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  • GEOLOGIC MAP OF THE RICHFIELD 30' x 60' QUADRANGLE
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30 20 25 11 20 18 12 12 16 8 14 12 5 72 10 10 55 12 20 20 5 35 10 30 30 30 18 16 24 26 5 26 12 10 9 17 20 18 16 22 17 20 2 45 45 70 30 60 30 30 40 9 5 4 5 7 5 8 5 8 75 43 25 4 8 40 50 45 15 12 6 7 12 2 3 6 10 5 20 17 30 16 18 19 31 21 28 15 30 17 17 22 9 11 11 20 15 12 48 80 25 30 5 10 4 4 8 8 7 8 8 7 10 20 10 15 25 47 10 21 23 15 26 26 11 24 18 15 15 14 30 20 25 15 10 5 5 6 7 10 10 7 10 7 20 7 10 6 10 12 11 14 9 10 11 9 10 6 25 20 20 30 30 30 25 15 25 20 10 20 10 25 28 35 55 5 15 50 46 30 24 30 45 25 40 16 60 40 5 20 5 10 30 20 30 50 14 20 13 18 45 40 45 20 35 55 40 50 25 55 50 40 65 60 5 8 10 7 10 8 5 7 6 25 35 30 35 40 20 30 30 20 10 40 17 37 15 20 20 10 15 45 15 20 15 15 12 3 9 10 12 20 20 20 20 9 8 23 23 28 30 28 25 30 27 20 25 20 30 4 25 20 10 25 5 10 5 15 32 31 20 20 16 8 4 3 4 15 2 10 4 5 10 25 15 10 25 15 10 15 10 25 8 10 15 45 60 30 2 2 5 10 25 15 10 15 12 15 30 10 15 14 9 25 25 38 20 30 82-3 60-1 82-1 81-4 79-3 78-4 78-3 78-2 Ttl DRY WASH FAULT MONROE PEAK CALDERA ZONE ELSINORE FAULT ZONE SEVIER FAULT ZONE RED RIDGE THRUST PAVANT THRUST Dsy Toi Tse Qac Tmj Qac Tmi Tmpu Toi Tmr Tmpu Tmr Tmj Qms Tbc Tmj Tmpf Qms Tmr Tmh Tmh Tmpl Tmj Tbc Qms Tmpl Tci Tmb Tmf Qms Tmj Qaf 2 Tisg Qac Tmpf Tmpi Tmh Qms Tbc Toi Trd Tdd Qms Qac Qms Tigp Tmj Trd Qac Tbc Tmi Tsm p-Cg Qac Tbci Tmi Qst Toi Tgd To Qms Tci Tmj To Tmb Tci Qms Qal 1 Tbc Qaf 2 Tbci Tmpl Tmpf Tmpl To Tbci Tmpl Qal 1 Tmi Tqm Tsm Tgd Qms Tmi Tb Trd Tmpl Tp-Cg Qms Tse Qms Tbci Tbc Tci Tp-Cg Tqm Tbc Tmd Tmd Tm Toi Tmj Qvrt Tdd Trd Tmpl Tbc QTaf Qaf 1 Tbc Tmb Tmpf Tse Tbci Qms Tmi Tmb Tmb Tmi Toi Toi Tmpf Tbct Qck Tbci Qac Qac Tgd Tmm Tmpi Tsm Tmd Qvrd Tbct Tbc Tmpi Tbc Tmps Tmpl Tbc Tmj Trd Qms Tbct Tmps Tp-Cg Trg Tbc Toi Trd Tmps Trg Tse Tbc Tbc Tmb Tmpf Tmj Qac Tbc Toi Qll Tmj Tmd Trg Tmpf Qaf 2 Trd Tsm Tgd Tp-Cg Tgd Tac Trg Tmj Trg Qms Qaf 2 Tmpi Tqm Qms Qlg Toi Tmj Tmpl Qaf 2 To Tmpi Tbct Tbc Qms Qms Tmj Tmj Tmpf Tb Tbci Tgd Tb Toi Qac Qms Qms Qea Tbc Trd Qms Qaf 2 Tmpl Tmpf Tbc Tac Tmpu Qac Tbc Trg Tbci Trd Tgd Tmpl Trd Tdm Tbct Tmps Qms Qla Tmpl Tbc Tb Tmj Qea Tmj Qal 1 Qea Qaf 2 Tmpf Tsm Tmj Tmpf Tmj Tmj Tmpf Qgt Trd To Qll Tp-Cg Tmj Qaf 2 Qms Trd Tbc Tmpa Qms Toi Qlg Tbci Tmpl Qms Tse Tbci Qrk Qms Qms Qms Tbc Tmpl Trd Qaf 2 Tmj Qms Qea To Tw Qcg Tp-Cg Tmj Qms To Tmpf Qla Qms Qms Tmpa Qac Qvb4 Tbc Tgd Trd Jn Tmpl Tbct Qms Tmpi Qac Tbct Tmpl Tmpf Jn Trd Tmpi Trd Tzt Trd Qms Tbc Tmpi Tmpi Qms Tmpa Tdm Qgt QTaf Tse Tse Qcg To Tmpl Tdm Tmj Tmpf Tmpi Trd Tmj Tqm Qcf Tse Tqm Toi Toi Tmj Tbct p-Cg Qaf2 Qea Tqm Tbci Tgm Tmj Tac QTaf Tmpa Qea Tbc Tmpi Tmpi Qgt Qms QTaf Tbci Tac Qea Qaf 1 Tbct Tdm Trd To QTaf Tmpi Qaf 1 Tqm Qms Tdm Tac Qal 1 Qea Tbc Tbc Tmpb To Tbc Tdm Qms Tse Tdm Trd Qea Tqm Tbct Tmj Tmpb Qms Tbc Qea Qms Toi Tse Tbc Tmpb Tmpl Qal 2 Tmj Qac Qea Tse Toi Tzt Tse Toi To Qac To Tmj Tmj QTaf To Tzt Toi Tsg Qac Tse To Qlg To QTaf To Tmj Tse Trd To Tmj Qms Tqm Tbci Tzt Tmj Tmj Tqm Tbc Tmj To Tgm Tmj Tbc Qac Tdm Tdm Tbc Tbct Tgm Tse Qal 1 Tqm Tba Tmj Qcf Qaf 1 Tzt Tmj Tse Qed To Qea Qea Tse Qac p-Cg Tmj Tbct Tmj Tmj Tbc Tse To Qaf 1 Trd Tse Tdv Tzt Qaf 2 Tmj Tzt Tmj Tbc Tbc To Qms Qms Tmj To To Tac Tzt Tmj Trd To Tmj To Qaf 1 Tse Qea Tmj Tbct Qms Tse Tmj Tmpi Qaf 1 Trd Trd Tse Qaf 2 Tmj Tac To Trd Tzt To Tzt Tzt Tdv Qvb 4 Tzt Tse Tac Qea To Tcc Qms To Taa To To To Tzt Qal 1 Trd To Tmj Tw Qea Tbct Tac Tzt To Qaf 2 Tac Qaf 1 Tcc Tw Tzt Tw Tbct Qaf 2 Tsg Qaf 2 Tb Qms Tbct Qvb 4 To Tbci Qaf 1 To Tgm -Cdh Qea Tbc Tmj To Tw Qaf 2 Tbc Qal 1 To Taa Tzt Tmj To Qst Qea Qea Tac Cp -Cdh Tbct Qms Qcg Tbc Tw Qaf 2 Tdv Tmj Tdv Qms To Tsg Tw Tbct Tdv Qaf 2 Qla -Cdh Tdv Qaf 2 -Cpm -Cp Qal 1 Tcc Qms Qal 1 Qms Qac -Cdh Tmj Qaf 2 -Cpm Tac Tmj Tdv Tac Tb Tb Qvb 4 To Tdv Tac Taa Tsg Tac Qea Tse Tdv Tac Qcf Tbc Tmj Tbc -Cpm -Cdh Tmpi -Cdh Tsg Tbct Tbct Tse Qst Tmj Tbct -Cpm Taa Qea Qal 2 Tbc Tmpi Tbct Tsg Qaf 1 Tbct Qaf 2 Tsg Tw Qsa Tmj Qaf 2 Tmj Tdv -Cpm -Cdh Qcf -Cdh Tcc Qea Tbct Qaf 2 Tcc Tcc Kcg Qgt Qcf Tql -Cdh Tbc Qms -Cdh To QTaf Qaf 1 -Cpm Tmj Tbct Qal 2 Tdv Tbc Tcc Tcc Qms Qea -Cp Tql Tau -Cdh Tbct -Cwt? Tsg Tse Qal 2 Tbci Tbct Taa Tbc Qlg -Cp Qcf Tbc -Cpm Pq Tse Tsg Qaf 1 IPc Tau Tau To Qaf 1 Qgt Tcc Tbct -Cpm Taa Tmj Tba Qaf 2 Qms Qal 2 -Cwt? Tsg Tcc Tse Qaf 2 Tcc To To Tau Qal 1 Tbc Kcg Tw Tbc Tmj Qgt Tql Tau IPc Tdv Tac Qst -Cpm Qvb 4 -Cwt? Qaf 2 Tau Tw Qst Pq Tbc To Tsg Tda Tse Tw Tse Qaf 2 Mr Ppk Tbct -Cp Tcc -Cwt? -Cdh Qms (Tdv) Tbct Qms Tac Tac IPc Qmu -Cp Tdv Tse Qaf 2 Qac Tdv Tw Qms Qac Tbct Qaf 1 Tbct Tbct Tse -Cpm To Tcc Tba Tsg Tsg -Cpm Tse Qms Qlg To Tbct Tw Tw Qms Tbc Qaf 2 Ttl Tac Qal 3 -Cpm QTaf Tse Tse Tsg Qal 2 Tw Qac Tau Tau Tse Tac Tac Qal 1 To Tdv Tdt Qaf 2 Tba Qvb 5 Tdv Tbct Tac Pq Qlg Tba Tdv Dc Dg Qaf 2 Qac Tw Tw Pq Qvb 5 Pq Ppk Tdv To Tbct Tdv Pq Tse Qms Tdv Tba Ppk QTaf Ttl Mr QTaf Tdv Tda Tdt Qgt IPc Tba Tsg Tsg Tbct Tau Qac Pq Ttl To Qlg Ppk Tac Tcc Tse Qms Tba SOu Tdv SOu Mr Qms Qlg Tdt Ttl Tau Qms IPc QTaf To Qaf 2 Tba Ppk Tac Toc Ttl Tcc Qla Dc Ttl To Pk Tcc Qms Dg QTaf Qac Tau Qal 3 Qal 1 Pq Qla/ Qvb 5 SOu Ppk T Rm Qaf 2 Tse Tba Tsg Dsy Tba Qaf 1 Qaf 2 Ppk Pq Tdv Qms Pq Tsg Tba Qms Tac Tdv Tbct Qms Tbct Ttl Tsg Qac QTaf Qaf 2 IPc Pq To Tda Ppk SOu Pq SOu Tba Tcc Tau Tcc Oe Toc Tbct Tba Tbct Tac Toc Qms Pk Dc Tba Tse Tse Ttl Tse Tac Qaf 1 Tql Ttl Tcc IPc Qaf 2 Tse Ttl Qmu Tba Tf Tse Pq To Tbct Pk Qaf 1 Qaf 2 Pk To Tac Tbct Mr Tac To Ttl Tw Ds Ttl T Rcs Qaf 2 Qms Tbct Toc To Tbct Ttl Qms Qaf 2 To Ttl Tac To Toc Tcc Oe To Qac Tbct Tba Qlg Mr Ttl T Rcu Pk Qaf 2 Dg Tac T Rm Tse Pk Qed Tcc Pk Pq Tba Pk Qmu Dc Dg Tac Tsg Tac Dsy Pk Qms (Tbct) Qac Qms (Ttl) Qac Tcc To Tac Oe Ttl Tbct Qac Tsg Op Tac Toc Tba Tbct SOu Pq Tcc Tcc Qms Tac Tbct Ttl Tbct Tse Qms (Tbct) SOu Mr Tac To Tbct Pq Tac Dsy Qms Qaf 1 Tbct Qaf 2 Tac To Pk Qms Ttl Tsg Tf Tau Qla/ Qvb 5 Tau Qac Qaf 1 Tba Op Qac Dc Qac Qed Tf T Rm Tf T Rcs Qms To Dg Tcc Tac T Rcu Dsy Qal 2 Op Tcc Dc Tbct Qla Ttl Mr Qac Qac Oe Tac T Rm Qms (Tdv) Ttl Tbct Tac Dg Tac Tse T Rm Tb Qac Tw Tdt Tw Qms SOu Tw Tbm Qms (Tdv) Tbct Tau Pk Tba T Rcu Dg Tba Tdt Qac Tf Tbct Dsy Tcc Qal 1 T Rcs Tdt Ttl Oe Qac Jn Tac Tse Qms Pq Dsy Tsg Qms Op Tac Tbct Tcc Tau Tau Qal 2 /Qvb 5 Tac Tbct Ppk T Rcs Ttl Tcc Tdt Qms Ds Tba Qms IPc Tf Tac Tbct Tau Oe Tac Tdv SOu Qaf 2 Tcc Tbct Dsy Qms (Tdv) Qms (Tdv) Oe Ttl Tau Qac Tbct Tdt Qvb 5 Dsy Tbct Tf Tac Ttl T Rm T Rm Qms Toc Ttl Ttl Qac -Ca Tsg Tbct Qac Qed Qal 1 Qac Tac Tau Tdt Tau Pk Qms Tcc Qms Tcr Tac Qac SOu Qmu Tse Ttl Tac T Rm Qms (Tbct) Op T Rm Toc Qac Mr Qac Qms (Tac) Ttl Qaf 1 Qac Tdvt Tac Qms Pk To Tau Qac Tac Qac Tac Op Tsg Tcc Tac Pk Qac Ttl Tac Pq Op Tse Tcr Ttl Qac IPc Ds Tau Ppk Qac Dc Qac Tbct Toc Ttl Toc Qac Tdt Dg Tcp Qmu Tf Qac IPc Qac Qlg Tsg Qms Tac Qms Qms Tac Tcc Tsg Qac Dsy Tau SOu SOu Qac Tac Tcc Qmu Tau Qac Tdv Dc Tau Qac Tbct Qaf 2 /Qvb 5 Tf Qac Tau Toc Dc Tau Tdvt Ttl Tau Tda Tau Ds T Rcs Tcc Dsy Ttl Dc Tau Qms (T Rcu) Tcr Tf Tf T Rcu Oe Tf Dg Toc Qac Tcc Op Tau Toc Qmu Ttl To IPc Tfmw Qmu Tau Dc Tdv Tbct Tdv T Rm Tfur Qlf Tac Qms Dc T Rcs Tcc Qal 2 Ttl Qac Tac Tf T Rm Qaf 2 Qms (Tcc,Ttl) Dc Qac Ds Toc Qac Qmu Ttl Tac T Rm Tcc Qaf 2 Ttl Tbct Tcr Tau Qaf 1 Pk Qal 1 Qlf T Rcs Qmu Tf Dg T Rm Qac Toc Tac Qms (T R) T Rcu Tau T Rcs Tsg Dsy Toc Tcc Tf Toc Tcc Tbct Tf Tac Tac Tda Op Qac Qaf 1 T Rm Tcc Toc T Rcu Tfuw Tac Toc Qmu Qac T Rcs Toc Tbct Tda Tov Oe Dsy Qal 2 SOu Dg Tcc Dg Qmu Qms Ds Dc Qms (Jn) Tcp Qac Pk Qms (Tcc,Ttl) Toc Jn Tau Pq Tsg Dc Qms Qaf 1 Tcc Qlf Qac Jn Tfuw Tac Qaf 2 -Cum Dc Qac Ttl Tcc Tac Ttl Dg Tac Qms SOu Ttl Qms SOu -Ct Qmt Jn Tcp Tfur Qac Tbct Tau Mr Op Ttl Qaf 2 Jn Tf -Cop Mr T Rcs Tbct Ds Ppk Qms Tcc Tau Tac Tbct Oe Ttl Tcc Tflw Qac Tcc SOu Qms (Tcc,Ttl) Tfmw Tau Qac Oe IPc Tac Tbct QTlf QTlf Qac Tau -Ca Mr Qal 1 Tcc Qms Jn -Ct Qaf 1 SOu Tov Tcc Tbct Tau Tcc Op Tcp Tfur Tg Jn Tf Ttl Qlg Tcr Qms (Tac, Tbct) Tsg T Rm Ttl Dg Tbm SOu -Cox Tbct Tcc Toc Toc -Cum Oe Pq Qac Op Toc Ds Tbct Tcr Tac Qlg -Ct Qaf 2 Tfur Tfur Ttl Qaf 1 Tfuw Ppk Pk T Rm Qla SOu -Cum Tfur Tcc -Ca Ttl Qac Mr Tfur T Rcs Qls Tdvt Toc Qms (Tac, Tbct) Mr Qla Toc Tfur Tau Toc Tac T Rcs Tflw Tfmw Toc Qaf 1 -Cox Pk Pq Ppk -Ct Jn SOu Mr Dc -Cop Tch Tfuw Tg Qaf 2 Tfur Dsy Qms (Tac,Tbct) Toc -Ct Tch Jn Toc -Ct Trt Pk T Rm Qmu Ttl Ccm Tch Qlg Pq T Rm Qlg -Ct Tcr Ttl Pk Qms (Tcc,Ttl) Mr QTlf Op Qlg -Ct Jn Tg Tcr -Cwt Ttl Ttl -Cum Pq Qaf 2 Qms Tfmw QTlf Qlg Ttl Oe Kc Qac Ttl Tfuw Tfur Qmu Oe SOu Mr Kc Tcp SOu Tau Oe Tcr Tflr Qac Op Qac Qls Qst Tfur Qms Qac Qaf 1 Qms Tfur Qlg Ttl Toc Tcc Tcr -Cum Qaf 2 -Cop Tch Qaf 2 Qlg Tau Tau Toc Tau Qmt -Ct Tg Qal 1 Qlg Qaf 2 Toc Tau -Cum Tfur QTlf Tch Tdvt Qaf 1 -Cum Qal 1 Ttl -Ct Tfur Qlg Ttl Qls Qmt To -Ct Tch -Ct Qlf Tac QTlf Tfmw Tfmr Qlg Tau Qlg Qmu Qlg Tau -Cop Qlg -Ct Qaf 2 Qla Tau Tbr -Cum Qla Qlg Jn Trt Qaf 2 -Cum Qms (Tg) Qms (Tch) Qlm Tfuw Ttl Qmt Tfur Toc -Ct Qlg Qms Qlg Tfur Tg Qls Qmu Toc Tg Tch Tf Toc -Cop -Cop -Ct Qlf Qlg QTlf Qmt Qlf/Qvb 5 Tg Qms (Tg) Tch -Ct Qac Qla -Cop -Cum Qlf Qms Qlg Qlg Qlg -Cum Qms (Tch) Qlg QTlf Qlg Qla -Ct Tg Tg -Ct Tfuw Qms (Tg) Tg Qvb 4 Qms Qlf Qaf 1 Qla Qed Tfmr Qaf 2 Qla Tf Qms (Tg) Qla Tg Qlg Qla Qls Qlg Qlg Tfur Qlf Tcr Tch Tfuw Qaf 2 Qlg Tf Tfur Qlf Qms (Tch) Qmt Qlg Tfur Ttl -Cw Qms (Tch) Tch Qac Qla Qmu Tfmw Tg Qaf 2 Tg Qac Qlg Qaf 1 Jn Qlg Tf Tfuw Qls Qlg Tcr Qla Qlg Tch Pq Ttl Qac Tfmw Qlg QTlf Toc Toc Qlm Qll Tcc Qmu Tfuw Tfmw Tfmw Qaf 1 Qvb 4 Qmu Qla Qms Pk Tfur Pk Tf Tfuw Qms Qmu Tfur Ttl QTlf Tcr Qla Mr Tfmr -Cw Tfmr Tbr Pk Qlg Tfmw Qlg Tcr Qlg Toc Tbr Qac QTaf Tf Qlg Tcr Ttl Pk QTlf Qmt Qac Mr Qlg Qal 2 Qaf 1 Trt Qms Qls Tfmr QTlf Mr Qaf 1 T Rm Qla Tbr Qmt Qaf 2 Pk Mr Tfmw Tbr Qlg Qaf 2 Tfmw -Cp Qal 2 Qls T Rm Tfmw Mr Tcr Qvb 4 Trt Qal 1 Tfmr Qlg Qlm Tbr Qaf 1 Tfmr Tcr Tcr Qms (Tg) Ttl Tfur Ktm Jn Tcr Qaf 2 Tbr Qlg Qvb 4 Pk Tfuw Qvb 4 Qlm Tbr T Rm Pk Qls Tcr Tlr Tcr Qvb 4 Qls -Ccm Qla/ Toc -Cp T Rcu Qlm Qaf 2 T Rcs QTlf Pk Qms Tcr Tg Tfur Tfuw Tfur Tbr QTlf Qmt Tcr Qlg Qaf 2 Ttl Tfmw Qac Pk Tfmw Tbr Qlg Qmt Ttl Jn Qms Qac Qaf 1 Qls Ttl Tg Qac Qlg Qac Qaf 1 Tfur Qaf 2 Jn -Cp Tcr Qac Tfuw Tcr Qlg Tg Qlg Qaf 2 Qla Qvb 4 Qlg Qls Qal 2 Tch Toc Qla Qlg QTlf Qlg Tbr Tbr Pk Tfur Tfur Qaf 2 Qvb 4 Qaf 1 Qls Qms T Rm -Cdh QTlf Qmt Qla Qal 1 -Cwt Tg Toc? Tg Tfuw Tbr Tfmr Qla Tfur T Rcu T Rcs Qmt Tbr Tcr Tcr Qaf 2 Tbr Qac Tfmr Tfur Qac Tcr Tfur Qlg Tfmw Qla Tfmw QTlf Qla -Cw Qlf Qaf 2 Tfmr Tbr T Rcs Qaf 2 Tfmw T Rm -Cw Tg Pk Qmt Tfmr Qlg Tbr Qlf/ Qvb 4 Qlg Qmt Qlg Tfmr Qmt Tbr Toc? Qac Tbr Qla Tfur Cwt Qlg Qlg Qaf 1 Qaf 1 Qmt Tflw -Cw Tbr Tfmw Qac Tbr Qaf 2 -Ccm Qaf 1 Qal 2 Qla Tfmr Tg Tac -Cwt Qdg Tbr Qac Tfmr Qla Tbr -Cwt T Rm -Cwt Pk Qlg Tfuw Tbr Qac Qaf 2 -Cwt -Cwt -Cp Qmt -Cw Qaf 2 Tg -Cob Tfmr O-Cn Qls Tac Qac Tch Tbr -Cou T Rm Tfuw Tfmr Tbr Qac Tg Pk Qaf 1 Qmt Qed Tac -Cob Tfmr -Cwt Tfur Ktm Qac -Cwt Qmt Qst -Cob Qmu Qac Tg Tbr Qlf Tg Tg Tfuw Tac Qms Ktm Tdvt Tfuw -Cwt Tfmw Tfur Qac Tau Tfur Qla Tg Qaf 2 Qvb 4 Tf Tf -Ccm T Rm Tg Qdf Pk Tf Tfmw Toc Tch Qmt -Cwt Tac Qlf Tf Tfmr Tf Qmt Qla Qaf 1 Qaf 2 Tfmr Tfmw -Cob -Cwt Qgt Qmu -Cp Qdg Tflr Qvb 4 Qmt Qac -Cwt Qla -Cob QTlf -Cob Qms (Jn,T Rcu) Qst -Ccm -Cw Qaf 1 Qaf 1 -Cob Tflw -Cob Tf -Ccm Tg -Cp Qed Qac Qaf 2 Tf -Cwt Qlg Qed Qlg Tf Tflr Tch Tflr Qlg Qlf/Qva 5 -Cwt Qlf -Cwt Qms (T Rcu) Qaf 2 Jn Qmt Qmt Tg Qla -Cop -Cp Qlg -Cwt T Rcu Tfmw Qla -Cwt -Ccm -Cwt Tfmr Tfmw Qed Tf Qgt Qdf Tflw Qaf 2 Qdg Qlf Tfmr T Rm Qgt TKn Qgt T Rcu Jn Qmt Jn Qlg Qlg -Cwt Tflw Tf T Rm T Rm Tf Pk Tfmw Tch Qlm Ppk Qms (Tg) Qed Qaf 2 -Ccm IPc Qed Tflw Mr T Rcu TKn Tfmr Qed/Qlf/Qva 5 Qla Tflw Qlf Tf Qed Tg Tfmr Qlf Tfmr Kc Tfmw Qlg IPc Qla T Rm Mr Qdf Tflw T Rcs Qms Tfmr T Rcs Tflw Qac T Rcs -Cdh Tfmr Qms (Jn, T Rcu) Ppk Qac Qlf IPc Tf Kc Jn Qlg Qac TKn Qaf 2 Jn Ppk Jn Qlf/Qvb 4 Qla Pk T Rcu Tfmr T Rcu Kc Qed/Qlf Qaf 1 Qed Tg Tf Qdf Qaf 1 Tflr T Rcu Tfmr Qac Tch Qlf Tfmw Qlf Tfmw Tfmr QTaf Tfmr T Rcs Tf Qlf Tflw Tg Tflw Qed Qed Qla Tf Qlf Pk Qac QTaf Qac Pk Tflw TKn Qmu QTlf Tf T Rm Tf Tg Qac QTaf Tfmr Qdf Tfmr T Rcu T Rcs Qpm Dc Ktm Qlf/Qva 5 Tflw Kc Qaf 1 Tg Tfmr Tfmr QTlf Qaf 2 Tg Tf -Cop -Ct Qlf Qac TKn Tg Qaf 2 Tfmr Tflr Jn TKn QTaf Qlg TKn Qvr 4 Qlf Qac Toc TKn Tf QTlf Qed Qlf Tch -Cob Tch Tbr Qed/Qlg Tflr Qed/Qlf/Qva 5 Qlg Tf Qac Qlf QTaf Tflr Tf Qlg Tfmr Tch Tf Tf Qdg Tf Tg QTaf Tg Qlf Tflw Qac Tflr Qlf/Qvb 4 Qdg Qac Tfmr Qdf Qaf 2 Tbr QTlf TKn Tflr Tflr Qms Tg Tf Qaf 1 Tfmr Kc Qlf Tg Qlf Tflw Qac Tg Qac Qvb 2 Tbr Tfmr T Rcu Tg Ktm Tflw Tbr Tbr Qac TKn Qed Qdf Ktm Qac Qac -Cpm Qac Jn Qac Qac Tg Toc Toc Ktm Tf Toc Qed TKn Qll Qpm Qlg Qac Tg Qls TKn Qaf 2 Qdg Qac Qac Toc Tflr Qlf Tg Qaf 2 T Rm Tflr Qed/Qlg Qed/Qdg Qlg T Rcs Qla T Rcu Qal 1 Qdg Qac Qla Qdf Qal 1 Qac TKn Qed/Qll -Cwt Qal 2 Toc -Cw Qla Qlg Qed/Qlf/Qvb 4 Tg Toc Qed/ Qdg Qac Tflw QTaf Tflr Qla Qlg Qac Tg Qdf Qed Tht Qll Qac T Rcu Qac Tg T Rcs -Ct Jn Toc QTlf QTaf Tg Qlf/Qvb 2 Qlg Qpm Qac Qal 1 Tg Tg Tflr Qac QTlf Tflr -Cdh Tflw T Rm Tflr Kc Qlg Tflw QTaf Toc Toc Qed/Qvb 1 Tflr QTaf Qlg -Cop Qgt Qed/Qlg Qlg QTaf Qed Qal 1 -Cdh Qaf 2 Qmu QTaf Qaf 2 Tflr Qac -Cw Qac Qac Toc -Cop Qgt Tf Toc QTaf QTlf Tse Tf Qac -Ccm Tg -Cdh Qac Qac Qed Qaf 2 Tf -Cop Qdg Qac Tf Qlg Qls Tf Qla Toc Qac Kc Tg Qac Tg Tf QTaf Jn Qal 1 QTaf Qgt TKn QTlf QTlf Qgt -Cpm Qgt TKn Tht -Cum Toc Toc Toc Qaf 2 Toc Tf Qla QTlf Qlg Qlg/Toc Qlg Qlf Qlf Qdg Qvb 1 Qed/Qvb 3 Qed/Qlf Qdg -Cp Qdg - Cpm Qlf Qaf 1 Qdg -Cpm Qla Qla Qla Tf Qaf 1 Qaf 2 Qlg Qla -Cp -Cpm -Cp -Cdh - Cpm Qaf 2 -Cpm -Cp -Cdh -Cdh - Cp -Cpm - Cpm - Cp - Cp -Cdh -Cdh -Cdh -Cdh -Cdh -Cp -Cp -Cpm -Cdh Qaf 2 Qaf 1 Qvb 1 Qed/Qvb 1 Qlf Qal 1 Qaf 2 -Cum -Cum Qaf 2 Qaf 2 -Cum -Cum -Ct Kc -Cop TKn Tflr Qaf 2 Qaf 2 Qaf 2 Qaf 2 Qaf 2 Qac -Cum -Ct Qaf 2 Qlf Qed/ Qlf/ Qvb 4 Qed/Qlf Qed/Qlf Qed/Qlf Qed/Qlf/Qvb 4 Qal 1 Qaf 2 -Ccm -Cdh -Ccm -Ccm -Ccm -Ccm -Cdh -Cdh Qaf 2 -Cpm -Cdh -Cw -Ccm -Cp -Cp -Cw -Ccm -Cdh -Cdh -Cp -Cdh -Cpm Qaf 1 -Cpm Qaf 2 -Cpm -Cdh -Cp -Cpm -Cdh -Cdh -Cp -Cdh -Cdh -Cp -Cp -Cdh -Cdh -Cdh -Cw -Ccm -Ccm -Cw -Cdh -Ccm -Cw -Ccm -Ccm -Ccm -Cwt -Cwt -Cwt -Cwt -Cwt -Cwt -Cwt Qaf 1 -Ct -Cum -Cop -Cum -Cum -Ct -Ct T Rcu -Ct -Ct -Ct -Ct -Cop -Cum -Cum -Cum TKn Tflw Tflw Qaf 2 Qaf 2 Qaf 2 Tfmr Qaf 2 Qaf 2 Qac -Cum Qac -Cum -Cop -Cum Jn -Cum T Rm -Cop Qlf Qlf/ Qvb 4 -Cwt Qaf 2 Qaf 2 Qaf 2 -Cob -Cob -Cou -Cob -Cwt -Cwt -Cwt -Cwt -Cob -Cwt -Ccm -Ccm -Cdh -Ccm -Cw -Ccm -Cdh -Cdh -Cdh -Ccm -Cw -Cw -Cw T Rcs Tbr -Ccm -Cum -Cwt -Ccm -Cdh -Cwt -Cob -Cob -Cob Qlf Qlf/Qvb 4 Qlf/ Qvb 4 Qlf Qal 1 Qal 1 -Ct -Ct -Cum -Cum Tflr Tflr Tflr Tflw Tfmw Qaf 2 -Cop -Cob -Ccm Tbr -Cdh -Ccm Qaf 2 Jn Qlf Qlf Qal 1 Qal 1 Qal 1 Qal 1 Qal 1 Qaf 1 Qla Qla T Rm -Ct -Ct -Ct -Cum Tflr Tfmr Tfmr Tfmr Tfmr Qaf 1 Qaf 1 Qal 1 Qaf 1 -Cop -Cop -Cum Tdv Tdv Mr Qaf 1 -Ct -Ct Qaf 2 Qla Qal 1 Qal 1 Qaf 2 Qal 2 Toc IPc Tfuw Qms (Tch) Tac Jn IPc Tcc Qlf Qaf 2 Qal 1 Toc Qaf 1 Tf Tdv Qal 1 Qaf 1 Qaf 1 Tdv Tdv Tdv Pk Qms (Tcc, Ttl) Qal 1 Qlg Qlf Qlf Qla -Cp Qaf 2 Tbm Tcc Qaf 2 Tac Tac Tbct Tbct Qcf Qaf 2 Tdv Qaf 2 Qaf 2 Taa Tbc Tbct Qaf 1 Qaf 1 Tmj Qaf 1 Tbc Qaf 2 Qaf 2 Qaf 2 Qaf 2 Qaf2 Qaf 2 Qaf 2 Qed Qaf 1 Qaf 1 Trg Qcf Tbci Tmj Tse Tmj Qaf 1 Toi Toi Qaf 2 Qaf 2 Qaf 2 Qaf 2 Qal 1 Qlf Tbr Qls Qac Tfuw Qaf 2 /Qvb 5 Qaf 2 Qaf 2 Pk Qaf 2 Dg Ppk Tdv Pk Qaf 2 Jn Tdv Tac Tbc Tmj Qaf 2 Tmj Tmj Tmb Qla Qlf Qlf Qlf Qaf 2 Tcr Tcc Tsg Qaf 2 Tse Trd Trd Qal 1 Tse -Cdh -Cdh T Rm -Cou -Cwt Tbct Tse -Cp Qed/ Qvb 2 Dg Tbci Tsg Jn Jn -Cum Qaf 2 -Ccm T Rcs Qaf 2 Qal 1 Tf Jn Qaf 1 Tmpf Tse Tbc Tbc Tbc Tse Tmj Tmj Pk Qcf Qcf Tbct Tbc Qcf Qaf 2 Qaf 2 Qcf Qal 1 Qaf 2 Qaf 2 Toc Qal 1 Tcc Toc Qal 1 Qla Qaf 2 1 575 000 FEET (CENTRAL) SCALE 1:100,000 Contour interval 40 meters Supplementary contour interval 10 meters 2 1 1 Miles Kilometers 10 4 2 0 2 8 6 4 2 0 GEOLOGIC MAP OF THE RICHFIELD 30' x 60' QUADRANGLE, SOUTHEAST MILLARD COUNTY AND PARTS OF BEAVER, PIUTE, AND SEVIER COUNTIES, UTAH by Lehi F. Hintze 1,2 , Fitzhugh D. Davis 2 , Peter D. Rowley 3 , Charles G. Cunningham 4 , Thomas A. Steven 4 , and Grant C. Willis 2 2003 1 Brigham Young University 2 Utah Geological Survey 3 Geologic Mapping, Inc. 4 U.S. Geological Survey Plate 1 of 2 Utah Geological Survey Map 195 Utah Geological Survey a division of Utah Department of Natural Resources in cooperation with U.S. Geological Survey National Cooperative Geologic Mapping Program Statemap Agreement No. 00HQAG0109 GIS compilation: Basia Matyjasik, Angela Wadman (UGS), and Jeremiah B. Workman (USGS) Cartographer: James W. Parker Project Manager: Jon K. King 13°00' 231 MILS 2002 MAGNETIC DECLINATION AT CENTER OF SHEET Base from U.S.G.S. Richfield 30' x 60' quadrangle, 1980 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. 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. UTAH Millard Co. A B A' B' C C' D D' E E' 38°30' 112°00' 39°00' 112°00' 39°00' 113°00' 38°30' 113°00' R 10 W 3 3 0000m E 850 000 FEET (SOUTH) T 21 S 1 600 1 600 00 FEET (SOUTH) 3 4 R 9 W 1 625 1 625 45' R 8 W 1 750 3 8 R 5 W 30' 1 725 1 725 1 700 1 700 R 6 W 1 650 1 675 1 675 3 6 R 7 W R 4 W 3 9 1 775 15' 1 800 1 800 R 3 W 4 0 1 825 1 825 R 21/2 W 1 850 000 FEET (CENTRAL) R 2 W 43 1 T 21 S FEET 225 000 (CENTRAL) 825 200 800 T 22 S 43 0 175 775 T 23 S 42 9 45' 150 750 T 24 S 125 42 8 725 100 T 25 S 700 42 7 0000m N 75 675 000 FEET (SOUTH) T 26 S R 2 W 1 850 000 FEET (SOUTH) 1 825 4 0 0000m E 1 800 1 800 1 775 1 775 3 9 15' 3 8 1 750 1 725 1 725 R 5 W 3 7 30' R 6 W 1 700 1 700 3 6 1 675 R 7 W 1 650 1 650 R 8 W 45' 3 4 1 625 1 625 1 600 1 600 R 9 W R 10 W 75 000 FEET (CENTRAL) 675 700 100 42 7 T 26 S T 25 S 725 42 8 125 750 150 T 24 S 42 9 45' 775 175 T 23 S 43 0 800 200 T 22 S 225 43 1 0000m N MT. BELKNAP CALDERA B B B P P P P P P P P P P P P P P P P P ? ? ? ? B B B B B B B B B B B B B B B B B B B B B B B B B B B B B B B B P P P P P P P P P P P P P P P P P P P P P P P P P P P P P B B B B B B B B B B B B B B B B B B B B B B B B B B B B B B B B B B B

GEOLOGIC MAP OF THE RICHFIELD 30' x 60' QUADRANGLE

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Page 1: GEOLOGIC MAP OF THE RICHFIELD 30' x 60' QUADRANGLE

30

20

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Tmm

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Tbc Toi

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Tgd

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Trg

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Qlg

ToiTmj

Tmpl

Qaf2To Tmpi

TbctTbc

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Qms

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Tb

Tbci

TgdTb

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Qea TbcTrd

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Qaf2Tmpl Tmpf

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Tac Tmpu

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Tgd

Tmpl

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Qla

Tmpl

Tbc

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Trd

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TbciTmpl

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TseTbci

Qrk

Qms

QmsQms

Tbc

Tmpl

Trd

Qaf2Tmj

QmsQea

ToTw

Qcg

Tp-Cg

TmjQms

To

Tmpf

Qla

Qms

Qms

Tmpa

Qac

Qvb4

TbcTgd

Trd

Jn

Tmpl

Tbct

Qms

Tmpi

Qac

Tbct

Tmpl

TmpfJnTrdTmpi

Trd

Tzt

TrdQms

TbcTmpi

Tmpi

Qms

Tmpa

Tdm

Qgt

QTaf

Tse

Tse

Qcg

To Tmpl

Tdm

Tmj

TmpfTmpi

TrdTmj

Tqm Qcf

Tse

Tqm

Toi

Toi

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p-CgQaf2

QeaTqm

Tbci

Tgm

Tmj

Tac

QTaf

Tmpa

Qea

Tbc

Tmpi

Tmpi

Qgt

Qms

QTafTbciTacQea

Qaf1

Tbct

TdmTrd

To

QTaf

Tmpi

Qaf1

Tqm

QmsTdm

TacQal1

Qea

Tbc

Tbc

TmpbTo

Tbc

Tdm

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Tdm

Trd

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Tmpb

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Toi

Tse

Tbc

Tmpb

Tmpl

Qal2

Tmj

Qac

Qea

Tse

Toi

Tzt Tse

Toi

ToQac

To

Tmj

TmjQTaf

To

Tzt

Toi

Tsg

Qac

Tse

To

Qlg

To

QTaf To

Tmj

Tse

Trd

To

Tmj

Qms

Tqm

Tbci

Tzt TmjTmj

Tqm

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TdmTdm

Tbc

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Tse Qal1

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Tba

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Qaf1

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Qed

ToQea

QeaTse

Qac

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Tmj

Tbc

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Trd

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Tdv

Tzt

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TmjTbc

Tbc

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TwQea

Tbct

Tac

TztTo

Qaf2

Tac

Qaf1

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TztTw

Tbct

Qaf2

Tsg

Qaf2

Tb

Qms TbctQvb4

To

Tbci

Qaf1

To

Tgm-Cdh Qea

Tbc

Tmj

ToTw

Qaf2 Tbc

Qal1 ToTaa

Tzt

Tmj ToQst

Qea

Qea

Tac

Cp

-Cdh Tbct

Qms

Qcg

Tbc

Tw

Qaf2Tdv

TmjTdv

Qms

To

Tsg

Tw

Tbct

TdvQaf2

Qla

-Cdh

TdvQaf2

-Cpm -Cp

Qal1

TccQms

Qal1

QmsQac

-Cdh

Tmj

Qaf2

-Cpm

Tac

Tmj

Tdv

Tac

TbTb

Qvb4

To

TdvTac

TaaTsg

Tac

Qea

Tse

Tdv Tac

Qcf

Tbc

Tmj

Tbc

-Cpm

-Cdh

Tmpi

-Cdh

TsgTbctTbct

Tse

QstTmjTbct

-Cpm Taa

Qea

Qal2 Tbc

Tmpi

Tbct

Tsg

Qaf1

Tbct

Qaf2

Tsg

TwQsa

Tmj

Qaf2Tmj

Tdv

-Cpm

-Cdh Qcf-Cdh Tcc

Qea

Tbct

Qaf2

Tcc

Tcc

Kcg

Qgt

Qcf Tql-Cdh

Tbc

Qms-Cdh

To

QTaf

Qaf1-Cpm

Tmj

Tbct

Qal2Tdv

Tbc

Tcc

Tcc

Qms

Qea-Cp

Tql

Tau-Cdh Tbct

-Cwt?

Tsg

Tse

Qal2 TbciTbct

TaaTbcQlg

-Cp

Qcf

Tbc

-Cpm

Pq

Tse

Tsg

Qaf1

IPc

Tau Tau ToQaf1

Qgt

Tcc

Tbct-Cpm

Taa

TmjTba

Qaf2

Qms

Qal2-Cwt?

Tsg

Tcc

Tse

Qaf2Tcc

ToToTauQal1

TbcKcg

Tw

Tbc

Tmj

Qgt

Tql

TauIPc

Tdv

Tac Qst

-CpmQvb4

-Cwt?

Qaf2

TauTw

Qst

Pq

Tbc

To

Tsg

Tda

TseTw

Tse

Qaf2Mr

Ppk

Tbct-Cp

Tcc-Cwt?-Cdh

Qms(Tdv)

TbctQmsTac Tac

IPc

Qmu

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Tse

Qaf2

Qac

TdvTw

Qms

Qac

Tbct

Qaf1

Tbct

Tbct

Tse-Cpm

To

Tcc

Tba

Tsg

Tsg-Cpm

Tse

Qms

Qlg

To

Tbct

TwTw

QmsTbc

Qaf2

Ttl

Tac

Qal3

-Cpm

QTafTse

Tse

TsgQal2

Tw

Qac

Tau

Tau

TseTac

Tac Qal1ToTdvTdt

Qaf2

Tba

Qvb5

Tdv

Tbct

TacPq

Qlg

Tba

Tdv

Dc

Dg

Qaf2

Qac

TwTw

Pq

Qvb5

Pq

Ppk

Tdv

To

Tbct

Tdv

Pq

TseQmsTdv

Tba

Ppk

QTaf

Ttl

Mr

QTaf

Tdv Tda

Tdt Qgt

IPc

Tba

Tsg

Tsg

Tbct

Tau

QacPq

Ttl

To

Qlg

Ppk

Tac

Tcc

Tse

Qms

TbaSOu

Tdv

SOu

Mr

Qms

Qlg

Tdt

Ttl

Tau

QmsIPc

QTaf To

Qaf2

TbaPpk

Tac

Toc

Ttl

Tcc

Qla

Dc

Ttl ToPk

TccQms

Dg QTafQac

Tau

Qal3

Qal1

Pq

Qla/Qvb5

SOuPpk

TRm

Qaf2

TseTba

Tsg

Dsy

Tba

Qaf1Qaf2

Ppk

Pq

Tdv Qms

Pq

Tsg

Tba

Qms

Tac

TdvTbct

QmsTbct

Ttl

Tsg

Qac

QTaf

Qaf2IPc PqTo

Tda

Ppk

SOu

Pq

SOu

Tba

Tcc Tau

Tcc

Oe

Toc

Tbct Tba TbctTac

Toc

Qms

PkDc

Tba TseTseTtl

Tse

TacQaf1

Tql

Ttl

Tcc

IPc

Qaf2

Tse

Ttl

Qmu

Tba

Tf

TsePq

To

TbctPk

Qaf1

Qaf2

Pk

To

Tac

TbctMr

Tac

To

Ttl Tw

Ds

Ttl TRcs

Qaf2

Qms

Tbct

Toc

To

TbctTtl

Qms

Qaf2

ToTtlTac

To

TocTcc

OeTo

Qac

Tbct

Tba

Qlg

Mr

Ttl

TRcuPk

Qaf2Dg

TacTRm Tse

Pk

Qed

TccPk

Pq

Tba

Pk

Qmu

DcDg

Tac

Tsg

Tac

Dsy

PkQms(Tbct)

QacQms(Ttl)

QacTcc

ToTac

OeTtl

Tbct

Qac

Tsg

OpTac

Toc

TbaTbct

SOu

PqTcc

Tcc

Qms

Tac

Tbct

Ttl

Tbct

Tse

Qms (Tbct)

SOu

Mr

TacTo

TbctPq

Tac

Dsy Qms

Qaf1

Tbct

Qaf2

Tac

ToPk

Qms

Ttl

Tsg

Tf

Tau

Qla/Qvb5

Tau

Qac

Qaf1

Tba

Op

Qac

Dc

Qac

Qed

Tf

TRm

Tf

TRcs

QmsTo

DgTcc

Tac

TRcuDsy

Qal2

Op

Tcc

Dc

TbctQla

TtlMr

Qac

Qac

Oe

TacTRm

Qms(Tdv)

TtlTbct Tac

Dg Tac

Tse

TRm

Tb

Qac

TwTdt TwQms

SOu

TwTbm

Qms(Tdv)

Tbct

Tau

Pk

Tba

TRcuDg

Tba

Tdt

Qac

Tf

Tbct

DsyTcc

Qal1

TRcs Tdt

Ttl

Oe

Qac

Jn

Tac

TseQmsPq

Dsy

Tsg

QmsOp Tac

Tbct

Tcc

TauTau

Qal2/Qvb5

Tac

Tbct

Ppk

TRcsTtl

Tcc

Tdt

Qms

DsTba

Qms

IPc

Tf

Tac

Tbct

TauOe TacTdv

SOu

Qaf2

Tcc

Tbct

Dsy

Qms(Tdv)

Qms(Tdv)OeTtl

Tau

Qac

TbctTdt

Qvb5

Dsy

TbctTf

Tac

Ttl

TRm

TRmQms

Toc

Ttl

Ttl

Qac-CaTsg

Tbct

Qac

Qed

Qal1

Qac

Tac

TauTdt Tau

Pk

Qms

Tcc

Qms

Tcr

Tac

Qac

SOu

Qmu

Tse

TtlTac

TRm Qms (Tbct)

OpTRm

Toc

Qac

Mr

Qac

Qms (Tac)

TtlQaf1

QacTdvt

Tac

Qms

Pk

To

Tau

Qac

TacQac

Tac

Op

Tsg

Tcc

Tac

Pk

Qac

Ttl TacPq

Op Tse

Tcr

Ttl QacIPcDs

TauPpk QacDcQac

Tbct

Toc

Ttl

Toc

Qac Tdt

Dg

Tcp

Qmu Tf

Qac

IPc

Qac

Qlg

Tsg

Qms

Tac

Qms

Qms

Tac

Tcc

Tsg

Qac

Dsy

Tau

SOu

SOu

Qac

Tac

Tcc

Qmu

Tau

Qac

Tdv

Dc

Tau

Qac

Tbct

Qaf2/Qvb5

Tf

Qac

Tau

Toc Dc

Tau

Tdvt

Ttl

Tau

TdaTau

Ds TRcs

Tcc

Dsy

Ttl

DcTau

Qms (TRcu)

Tcr

Tf

Tf

TRcu

OeTf

Dg

Toc Qac

Tcc

Op

Tau

Toc

Qmu

TtlTo

IPc

Tfmw

Qmu

Tau

Dc

Tdv

TbctTdv

TRmTfur

Qlf

TacQms

DcTRcs

Tcc

Qal2

Ttl

Qac

Tac

Tf

TRm

Qaf2

Qms (Tcc,Ttl)

Dc QacDs

Toc

Qac

Qmu

Ttl

Tac

TRm

Tcc

Qaf2

Ttl

Tbct

Tcr Tau

Qaf1

PkQal1

Qlf

TRcs

Qmu

Tf

Dg

TRm

Qac

Toc

TacQms (TR)

TRcu

Tau

TRcs

Tsg

DsyTocTcc Tf

Toc

Tcc

TbctTf

Tac

Tac TdaOp

Qac Qaf1

TRm

TccToc

TRcu

Tfuw

Tac

Toc

QmuQac

TRcsToc

Tbct

Tda

Tov

OeDsy

Qal2

SOu DgTccDg

Qmu

Qms

Ds

Dc

Qms(Jn)

Tcp

Qac

Pk

Qms(Tcc,Ttl)

Toc

JnTau

Pq

TsgDc

Qms

Qaf1

Tcc

Qlf

Qac

Jn

TfuwTac

Qaf2

-CumDc

Qac

Ttl

Tcc

Tac

Ttl

DgTac

Qms

SOu

Ttl

Qms

SOu

-Ct

Qmt

Jn

Tcp

Tfur QacTbctTau

Mr

Op

Ttl

Qaf2Jn

Tf-CopMr

TRcs Tbct

Ds

Ppk

Qms

Tcc

TauTac

TbctOeTtl

Tcc

Tflw

Qac

Tcc

SOu

Qms(Tcc,Ttl)

Tfmw

Tau

Qac

Oe

IPc

Tac

Tbct

QTlf

QTlf

Qac

Tau

-CaMr

Qal1

Tcc

QmsJn

-CtQaf1

SOu

Tov

Tcc

Tbct

Tau

Tcc Op

TcpTfur

Tg

Jn

TfTtl

QlgTcr

Qms(Tac,Tbct)

Tsg

TRm

Ttl

Dg

Tbm

SOu

-Cox

Tbct

TccTocToc

-Cum

Oe

Pq

Qac

Op

TocDs

Tbct

Tcr

Tac

Qlg

-Ct

Qaf2

Tfur Tfur

Ttl

Qaf1

Tfuw

Ppk

Pk

TRm

Qla

SOu-Cum

Tfur

Tcc

-Ca

Ttl

Qac

Mr

TfurTRcs

Qls

Tdvt

Toc

Qms(Tac,Tbct)

Mr

Qla

Toc

Tfur

Tau

Toc

Tac

TRcs

Tflw

Tfmw

Toc

Qaf1

-Cox

Pk

Pq

Ppk

-Ct

Jn

SOu

Mr

Dc

-Cop

Tch

Tfuw

Tg

Qaf2

Tfur

Dsy Qms (Tac,Tbct)

Toc-Ct

Tch

JnToc -Ct

Trt

Pk

TRm

Qmu

Ttl

Ccm

Tch

Qlg

Pq

TRm

Qlg

-Ct

TcrTtl

Pk

Qms (Tcc,Ttl)

Mr

QTlfOp

Qlg -Ct

Jn

TgTcr-Cwt

TtlTtl

-Cum

Pq

Qaf2

Qms

Tfmw

QTlf

Qlg

Ttl Oe

Kc Qac

Ttl Tfuw

Tfur

QmuOe

SOu

MrKc

Tcp

SOu

Tau

Oe

Tcr

Tflr

Qac

Op

QacQls

Qst

Tfur QmsQac

Qaf1

Qms

TfurQlg

Ttl

TocTcc

Tcr

-Cum

Qaf2 -Cop

TchQaf2Qlg

Tau Tau

Toc

Tau

Qmt

-Ct

Tg

Qal1

Qlg

Qaf2

Toc

Tau

-CumTfur

QTlf

TchTdvt

Qaf1

-Cum

Qal1

Ttl

-Ct

Tfur

Qlg

Ttl

Qls

Qmt

To

-Ct

Tch-Ct

Qlf

Tac

QTlf

Tfmw

TfmrQlg

Tau

Qlg Qmu

Qlg

Tau

-Cop

Qlg-Ct

Qaf2Qla Tau

Tbr

-Cum

Qla

Qlg

Jn

Trt

Qaf2

-Cum

Qms (Tg)

Qms (Tch)Qlm

TfuwTtl

QmtTfurToc

-Ct

Qlg

Qms

Qlg

Tfur

Tg

Qls

Qmu

Toc

Tg

Tch

Tf

Toc

-Cop

-Cop

-Ct

Qlf

Qlg

QTlf

Qmt

Qlf/Qvb5

TgQms (Tg)

Tch

-Ct

Qac

Qla-Cop

-Cum

Qlf

Qms

Qlg

Qlg

Qlg-Cum Qms

(Tch)Qlg

QTlf

QlgQla

-Ct

Tg

Tg-Ct

Tfuw

Qms (Tg)Tg

Qvb4 Qms

QlfQaf1

Qla

Qed

Tfmr

Qaf2Qla

Tf

Qms (Tg)

Qla

TgQlg

QlaQls

Qlg Qlg

Tfur

Qlf

Tcr

Tch

Tfuw

Qaf2

Qlg

Tf

Tfur

Qlf

Qms (Tch)QmtQlg Tfur

Ttl

-Cw

Qms (Tch)Tch

Qac

Qla

Qmu

Tfmw

Tg

Qaf2

TgQacQlg

Qaf1

Jn

Qlg

Tf

Tfuw

QlsQlgTcr

Qla Qlg

Tch

Pq

Ttl

QacTfmw

Qlg

QTlf

Toc

Toc

Qlm

Qll

Tcc

QmuTfuw

Tfmw

TfmwQaf1

Qvb4Qmu

QlaQmsPk

Tfur

Pk

Tf

Tfuw Qms

Qmu

Tfur

Ttl

QTlfTcr Qla

Mr

Tfmr

-Cw

Tfmr

Tbr

PkQlg

TfmwQlg

Tcr

QlgToc

Tbr

Qac

QTaf

TfQlg Tcr

Ttl

Pk

QTlf

Qmt Qac

Mr

Qlg

Qal2

Qaf1

Trt

Qms

Qls

Tfmr

QTlf

Mr

Qaf1

TRm

Qla

Tbr

QmtQaf2Pk

Mr

Tfmw

Tbr

Qlg

Qaf2

Tfmw-Cp

Qal2Qls

TRmTfmw

Mr

Tcr

Qvb4

Trt

Qal1

Tfmr

Qlg Qlm

Tbr Qaf1

TfmrTcr

Tcr

Qms(Tg)

Ttl

TfurKtm

JnTcr

Qaf2

Tbr

Qlg

Qvb4

Pk

TfuwQvb4

QlmTbr

TRm Pk

Qls

Tcr

Tlr

Tcr Qvb4

Qls

-CcmQla/Toc

-Cp

TRcu

Qlm

Qaf2

TRcs

QTlf

Pk QmsTcr

Tg Tfur

Tfuw

TfurTbr QTlf

Qmt

Tcr

QlgQaf2 Ttl

Tfmw

Qac

Pk

Tfmw

TbrQlg

Qmt

Ttl

Jn

Qms

Qac

Qaf1

QlsTtl

Tg

Qac

Qlg

QacQaf1

Tfur

Qaf2Jn

-Cp

Tcr

Qac

Tfuw

Tcr

Qlg

Tg

Qlg

Qaf2

Qla

Qvb4

QlgQls

Qal2

Tch

Toc

Qla Qlg

QTlf QlgTbr

Tbr

Pk

Tfur

Tfur

Qaf2

Qvb4

Qaf1

QlsQms

TRm

-Cdh

QTlf

Qmt

Qla

Qal1

-Cwt

Tg

Toc?

Tg

Tfuw

Tbr

Tfmr

Qla

Tfur

TRcu

TRcs

Qmt

TbrTcr

Tcr

Qaf2

Tbr

Qac

Tfmr

Tfur

Qac

Tcr

Tfur

Qlg

Tfmw

Qla

Tfmw

QTlf

Qla

-Cw

Qlf

Qaf2

Tfmr

Tbr

TRcs

Qaf2

Tfmw

TRm

-Cw

TgPk

QmtTfmr

QlgTbr

Qlf/Qvb4

Qlg Qmt

Qlg

Tfmr

Qmt

Tbr

Toc?Qac

Tbr

Qla

Tfur

Cwt

Qlg

Qlg

Qaf1

Qaf1

Qmt

Tflw

-Cw

Tbr

TfmwQac

Tbr

Qaf2

-Ccm

Qaf1

Qal2

Qla

TfmrTg

Tac

-CwtQdg

Tbr

QacTfmr

Qla

Tbr

-Cwt

TRm

-Cwt

Pk

Qlg

Tfuw

Tbr

Qac

Qaf2

-Cwt

-Cwt

-Cp

Qmt

-Cw

Qaf2

Tg

-Cob

Tfmr

O-Cn

Qls

TacQacTch

Tbr

-CouTRm

Tfuw

Tfmr

Tbr

Qac

TgPk

Qaf1

Qmt

Qed

Tac

-CobTfmr-Cwt

Tfur

Ktm

Qac

-Cwt

Qmt

Qst-Cob

Qmu

Qac

Tg

Tbr

Qlf

TgTg

Tfuw

Tac

Qms

Ktm

TdvtTfuw

-Cwt

Tfmw

TfurQac

Tau

Tfur

Qla

Tg

Qaf2

Qvb4Tf

Tf-Ccm

TRm

Tg

Qdf

Pk

Tf

Tfmw

Toc

Tch

Qmt-Cwt

Tac

Qlf

Tf

Tfmr

Tf

Qmt

Qla

Qaf1

Qaf2

Tfmr

Tfmw

-Cob

-Cwt

QgtQmu

-Cp

Qdg

TflrQvb4

Qmt

Qac

-Cwt

Qla

-Cob

QTlf

-Cob

Qms(Jn,TRcu)

Qst-Ccm

-Cw

Qaf1 Qaf1-Cob

Tflw

-Cob

Tf-Ccm

Tg

-Cp

Qed

Qac

Qaf2

Tf -Cwt

QlgQed

QlgTfTflr

TchTflr

Qlg

Qlf/Qva5

-Cwt Qlf-Cwt

Qms(TRcu)

Qaf2

Jn

QmtQmt

Tg

Qla

-Cop-Cp Qlg

-Cwt

TRcu TfmwQla

-Cwt-Ccm -Cwt

Tfmr

Tfmw

Qed

Tf

Qgt

QdfTflw

Qaf2

Qdg Qlf

TfmrTRm

QgtTKn

Qgt

TRcu

Jn

Qmt

JnQlg

Qlg-Cwt

Tflw

Tf

TRmTRm

Tf

Pk

Tfmw Tch

Qlm

Ppk

Qms(Tg)

Qed

Qaf2-Ccm

IPc

Qed TflwMr

TRcu

TKn

Tfmr

Qed/Qlf/Qva5Qla

Tflw

Qlf

Tf

Qed

Tg

Tfmr

Qlf

TfmrKc

TfmwQlg IPc

Qla

TRmMr

Qdf

Tflw

TRcs

Qms TfmrTRcs

Tflw

Qac

TRcs

-Cdh

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(Jn, TRcu)

Ppk

Qac

Qlf

IPc

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TKn

Qaf2

Jn

Ppk

Jn

Qlf/Qvb4

Qla

Pk

TRcu

Tfmr

TRcu

Kc

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Qaf1Qed

Tg

Tf

QdfQaf1

TflrTRcuTfmr

Qac Tch

Qlf

Tfmw

Qlf

Tfmw Tfmr

QTaf

Tfmr

TRcs

Tf

QlfTflw Tg

TflwQed

Qed

Qla

Tf

Qlf

Pk

QacQTaf

Qac

Pk

Tflw

TKnQmu

QTlfTf

TRm

Tf

TgQacQTaf

Tfmr

Qdf

Tfmr

TRcuTRcs

Qpm

DcKtm

Qlf/Qva5

TflwKc

Qaf1

Tg

TfmrTfmr

QTlf

Qaf2

Tg

Tf

-Cop-Ct

Qlf

QacTKn TgQaf2

TfmrTflr

Jn

TKn QTaf

Qlg

TKnQvr4

Qlf

Qac

Toc

TKnTf

QTlf QedQlf

Tch

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TchTbr

Qed/Qlg

Tflr

Qed/Qlf/Qva5

Qlg

Tf

Qac

Qlf

QTafTflr

Tf

QlgTfmr

Tch

Tf

TfQdg

Tf

TgQTaf

Tg

Qlf

TflwQac

Tflr

Qlf/Qvb4

Qdg

QacTfmr

Qdf

Qaf2

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Tflr

QmsTg

Tf

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Tfmr

KcQlf

Tg

Qlf

Tflw

Qac

Tg

Qac

Qvb2

Tbr

TfmrTRcu

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TflwTbr

TbrQac

TKn

Qed

Qdf

Ktm

Qac

Qac

-Cpm

Qac

Jn

Qac

Qac

TgToc

Toc

Ktm

Tf

Toc

Qed

TKn

Qll

Qpm

Qlg

Qac

Tg

Qls

TKn

Qaf2

Qdg

Qac

Qac

Toc

Tflr

Qlf

Tg

Qaf2

TRm

Tflr

Qed/Qlg

Qed/Qdg

Qlg

TRcs

Qla

TRcu

Qal1

Qdg

Qac

Qla

Qdf Qal1

Qac TKn

Qed/Qll

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Toc

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Qlg

Qed/Qlf/Qvb4

Tg

Toc

Qed/Qdg

Qac

Tflw QTaf

TflrQla

Qlg

Qac

TgQdf

Qed

Tht

Qll

Qac

TRcu

QacTg

TRcs

-Ct

Jn

Toc

QTlf

QTaf

Tg

Qlf/Qvb2Qlg Qpm

Qac

Qal1

TgTg

TflrQac

QTlfTflr

-Cdh

Tflw

TRm

Tflr

Kc

Qlg

Tflw

QTafToc

TocQed/Qvb1

Tflr

QTaf

Qlg

-Cop

Qgt

Qed/Qlg

Qlg

QTaf

Qed

Qal1

-Cdh

Qaf2

Qmu

QTaf Qaf2

Tflr

Qac

-Cw

Qac

Qac

Toc -Cop Qgt

Tf

TocQTaf

QTlf

Tse

Tf

Qac

-Ccm

Tg-Cdh

Qac

Qac

Qed

Qaf2

Tf

-Cop

Qdg

Qac

Tf

Qlg

QlsTf

Qla

Toc

QacKc

TgQac

TgTfQTaf

Jn

Qal1QTaf

Qgt

TKn

QTlf

QTlf

Qgt

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Qgt

TKn

Tht

-Cum

Toc

TocToc

Qaf2Toc

TfQla

QTlf

Qlg

Qlg/TocQlgQlf

Qlf

Qdg

Qvb1

Qed/Qvb3Qed/Qlf

Qdg

-Cp

Qdg

-Cpm

QlfQaf1

Qdg-Cpm

Qla

Qla

Qla

TfQaf1

Qaf2

Qlg

Qla -Cp

-Cpm

-Cp

-Cdh

-Cpm

Qaf2

-Cpm

-Cp-Cdh

-Cdh

-Cp -Cpm

-Cpm

-Cp

-Cp

-Cdh

-Cdh

-Cdh

-Cdh

-Cdh-Cp

-Cp-Cpm

-Cdh

Qaf2

Qaf1

Qvb1

Qed/Qvb1

Qlf

Qal1Qaf2

-Cum

-Cum

Qaf2

Qaf2

-Cum

-Cum

-Ct

Kc

-Cop

TKn

Tflr

Qaf2

Qaf2

Qaf2

Qaf2

Qaf2

Qac

-Cum

-Ct

Qaf2

Qlf

Qed/Qlf/

Qvb4

Qed/Qlf

Qed/Qlf

Qed/Qlf

Qed/Qlf/Qvb4

Qal1

Qaf2

-Ccm-Cdh

-Ccm -Ccm-Ccm

-Ccm

-Cdh

-Cdh

Qaf2

-Cpm

-Cdh

-Cw

-Ccm

-Cp

-Cp

-Cw

-Ccm-Cdh

-Cdh

-Cp

-Cdh

-Cpm

Qaf1-Cpm

Qaf2

-Cpm

-Cdh

-Cp

-Cpm

-Cdh

-Cdh

-Cp

-Cdh

-Cdh

-Cp

-Cp-Cdh

-Cdh

-Cdh

-Cw

-Ccm-Ccm

-Cw

-Cdh-Ccm

-Cw

-Ccm

-Ccm

-Ccm-Cwt

-Cwt

-Cwt

-Cwt

-Cwt -Cwt

-Cwt

Qaf1-Ct

-Cum

-Cop-Cum

-Cum

-Ct

-Ct TRcu

-Ct

-Ct

-Ct -Ct

-Cop

-Cum

-Cum

-Cum

TKn

Tflw

Tflw

Qaf2

Qaf2

Qaf2

Tfmr

Qaf2

Qaf2

Qac-Cum

Qac

-Cum

-Cop

-Cum

Jn

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TRm

-Cop

Qlf

Qlf/Qvb4-Cwt

Qaf2

Qaf2

Qaf2

-Cob

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-Cob

-Cwt-Cwt

-Cwt

-Cwt

-Cob

-Cwt

-Ccm

-Ccm-Cdh

-Ccm

-Cw

-Ccm

-Cdh

-Cdh

-Cdh-Ccm

-Cw

-Cw -Cw

TRcs

Tbr

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-Cdh

-Cwt

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-Cob

-Cob

Qlf

Qlf/Qvb4

Qlf/Qvb4

Qlf

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Qal1

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TflrTflr

Tflr

Tflw

TfmwQaf2

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Tbr

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Jn

Qlf

Qlf

Qal1

Qal1

Qal1

Qal1

Qal1

Qaf1

Qla

Qla

TRm

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-Cum

Tflr

Tfmr

Tfmr

Tfmr

Tfmr

Qaf1

Qaf1

Qal1

Qaf1

-Cop

-Cop

-Cum

Tdv

Tdv

Mr

Qaf1

-Ct

-Ct

Qaf2

QlaQal1

Qal1

Qaf2

Qal2Toc

IPc

Tfuw

Qms (Tch)

Tac

Jn

IPc

Tcc

Qlf

Qaf2

Qal1 Toc

Qaf1

Tf

Tdv

Qal1

Qaf1

Qaf1

Tdv

Tdv

Tdv

Pk

Qms(Tcc,Ttl)

Qal1

Qlg

Qlf

Qlf

Qla

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Qaf2

Tbm

Tcc

Qaf2

Tac

Tac

Tbct

Tbct

Qcf

Qaf2

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Qaf2 Qaf2

Taa

Tbc

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Qaf1

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Qaf2

Qaf2Qaf2Qaf2

Qaf2

Qaf2

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Qaf1

Qaf1

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Qcf

Tbci

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Tse

Tmj

Qaf1

Toi

Toi

Qaf2

Qaf2

Qaf2

Qaf2

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Qls

Qac

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Qaf2/Qvb5

Qaf2

Qaf2

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Qaf2

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Qaf2

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Tmb

Qla

Qlf

Qlf

Qlf

Qaf2

Tcr

Tcc

Tsg

Qaf2

Tse

Trd Trd

Qal1

Tse

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TRm

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-Cwt

Tbct

Tse

-Cp

Qed/Qvb2

Dg

Tbci

Tsg

Jn

Jn

-Cum

Qaf2

-Ccm

TRcs

Qaf2

Qal1

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Jn

Qaf1

Tmpf

Tse

Tbc

Tbc

Tbc

Tse

Tmj

Tmj

Pk

Qcf Qcf

Tbct

Tbc

Qcf

Qaf2

Qaf2

Qcf

Qal1

Qaf2Qaf2

Toc

Qal1

Tcc

Toc

Qal1

Qla

Qaf2

1 575 000 FEET (CENTRAL)

SCALE 1:100,000Contour interval 40 meters

Supplementary contour interval 10 meters

2 1

1 Miles

Kilometers10

4202

86420

GEOLOGIC MAP OF THE RICHFIELD 30' x 60' QUADRANGLE,SOUTHEAST MILLARD COUNTY AND PARTS OF BEAVER, PIUTE, AND SEVIER COUNTIES, UTAH

byLehi F. Hintze1,2, Fitzhugh D. Davis2, Peter D. Rowley3, Charles G. Cunningham4, Thomas A. Steven4, and Grant C. Willis2

2003

1Brigham Young University 2Utah Geological Survey 3Geologic Mapping, Inc. 4U.S. Geological Survey

Plate 1 of 2Utah Geological Survey Map 195

Utah Geological Surveya division of

Utah Department of Natural Resourcesin cooperation with U.S. Geological Survey

National Cooperative Geologic Mapping ProgramStatemap Agreement No. 00HQAG0109

GIS compilation: Basia Matyjasik, Angela Wadman (UGS),and Jeremiah B. Workman (USGS)

Cartographer: James W. ParkerProject Manager: Jon K. King

13°00'231 MILS

2002 MAGNETIC DECLINATIONAT CENTER OF SHEET

Base from U.S.G.S. Richfield 30' x 60' quadrangle, 1980

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. 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.

UTAHMillard

Co.

A

BA'

B'

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D

D'

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38°30'112°00'

39°00'112°00'

39°00'113°00'

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850 000FEET

(SOUTH)

T 21 S

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Page 2: GEOLOGIC MAP OF THE RICHFIELD 30' x 60' QUADRANGLE

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M I N E R A LM O U N T A I N S

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Surficial Geology1. Oviatt, C.G., 1991, Quaternary geology of the Black Rock Desert, Millard

County, Utah: Utah Geological and Mineral Survey Special Study 73, 23p., scale 1:100,000; locally modified by L.F. Hintze and F.D. Davis, 1991and 1992, unpublished mapping for this publication, scale 1:24,000.

2. Davis, F.D., and Hintze, L.F., 1991, 1992, and 1999, unpublished mappingfor this publication, scales ~1:50,000 and 1:24,000.

Bedrock Geology3. Coleman, D.S., Bartley, J.M., Walker, J.D., Price, D.E., and Friedrich, A.M.,

1997, Extensional faulting, footwall deformation and plutonism in theMineral Mountains, southern Sevier Desert: Brigham Young UniversityGeology Studies, v. 42, part 2, p. 203-233, scale 1:21,300; Walker, J.D.,and Bartley, J.M., 1992, unpublished map, scale 1:12,000; and Sibbett, B.S.,and Nielson, D.L., 1980, Geology of the central Mineral Mountains, BeaverCounty, Utah: Earth Science Laboratory, University of Utah ResearchInstitute Report ESL-33 (DOE/ET/28392-40), 42 p., scale 1:24,000.

4. Crosby, G.W., 1959, Geology of the south Pavant Range, Millard and SevierCounties, Utah: Brigham Young University Geology Studies, v. 6, no. 3,59 p., scale 1:65,000; modified by L.F. Hintze, 1992, unpublished mappingfor this publication, scale 1:24,000.

5. Davis, R.L., 1983, Geology of the Dog Valley-Red Ridge area, southernPavant Mountains, Millard County, Utah: Brigham Young University GeologyStudies, v. 30, part 1, p. 19-36, scale 1:24,000; modified locally by L.F.Hintze, 1992, for this publication, scale ~1:50,000. Mapping of volcanicrocks by L.F. Hintze, 1992 for this publication, scale 1:24,000, withclarification from G.C. Willis, 2001-02, sketch maps; modified from Steven,T.A., and Morris, H.T., 1983, Geologic map of the Cove Fort [15'] quadrangle,west-central Utah: U.S. Geological Survey Miscellaneous InvestigationsSeries Map I-1481, scale 1:50,000.

6. George, S.E., 1985, Geology of the Fillmore and Kanosh quadrangles,Millard County, Utah: Brigham Young University Geology Studies, v. 32,part 1, p. 39-62, scale 1:24,000; modified locally by L.F. Hintze for thispublication.

younger alluvium; thickness probably 10 feet (3 m) or less.Lacustrine lagoon deposits--Sand, silt, clay, and silty marl thataccumulated in lagoons behind (landward from) gravel barrierbeaches of Lake Bonneville; present south of Borden and east ofTwin Peaks; locally includes younger alluvium; generally less than10 feet (3 m) thick.

Lacustrine marl--Fine-grained, thinly bedded to laminated, white tolight-gray, offshore to deep-water marl deposited in Lake Bonneville;ostracodes are abundant throughout marl and, locally, gastropodsare present at top and base of marl; 0 to 30 feet (0-9 m) thick. Alayer of basaltic ash of Pahvant Butte is interbedded in the upperpart of Qlm and is commonly 1 to 6 inches (2.5-15 cm) thick. Thisgray to black basaltic ash was blown into the atmosphere during ahydrovolcanic eruption when Lake Bonneville was near its highestlevel about 15,500 yr B.P.

Lacustrine and alluvial deposits, undifferentiated--Mixed and reworkedgravelly lacustrine and alluvial deposits on piedmont slopes; gradesfrom pebbly sand and silt to sandy pebble gravel; generally 0 to 12feet (0-4 m) thick, but may be thicker locally.

Basalt of Ice Springs--Contains 2 % phenocrysts and has a greaterglass content than other lavas in the Black Rock Desert; estimatedto be between 4,000 and 660 years old; may be as much as 200 feet(60 m) thick.

Basalt of Tabernacle Hill--Fine-grained holocrystalline basalt witholivine and plagioclase in a groundmass made opaque byclinopyroxene aggregates formed by quenching of the lava duringits eruption into Lake Bonneville; radiocarbon age 14,320 ± 90 yrB.P.; maximum thickness about 200 feet (60 m).

Basalt of Pahvant Butte--Basalt flows of probable late and/or middlePleistocene age; K-Ar dated as 0.031 to 0.22 Ma; 0 to about 100feet (0-30 m) thick.

Basaltic andesite of Cedar Grove--Dark-gray to black, porphyriticbasaltic andesite with phenocrysts of plagioclase, clinopyroxene,hypersthene, magnetite, and olivine in a felted matrix; maximumthickness about 200 feet (60 m); age about 0.3 Ma.

Rhyolite dome of White Mountain--Black obsidian and devitrifiedfelsite with spherulites and lithophysae; about 120 feet (40 m) high;age about 0.4 Ma.

Basaltic andesite of Cove Fort--Dark-gray to black, vesicular to densebasaltic andesite containing small phenocrysts of plagioclase,pyroxene, magnetite, olivine, and sparse corroded quartz in a feltedto glassy matrix; age about 0.5 Ma; maximum thickness about 800feet (250 m).

Rhyolite of Mineral Mountains, dome--Tan perlitic glassy dome,commonly pumiceous and brecciated and containing scattered blackobsidian fragments; northernmost of several similar domes in theMineral Mountains; age 0.54 Ma.

Rhyolite of Mineral Mountains, tuff--White to tan, poorly consolidatedtuff vented from nearby rhyolite dome in Mineral Mountains; lessthan 100 feet (30 m) thick; probably same age as nearby rhyolitedome (Qvrd).

Basalt of Kanosh--Red-weathering, vesicular basalt with largeplagioclase phenocrysts and small phenocrysts of olivine andclinopyroxene in a microcrystalline matrix; age 0.67 Ma; locallystands as much as 300 feet (90 m) above the desert floor west ofKanosh.

Basalt of Beaver Ridge--Consists of older flow series, dated at 0.9Ma, of diabasic basalts about 80 feet (24 m) thick, and youngerseries, dated at 0.5 Ma, of similar composition but fine-grained toglassy, and about 120 feet (37 m) thick.

Basalt of Mineral Mountains--Dark-gray, vesicular basalt that formstwo spatter cones and flow remnants on northeast end of the MineralMountains; dated at 0.9 Ma; cone is about 200 feet (60 m) high.

Basaltic andesite of Red Knoll--Dark-gray to black, dense to vesicular,porphyritic basaltic andesite to latite lava flow with a blockyscoriaceous surface; contains 30 to 45 % phenocrysts, mostlylabradorite and pyroxene, in glassy to finely crystalline matrix;located southwest of Cove Fort and overlies basaltic andesite ofCrater Knoll; vent lies a mile (1.6 km) south of map area; maximumthickness less than 200 feet (60 m).

Basaltic andesite of Crater Knoll--Dark-gray to black, porphyriticbasaltic andesite lava flows similar to Qrk; 40 to 45 % phenocrysts,mostly labradorite and pyroxene; glassy to finely crystalline matrix,containing microlites of plagioclase, pyroxene, olivine(?), andopaque minerals; vent is 2 miles (3 km) south of map area southwestof Cove Fort; age 1.0 Ma; thickness in map area less than 100 feet(30 m).

Basalt of Black Rock--Dark-gray, vesicular basalt composed of about40% small zoned plagioclase phenocrysts, with lesser phenocrystsof clinopyroxene, olivine, and Fe-Ti oxides; age about 1.0-1.3 Ma;maximum thickness about 200 feet (60 m).

Andesite of Beaver Ridge--Dark-gray, crystal-poor andesitecharacterized by small microlites of resorbed quartz, plagioclase,and pyroxene crystals; age about 1.5 Ma; thickness about 200 feet(60 m).

Fine-grained lacustrine deposits of Sevier Desert--Brown and light-olive-gray, calcareous, lacustrine silt and silty clay with minor sand;offshore to deep-water sediments; Pliocene to middle Pleistocenein age; 0 to 872 or more feet (0-255+ m) thick; contains sinkholes.

Quaternary-Tertiary alluvial-fan deposits--Poorly sorted silt, sand,and gravel, including boulders, in Dog Valley, upper Cove Creek,and in northeast corner of map area; locally has a calcic soil witha stage IV carbonate morphology (so early Pleistocene age) nearthe top of the deposit; 0 to 300 feet (0-90 m), or more, thick.

Tertiary volcanic and sedimentary units, undivided--On cross sectionsonly; for included units see correlation chart and descriptions.

Basaltic andesite of Burnt Mountain--Black to medium-gray, fine-to medium-grained, porphyritic, crystal-rich basaltic andesite withphenocrysts of labradorite, olivine, orthopyroxene, and clinopyroxene;map unit includes vent cone; age about 2.1 Ma; maximum thicknessabout 500 feet (150 m).

Rhyolite of North Twin Peak, South Twin Peak, and Mid-Dome--Light-brownish-gray rocks from these three rhyolite domes are ofsimilar, but not identical, composition; phenocryst content from 3to 30 % and includes plagioclase, quartz, sanidine, and biotite;groundmass is microcrystalline quartz, feldspar, Fe-Ti oxides, apatite,sphene, and zircon; age 2.35 to 2.5 Ma; thickness (exposed height)up to 1,000 feet (300 m).

Basalt of Cove Creek--Dark-gray, olivine-tholeiite flow rock; mapunit includes cone; age about 2.55 Ma; maximum thickness about400 feet (120 m).

Limestone of Twin Peaks--Light-gray to yellowish-gray lacustrinelimestone and marlstone with thin interbeds of silt, sand, and pebbleconglomerate; locally prone to slumping; maximum thickness 262feet (80 m).

Basalt of Lava Ridge--Dark-gray olivine-normative basaltic andesite;age about 2.2 to 2.5 Ma; maximum thickness about 200 feet (60m).

Rhyolite of Cudahy Mine--Interbedded black obsidian and light-grayfelsite; felsite is devitrified and shows relict flow-layering, spherulites,and lithophysae; obsidian commonly shows "snowflake" clusters;age about 2.2 to 2.6 Ma; maximum thickness about 500 feet (150m).

Rhyodacite of Coyote Hills--Light-gray to medium-brownish-graywith less than 15 % phenocrysts of zoned plagioclase and sanidinein a microcrystalline matrix of plagioclase, quartz, sanidine, Fe-Tioxides, and zircon; age about 2.7 Ma; maximum thickness about650 feet (200 m).

Oak City Formation--Sandy, bouldery gravel; poorly to well cemented;forms dissected alluvial apron on west side of Pahvant Range; bedof Cudahy Mine pumice, K-Ar dated as 2.6 Ma, is within upperOak City Formation in map area, so upper Pliocene and Miocene(?)age; base of formation not exposed; estimated thickness as muchas 2,000 feet (600 m).

Sevier River Formation--In northeast corner of map area in SevierCounty, light-gray, yellowish- or greenish-gray, poorly to moderatelysorted mudstone, sandstone, conglomerate, and carbonaceousmudstone that is probably more than 600 feet (180 m) thick. Southof Richfield in Sevier County, mostly moderately indurated, palebrownish- or reddish-gray sandstone, pebble to boulder conglomerate,mudstone, and siltstone of fluvial and, locally, lacustrine origin;volcanic clasts are common in south, decreasing northward; localinterbedded tuffs and intertongued basalts yield K-Ar ages of 5.6to 13.6 Ma; exposed thickness at least 330 feet (100 m), but totalthickness may be up to 1,000 feet (300 m).

Basalt flows in northern Tushar Mountains--Dark-gray, black, andred, locally vesicular and amygdaloidal olivine basalt and basalticandesite lava flows, flow breccia, and cinder cones, scoria, and ash;not isotopically dated within map area, but similar basalts K-Ardated as at least 10.9 to 12.9 Ma, and other basalts are as young as7.4 Ma; maximum thickness about 425 feet (130 m).

Rhyolite of Gillies Hill--Lava flows and domes of light-gray to white,flow-layered, dense to vesicular rhyolite; aphyric to porphyritic,with phenocrysts of plagioclase and biotite; located south-southwestof Cove Fort; age about 9 Ma; more than 1,000 feet (300 m) high.

Tuff of Holden--White tuff interbedded with pink to white, shalysiltstone, clay, grit, and gravel exposed east of Fillmore; age probably10.5 to 10.8 Ma; may be as much as 200 feet (60 m) thick.

Rhyolite porphyry dikes--Speckled gray rock with about 10 %phenocrysts each of K-feldspar and quartz, and a trace to 3 % biotitein a matrix of granophyric intergrowths; age about 11-12 Ma; dikescut granodiorite stock (Tgm) and quartz monzonite (Tqm) in MineralMountains.

Intrusion and gneiss complex--Tertiary dikes and other intrusivebodies interleaved with Precambrian(?) gneisses; individual unitscannot be shown at map scale; age of youngest dikes (Trd) 11 Ma;exposed on west side of Mineral Mountains.

Microdiorite dikes--Thin, resistant, dark-green to black dikes withsubdiabasic texture; contain plagioclase (andesine), hornblende,actinolite, and biotite, with minor K-feldspar, and 1 to 3 % eachsphene, Fe-Ti oxides, apatite, orthopyroxene, and alteration minerals;cut granite dikes (Tgd) and quartz monzonite (Tqm) in MineralMountains, so less than 18 Ma.

Granite dikes--Includes fine-grained, leucocratic, and biotite-richvarieties, listed youngest first from intrusive relations; contain about54 % K-feldspar, 27 % quartz, 9 to 16 % plagioclase, and 3 to 7 %biotite; biotite-granite dikes are medium grained and older than thesyenite (Tsm); dikes intrude Tqm in Mineral Mountains, so lessthan 18 Ma.

Syenite of Mineral Mountains--Light-gray, coarse- to medium-grainedsyenite stock; weathers to grus; contains microcline, lesser plagioclaseand quartz, minor biotite and sphene, and accessory Fe-Ti oxides,apatite, hornblende, and zircon; cut by most granite dikes, intrudesunit Tqm in Mineral Mountains, so less than 18 Ma.

Quartz monzonite of Mineral Mountains--Speckled gray, biotite-rich,coarse-grained quartz monzonite that forms massive light-brownish-gray stock exposed extensively in the central Mineral Mountainssouth of the Millard County line; age about 18 Ma.

Diorite of Mineral Mountains--Medium-grained, equigranular, biotitehornblende diorite; contains small apatite and sphene crystals;exposed on northwest flank of Mineral Mountains; age between 18and 25 Ma based on intrusive relationships with Tqm and Tgm.

Mount Belknap Volcanics and related rocks--Derived from severalvolcanic centers, mostly located in the Tushar Mountains; site ofuranium, molybdenum, and alunite mineral deposits; Mount Belknapcaldera fill equivalent to Joe Lott Tuff Member of Mount BelknapVolcanics, which is caldera outflow; age 12 to 21 Ma; units describedseparately.

Late rhyolite dikes, stocks, and domes--Moderately resistant, grayand pink, flow-foliated, crystal-poor, glassy to aphanitic, rhyolitedikes, small stocks, volcanic domes, and lava flows from scatteredvents; age 14-19 Ma; domes as thick as 330 feet (100 m); includesrhyolite of Big Star of Cunningham and others (1983).

Red Hills Tuff Member, Mount Belknap Volcanics--Reddish-brownto reddish-tan and light-gray, crystal-poor, densely welded, rhyoliteash-flow tuff; erupted from small Red Hills caldera just south ofmap area, about 3 miles (5 km) north of Marysvale; K-Ar age 18.9Ma; maximum thickness about 600 feet (180 m).

Joe Lott Tuff Member, Mount Belknap Volcanics--Light-gray orbrownish-gray, crystal-poor, slightly to moderately welded, alkali-rhyolite ash-flow tuff containing 1 to 2 % phenocrysts of quartz,sodic plagioclase, sanidine, and a trace of biotite; outflow fromMount Belknap caldera, mostly south of map area; age about 19Ma; thickness about 200 feet (60 m) near Cove Fort and as muchas 400 feet (120 m) to east in Sevier County.

Mount Baldy Rhyolite Member, Mount Belknap Volcanics--Resistant,light-gray, flow-foliated, crystal poor, rhyolite lava flows and dikes;consist mostly of fine-grained mosaic of quartz and alkali feldspar,with minor plagioclase, biotite, and hematite; deposited mostlywithin Mount Belknap caldera; age uncertain; maximum exposedthickness about 2,600 feet (800 m) is in caldera that is mostly southof map area.

Middle tuff member--Light-gray and tan, poorly welded, crystal poor,intracaldera rhyolite ash-flow tuff; lithologically similar to, and,locally, continuous across Mount Belknap caldera margin into upperpart of Joe Lott Tuff Member (19 Ma; Tmj); thickness to south upto about 1,640 feet (500 m), but thinner in map area.

Lower heterogeneous member--Gray rhyolite volcanic domes, lavaflows, and subordinate ash-flow tuff and fluvial volcanic sandstone;vent probably located just south of map area, northwest of Marysvale;about 230 feet (70 m) thick.

Fine-grained granite--Resistant, gray and greenish-gray, fine-grainedgranite and granodiorite stock and associated dikes; cuts the Centralintrusion (Tci), but is also within and may be a late phase of theMonroe Peak caldera; hosts uranium-bearing veins in Central miningarea, just south of map area; age 20-21 Ma.

Crystal-rich volcanic domes and plugs--Resistant, tan, pink, and gray,flow-foliated, crystal-rich rhyolitic domes and intrusive feeders fordomes; commonly contain phenocrysts of sanidine, plagioclase,biotite, hornblende, quartz, and minor apatite, sphene, and magnetitein a devitrified or glassy matrix; present in southeast Antelope Rangequadrangle; age about 21 Ma; maximum dome height about 820feet (250 m).

Volcanics of Monroe Peak Caldera--Includes lava flows of variedcomposition, Osiris Tuff, intracaldera intrusions, airfall tuff, andfluvial and lacustrine sedimentary rocks deposited in Monroe Peakcaldera after subsidence.

Intracaldera rocks, undivided--Mapped only where hydrothermalalteration precludes identification of individual units describedbelow.

Intracaldera intrusions, undivided--Resistant, tan, light-gray, andlight-green, monzonite porphyry and quartz monzonite porphyryintruded into late intracaldera deposits and the Osiris Tuff; age about21-22 Ma.

Central intrusion--Resistant, gray and green, porphyritic to locallyequigranular quartz monzonite to monzonite stock, with a fine-grained chilled margin; distinct from other intracaldera intrusions;age about 22 Ma.

Sedimentary rocks--Mostly poorly resistant, tan, gray, yellow, brown,pink, and green, thin- to medium-bedded, fine- to coarse-grainedtuffaceous sandstone and airfall tuff, with minor intertongued crystal-poor and crystal-rich lava flows, siltstone, and conglomerate;primarily fluvial but locally lacustrine deposits; commonly alteredand silicified; maximum thickness 200 feet (60 m).

Lava flows of Monroe Peak--Mostly resistant, gray, pink, and dark-green, vesicular and amygdaloidal, generally crystal-rich rhyodaciticlava flows; includes minor crystal-poor lava flows, flow breccia,volcanic mudflow breccia, fluvial sandstone, and airfall tuff; K-Arage 21.3 Ma; maximum exposed thickness 500 feet (150 m); includesdacite of Big Flat of Cunningham and others (1983).

Volcanic rocks of Sage Flat--Mostly resistant, medium- to dark-grayor black, crystal-poor, andesitic lava flows; includes minor volcanicmudflow breccia, and fluvial sandstone and conglomerate; about200 feet (60 m) thick.

Lava flows of Monkey Flat Ridge--Moderately resistant, reddish-brown, gray and green, locally vesicular or amygdaloidal dacitic torhyodacitic lava flows and minor fluvial sandstone and conglomerate;maximum exposed thickness 500 feet (150 m).

Lava flows of Bagley Meadows--Resistant, light- to medium-grayand pink, locally vesicular and amygdaloidal, locally flow-foliated,crystal-rich, dacitic lava flows or a volcanic dome; containsphenocrysts of plagioclase, pyroxene, sanidine, olivine, and Fe-Tioxides; maximum thickness 650 feet (200 m).

Osiris Tuff, intracaldera facies--Soft to resistant, orange and tan,densely welded ash-flow tuff and lava flows(?); confined to sourceMonroe Peak caldera and includes caldera collapse breccia; similarto outflow facies but generally altered to clay by intracaldera

CORRELATION OF GEOLOGIC UNITS

DESCRIPTION OF GEOLOGIC UNITS intrusions (Tmpi, Tci); age about 23 Ma; thickness at least 1,150feet (350 m), base not exposed.

Osiris Tuff, outflow facies--Resistant light-gray and reddish-brown,moderately crystal-rich, densely welded, rhyodacitic ash-flow tuffwith drawn-out pumice fragments; contains one or two coolingunits, commonly with basal black vitrophyres; outflow from MonroePeak caldera in southeast part of map area; age 23 Ma; maximumthickness about 200 feet (60 m).

Syenite of Cedar Grove--Medium to coarse-grained, porphyritic toequigranular rock containing mostly orthoclase and plagioclase,lesser hornblende and pyroxene, and sparse biotite; cuts gabbroporphyry (Tigp); age 23 Ma.

Gabbro porphyry of Cedar Grove--Dark-gray, strongly porphyriticgabbro with phenocrysts of labradorite and clinopyroxene in a feltedmatrix of plagioclase microlites and Fe-Ti-oxide grains; cuts andalters Bullion Canyon Volcanics (Tbc) southwest of Cove Fort.

Granodiorite of Mineral Mountains--Speckled gray, medium-grained,equigranular, locally foliated rock composed of plagioclase, K-feldspar, quartz, hornblende, biotite, and trace minerals; stockweathers to gray, sandy grus; age about 25 Ma.

Zeolite tuff--Soft, white, partially welded, crystal-poor, rhyolitic ash-flow tuff; contains 10 to 30 % lithic fragments; matrix altered tothe zeolite mineral clinoptilolite; may correlate with 24.6 Ma(corrected) Leach Canyon Formation; exposed near Cove Fort whereit overlies the tuff of Albinus Canyon and intertongues with BullionCanyon Volcanics; about 400 feet (120 m) thick.

Volcanic rocks of Signal Peak--Gray, black, brown, reddish-brown,and red, mostly crystal-poor, andesitic lava flows and flow breccia,and lesser volcanic mudflow breccia, densely welded ash-flow tuff,and conglomerate; overlies tuff of Albinus Canyon northeast ofAnnabella; vent facies rocks and lesser alluvial-fan facies rockserupted from shield volcano complex in northern Sevier Plateau;as much as 2,100 feet (650 m) thick.

Basaltic andesite, Antimony Tuff, and tuff of Albinus Canyon,undivided--Only used in hills southeast of town of Joseph whereindividual units (Tba, Tda, Tac) cannot be separated.

Basaltic andesite lava flows--Resistant, dark-gray and black, locallyvesicular and amygdaloidal, crystal-poor, basaltic andesite lavaflows; exposed in southeast Pahvant Range; intertongued withAntimony Tuff and tuff of Albinus Canyon; may be part of unit Tsgwith vents east of Sevier Valley; maximum thickness about 500 feet(150 m).

Antimony Tuff Member, Mount Dutton Formation--Resistant, mostlyred, densely welded, crystal-poor, trachytic ash-flow tuff; containsmedium-grained phenocrysts of plagioclase, sanidine, and minorpyroxene and Fe-Ti oxides, and drawn-out pumice lenticules;interlayered with volcanic rocks of Signal Peak; K-Ar age 25.4 Ma;maximum thickness 200 feet (60 m).

Tuff of Albinus Canyon--Red to gray, crystal-poor, densely welded,trachytic ash-flow tuff; contains few phenocrysts; flow structuresand lineate vesicles are characteristic; has several thin cooling units,locally separated by thin beds of volcanic mudflow breccia,conglomerate, and sandstone in map area; lithologically similar tooverlying Antimony Tuff Member of the Mount Dutton Formation;age 25.3 Ma; maximum thickness about 650 feet (200 m).

Crystal-poor dacitic lava flows--Moderately resistant, light-gray,light- to medium-green, and light-reddish-gray, locally vesicular oramygdaloidal, aphanitic dacitic lava flows and red volcanic mudflowbreccia; exposed northeast of Annabella underlying tuff of AlbinusCanyon and overlying Three Creeks Tuff; 100 to 160 feet (30-50m) thick.

Bullion Canyon Volcanics--Widely distributed, heterogeneous,varicolored, volcanic mudflow breccia, lava flows, flow breccia,ash-flow tuff, and fluvial volcanic conglomerate and sandstone;erupted and eroded from several clustered stratovolcanoes; lavaflows are mostly crystal-rich dacite with some fine-grained, crystal-poor, black andesite, as well as rhyodacite and quartz latite lavaflows; age at least 30 to 22 Ma; maximum thickness at least 5,000feet (1,500 m) in Sevier County.

Monzonitic/latitic intrusions in Bullion Canyon Volcanics--Dark- tolight-gray, tan, and brown, crystal-rich monzonite and quartzmonzonite and strongly porphyritic latite and quartz latite in smallplutons and plugs; probably solidified magma sources of other rocksin the Bullion Canyon Volcanics; ages cluster about 23 Ma; nearCove Fort intrusions cut Three Creeks Tuff (27 Ma) and areunconformably overlain by Osiris Tuff (23 Ma).

Metamorphosed rock--Calc-silicate hornfels and quartzite at contactwith quartz monzonite of unit Tbci (age about 23 Ma); thought tobe metamorphosed Toroweap Formation (Lower Permian),interbedded dolomite, limestone, and sandstone.

Three Creeks Tuff Member, Bullion Canyon Volcanics--Resistant,light-gray to light-brown, crystal-rich, moderately to densely welded,dacitic ash-flow tuff containing 40 to 60 % phenocrysts, mostlyplagioclase, with lesser hornblende, biotite, and quartz, and tracesof sanidine and Fe-Ti oxides; erupted from caldera north of I-15and east of Cove Fort; age 27 Ma; maximum thickness about 720feet (220 m).

Quartz-latite volcanic dome and rhyodacite flow--Resistant, gray,crystal-rich, quartz latite volcanic dome and overlying dark-gray,crystal-poor, rhyodacitic lava flow in Joseph Peak quadrangle; ageuncertain; maximum thickness about 650 feet (200 m).

Volcanic rocks of Wales Canyon--Moderately resistant, red, moderatelycrystal-rich, intermediate-composition lava flows and densely weldedash-flow tuff; exposed near Cove Fort; overlies volcanic rocks of

Dog Valley and locally intertongues with Three Creeks Tuff onnorth margin of Marysvale volcanic field; about 440 feet (135 m)thick. Locally resembles Wah Wah Springs Formation.

Tuff of Dog Valley - Mostly resistant, gray, tan and pink, crystal-rich, moderately welded, dacitic, ash-flow tuff; exposed near CoveFort and on the north flank of the Marysvale volcanic field; locallyinterlayered with volcanic rocks of Dog Valley; looks like tuff ofWah Wah Springs Formation and Three Creeks Tuff; Ar/Ar age33.6 Ma; maximum thickness about 400 feet (120 m).

Volcanic rocks of Dog Valley--Heterogeneous assemblage of andesiticto dacitic rocks including lava flows, volcanic mudflow breccias,and minor moderately welded ash-flow tuff similar to some in theNeedles Range Group, but here recognized as tuff of Dog Valley;age about 33 Ma; maximum thickness up to 1,200 feet (370 m).

Older volcanic rocks--Poorly to moderately resistant, light-gray,light- to dark-green, brown, and red volcanic mudflow breccia andsubordinate lava flows; flows and clasts are dacitic; exposed innortheast Annabella quadrangle, underlying Three Creeks Tuff andoverlying Aurora Formation; lower part may be lateral equivalentof upper Dipping Vat; 660 feet (200 m) thick.

Dipping Vat Formation--Poorly cemented, light-gray to pale-bluish-gray, volcaniclastic sandstone, conglomerate, and reworked volcanictuff; conglomerate beds are poorly sorted and include clasts ofwelded tuffs, quartzite, limestone, and dolomite up to boulder size;younger than 35 Ma and older than overlying 27 Ma Three CreeksTuff; maximum thickness in map area about 600 feet (180 m).

Aurora Formation--Mostly poorly resistant, pale-gray, reddish-, andyellowish-gray, bentonitic siltstone and claystone, with beds of thin-to medium-bedded, medium-gray limestone, fine-grained sandstone,and pebble to cobble conglomerate; contains upwardly increasingamounts of fine-grained rhyolitic ash and reworked volcanic detritus;coarsens to southwest; 38 to 40 Ma age implies volcanic source inwest-central Utah; maximum thickness about 1,200 feet (360 m)southeast of Kanosh thinning to 550 feet (170 m) near Richfield,and to less than 200 feet (60 m) near Cove Fort.

Crazy Hollow Formation--Mostly moderately resistant, brownish-orange to brownish-red, very thin- to thin-planar-bedded, fine-grained sandstone, siltstone, and mudstone; contains 25 % interbedsof pale-grayish-orange, lenticular, channel sandstone; black chertpebbles in few thin conglomerate lenses are diagnostic for formation;350 feet (107 m) thick west of Richfield, thinning to zero a shortdistance to southwest.

Green River Formation--Yellowish-gray to pale-brown, cherty, algal,and oolitic limestone and dolomite, calcareous, fine-grainedsandstone, and greenish-gray shale; about 800 feet (245 m) partialthickness exposed in northeast map area and thins to absencesouthwest of Richfield.

Flagstaff Formation--Interbedded pinkish-weathering, freshwaterlimestone, sandstone, siltstone, mudstone, and conglomerate; typicallybioturbated; in southwestern Pahvant Range conglomerate isdominant lithology exposed and strata may grade into upper NorthHorn Formation; 300 to 585 feet (90-190 m) thick in CricketMountains; maximum thickness in Pahvant Range is about 3,500feet (1,070 m), thinning to nothing east of Dog Valley in southernPahvant Range. In most of Pahvant Range divided into six informalmembers described below:

Upper white member - Pale-gray, pale-purplish-gray or pale-yellowish-gray, calcareous mudstone, siltstone and sandstone, and sandylimestone; less resistant than other Flagstaff members, forms a broadslope with a few ledges; commonly covered by rubble from overlyingformations; 170 to 185 feet (51-56 m) thick.

Upper red member - Interbedded dark-reddish-brown, calcareousmudstone, siltstone, and sandstone, and local conglomerate; formsa distinct red, ledgy slope with local cliffs; less than 50 to at least162 feet (15-49+ m) thick; thins to northeast.

Middle white member - Interbedded pale-gray, pale-yellowish-grayor pale-pinkish-gray, calcareous sandstone, sandy limestone, andlimestone cliffs and ledges, with minor sandy mudstone slopes;lower part mostly gypsiferous mudstone that grades to southwestinto mostly limestone and sandstone; 515 to 580 feet (157-177 m)thick.

Middle red member - Interbedded reddish-brown sandstone, siltstone,and mudstone; minor conglomerate beds contain mostly quartziteand carbonate clasts less than 6 inches (15 cm) in diameter; formscliffs and ledges typically 10 to 50 feet (3-15 m) high separated bysteep slopes; about 600 feet (180 m) thick.

Lower white member - Interbedded pale-gray to pale-reddish-gray,calcareous sandstone, sandy limestone, and pale-purplish-gray, siltyto sandy mudstone; white, clayey limestone beds, locally as thickas 150 feet (45 m) cap the member; less resistant calcareous mudstone,siltstone and sandstone beds comprise middle part; resistant, blockylimestone beds in lower part are up to 200 feet (60 m) thick; totalthickness 0 to about 700 feet (0-215 m), thinning to southwest.

Lower red member - Interbedded reddish sandstone, siltstone,mudstone, conglomerate; forms cliffs and steep slopes; less than200 feet (60 m) thick in southwesternmost exposures to about 1,300feet (400 m) east of Kanosh to about 600 feet (180 m) thick onPahvant Range crest east of Fillmore.

Breccia of Cat Canyon--Coarse, recemented breccia of gray, Cambriancarbonate rocks in Cricket Mountains; likely an indurated talus orrubble, rather than of tectonic origin; as much as 165 feet (50 m)thick.

North Horn Formation--Predominantly yellowish-gray sandstonewith interbeds of siltstone, mudstone, conglomerate, and limestone;as much as about 2,500 feet (760 m) thick in Pahvant Range eastof Fillmore, but absent from about Meadow Creek southward; either

thins rapidly to south or grades into lower red member of FlagstaffFormation.

Conglomerate of Mineral Mountains--Pebble-cobble conglomerateof limestone, quartzite, sandstone, and chert clasts in a sandylimestone matrix where it rests on Cambrian rocks; similarconglomerate present beneath overthrust Cambrian quartzite; maybe Tertiary where it rests on other Cambrian rocks; about 110 feet(33 m) thick.

Canyon Range Conglomerate--Massive, reddish-gray conglomeratewith interbedded sandstone lenses; present locally beneath NorthHorn Formation in the central Pahvant Range and southwest ofKanosh; rests unconformably on Paleozoic strata; maximum exposedthickness about 850 feet (260 m).

PAVANT THRUST FOOTWALL, PAHVANT RANGETectonic melange beneath Pavant thrust plate--Mixture of rocks fromTriassic and upper Paleozoic strata that were dragged along beneaththe thrust plate; thickness up to 200 feet (60 m), or more locally.

Navajo Sandstone--Reddish-brown, fine-grained, cross-bedded, cliff-forming sandstone; exposed thickness about 2,000 feet (600 m).

Triassic strata, undivided--On cross sections only; for included unitssee correlation chart and descriptions.

Chinle Formation, Upper Member--Interbedded, varicolored sandstone,siltstone, mudstone, and shale; prone to slump; thickness 69 to 274feet (21-83 m).

Chinle Formation, Shinarump Conglomerate Member--Interbeddedquartzite pebble conglomerate and white to brown, coarse sandstonethat contains petrified wood; thickness 177 to 566 feet (54-172 m).

Moenkopi Formation--Interbedded brownish-red sandstone, siltstone,shale, and gray limestone; minor cross-beds, mud cracks, and ripplemarks are common; fossil brachiopods and ammonoids abundantlocally; maximum thickness 1,876 feet (572 m).

Permian strata, undivided--On cross sections only; for included unitssee correlation chart and descriptions.

Kaibab Limestone--Gray, medium-crystalline, medium-bedded,dolomitic limestone; locally sandy and contains abundant brownchert; thickness in map area 497 (subsurface) to 1,160 feet (152-353 m); lower third of this map unit is likely Toroweap Formationequivalent.

Queantoweap Sandstone--Pinkish- or light-brownish-gray, fine-grained, cross-bedded sandstone; locally poorly cemented; thickness817 feet (249 m).

Pakoon Dolomite--Medium- to light-gray, sandy dolomitecharacterized by small, white calcite blebs; basal 50 feet (15 m) isa chert pebble conglomerate; thickness 445 feet (136 m).

Pennsylvanian and Mississippian strata, undivided--On cross sectionsonly; for included units in footwall see correlation chart anddescriptions.

Callville Limestone--Medium- to light-gray, fine- to medium-bedded,medium- to thick-bedded, cherty limestone and dolomite with a fewthin pinkish-gray sandstone beds; thickness 538 feet (164 m).

Redwall Limestone--Upper third is interbedded calcareous sandstone,limestone, and dolomite; middle part is gray, cherty, fossiliferouslimestone; basal one-quarter is medium-gray interbedded dolomiteand limestone; thickness 1,545 feet (471 m).

Devonian strata, undivided--On cross sections only; for includedunits in footwall see correlation chart and descriptions.

Cove Fort Quartzite--Yellowish-gray, medium-grained quartzite withthin interbeds of dolomitic quartzite in middle third; forms prominentledges; thickness 82 to 160 feet (25-49 m).

Guilmette Formation--Dark-gray, medium-grained, medium-beddeddolomite with a few interbeds of brown-weathering quartzite;thickness 575 feet (175 m).

Simonson Dolomite--Light-brownish-gray, medium- to coarse-grained, thin-bedded dolomite; thickness 185 feet (56 m).

Sevy Dolomite--Very-light-gray, fine-grained, medium-bedded,clayey dolomite; rare fossil fish fragments found in Sevy strata inDog Valley quadrangle; thickness 710 feet (217 m).

Silurian and Upper Ordovician strata, undivided--On cross sectionsonly; for included units see correlation chart and descriptions.

Laketown and Fish Haven Dolomites, undivided--Dark-gray, chertydolomite with stromatolites and rugose corals; thickness 566-1,000feet (173-300 m).

Middle and Lower Ordovician strata, undivided--On cross sectionsonly; for included units see correlation chart and descriptions.

Eureka Quartzite--Light-pinkish-gray, vitreous quartzite with thin-bedded fucoidal sandstone and shale in lower half; forms ledges;thickness 150 to 180 feet (45-55 m).

Pogonip Group--Medium-gray, medium- to thin-bedded limestoneand intraformational conglomerate, locally cherty or fine sandy;upper 89 feet (27 m) includes interbeds of olive shale that containsorthid brachiopods; total thickness 1,125 feet (343 m).

Upper Cambrian strata, undivided--On cross sections only; forincluded units see correlation chart; may also include MiddleCambrian strata.

Ajax(?) Dolomite--Highly fractured, nondescript dolomite exposedin Baker Canyon; likely part of Ajax Dolomite.

PAVANT THRUST SHEETLaketown and Fish Haven Dolomites, undivided--Interbedded light-gray and medium dark-gray to brownish-gray, medium- to thick-bedded dolomite; brown chert bands in middle of exposed strata,so Laketown may or may not be exposed; incomplete 200 foot (60m) thickness exposed in upper Corn Creek Canyon.

The views and conclusions contained in this documentare those of the authors and should not be interpretedas necessarily representing the official policies, either

expressed or implied, of the U.S. Government.

7. Hintze, L.F., 1984, Geology of the Cricket Mountains, Millard County, Utah:U.S. Geological Survey Open-File Report 84-683, 14 p., plates 4, 5, and 7,scale 1:24,000.

8. Hintze, L.F., 1984, Geology of the Cricket Mountains, Millard County, Utah:U.S. Geological Survey Open-File Report 84-683, 14 p., plate 8, map scale1:24,000; mapping of volcanic rocks by L.F. Hintze for this publication, scale1:24,000, modified from Crecraft, H.R., Nash, W.P., and Evans, S.H. Jr., 1981,Late Cenozoic volcanism at Twin Peaks, Utah, geology and petrology: Journalof Geophysical Research, v. 86, p. 10,303-10,320, scale 1:200,000.

9. Hintze, L.F., 1990 and 1991, unpublished mapping for this publication, scale1:24,000.

10. Hintze, L.F., 1991, unpublished mapping for this publication, scale 1:24,000,partly modified from Crecraft, H.R., Nash, W.P., and Evans, S.H. Jr., 1981,Late Cenozoic volcanism at Twin Peaks, Utah, geology and petrology: Journalof Geophysical Research, v. 86, p. 10,303-10,320, scale 1:200,000.

11. Hintze, L.F., 1992, and Hintze, L.F., and Willis, G.C., 1999, unpublishedmapping for this publication, scale 1:24,000, partly modified from Hickox,C.W., 1971, Geology of a portion of the Pavant Range allochthon, MillardCounty, Utah: Houston, Texas, Rice University, Ph.D. dissertation, 67 p.,scales 1:63,360 and 1:31,360.

12. Hintze, L.F., 1992, and Hintze, L.F., and Willis, G.C., 1999, unpublishedmapping for this publication, scale 1:24,000 and ~1:50,000; modified fromSteven, T.A., 1979a, Geologic map of the Monroe NW (Elsinore) quadrangle,west-central Utah: U.S. Geological Survey Miscellaneous Field Studies MapMF-1107, scale 1:24,000.

13. Lautenschlager, H.K., 1952, Geology of the central part of the Pavant Range,Utah: Columbus, Ohio State University, Ph.D. dissertation, 188 p., map scale1:31,680; modified locally using Hickox, C.W., 1971, Geology of a portionof the Pavant Range allochthon, Millard County, Utah: Houston, Texas, RiceUniversity, Ph.D. dissertation, 67 p., scales 1:63,360 and 1:31,360; modifiedby L.F. Hintze, 1991, and L.F. Hintze and G.C. Willis, 1999, unpublishedmapping for this publication, scale 1:24,000.

14. Rowley, P.D., Steven, T.A., and Kaplan, A.M., 1981, Geologic map of theMonroe Peak NE (Annabella) quadrangle, Sevier County, Utah: U.S. GeologicalSurvey Miscellaneous Field Investigations Map MF-1330, scale 1:24,000;partly modified by G.C. Willis, 1999.

15. Rowley, P.D., Cunningham, C.G., Steven, T.A., Workman, J.B., Anderson,J.J., and Theissen, K.M., 2002, Geologic map of the central Marysvale volcanicfield, southwestern Utah: U.S. Geological Survey Geologic InvestigationsMap I-2645A, scale 1:100,000; with clarification locally from Cunningham,C.G., Steven, T.A., Rowley, P.D., Glassgold, L.B., and Anderson, J.J., 1983,Geologic map of the Tushar Mountains and adjoining areas, Marysvale volcanicfield, Utah: U.S. Geological Survey Miscellaneous Investigations Map I-1430,scale 1:50,000.

16. Steven, T.A., 1979, Geologic map of volcanic rocks in the Sevier NE (JosephPeak) quadrangle, west-central Utah: U.S. Geological Survey MiscellaneousField Studies Map MF-1108, scale 1:24,000; and Hickox, C.W., 1971, Geologyof a portion of the Pavant Range allochthon, Millard County, Utah: Houston,Texas, Rice University, Ph.D. dissertation, 67 p., scales 1:63,360 and 1:31,360;modified by L.F. Hintze, 1991, and L.F. Hintze and G.C. Willis, 1999,unpublished mapping for this publication, scale 1:24,000.

17. Steven, T.A., and Morris, H.T., 1983, Geologic map of the Cove Fort [15']quadrangle west-central Utah: U.S. Geological Survey Miscellaneous Inves-tigations Series Map I-1481, scale 1:50,000; modified by L.F. Hintze, 1991,1999, unpublished mapping for this publication, scale 1:24,000.

18. Whelan, J.A., and Bowdler, James, 1979, Geology of the Antelope Springsquadrangle, Millard County, Utah: Utah Geology, v. 6, no. 2, p. 81-85, scale1:62,500; and Hintze, L.F., 1991-1992, unpublished mapping for this publication,scale 1:24,000; north end of Mineral Mountains from Coleman, D.S., Bartley,J.M., Walker, J.D., Price, D.E., and Friedrich, A.M., 1997, Extensional faulting,footwall deformation and plutonism in the Mineral Mountains, southern SevierDesert: Brigham Young University Geology Studies, v. 42, part 2, p. 203-233,scale 1:21,300.

19. Willis, G.C., 1994, Interim geologic map of the Richfield [7.5'] quadrangle:Utah Geological Survey Open-File Report 309, 105 p., scale 1:24,000.

20. Zimmerman, J.T., 1961, Geology of the Cove Creek area, Millard and BeaverCounties, Utah: Salt Lake City, University of Utah, M.S. thesis, 91 p., scale1:24,000; and Hintze, L.F., 1991, unpublished mapping for this publication,scale 1:24,000, partly modified from Crecraft, H.R., Nash, W.P., and Evans,S.H. Jr., 1981, Late Cenozoic volcanism at Twin Peaks, Utah, geology andpetrology: Journal of Geophysical Research, v. 86, p. 10,303-10,320, scale1:200,000.

Plate 2 of 2Utah Geological Survey Map 195

GEOLOGIC MAP OF THE RICHFIELD 30' x 60' QUADRANGLE,SOUTHEAST MILLARD COUNTY AND PARTS OF BEAVER, PIUTE,

AND SEVIER COUNTIES, UTAHby

Lehi F. Hintze, Fitzhugh D. Davis, Peter D. Rowley, Charles G. Cunningham,Thomas A. Steven, and Grant C. Willis

2003

UTAH GEOLOGICAL SURVEYa division of

UTAH DEPARTMENT OF NATURAL RESOURCESin cooperation with

THE UNITED STATES GEOLOGICAL SURVEYNATIONAL COOPERATIVE GEOLOGIC MAPPING PROGRAM

STATEMAP Agreement No. 00HQAG0109

Index map showing sources of geologic mapping and 7.5-minute quadrangles

Eureka Quartzite--Light-colored, medium-bedded, vitreous quartzitewith lower half thinner bedded quartzite, sandstone, and dark, fissileshale; 172 feet (52 m) thick in upper Corn Creek Canyon.

Pogonip Group--Fossiliferous, interbedded shale and limestone attop; underlain by medium-gray, thin- to medium-bedded limestone,with intraformational conglomerate and sparse chert, and thin shaleinterbeds; 1,200+ feet (350+ m) thick in upper Corn Creek Canyon.

Ajax Dolomite--Dark-gray, massive dolomite with a few interbedsof light-gray dolomite and bluish-gray limestone with "algal"stromatolites; thickness about 700 feet (210 m) in upper Corn CreekCanyon.

Opex Formation--Medium-gray, medium-bedded, bioclastic limestonewith a few thin interbeds of dolomite and shale; containsTricrepicephalus trilobites; thickness 390 feet (120 m) in upperCorn Creek Canyon.

Upper and Middle Cambrian carbonate rocks, undivided--Includes:strata between Opex and Ophir Formations in upper Corn CreekCanyon, strata between the Ajax and Ophir on the north margin ofmap area, and may include all Cambrian strata above the OphirFormation in thicker exposures between these two areas and oncross sections. Only includes Middle Cambrian strata above theOphir southwest of Kanosh. These carbonate rocks are unfossiliferousand mostly dolomites that range from light- to dark-gray, laminatedto massive, and include bioturbated, mottled dolomite and limestonebeds; the carbonates are generally medium-bedded to massive andgenerally form cliffs except where tectonically brecciated; thicknessup to about 2,400 feet (735 m).

Ophir Formation--Upper part is medium- to thick-bedded limestonewith some shale interbeds, uppermost of which bears Ehmaniellatrilobites; basal third is phyllitic quartzite, shale, and thin-beddedlimestone bearing Glossopleura trilobites; both parts form slope-ledge topography; thickness about 850 feet (260 m).

Tintic Quartzite--White to brownish-orange-weathering, vitreousquartzite, with a few quartzite pebble conglomerate beds; commonlysheared and fractured; estimated thickness 3,300 feet (1,000 m).CAMBRIAN STRATA IN THE CRICKET AND MINERAL

MOUNTAINSUpper Cambrian strata, undivided--On cross sections only; forincluded units see correlation chart and descriptions.

Notch Peak Formation--Medium-dark-gray, massive limestone; onlybasal 100 feet (30 m) preserved in map area.

Orr Formation, upper members, undivided--In descending order, thefollowing members constitute this combined unit: SneakoverLimestone Member, 100 feet (30 m) thick; Corset Spring ShaleMember, 40 feet (12 m) thick; Johns Wash Limestone Member, 100feet (30 m) thick; and Candland Shale Member, 165 feet (50 m)thick.

Orr Formation, Big Horse Limestone Member--Pinkish- to dark-graylimestone with dolomitic "algal" stromatolites and boundstone inthe middle; bioclastic beds contain Crepicephalus trilobites; thickness656 feet (200 m).

Middle Cambrian strata, undivided--On cross sections only; forincluded units see correlation chart and descriptions.

Wah Wah Summit Formation and Trippe Limestone, undivided--Wah Wah Summit Formation includes a white dolomite and limestonesequence that makes up the upper third of the formation, and a dark-gray, ledge- and cliff-forming, carbonate sequence below; thickness575 to 640 feet (175-195 m). Trippe Limestone includes the FishSprings Shale Member, about 100 feet (30 m) thick, beneath whichthe lower member consists of alternating dark-gray, ledge-forminglimestone, and light-gray, laminated, slope-forming, dolomiticboundstone, 660 to 760 feet (200-230 m) thick. Combined mapunit about 1,420 feet (433 m) thick; structurally thinned andidentification uncertain in Mineral Mountains.

Limestone of Cricket Mountains--Interbedded, dark-gray limestone,brownish-gray dolomitic limestone, and light-gray, laminated,dolomitic boundstone; forms cliffs and ledges; thickness 1,970 feet(600 m).

Whirlwind Formation-Light-olive-gray shale interbedded with thin-bedded, nodular limestone bearing coquinas of the trilobiteEhmaniella; forms recessive slopes; thickness 200 to 265 feet (60-80 m).

Dome-Chisholm-Howell Formations, undivided--Listed from topdownward. Dome Limestone is gray, massive, forms cliffs, andis 230 to 330 feet (70-100 m) thick. Chisholm Formation consistsof lower and upper shales, bearing the trilobite Glossopleura,separated by dark-gray, oncolitic limestone; 165 to 265 feet (50-80m) thick. Howell Limestone forms cliffs that are light-gray in theupper third and dark-gray below; thickness about 300 to 360 feet(90-110 m). Peasley Limestone is lateral equivalent of Chisholmin Mineral Mountains, where entire map unit is structurally thinned.

Lower Cambrian strata, undivided--On cross sections only; forincluded units see correlation chart and descriptions.

Pioche Formation--Mostly interbedded dark-brown quartzite anddark-greenish-gray, phyllitic siltstone characterized by abundanttrace fossils; upper tenth includes beds of orange-weatheringdolomite; thickness about 800 feet (245 m).

Prospect Mountain Quartzite--Grayish-pink, vitreous quartzite rangingfrom very fine- to coarse-grained with some thin, quartzite-pebbleconglomerate beds; forms ledges and cliffs; at least 4,000 feet (1,200m) thick.

Banded gneiss--Light bands are composed of quartz and K-feldsparwith minor biotite and plagioclase; dark bands are mostly biotite,plagioclase, and quartz with minor hornblende and K-feldspar;accessory minerals are apatite and rounded zircon; present in MineralMountains; age 1,750 Ma.

LITHOLOGIC COLUMN

Quaternary surficial units, undivided--On cross sections only; forincluded units see correlation chart and descriptions.

Alluvium, late Holocene--Youngest alluvium in the channels,floodplains, and low terraces of the Sevier River, Beaver River,Chalk Creek, Corn Creek, Cove Creek, and other large streams;includes overbank and marsh deposits in abandoned meanders ofthe Sevier River; consists of sand, silt, and clay with lenses ofgravel; silt in lower Pahvant Valley; less than 100 feet (30 m) thickalong Sevier River; mostly 0 to 20 feet (0-6 m) thick, but may bethicker locally.

Alluvium, middle and early Holocene--Sand, silt, and clay in thefloodplain of Cove Creek, isolated remnants of older Chalk Creekand Corn Creek sand and gravel near Fillmore and Kanosh(respectively), along a stream near White Sage Flat, in the PahvantRange along East Creek, and south of the Sevier River southwestof Elsinore; 0 to 30 feet (0-9 m) thick.

Alluvium, pre-Lake Bonneville(?)--Silt, sand, and pebble to bouldergravel in faulted and tilted terraces along Sevier River southwestof Elsinore; 0 to 40 feet (0-13 m) thickness exposed; age uncertain,might be Holocene.

Younger alluvial-fan deposits--Poorly sorted silt, sand, and pebble,cobble, and boulder gravel deposited by streams, sheetwash, debrisflows, and flash floods on alluvial fans, and in canyons and mountainvalleys; post-Bonneville shoreline in age; mostly 0 to 60 feet (0-18 m) thick, but may be up to 165 feet (50 m) thick along upperSevier River.

Older alluvial-fan deposits--Poorly sorted silt, sand, and pebble,cobble, and boulder gravel deposited by streams, debris flows, andflash floods on alluvial fans, and in canyons and mountain valleysabove the Bonneville shoreline; includes colluvium in canyons andmountain valleys; on flanks of Mineral Mountains is mostly pea-sized grus, locally including larger clasts and significant eolian silt;mostly pre-Lake Bonneville in age, but locally includes youngermaterial; up to 200 feet (60 m), or more, in thickness.

Alluvium and colluvium, undifferentiated--Mixed alluvial andcolluvial deposits that consist of fluvially reworked coarse-grainedcolluvium and/or alluvium with a significant colluvium component;also includes talus; generally 0 to 50 feet (0-15 m) thick, but maybe thicker locally.

Mass movements, undivided--Masses of soil, sand, rock, and bouldersthat have moved downslope under the influence of gravity; includessoil creep, slopewash, talus, and fan alluvium, and locally slidesand slumps; 0 to 100 feet (0-30 m) thick. Includes dissected olderdeposits on and near Bull Claim Hill southeast of Richfield.

Mass movements, talus--Poorly sorted, angular boulders with minorfine-grained interstitial material on and at the base of steep slopesin the Pahvant Range; only the largest deposits can be shown atmap scale; thickness less than 100 feet (30 m).

Mass movements, slides and slumps--Volcanic and sedimentary rockmasses that have slumped and slid downslope, chiefly on softer,underlying rocks; small isolated slides or slumps are present inmany mountainous areas, but are too small to show at 1:100,000scale; up to 250 feet (75 m) thick.

Eolian dunes--Chiefly parabolic, longitudinal, and barchan sanddunes that are active and not stabilized by vegetation; composedof well-sorted, fine-grained quartz sand; also gypsum dunes in thevicinity of White Mountain and silt dunes downwind from playasand blowouts; 3 to 35 feet (1-11 m) thick.

Eolian and alluvial deposits, mixed--Interbedded and mixedwindblown and alluvial sand and silt in the volcanic terrain westof Cove Fort; up to 20 feet (6 m) thick.

Playa mud--Laminated, silty, fine sand, silt, and clayey silt infusedwith various salts, gypsum, and calcium carbonate; thicknessprobably 20 feet (6 m) or less.

Spring travertine--Cellular to dense and banded, spring-depositedtravertine in southern Pahvant Valley and in White Sage Flat,siliceous spring deposits near Roosevelt Hot Springs in BeaverCounty, and calcareous spring deposits southeast of Joseph and eastof Monroe in Sevier County; 0 to 90 feet (0-30 m) thick.

Altered material--White, porous aggregates of opaline silica, gypsum,native sulfur, and anhydrite, and remnant quartz and cristobaliteproduced by acid leaching; related to geothermal system; locatednear Cove Fort in Holocene(?) and likely Pleistocene alluvial fansand bedrock; only the largest area, exposed in a pit, is mapped; upto 105 feet (33 m) thick in this pit.

Glacial till--Unsorted mixtures of clay, silt, sand, and angular pebbles,cobbles, and boulders in Pahvant Range; includes lateral and othermoraines and outwash on Sevier Plateau; probably late Wisconsin(Pinedale) in age; 0 to 200 feet (0-60 m) thick.

Underflow-fan deposits--Thin-bedded to laminated, calcareous siltwith minor interbedded very fine sand in thin beds; deposited inthe Lake Bonneville delta of the Beaver River south of Borden; 0to more than 30 feet (0-10+ m) thick.

Deltaic sand and gravel--Silty, fine- to coarse-grained sand and graveldeposited by the Beaver River in Lake Bonneville and then distributedby waves and currents; 0 to 24 feet (0-7 m) thick.

Lacustrine gravel--Silty, fine- to coarse-grained sand and gravel inshore zone deposits of Lake Bonneville; 0 to 30 feet (0-9 m) thick.

Lacustrine sand--Fine- to coarse-grained sand, marly sand, andpebbly sand deposited in shore zone of Lake Bonneville as beaches,spits, and offshore bars; 0 to 30 feet (0-9 m) thick.

Fine-grained lacustrine deposits--Tan to light-gray, calcareous siltsthat are deep-water sediments of Lake Bonneville; locally includes

MAP AND CROSS-SECTION SYMBOLS

*Also on main lithologic column

MARYSVALE VOLCANIC FIELD LITHOLOGIC COLUMN

THICKNESSMAP UNITMAPSYMBOL Feet

Late rhyolite rocks

Red Hills Tuff Member

*Joe Lott Tuff Member

Mount Baldy Rhyolite Member

Middle tuff member

Lower heterogeneous member

Fine-grained granite

Crystal-rich domes and plugs

Intracaldera intrusions

Sedimentary rocks

Lava flows of Monroe Peak

Volcanic rocks of Sage Flat

Lava flows of Monkey Flat Ridge

Lava flows of Bagley Meadows

*Osiris Tuff (i=intracaldera)

Zeolite tuff

---- ----

<600 <180

0-400 0-120

<2,600 <800

<1,640 <500

230 70

intrusions

---- ----

200 60

500 150

200 60

<500 <150

0-1,150+ 0-350+

400 120

200 602,100 650

100-160 30-505,000±

intrusions

0-720 0-220

650 200

intrusions

Antimony Tuff Member, Mt. Dutton Fm.

*Tuff of Albinus Canyon

Volcanic rocks of Signal Peak

Crystal-poor dacitic lava flowsBullion Canyon Volcanics

Monzonitic / latitic intrusions

*Three Creeks Tuff Member

Quartz latite dome and rhyodacite flow

650 200

intra

cald

era

rock

s,un

divi

ded

Mou

nt B

elkn

ap V

olca

nics

MI

OC

EN

EO

LI

GO

CE

NE

Basaltic andesite lava flows 500 150

14-19 Ma

18.9 Ma K-Ar

Age uncertainPresent inupper Tmj

20-21 Ma

21-22 Ma

21.3 Ma K-Ar

Andesitic

Dacitic

Flows or domeMonroe Peakcaldera is source24.6 Ma?

25.4 Ma K-ArMay be partof unit Tsg

22-30 Ma

23-27 Ma

Andesitic

AG

E

0-650 0-200

SCHEMATICCOLUMN

OTHERINFORMATION

?

25.3 Ma

27 Ma

Mount Belknapcaldera is source

Meters

11-13 Ma?Basalt flows in northernTushar Mountains 0-425 0-130

Age uncertain

1,500+

Volca

nics

of M

onro

e Pea

k Cald

era

15257

70

Millard Co. Sevier Co.

Fillmore

Richfield

Bea

ver C

o.

Mill

ard

Co.

Kanosh

SOURCE LIST FOR GEOLOGIC MAPPING

Note: “Pavant” and “Pahvant” are both used in thisdocument. “Pahvant” is now the accepted spelling forgeographic features. “Pavant” usage is for geologic

features named in publications.

CONTACT-- Dashed where location inferred; queried where speculative oncross sections

NORMAL FAULT-- Dashed where location inferred; dotted where concealed;queried where existence uncertain; bar and ball on downthrown side; arrowsshow relative movement on cross section

STEEPLY DIPPING FAULT-- Sense of motion not known or complex; dashedwhere location inferred; dotted where concealed

NORMAL FAULT-- Inferred and delineated from gravity data; concealed; barand ball on downthrown side

TEAR FAULT-- High-angle fault with strike-slip offset; dashed where locationinferred; dotted where concealed; arrows show relative movement on map

THRUST FAULT-- Dashed where location inferred; dotted where concealed;barbs on upper plate; arrows show relative movement on cross sections

ATTENUATION FAULT -- Younger over older rocks with strata thinned andcut out between; present in Mineral Mountains; barbs on upper plate

CALDERA MARGIN-- Dashed where location inferred; dotted where concealed;hachures on downthrown side; mostly topographic boundary of caldera.

DETACHMENT RELATED TO MASS MOVEMENTS-- Dashed where locationinferred; present on west side of Pahvant Range (where Navajo Sandstone hascrept downslope on underlying Chinle)

LINEAMENT -- Shown west of White Sage Flat, may be concealed fault trace

FOLD AXES -- Dotted where concealed (arrows on axes show plunge)

anticline

syncline

overturned anticline

ESCARPMENT AT HEAD OF SLUMP/SLIDE AREA

STRIKE AND DIP OF BEDDING--

inclined

vertical

overturned

horizontal

STRIKE AND DIP OF PLANAR FEATURES IN ASH-FLOW TUFF

DEEP EXPLORATION WELL-- map symbol on left, cross section symbol onright

SINKHOLE (in QTlf)

VOLCANIC VENT/CINDER CONE

SHORELINES-- dashed where inferred; dotted where concealed; queried whereconjectural

Provo shoreline of Lake Bonneville-- queried where uncertain

Bonneville shoreline of Lake Bonneville

Indicates thin cover of the first unit overlying the second unit

Indicates unit(s) involved in mass movement

Although this product represents the work of professionalscientists, the Utah Department of Natural Resources,

Utah Geological Survey, makes no warranty, expressedor implied, regarding its suitability for a particular use.

The Utah Department of Natural Resources, UtahGeological 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.

FEET

Sea level

4,000

8,000

-2,000

2,000

6,000

10,000

METERS

2,500

1,500

500

-500

3,000

2,000

1,000

Sea level

-1,000

P a h v a n t R a n g ePavantthrust

Pavantthrust

A NORTHWEST SOUTHEAST A'

FEET

-8,000

-4,000

Sea level

4,000

8,000

-6,000

-2,000

2,000

6,000

10,000

METERS3,500

2,500

1,500

500

-500

-1,500

-2,500

3,000

2,000

1,000

Sea level

-1,000

-2,000

P a h v a n t R a n g e

Pavantthrust Corn

CreekRed Ridge(?)

thrust

WoolseyRidge

B NORTHWEST SOUTHEAST B'

FEET

Sea level

4,000

8,000

2,000

6,000

METERS

2,500

1,500

500

2,000

1,000

Sea level

Red Ridgethrust

C NORTHWEST SOUTHEAST C'

FEET

Sea level

4,000

8,000

2,000

6,000

METERS

2,500

1,500

500

2,000

1,000

Sea level

CoveCreek

Red Ridge(?)thrust

D NORTHWEST SOUTHEAST D'

FEET

Sea level

4,000

2,000

6,000

METERS

1,500

500

2,000

1,000

Sea level

B l a c k R o c kD e s e r t

Georges synclineC r i c k e t M o u n t a i n s

Precambrianstrata

E WEST EAST E'

Piute Co.

OTHER INFORMATIONMAP UNITAGE MAPSYMBOL

0-300± 0-90±Alluvial, eolian, glacial, and Lake Bonneville deposits

Basalt of Ice Springs0-200 0-600-1000-120 0-40

0-200 0-60

0-800 0-2500-300 0-90

0-200 0-600-1,000 0-3000-500 0-150------ ------

0-200 0-60

0-200? 0-60?

0-650 0-200

0-3,500 0-1,070

0-200 0-600-866 0-264

2,000± 600±

177-566 54-172

1,876 572

1,160 353

817 249

538 164

1,545 471

82-160 25-49

575 175

185 56

710 217

100+ 30+

1,970 600

200-265 60-80

850± 260±

800± 245±

4,000+ 1,200+

Basalt of Tabernacle HillBasalt of Pahvant Butte

Rhyolite of White Mountain and Mineral MountainsBasaltic andesite of Cedar Grove (cg), Cove Fort (cf)

Basalt of Kanosh, Beaver Ridge and Mineral Mountains

Fine-grained lake sediments (lf); alluvial-fan deposits (af)Basaltic andesite of Burnt Mountain

Rhyolite of N. Twin Peak, S. Twin Peak, Mid-DomeBasalt of Cove Creek

Basalt of Lava Ridge

Tuff of Holden

Joe Lott Tuff Member, Mt. Belknap Volcanics

Tuff of Albinus Canyon

Tectonic melange beneath Pavant thrust plateCanyon Range Conglomerate, Conglomerate of Mineral Mtns.

Navajo Sandstone

Chinle Formation, upper member

Moenkopi Formation

Queantoweap Sandstone

Kaibab Limestone

Pakoon Dolomite

CA

MB

RIA

NPR

ECA

M.

MID

DLE

MIS

S.S.

PER

MIA

NOR

DOVI

CIAN

IP.

CR

ET. PA

LEO.

-EO.

TERT

IARY

PLIO

CEN

EQ

UAT

ERN

ARY

2,400 ft(735 m)

850 ft(260 m)

700 ft(210 m)390 ft

(120 m)

AjaxDolomite

OpexFormation

Upper andMiddle

Cambriancarbonate

rocks

OphirFormation

TinticQuartzite

Paleozoic sequencelisted above is part

of the parautocthonousPavant thrust plate

in the eastern part ofthe quadrangle.

Redwall Limestone

Cove Fort Quartzite

ProspectMountainQuartzite

Limestone ofCricket Mountains

Whirlwind Fm.Dome-Chisholm

(Peasely)-Howell Fms.

Pioche Formation

Notch Peak Fm.

Cambrian rocks above are exposed in the Cricket Mountains (on theCanyon Range thrust plate), and are partially exposed and structurallythinned in the Mineral Mountains

660?-4,000? years old

0.4 and 0.5 Ma, respectively0.3 and 0.5 Ma, respectively0.5 to 0.9 Ma

0.7-2.0 Ma in Sevier Lake2.1 Ma2.35-2.5 Ma

Lacustrine

Freshwater limestone,bioturbated

Clayey, prone to slump

Cherty; 497 feet (152 m) thickin subsurface

Tricrepicephalus

Glossopleura

Intraformational conglomerate

Diagram is schematic-- no fixed thickness scale

Basaltic andesite of Red and Crater KnollsBasalt of Black Rock, Andesite of Beaver Ridge

Limestone of Twin Peaks

Rhyolite of Cudahy Mine, Rhyodacite of Coyote Hills

Intrusions and gneiss complex in Mineral Mountains

Osiris Tuff

Granodiorite of Mineral Mountains

Three Creeks Tuff Member, Bullion Canyon Volcanics

Volcanic rocks of Dog Valley

Green River Formation

Flagstaff Formation

Breccia of Cat CanyonNorth Horn Formation

Chinle Formation, Shinarump Conglomerate Member

Callville Limestone

LOW

ERU

PPER

Guilmette Formation

Simonson Dolomite

Sevy Dolomite

Laketown and Fish Haven Dolomites, undivided

Eureka Quartzite

Pogonip Group

566-1,000 173-300

150-180 45-55

1,125-1,200 343-350

Orr Fm, upper mbrs.Orr Fm, Big Horse Mbr.

Wah Wah Summit - TrippeFms., undivided

Banded gneiss in Mineral Mountains

DEV

ON

IAN

TRIA

SSIC

JUR

.O

LIG

OC

ENE

OakCity Fm.0-2,000 ft(0-600 m)

0-400 0-1200-262 0-80

0-650 0-200

0-2000-120

0-720 0-220

0-1,200 0-370

0-800 0-245

0-165 0-500-2,500 0-760

69-274 21-83

445 136

0-30

0-200 0-60

Stock

0-400Stock

est.3,300 ft

(1,000 m)

405 122656 200

1,420± 433±

14,320 yrs B.P.

1.0-1.5 Ma

2.55 Ma

2.5 Ma2.6 & 2.7 Ma

10.5-10.8 Ma?11-25 Ma

19 Ma, from Mt. Belknap caldera23 Ma, from Monroe Peak caldera

25 Ma25.3 Ma27 Ma

~33 Ma

Hiatusandunconformity

Sandstone and pebbleconglomerate

Eolian, cross-bedded

Ripple marks, marine fossils

Fossil corals and gastropods

Stromatoporoids

Light-gray dolomite

Orthid brachiopods at top

Ehmaniella

Eldoradia

NOTE: Ma agesare from K-Ar data

and may containsubstantial error.

Most units are localand thus not

superposed on oneanother. Stackingon this chart is a

best estimate. Somethicknesses wereestimated from

topographic maps.

MIO

CEN

E

THRUST FAULTED BASE

Top not preserved inmap area

1,750 Ma

Trace fossils

Pink vitreousquartzite

Pinyon Peak Ls equivalent

*Unit mostly in Beaver County

THICKNESS SCHEMATICCOLUMN

?

Aurora Formation 0-1,200 0-360Dipping Vat Formation, older volcanic rocks ~600 ~180 Age uncertain

38-40 Ma

Tuff of Dog Valley 400± 120±

Volcanic rocks of Wales Canyon 440 135

Quartz monzonite of Mineral Mountains

0-60

18 Ma

Syenite (sg) and gabbro (gp) of Cedar Grove ~23 MaIntrusions

600-1,000 180-300Sevier River Formation------ ------Rhyolite of Gillies Hill ~9 Ma

5 to 14 Ma

~1.0 Ma

Feet Meters

33.6 Ma Ar/Ar

Crazy Hollow Formation 0-350 0-107

--------

Q

Qal1

Qal2

Qal3

Qaf1

Qaf2

Qac

Qmu

Qmt

Qms

Qed

Qea

Qpm

Qst

Qsa

Qgt

Qdf

Qdg

Qlg

Qls

Qll

Qlm

Qla

Qvb1

Qvb2

Qvb3

Qcg

Qvr4

Qcf

Qvrd

Qvrt

Qvb4

Qvb4

Qvb4

Qrk

Qck

Qvb5

Qva5

QTlf

QTaf

Tbm

Trt

Tcc

Ttl

Tcr

Toc

Tse

Tb

Trg

Tht

Trd

Tp-Cg

Tdd

Tgd

Tsm

Tqm

Tdm

Tmd

Tmr

Tmj

Tmb

Tmm

Tmh

Tmf

Tmi

Tmpu

Tmpi

Tci

Tmps

Tmpl

Tmpa

Tmpf

Tmpb

Toi

To

Tisg

Tigp

Tgm

Tzt

Tsg

Taa

Tba

Tda

Tac

Tcp

Tbc

Tbci

Tm

Tbct

Tql

Tw

Kcg

Kc

Ktm

Jn

TRcu

TRcs

TRm

P

Pk

Pq

Ppk

IPM

IPc

Mr

D

Dg

Ds

Dsy

SO

SOu

O

Oe

Op

-Cu

-Ca

SOu

Dc

Op

-Ca

Qlf/QTaf

Qms (TRc)

Toi,To

Tzt

Tsg

Taa

TcpTbc

Tbci

Tbct

Tql

TdaTba

Tac

Tmps

Tmpi, Tci

Tmj

Tmb

Tmm

Tmh

Tmf

Tmi

Tmpl

Tmpa

Tmpf

Tmpb

Tmd

Tmr

Tb

Tmpu

131,7

1,7

1,10

2

1,7

1,8

2,3

1,9 1,4

2,5

2,17

2,11

132,61

1,6

11

2,20

2,17

1,18

13 19

2,5 16 12 14

15

CANDLA

NDSP

RING

BORDEN

SAND R

IDGE

TABE

RNACLE

HILL

MEADOW

FILLM

ORE

MT. CAT

HERIN

E

BEEH

IVE

PEAK

CAT C

ANYO

N

CRUZ

BLAC

K PO

INT

SIXM

ILE P

OINT

KANOSH

SUNSE

T PEA

K

WHITE PIN

EPEAK

BLAC

K ROCK

ANTE

LOPE

SPRIN

G

ANTE

LOPE

VALL

EY

DOG VALL

EYPE

AK

RED R

IDGE

JOSE

PH P

EAK

READ

PINNAC

LEPA

SS

CINDER

CRAT

ER

COVE FO

RT

ELSI

NORE

TRAI

L MOUNTA

IN

RICHFIE

LD

ANNAB

ELLA

MONROE PE

AK

ANTE

LOPE

RANGE

MARYS

VALE

CANYO

N

Tlr

Tcr

Oe

TR

Tdt

Tdv

Tov

Tdvt

Tau

Tch

Tg

Tf

Tfuw

Tfur

Tfmw

Tfmr

Tflw

Tflr

Tbr

TKn

QlfTvs

T.D. 8,762 feet

-CumQ

-Cop

-Cop

-Ct

TRTR

P

IPM

D

SO

Sunset Canyonwell (60-1)

Jn

Subsurface structure conjectural

IPMD

TRJn

-Ct

-Cop

OD IPM

?

?

Tf

SO

-Cum ?

Thin surficial deposits not shown

-Cop

SO

Thin surficial deposits not shown

Paxtonwell

(82-3)

splay(?) thrust

splay thrustPaxton thrust

Jurassic strataT.D. 14,826 feet

TR

P

IP

M/D

D

MM

Tf (+ TKn?)

?Tvs

?

?

??

TR

IPM

Jn

PIPM

PQQ

-Ct -CumO

SO

D -Cambrian

IPM

PTR

Subsurface structure conjectural

Millard County Sevier County

-Cop Tf

-Cop

-Ct

-Ct

-Cu+-Cm

-Ct O SO

SO

OO

D

D

SO

D

IPM

IPMIPM

P

IPM

IPM

P

P TRTR

PP

TRP

Tf

Jn

IPM

Tvs

Modified from George (1985) and Davis (1983)

PP

Q

O-Cu

TR

Thin surficial deposits not shown

IPM

D

SO

Thin surficial deposits not shown Subsurface relationships conjectural

? ? ??

TR

SO

No log, fractured

OTvs

D IPM

P

IPM I-15P

TR

-Cu

IPMD

SOTvs

O?

?

Tvs

Paleozoic andMesozoic(?) strata

ProbablyPaleozoic strata

T.D. 5,209 feet

Tvs Tvs Tvs

Well78-3P Tvs

Probably folded Paleozoic strata

TvsSO

?

PTR -Cu

Q

??

?Tbci

Tf

-Cl

-Cl -Cl

-Cm-Cm-Cm

-Cm-Cl

Tbr Q Tbr -CuQ

-Cl-Cu +-Cm

Tvs

Some thin surficial deposits and faults with offset not shown

Q-various

Qvb1

Qvb3

*Qrk,*Qck

Toc

Qcg,Qcf

TccTtlTlrTcr

Tac

Tht*various

TmjTo

Tgm

Tbct

Tdv

Trt

Qvb2

Qvb5,Qva5

Qvb4

Qvr4,*Qvrt,*Qvrd

Tf-various

KtmKc,Kcg

Jn

Pk

Pq

Ppk

IPc

Mr

Dc

Dg

Dsy

Tg

TbrTKn

TRcu

Ds

SOu

Oe

Op

TRcs

TRm

C- a

C- ox

C- op

C- t

OC- n

C- ob

C- wt

C- cm

C- w

C- dh

C- p

C- pm

pC- g

C- um

C- ou

TchTau

Tdvt, TovTdt

Tw

Tqm

*Tisg, *Tigp

QTlf,QTafTbm

Tse*Trg

-Cox

-Cum

-Cop

-Ct

-Cu

O-Cn

-Cou

-Cob

-Cm

-Cwt

-Ccm

-Cw

-Cdh

-Cl

-Cp

-Cpm

p-Cg


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