thaynes, and lower member of Ankareh) likely not exposed in Durst Mountain quadrangle; upper Ankareh member reportedly 515 feet (155 m) thick near Devils Slide (Schick, 1955), but an estimated 600 to 680 feet (185-210 m) thick in Devils Slide quadrangle. Undivided TRa map unit reportedly about 1100 feet (335 m) thick near Devils Slide (Eardley, 1944; Schick, 1955) and about 1150 feet (350 m) thick in Lost Creek drainage (Coogan, 2004a). To east in Lost Creek drainage the lower units are about 200 feet (60 m) thick and in descending order are: gray and greenish-gray, quartz-granule sandstone (Higham Grit); gray-green lithic-pebble conglomerate (Timothy Sandstone Member of Thaynes); limestone (Portneauf Limestone Member of Thaynes); and purple and brownish-red shale, siltstone, and sandstone (Lanes Tongue of Ankareh) (Coogan, 2004a). Closer to southeast at Devils Slide, units are gritty to conglomeratic sandstone 30 to 43 feet (15 m) thick (Gartra Grit?) and lower brownish red unit (Mahogany Member) like the Lanes that is reportedly 465 to 920 feet (140-280 m) thick (Schick, 1955; Smith, 1969), but here estimated as 600 to 725 feet (185-220 m) thick in Devils Slide quadrangle.

TRt Thaynes Formation (Lower Triassic) - Regionally comprised by brownish-gray and gray, calcareous siltstone and limestone in upper and lower part, separated by resistant, gray, limestone ridge (see Kummel, 1954); several hundred feet exposed near Bennett Creek but neither top nor bottom contacts exposed, so upper tongue of Dinwoody may or may not be present; regionally 1835 feet (560 m) thick in Lost Creek drainage (supercedes Coogan, 2004a), with the same estimated thickness in the Devils Slide quadrangle, though 2200 feet (670 m) thickness reportedly exposed near Devils Slide (Eardley, 1944).

12 TRw Woodside Formation (Lower Triassic) - Dark-red, sandy shale and siltstone, with some sandstone; basal part exposed near Sheep Herd Creek; about 500 foot (150 m) thickness estimated in the Devils Slide quadrangle and 990 feet (300 m) reported by Smith (1969), with about 800 feet (245 m) thickness shown by Mullens and Laraway (1964, cross section).

TRd Dinwoody Formation (Lower Triassic) - Greenish-gray and tan, calcareous siltstone and silty limestone; uncertain thickness exposed near Sheep Herd Creek, but seems to be about the 500 foot (150 m) thickness shown by Mullens and Laraway (1964, cross section) in Devils Slide quadrangle; about 300 feet (90 m) thickness estimated and 290 feet (90 m) reported by Smith (1969) in the Devils Slide quadrangle.

PERMIAN Pp Park City and Phosphoria Formations, undivided - Not subdivided near Bennett Creek; Eardley identified these brecciated rocks as Weber quartzite (Coody, 1957); stratigraphic offset on the adjacent Bennett Creek thrust is in excess of 4000 feet (1200 m). Total thickness in Hardy Hollow, Durst Mountain quadrangle 675 feet (205 m) (Schell and Moore, 1970); 857 feet (260 m) thick to southeast near Devils Slide, but lower two units may be faulted (Cheney and others, 1953; Cheney, 1957); subdivided between Sheep Herd Creek and Hardy Hollow into members. Ppf Franson Member of Park City and Rex Chert Member of Phosphoria - Interbedded gray to pinkish-gray to dark-gray, vuggy, cherty limestone, with lesser gray shale and calcareous sandstone, and dark-gray and black, bedded chert; 43 feet (15 m) thickness of Rex Chert(?) Member of Phosphoria and 241 feet (75 m) thickness of Franson near Hardy Hollow, with 242 feet (75 m) thickness of combined Franson/Rex near Devils Slide. Ppm Meade Peak Phosphatic Shale Member of Phosphoria - Gray limestone, dark-gray to black, phosphatic siltstone and shale, and gray, calcareous sandstone; typically less resistant than adjacent members; 171 feet (50 m) thick near Hardy Hollow, with 303 feet (90 m) near Devils Slide. Ppg Grandeur Member of Park City - Light-gray, thick-bedded, dolomitic sandstone with gray chert nodules; 220 feet (65 m) thick near Hardy Hollow with 312 feet (95 m) near Devils Slide.

PERMIAN AND PENNSYLVANIAN PIPw Weber Sandstone (Lower Permian and Pennsylvanian) - Gray, indurated, quartzose sandstone with dolomite and siltstone in lower part; 2500 to 3123 feet (760-952 m) thick near Morgan (Eardley, 1944; Bissell and Childs, 1958 [2260 feet Weber + 381 feet “Park City”]; Mullens and Laraway, 1973)(see also Williams, 1943). Divided into upper (Pwu) and lower (PIPwl) parts north of Hardy Hollow in Durst Mountain quadrangle, where about 400 feet (120 m) of each unit is exposed, with base of lower unit not exposed; because these exposures are thin, disconformity in unit (see Welsh and Bissell, 1979, p. Y22) is likely not at this contact; relation of limestone marker (PIPwls) Coogan mapped on Durst Mountain to these units and the disconformity is not known, the marker appears

13 to be in the upper unit that King (unpublished) mapped to the south in the Morgan quadrangle; both units mapped north of Hardy Hollow also appear to be in the upper unit of King (PIPwu this report). Where possible in the Durst Mountain quadrangle, and to south in Morgan quadrangle, King divided Weber into IPwl (lower) with distinct regular bedding and PIPwu (upper) with less distinct bedding; IPwl may be units 1-3 of Eardley (1944); pre Fusulina strata of Bissell and Childs (1958); or Desmoinesian strata of Welsh and Bissell (1979, p. Y23); the disconformity may or may not be at King’s subunit contact.

PENNSYLVANIAN IPm Morgan Formation (Pennsylvanian) - Sandstone, siltstone and limestone that grades northward into lower part of Weber Sandstone, “pinching” out to north in southern Durst Mountain quadrangle; thrust faulted “into” Weber rather than intertongued; queried on leading edge of west-directed back thrust where carbonate-bearing strata identified as Morgan might be in the lower Weber; 0 to 1000 feet (0-300 m) thick in Morgan area (Eardley, 1944; Bissell and Childs, 1958; Mullens and Laraway, 1973) (see also Williams, 1943).

IPr Round Valley Limestone (Pennsylvanian and possibly Mississippian) - Mostly light-gray, fine-grained limestone with regular bedding visible on aerial photographs; about 375 to 400 feet (115-120 m) thick near Morgan (Crittenden, 1959; Mullens and Laraway, 1973); Carey (1973) reported a thickness of 335 feet (102 m) at the type section east of Morgan, while Sadlick (1955) reported 394 feet (120 m).

MISSISSIPPIAN (Thickness estimates by King from outcrop pattern, dip, and topography on Durst Mountain in the Durst Mountain quadrangle) Doughnut Formation (Upper Mississippian) Mdu Upper member - Limestone and siltstone; about 290 and 334 feet (90 and 100 m) thick near Morgan (Mullens and Laraway, 1973; and Crittenden, 1959, respectively), and about 300 feet (90 m) estimated in Durst Mountain quadrangle. Nohara (1966) called this the upper Great Blue Limestone and reported it is about 400 feet (120 m) thick, with upper contact concealed. Mdl Lower, shale member - Poorly exposed siltstone, black shale, and limestone; typically less resistant than adjacent map units; about 100 to 200 feet (30-60 m) thick near Morgan (Mullens and Laraway, 1973; Crittenden, 1959), and about 200 feet (60 m) estimated in Durst Mountain quadrangle. Nohara (1966) called this the middle shale in Great Blue Limestone and reported about 100 feet (30 m) thickness.

Humbug Formation (Upper Mississippian) - About 600 feet (180 m) of tan- to reddish- weathering, quartzose sandstone and interbedded limestone (Crittenden, 1959); estimate total thickness as 700 feet (215 m); contact within Humbug placed so lower member is less resistant than upper member. Mhu Upper member - Limestone with sandstone beds near base; estimate thickness as 400 feet

14 (120 m); reportedly about 300 to 350 feet (90-105 m) thick in Morgan quadrangle (Mullens and Laraway, 1973). Lower Great Blue Limestone of Nohara (1966), about 330 or 400 feet thick. Mhl Lower member - Sandstone with limestone and dolomite interbeds; estimate thickness as 300 feet (90 m); reportedly about 400 to 600 feet (120-185 m) thick in Morgan quadrangle (Mullens and Laraway, 1973).

Mde Deseret Limestone (Mississippian) - Limestone, dolomite and sandstone, with dark, non- resistant, phosphatic shale at base (Delle Phosphatic Shale Member, locally mapped as Mdd); about 500 feet (150 m) thick in Morgan quadrangle (Mullens and Laraway, 1973) and estimated on Durst Mountain.

Ml Lodgepole Limestone (Lower Mississippian) - Gray, fossiliferous limestone, locally cherty; estimate thickness as 650 feet (200 m); reported thicknesses about 650, 755, and 800 feet (200, 230, 245 m) (Eardley, 1944, near Morgan; Williams, 1943, Durst Mountain; Mullens and Laraway, 1973, near Morgan, respectively); called Gardison Limestone to west in Ogden Canyon.

DEVONIAN Beirdneau, Hyrum, and Water Canyon names are from Willard thrust sheet and may not be appropriate for strata deposited in shallower water on the continental shelf, and in what is now the Crawford thrust sheet. Typically on the Crawford thrust sheet to the north and east Beirdneau=Three Forks and Hyrum=Jefferson with no Water Canyon equivalent (see Benson, 1966; Johnson and others, 1991). We chose to retain the Willard thrust sheet names because they have been used previously (Eliason, 1969; Williams, 1971), previous work on the Durst Mountain Devonian and upper Cambrian strata is confusing (see previous references as well as Eardley, 1944; Brooks and Andrichuk, 1953; Brooks, 1954; Schick, 1955; Brooks, 1959; Mullens and Laraway, 1973), and the distinct light-colored dolomite at the top of our Water Canyon unit is typical of Water Canyon strata on the Willard thrust sheet. Thickness estimates by King from outcrop pattern, dip, and topography south of Cottonwood Canyon in the Durst Mountain quadrangle. Devonian age subdivisions are not noted due to unit name uncertainty.

Db Beirdneau Sandstone - Reddish-tan to tan to yellowish-gray, calcareous sandstone, siltstone, some sandy dolomite and limestone, and lesser intraformational conglomerate; less resistant than adjacent map units; estimate thickness as 200 feet (60 m); field thickness on Durst Mountain of about 300 feet (90 m); reported thicknesses near Morgan about 185 and 230 feet (55 & 70 m) (Eliason, 1969; Three Forks of Mullens and Laraway, 1973, respectively). A bed of brownish-gray dolomite, resembling Hyrum Dolomite, is present in middle part of Beirdneau to northeast on the Crawford thrust sheet in Horse Ridge quadrangle (Coogan, 2006), and a thin (~10 feet [3 m]) bed seems to be present on Durst Mountain as well, though color is slightly different.

15 Dh Hyrum Dolomite - Dark- to medium-brownish-gray and gray, medium-bedded, coarsely crystalline dolomite; weathers distinctive dark-chocolate brown; more resistant at top and bottom with center of less resistant beds that grade laterally into reddish, dirty carbonate like the Beirdneau Sandstone; this gradation created problems in mapping Db-Dh contacts and faults cutting these units, and in estimating thicknesses; estimate thickness as 250 to 450 feet (75-140 m); reported thickness, about 136 feet (40 m) (Eliason, 1969), is too thin relative to adjacent units.

Dwc Water Canyon Formation - Interbedded calcareous sandstone and sandy dolomite and limestone with sandstone below carbonate and a distinctive very light-gray, yellow- weathering dolomite at top; estimate 200 feet (60 m) thick (see also Eardley, 1944, Cambrian units 9-12, 155 feet [47 m]); about 100 to 150 feet (30-45 m) thick to northeast on leading edge of Willard thrust sheet (Coogan, 2006).

SILURIAN and ORDOVICIAN – Missing in area, along with all or most(?) of St. Charles Formation equivalent strata (uppermost Cambrian), due to thinning over Tooele arch (Hintze, 1959; Rigby, 1959).

CAMBRIAN (Thickness estimates by King from outcrop pattern, dip, and topography south of Cottonwood Canyon in the Durst Mountain quadrangle.) Cn Nounan Formation (Upper and Middle Cambrian) - Medium-dark-gray, thick-bedded dolomite and limestone; estimate 350 to 400 feet (105-120 m) thick (see also Eardley, 1944, Cambrian units 6-8, 315 feet [95 m]). Bloomington Formation not present on Durst Mountain or Elk Mountain.

Cm Maxfield Limestone (Middle Cambrian) - Limestone and calcareous siltstone; estimate thickness as 300 feet (90 m); at least 280 foot (80 m) thickness inferred from Eardley (1944, Cambrian units 3-5), that is, at least to top of limestone edgewise (flat-pebble) conglomerate; Cambrian limestone of Mullens and Laraway (1973) includes Maxfield and upper two members of Ophir Formation.

Ophir Formation (Middle Cambrian) - Estimate at least 380 to 725 feet (115-220 m) thick in Durst Mountain and Morgan quadrangles; about 300 to 660 feet (90-200 m) thick in Ogden Canyon west of map area; Ophir of Eardley (1944) and Mullens and Laraway (1973) is lower argillite member. Cou Upper argillite member - Dark-brown-gray to olive-gray argillite with intercalated medium-gray limestone beds; slope-forming and rarely exposed; thickness highly variable, about 425 feet (130 m) thickness inferred from Eardley (1944, Cambrian unit 2), but likely structurally doubled where he measured; actual thickness here estimated as 180 feet (55 m). Com Middle limestone member - Thin- to medium-bedded, light- to medium-gray, ledge- forming, micritic limestone with local orange-gray silty ribbons; generally highly deformed, apparent thickness 60 to 165 feet (18-50 m); actual thickness about 100 feet

16 (30 m) (this report; Cambrian unit 1 of Eardley, 1944). Col Lower argillite member - Dark-brown, orange-brown, and olive-gray argillite, silty argillite, and siltstone with rare gray limestone beds; slope forming; interbedded siltstone and sandstone at base grades downward into Tintic Quartzite; thickness highly variable, about 100 to 400 feet (30-120 m) thick, due to structural deformation; actual thickness here estimated as 200 feet (60 m), the same as Eardley (1944) reported.

Ct Tintic Quartzite (Middle and(?) Lower Cambrian) - Tan, very-well-cemented quartzite, conglomeratic in lower half with Precambrian quartzite pebbles and cobbles; basal 50 to 100 feet (15-30 m) is arkosic conglomerate of Farmington Canyon Complex material; about 800 to 1500 feet (245-460 m) thick (Mullens and Laraway, 1973); Eardley (1944) reported about 1000 foot (300 m) thickness at Durst Mountain. Highly fractured knob of Tintic exposed on west margin of Durst Mountain quadrangle.

PROTEROZOIC Xf Farmington Canyon Complex (lower Proterozoic) - Micaceous schistose and gneissic crystalline rocks with small bodies of amphibolite and pegmatite, variously called dikes and pods; locally includes landslides, slumps, and flows that are too small to show at map scale; Barnett and others (1993) reported the various isotopic ages of the complex in the Wasatch Range and concluded it is Early Proterozoic (about 1700 Ma) in age. Xfpg Farmington Canyon Complex, pegmatite (lower Proterozoic) - A large conspicuous pegmatite on the south side of Cottonwood Creek Canyon and poorly exposed pegmatite along bladed road near graben in quadrangle are mapped separately (sections 14 and 26, T. 5N., R. 2E., respectively).

WILLARD THRUST SHEET PROTEROZOIC Zm Mutual Formation (upper Proterozoic) - Purplish quartzite, locally arkosic; 435 to 1200 feet (135-365 m) thick in Browns Hole (Crittenden and others, 1971; Crittenden, 1972) adjacent to map area.

Zi Inkom Formation (upper Proterozoic) - Argillite to psammite (meta-sandstone over meta- siltstone) with basal meta-tuff lenses; 360 to 450 feet (110-140 m) thick north of map area (Crittenden and others, 1971; Crittenden, 1972).

Zcc Caddy Canyon Quartzite (upper Proterozoic) - Mostly vitreous, almost white quartzite; 1500 to 2000 feet (460-610 m) thick just north of the map area (Crittenden and others, 1971; Crittenden, 1972).

Zkc Kelley Canyon Formation (upper Proterozoic) - Argillite to phyllite, with rare meta- carbonate; grades into overlying Caddy Canyon quartzite with increasing quartzite near Huntsville; 2000 feet (610 m) thick just north of map area (Crittenden and others, 1971).

17 REFERENCES Cited Barnett, Daniel, Bowman, J.R., and Smith, H.A., 1993, Petrologic and geochronologic studies in the Farmington Canyon Complex, Wasatch Mountains and Antelope Island, Utah: Utah Geological Survey Contract Report 93-5, 34 p.

Benson, A.L., 1966, Devonian stratigraphy of western Wyoming and adjacent areas: American Association of Petroleum Geologists Bulletin, v. 50, no. 12, p. 2566-2603. [p. 2570]

Bissell, H.J., and Childs, O.E., 1958, The Weber Formation of Utah and Colorado, in Symposium on Pennsylvanian rocks of Colorado and adjacent areas: Denver, Colorado, Rocky Mountain Association of Geologists, p. 26-30, plate 1.

Brooks, J.E., 1954, Regional Devonian stratigraphy in [northern,] central and western Utah [and eastern Nevada]: Seattle, University of Washington, Ph.D. dissertation, 193 p. [p. 179 on Durst Mountain]

Brooks, J.E., 1959, Devonian regional stratigraphy in north central Utah, in Williams, N.C., editor, Guidebook to the geology of the Wasatch and Uinta Mountains transition area: Intermountain Association of Petroleum Geologists Tenth Annual Field Conference, p. 54-59.

Brooks, J.E., and Andrichuk, J.M., 1953, Regional stratigraphy of the Devonian System in northeastern Utah, southeastern Idaho and western Wyoming, in Guide to the geology of northern Utah and southeastern Idaho: Intermountain Association of Petroleum Geologists Fourth Annual Field Conference, p. 28-31 and figure.

Bryant, Bruce, Naeser, C.W., Marvin, R.F., and Mehnert, H.H., 1989, Ages of late Paleogene and Neogene tuffs and the beginning of rapid regional extension, eastern boundary of the Basin and Range Province near Salt Lake City, Utah: U.S. Geological Survey Bulletin 1787K, 12 p.

Carey, M.A., 1973, Chesterian-Morrowan conodont biostratigraphy from northeastern Utah: Salt Lake City, University of Utah, M.S. thesis, 84 p.

Cheney, T.M., 1957, Phosphate in Utah: Utah Geological and Mineralogical Survey Bulletin 59, 54 p., 3 plates. [includes information on Mississippian Delle phosphatic mbr]

Cheney, T.M., Smart, R.A., Waring, R.G., and Warner, M.A., 1953, Stratigraphic sections of the Phosphoria Formation in Utah, 1949-1951: U.S. Geological Survey Circular 306, 40 p.

Coody, G.L., 1957, Geology of the Durst Mountain-Huntsville area, Morgan and Weber

18 Counties, Utah: Salt Lake City, University of Utah, M.S. thesis, 63 p.

Coogan, J.C., 2004a, Interim geologic map of the Francis Canyon quadrangle, Lost Creek drainage, Morgan, Rich, and Summit Counties, Utah: Utah Geological Survey Open-File Report 425, 10 p., scale 1:24,000.

Coogan, J.C., 2004b, Interim geologic map of the Lost Creek Dam quadrangle, Lost Creek drainage, Morgan and Weber Counties, Utah: Utah Geological Survey Open-File Report 426, 10 p., 1 plate, scale 1:24,000.

Coogan, J.C., 2006, Interim geologic map of the Horse Ridge quadrangle, leading margin of Willard thrust sheet, Morgan, Rich, and Weber Counties, Utah: Utah Geological Survey Open-File Report 480, 19 p., scale 1:24,000.

Crittenden, M.D., Jr., 1959, Mississippian stratigraphy of the central Wasatch and western Uinta Mountains, Utah, in Williams, N.C., editor, Guidebook to the geology of the Wasatch and Uinta Mountains: Intermountain Association of Petroleum Geologists Tenth Annual Field Conference, p. 63-74.

Crittenden, M.D., Jr., 1972, Geologic map of the Browns Hole quadrangle, Weber and Cache Counties, Utah: U.S. Geological Survey Geologic Quadrangle Series Map GQ-968, scale 1:24,000.

Crittenden, M.D., Jr., Schaeffer, F.E., Trimble, D.E., and Woodward, L.A., 1971, Nomenclature and correlation of some upper Precambrian and basal Cambrian sequences in western Utah and southeastern Idaho: Geological Society of America Bulletin, v. 82, p. 581-602.

Eardley, A.J., 1944, Geology of the north-central Wasatch Mountains, Utah: Geological Society of America Bulletin, v. 55, p. 819-894, plate 1, scale 1:125,000. [Norwood Tuff proposed and type area]

Eardley, A.J., 1955, Tertiary history of north-cental Utah, in Eardley, A.J., editor, Tertiary and Quaternary geology of the eastern Bonneville Basin: Guidebook to the geology of Utah, number 10, p. 37-44. [Huntsville fanglomerate proposal]

Eliason, J.F., 1969, The Hyrum and Beirdneau Formations of north-central Utah and southeastern Idaho: Logan, Utah State University, M.S. thesis, 86 p.

Evernden, J.F., Savage, D.E., Curtis, G.H., and James, G.T., 1964, Potassium-argon dates and the Cenozoic mammalian chronology of North America: American Journal of Science, v. 262, p. 145-198. [single date on volcanic rocks in Morgan Valley]

Hintze, L.F., 1959, Ordovician regional relationships in north-central Utah and adjacent areas, in

19 Williams, N.C., editor, Guidebook to the geology of the Wasatch and Uinta Mountains transition area: Intermountain Association of Petroleum Geologists Tenth Annual Field Conference Guidebook, p. 46-53.

Lofgren, B.H., 1955, Resume of the Tertiary and Quaternary stratigraphy of Ogden Valley, Utah, in Eardley, A.J., editor, Tertiary and Quaternary geology of the eastern Bonneville Basin: Guidebook to the geology of Utah, number 10, p. 70-84. [Huntsville fanglomerate described]

Johnson, J.G., Sandberg, C.A., and Poole, F.G., 1991, Devonian lithofacies of western United States, in Cooper, J.D., and Stevens, C.H., editors, Paleozoic paleogeography of the western United States II: Los Angeles, California, Pacific Section, Society of Economic Paleontology and Mineralogy, p. 83-105.

Kummel, B., 1954, Triassic stratigraphy of southeastern Idaho and adjacent areas: U.S. Geological Survey Professional Paper 254-H, 194 p.

Madsen, J.H., Jr., 1959, Geology of the Lost-Echo Canyon area, Morgan and Summit Counties, Utah: Salt Lake City, University of Utah, M.S. thesis, 65 p., scale 1:31,680.

Madsen, D.B., and Currey, D.R., 1979, Late Quaternary glacial and vegetation changes, Little Cottonwood Canyon area, Wasatch Mountains, Utah: Quaternary Research v. 12, p. 254- 270.

Mann, D.C., 1974, Clastic Laramide sediments of the Wasatch hinterland, northeast Utah: Salt Lake City, University of Utah, M.S. thesis, 112 p. [single date on volcanic rocks in East Canyon graben]

Mullens, T.E., 1971, Reconnaissance study of the Wasatch, Evanston, and Echo Canyon Formations in part of northern Utah: U.S. Geological Survey Bulletin 1311-D, 31 p.

Mullens, T.E., and Laraway, W.H., 1964, Geology of the Devils Slide quadrangle, Morgan and Summit Counties, Utah: U.S. Geological Survey Miscellaneous Field Studies Map MF-290, scale 1:24,000.

Mullens, T.E., and Laraway, W.H., 1973, Geologic map of the Morgan quadrangle, Morgan County, Utah: U.S. Geological Survey Miscellaneous Field Studies Map MF-318, scale 1:24,000.

Nohara, Tomohide, 1966, Microfauna of the Upper Mississippian Great Blue Limestone [Doughnut Formation] near Morgan, Utah: Salt Lake City, University of Utah, M.S. thesis, 88 p.

20 Rigby, J.K., 1959, Upper Devonian unconformity in central [sic, northern] Utah: Geological Society of America Bulletin, v. 70, p. 207-218.

Sadlick, Walter, 1955, The Mississippian-Pennsylvanian boundary in northeastern Utah: Salt Lake City, University of Utah, M.S. thesis, 77 p. [proposes Round Valley Limestone]

Schell, E.M., and Moore, K.P., 1970, Stratigraphic sections and chemical analyses of phosphatic rocks of Permian and Mississippian age in Weber County, Utah: U.S. Geological Survey Circular 635, 11 p.

Schick, R.B., 1955, Geology of the Morgan-Henefer area, Morgan and Summit Counties, Utah: Salt Lake City, University of Utah, M.S. thesis, 60 p., scale 1:31,680.

Smith, H.P., 1969, The Thaynes Formation of the Moenkopi Group, north-central Utah: Salt Lake City, University of Utah Ph.D. dissertation, 378 p., 13 plates.

Smith, K.A., 1997, Stratigraphy, geochronology, and tectonics of the Salt Lake Formation (Tertiary) of southern Cache Valley, Utah: Logan, Utah State University M.S. thesis, 245 p.

Sullivan, J.T., and Nelson, A.R., 1992, Late Quaternary displacement on the Morgan fault, a back valley fault in the Wasatch Range of northeastern Utah, in Gori, P.L., and Hays, W.W., editors, Assessment of regional earthquake hazards and risk along the Wasatch Front, Utah: U.S. Geological Survey Professional Paper 1500, p. I1-I19.

Sullivan, J.T., Nelson, A.R., LaForge, R.C., Wood, C.K., and Hansen, R.A., 1988, Central Utah regional seismotectonic study for U.S. Bureau of Reclamation dams in the Wasatch Mountains: Denver, Colorado, U.S. Bureau of Reclamation, Seismotectonic Report 88-5, 269 p.

Welsh, J.E., and Bissell, H.J., 1979, The Mississippian and Pennsylvanian (Carboniferous) Systems in the United States, Utah: U.S. Geological Survey Professional Paper 1110-Y, 35 p.

Williams, J.S., 1943, Carboniferous formations on the Uinta and northern Wasatch Mountains, Utah: Geological Society of America Bulletin, v. 54, no. 4, p. 591-624.

Williams, J.S., 1971, The [Devonian] Beirdneau and Hyrum Formations of north-central Utah: Smithsonian Contributions to Paleobiology, no. 3, p. 219-229.

Yonkee, W.A., DeCelles, P.G., and Coogan, J.C., 1997, Kinematics and synorogenic sedimentation of eastern frontal part of the Sevier orogenic wedge, northern Utah: Brigham Young University Geology Studies, v. 42, part 1, p. 355-380.

21 General Bryant, Bruce, 1988, Geology of the Farmington Canyon Complex, Wasatch Mountains, Utah: U.S. Geological Survey Professional Paper 1476, 54 p., scale 1:50,000.

Bryant, Bruce, 1990, Geologic map of the Salt Lake City 30' x 60' quadrangle, north-central Utah, and Uinta County, Wyoming: U.S. Geological Survey Miscellaneous Investigations Series Map I-1944, scale 1:100,000.

Carley, J.A., Jensen, E.H., Cambell, L.B., Barney, Marvin, Fish, R.H., Chadwick, R.S., and Winkelaar, Paul, 1980, Soil survey of Morgan area, Morgan County and eastern part of Weber County: U.S. Department of Agriculture, Soil Conservation Service and Forest Service, 300 p, 62 plates.

DeCelles, P.G., 1994, Late Cretaceous-Paleocene synorogenic sedimentation and kinematic history of the Sevier thrust belt, northeast Utah and southwest Wyoming: Geological Society of America Bulletin, v. 106, p. 32-56.

Gates, J.S., Steiger, J.I., and Green, R.T., 1984, Ground-water reconnaissance of the central Weber River area, Morgan and Summit Counties, Utah: Utah Department of Natural Resources Technical Publication 77, 59 p.

Leggett, R.M., and Taylor, G.H., 1937, Geology and ground-water resources of Ogden Valley, Utah: U.S. Geological Survey Water Supply Paper 796-D, 161 p.

Sorensen, M.L., and Crittenden, M.D., Jr., 1979, Geologic map of the Huntsville quadrangle, Weber and Cache Counties, Utah: U.S. Geological Survey Geologic Quadrangle Series Map GQ-1503, scale 1:24,000.

Mineralization Blackwelder, Eliot, 1910, Phosphate deposits east of Ogden, Utah: U.S. Geological Survey Bulletin 430[-I], p. 536-551.

Gloyn, R.W., Shubat, M.A., and Mayes, B.H., 1995, Mines and prospects in and around the Farmington Canyon Complex, northern Utah: Utah Geological Survey Open-File Report 325, 96 p.

Loughlin, G.F., 1920, The ore deposits of Utah, Morgan mountain: U.S. Geological Survey Professional Paper 120, p. 218-221.

Perry, L.I., and McCarthy, B.M., 1976, Lead and zinc in Utah, 1976, Argenta district: Utah Geological and Mineral Survey Open-File Report 22, p. 245-250.

Utah Department of Highways (now Transportation), 1963, Materials inventory, Morgan County:

41°30' Cz Tl Q Brigham Pzw Mzl Q City Pzw N Pzw Dairy Zw Ridge Mzl Q Pzw Q Cz Tl Tl Zw Zw Xf Pzw Browns Causey Horse Q Huntsville Pz O Hole Dam Ridge g Pzw d Zw e Ku Zw n Cz thrust

Zw Ogden a Mzl n thrust d Tl Zw Willard Xf Pz Mzl thrust M Bybee Lost Creek Q Ogden Durst o Knoll Dam Pz Mtn. thrust r g Xf Zw Snow a n Pz Tl Wasatch Front basin Basin Pz V

Wasatch Range Xf a Willard Wasatch l Durst l Ku e Mtn. Peterson y Devils s thrust Slide Km Crawford Ku Great Q Morgan Mzl Pz fault Tl Cz Z 41° Salt Porterville East Cyn. Km Kl Cz Xf Reservoir Lake Pz Xf Ogden zone Great Basin Tl Mzl Ku Province Cz Pz Tl Tl Antelope Cz Kl Mzl Scale Island Q Km Ku 0 5 10 mi Kl Kl Ku 0 10 20 km Salt Lake Kl 112° City Tv Mzl Mzl Mzl Tv Kl

Q Quaternary deposits Kl Cretaceous, lower Cz Cenozoic basin fill Mzl Mesozoic, lower Tl Tertiary, lower Pz Paleozoic Tv Tertiary volcanics Pzw Paleozoic, Willard thrust sheet Ku Cretaceous, upper Zw Late Proterozoic, Willard thrust sheet Km Cretaceous, middle Xf Farmington Canyon Complex

Figure 1. Generalized geologic map (modified from Yonkee and others, 1997), showing quadrangles referred to in text. Table 1. Heights of alluvial deposits above adjacent active drainages in the Durst Mountain quadrangle. Heights are similar in Weber River Valley in adjacent Morgan, Peterson, and Snow Basin quadrangles. Older ages (>150ka) from information in Sullivan and others (1988) and Sullivan and Nelson (1992).

Unit(s) Feet (m) above drainage Age (ka=1000) years Comments Qal, Qay, Qafy at to slightly above <~10 ka

Qa2 ~15 feet (5 m) <~13 ka Qat2 ~20 feet (6 m)

Qap 15 to 40 feet (5-12 m) Qatp 25 to 30 feet (8-9 m) ~13-15 ka Qafp ~ 40 to 45 feet (12-14 m)

Qab 40 to 80 feet (12-24 m) ~15-20 ka Qafb > ~40 feet (>14 m)

Apparently absent ~130-150 ka “Bull Lake” glaciation-related deposits

Qao 70 to 120 feet (20-37 m) Qato ~100 feet (30 m) Qafo ~70 to 110 feet (20-35 m) 300-600 ka where dated may really be Qafoe

Qaoe? 80 to 100 feet (24-30 m) correlation uncertain

Qaoe 120 to 200 feet (35-60 m) >730 ka where dated may really be QTay Qafoe ~160 feet (50 m)

QTay ~160 to 300+ feet (50-90+ m) >730 ka QTao ~320 to 800 feet (100-240 m) >730 ka height extremes from outside quadrangle

QTaf ~1000 feet (300 m) >730 ka may be entirely Pliocene Alluvial Lacustrine Glacial Mass-movement Mixed Human

Stream Terrace Fan General Gravel Sand General General Slide, Slump, and Flow General Rock Talus Collu- Alluvium Lacustrine Colluvial Mass Deltaic Deltaic Disturbed fall vium and and and movement and and Colluvium Alluvium Residual and Glacial Lacustrine Fan

Qal Qms Qh Qaf1 1 Qay Qafy Qmdf Qmsy Qal2 Qat2 Qa2

Holocene ? ?

Bonneville Qafp Qaf Qap Qa Qmrf Qla Qmg Regressive Qatp Qat Qc, Qlg Qls Ql Qms Qmc Qmt Qcg Qac Qng Qdlb Qfdb Bonneville Qafb ? Qab ? Qg, Transgressive Qgm, ? Qga ? Qato Qafo Qao Pre-Bonneville ? ? ? ? ? ? ? Qmso ? ?

Pleistocene Qafoe Qaoe ? ? ? ? ? ? ? ? ?

QUATERNARY QTay ? QTao ? ? QUATERNARY CORRELATION CHART QTaf Durst Mountain Quadrangle

TERT. ? unconformity Thv

Plio. ? unconformity

Tcy

Miocene ? Ts unconformity

Tca Tct Tcw TERTIARY

Oligocene Tcg ? ? Tn unconformity Paleo.-

Eocene Tw unconformity Tk

Keh K. unconformity

JUR. ? TRa

TRt

TRw TRIASSIC TRd unconformity Ppf Pp Ppm Ppg

PERMIAN Pwu PIPwu PIPwl ? ? PIPw disconformity ? ? PIPwls IPwl IPm IPr PENNSYLVANIAN Mdu Mdl Mhu Mhl

Mde

MISSISSIPPIAN Mdd Ml unconformity

Db unconformity

Dh unconformity DEVONIAN Dwc unconformity BEDROCK -C n CORRELATION unconformity CHART -C m Durst Mountain -C ou Quadrangle

-C om WILLARD CAMBRIAN THRUST -C ol SHEET -C t Zm unconformity Zi ? Xf Zcc

Xfpg Zkc PROTEROZOIC PROT. ? Diagrams areschematic--- scaleapproximate AGE EARLY TERTIARY AGE PROTEROZOIC CAMB. DEV. MISS. PENN. PERM. TRIASSIC ? JUR. K. Q. ? PROTER. P.-E. ? Oligocene ? M. Plio. Q-various Mhu, Mhl Mdu, Mdl - SYMBOL SYMBOL C ou,m,l PIPw Pp Ts QT-var. Mde Dwc MAP MAP Keh - IPm Zkc Zcc C m - TRw Zm TRd TRa Tw Dh Db C n - IPr Ml Jn TRt C t Xf Zi PIPwu PIPwl Ppm Ppg Thv Tc_ Tcy Ppf Tn ? Higham Gritand Timothy SsMbrof Thaynes Fm Hams ForkMemberofEvanstonFormation Grandeur MemberofParkCityFormation Franson MemberofParkCityFormation Meade PeakMemberofPhosphoriaFm younger unnamedconglomeraticrocks Ophir Formation(upper, middle,lower) alluvium, lakebeds,massmovements Lanes Shale Tongue of Ankareh Fm Wood Shale Tongue of Ankareh Fm Doughnut Formation(upper, lower) Humbug Formation(upper, lower) unnamed conglomeraticrocks Farmington CanyonComplex fanglomerate ofHuntsville Kelley CanyonFormation Water CanyonFormation Caddy CanyonQuartzite Round Valley Limestone Beirdneau Sandstone Lodgepole Limestone Woodside Formation Dinwoody Formation Norwood Formation Wasatch Formation Maxfield Limestone Thaynes Formation Deseret Limestone Nounan Formation Nugget Sandstone Morgan Formation Weber Sandstone Mutual Formation Hyrum Dolomite alluvium, gravel Tintic Quartzite MAP UNIT MAP UNIT Inkom Formation WILLARD THRUST SHEET Durst Mountain Quadrangle LITHOLOGIC COLUMN 500-3000 FEET METERS FEET METERS 360-450 380-725 650-800 200-400 40-1000 0-1000 35-200 0-1000 1,500- 5000+ 2500- 1835- 0-100 0-300 indeterminable 2,000 2,000 1,000 1,200 1100- ~350 ~350 ~300 ~800 ~650 ~600 1000 1500 3000 2200 up to 800- 435- 300 200 200 500 700 500 400 220 170 285 THICKNESS THICKNESS 115-220 460-610 135-365 200-245 760-915 560-670 335-460 150-900 245-300 110-140 60-120 12-300 1500+ 0-300 0-300 ~105 ~105 ~245 ~200 ~180 up to 9-60 0-30 0-90 ~90 610 300 150 215 150 120 90 60 60 65 50 85 SCHEMATIC SCHEMATIC COLUMN COLUMN - - - Base cutbythrust Argillitic tophyllitic Meta-tuff lenses Some feldspar locally Cross-bedded Purple topink Xfpg-- pegmatite Gneiss andschist 1,700± Ma Skolithus C ol200ft. C om100ft. C ou~200ft. MAJOR UNCONFORMITY Fossiliferous Delle PhosphaticMember-Mdd Absent tonorth See correlationchartfor DISCONFORMITY? Wells Formation? Includes RexChert UNCONFORMITY Not exposed Not exposed UNCONFORMITY ANGULAR 38.4 MaK-Ar(corrected) Protoreodon Altered tuff Tcg-Tn interbedded MAJOR UNCONFORMITY other units OTHER INFORMATION OTHER INFORMATION