geologic map of the richfield 30' x 60' quadrangle
TRANSCRIPT
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
1210
9
17
20
18
16
22
17
202
45
45
70
30
60
30
30
40
9
5
4
5
7
585
8
75
43
25
4
840
50
45
15
126
7
12
2
36
105
20
17
30
16
18
19
3121
28
15 30
17
17
229
11
11
20
15
12
48
80
25
305
10
4
4
8
8
7
8
8
7
10
20
10
15
2547
1021
23
15
26
26
11
24
18
15
1514
30 20
25
15
105
5
6 7
10
10
7
10
7
20
7
10
6
10
1211
14
9
10
11
910
625
20
20
30
303025
15
25
20
10
20
10
25
28
3555
5
15
50
46
3024
30
45
25 40
16
60
40
5
20
510
30
20
30
50
14
20
13
18
45
40
45
20
35
55
4050
25
5550
40
65
605
8
10
7
10
85
7
6
2535
30
35
4020
30
30
20
10
40
1737
15
20
20
10
15
45
1520
15
15
12
3
9
10
12
20
20
20
20
9
8
2323
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
1025
15
10
25
15 10
15
10
25
8
10
15
45
60
30
2
2
5
10
25
1510
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
FAU
LT
MONROE
PEAK
CALDERA
ZON
E
ELSI
NORE
FAULT
ZONE
SEVI
ER
FAU
LT
ZON
E
RED
RIDG
E
THRUST
PAVA
NT
THRUST
Dsy
Toi TseQac
TmjQacTmi Tmpu
ToiTmr
TmpuTmr
Tmj
Qms Tbc
TmjTmpf
Qms
TmrTmh
Tmh Tmpl
Tmj
TbcQms
TmplTci
TmbTmf
QmsTmj
Qaf2Tisg Qac
Tmpf
Tmpi
Tmh
Qms
TbcToi
TrdTddQms
QacQms
TigpTmjTrd QacTbc
TmiTsmp-Cg
Qac Tbci
Tmi
Qst
Toi
Tgd To
Qms
TciTmjTo
Tmb Tci
Qms
Qal1
TbcQaf2Tbci Tmpl
Tmpf
TmplToTbci
Tmpl
Qal1
Tmi
TqmTsm
Tgd
Qms
TmiTbTrd
Tmpl
Tp-Cg
Qms TseQms
TbciTbc Tci
Tp-CgTqm
TbcTmd
Tmd
Tm Toi
Tmj
QvrtTdd
Trd
TmplTbcQTaf
Qaf1Tbc
TmbTmpf
Tse
Tbci
QmsTmi
Tmb
Tmb Tmi
ToiToi
Tmpf
Tbct
QckTbci
Qac QacTgd
Tmm
TmpiTsm
Tmd
Qvrd
Tbct
Tbc
Tmpi
TbcTmps
TmplTbcTmj
Trd Qms
Tbct
TmpsTp-Cg
TrgTbc
ToiTrd
Tmps
Trg
TseTbc
Tbc
Tmb
Tmpf
TmjQac
Tbc Toi
Qll
TmjTmd
Trg
Tmpf
Qaf2
TrdTsm
Tgd
Tp-Cg
Tgd
Tac
Trg
Tmj
Trg
Qms
Qaf2
TmpiTqmQms
Qlg
ToiTmj
Tmpl
Qaf2To Tmpi
TbctTbc
Qms
Qms
Tmj
TmjTmpf
Tb
Tbci
TgdTb
Toi
Qac
Qms
Qms
Qea TbcTrd
Qms
Qaf2Tmpl Tmpf
Tbc
Tac Tmpu
Qac
TbcTrg
TbciTrd
Tgd
Tmpl
TrdTdm
Tbct
Tmps
Qms
Qla
Tmpl
Tbc
Tb
Tmj
Qea Tmj
Qal1
QeaQaf2
Tmpf
Tsm
Tmj
Tmpf
Tmj
Tmj
Tmpf
Qgt
Trd To
QllTp-Cg
TmjQaf2Qms
Trd
Tbc Tmpa
QmsToi
Qlg
TbciTmpl
Qms
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
TmjTbct
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
QmsTse
Tdm
Trd
QeaTqmTbct Tmj
Tmpb
Qms
TbcQea
Qms
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
Tbc
Tmj
To
Tgm Tmj TbcQac
TdmTdm
Tbc
TbctTgm
Tse Qal1
Tqm
Tba
Tmj
Qcf
Qaf1
Tzt
Tmj
Tse
Qed
ToQea
QeaTse
Qac
p-CgTmjTbctTmj
Tmj
Tbc
TseTo
Qaf1
Trd
Tse
Tdv
Tzt
Qaf2
TmjTzt
TmjTbc
Tbc
To Qms
Qms
Tmj To
To
Tac
TztTmj
Trd
ToTmj
To
Qaf1Tse
QeaTmj
Tbct
QmsTse
Tmj
Tmpi
Qaf1
TrdTrd
Tse
Qaf2
TmjTac
ToTrd Tzt
To
TztTztTdv
Qvb4
TztTse
Tac
QeaToTcc
Qms
To
TaaToTo
To Tzt
Qal1
TrdTo Tmj
TwQea
Tbct
Tac
TztTo
Qaf2
Tac
Qaf1
Tcc Tw
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
-CpTdv
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
TfmrQms
(Jn, TRcu)
Ppk
Qac
Qlf
IPc
Tf
KcJn
Qlg Qac
TKn
Qaf2
Jn
Ppk
Jn
Qlf/Qvb4
Qla
Pk
TRcu
Tfmr
TRcu
Kc
Qed/Qlf
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
-Cob
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
Tbr QTlf
TKnTflr
Tflr
QmsTg
Tf
Qaf1
Tfmr
KcQlf
Tg
Qlf
Tflw
Qac
Tg
Qac
Qvb2
Tbr
TfmrTRcu
TgKtm
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
-Cwt
Qal2
Toc
-CwQla
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
-Cpm
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
-Cum
TRm
-Cop
Qlf
Qlf/Qvb4-Cwt
Qaf2
Qaf2
Qaf2
-Cob
-Cob-Cou
-Cob
-Cwt-Cwt
-Cwt
-Cwt
-Cob
-Cwt
-Ccm
-Ccm-Cdh
-Ccm
-Cw
-Ccm
-Cdh
-Cdh
-Cdh-Ccm
-Cw
-Cw -Cw
TRcs
Tbr
-Ccm
-Cum
-Cwt
-Ccm
-Cdh
-Cwt
-Cob
-Cob
-Cob
Qlf
Qlf/Qvb4
Qlf/Qvb4
Qlf
Qal1
Qal1
-Ct
-Ct
-Cum
-Cum
TflrTflr
Tflr
Tflw
TfmwQaf2
-Cop-Cob
-Ccm
Tbr
-Cdh -Ccm
Qaf2
Jn
Qlf
Qlf
Qal1
Qal1
Qal1
Qal1
Qal1
Qaf1
Qla
Qla
TRm
-Ct
-Ct
-Ct
-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
-Cp
Qaf2
Tbm
Tcc
Qaf2
Tac
Tac
Tbct
Tbct
Qcf
Qaf2
Tdv
Qaf2 Qaf2
Taa
Tbc
Tbct
Qaf1
Qaf1
TmjQaf1
Tbc
Qaf2
Qaf2
Qaf2Qaf2Qaf2
Qaf2
Qaf2
Qed
Qaf1
Qaf1
Trg
Qcf
Tbci
Tmj
Tse
Tmj
Qaf1
Toi
Toi
Qaf2
Qaf2
Qaf2
Qaf2
Qal1Qlf
Tbr
Qls
Qac
Tfuw
Qaf2/Qvb5
Qaf2
Qaf2
Pk
Qaf2
DgPpk
TdvPk
Qaf2
Jn
TdvTac
Tbc
Tmj
Qaf2
Tmj
Tmj
Tmb
Qla
Qlf
Qlf
Qlf
Qaf2
Tcr
Tcc
Tsg
Qaf2
Tse
Trd Trd
Qal1
Tse
-Cdh
-Cdh
TRm
-Cou
-Cwt
Tbct
Tse
-Cp
Qed/Qvb2
Dg
Tbci
Tsg
Jn
Jn
-Cum
Qaf2
-Ccm
TRcs
Qaf2
Qal1
Tf
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'
C
C'
D
D'
EE'
38°30'112°00'
39°00'112°00'
39°00'113°00'
38°30'113°00'
R 10 W 330000mE
850 000FEET
(SOUTH)
T 21 S
1 600 1 600 00 FEET (SOUTH) 34R 9 W 1 625 1 625 45' R 8 W 1 75038R 5 W30' 1 725 1 7251 700 1 700 R 6 W1 650 1 675 1 675 36R 7 W R 4 W 391 775 15' 1 800 1 800 R 3 W 40 1 825 1 825 R 21/2 W 1 850 000 FEET (CENTRAL) R 2 W
431
T 21 S
FEET225 000
(CENTRAL)
825
200
800
T 22 S
430
175
775
T 23 S
429
45'
150
750
T 24 S
125
428
725
100
T 25 S
700
4270000mN
75
675 000FEET
(SOUTH)
T 26 S
R 2 W1 850 000 FEET (SOUTH)1 825400000mE1 800 1 8001 775 1 775 39 15'38 1 7501 725 1 725 R 5 W3730'R 6 W1 700 1 700361 675R 7 W1 650 1 650R 8 W45'34 1 625 1 6251 600 1 600 R 9 WR 10 W
75 000FEET
(CENTRAL)
675
700
100
427
T 26 S
T 25 S
725
428
125
750
150
T 24 S
429
45'
775
175
T 23 S
430
800
200
T 22 S
225
4310000mN
MT.
BE
LKN
AP
CA
LDE
RA
B
B
B
P
P
P
P
P
P P
P
P
P
P
P
PP
P
P
P
?
?
?
?
B
BB
B
B
B
B
B
B
B
BB
B
B
B
B
B
B
B
B
B
BB
B
B
B
B
B
B
B
B
B
P
P
PP
P
P
P
P
PP
P
P
P
P
P
P
P
P
P
P
P
P
P
P
P
P
P
P
P
B
BB
B
B
B
B
B
B
B
B
BB
B
B
B
B
B
B
B
BBB
BB
B
B
B
B
B
B
B
B
BB
Qcg
TE
RT
IA
RY
Tvs
Jn
TR
Jn
TRIA
SS
ICJU
R.
CR
ET.
TRm
Tht
Toc
TRcs
TRcu
TKn TKnKcg
Kc Ktm
Tf
?
?Tbr
?
?
Trg
Tcr
Tlr
Ttl
Tcc
Trt
Tbm?
?
Major unconformity
Q
?
Qls
Qal1
Qac QeaQed
Qgt Qdg
Qpm
QmsQmu Qst
QlfQdf Qlg
Qaf1
??
Qal2
Qll Qlm Qla
?
QTlf
?
?
Qaf2
QTaf
?
?
Qvb2
Qvb1
?
??
?
Qcf
Qvb3
Qvr4
Qvb4
Qvb5
Qva5
CrossSections Map
Plio
cene
QU
AT
ER
NA
RY
Ple
isto
cene
Hol
ocen
e
Late
Mid
dle
Ear
ly
Qrk
Qck
?
Tse
Unconformity
Tw
Tdv Tdt
Tigp
Tisg
Tau
Tch
Tg
Tf
Tfuw
Tfur
Tfmw
Tfmr
Tflw
Tflr
QvrdQvrt
Qmt
?
?
?
?
?
Qal3
?
Qsa
?
M A R Y S V A L E V O L C A N I C F I E L D
Dc
SOu
D
OpO
C- cm
C- w
C- dh
C- p
C- pmC- t
Major unconformity
Unconformity
Unconformity
C- m
C- wt
C- ob
C- u
Oe
Dsy
Dg
Unconformity
CA
MB
RIA
NO
RD
OV
ICIA
NS
IL.
DE
VO
NIA
NM
ISS
.P
ER
MIA
N
C- ou
OC- n
Ds
Mr
IPc
IPM
P
Ppk
pC-P
EN
N.
SO
pC- g
C- t
C- op
C- um C- um
C- ox
C- a
Unconformity
Unconformity
Pq
Pk
Unconformity
Unconformity
C- l
C- op
Unconformity
Tb
Tql
?
?
Tgm
Tdm
Tp C- g
Trd
Tdd
Tsm
Tqm
Tgd
?
?
?
?
Tmj
Tmr
Tmb
Tmm
TmhTmi Tmf
Tmps
Tmpl
Tmpf Tmpb
TmpaTmpu
Toi
Tzt
Tac
TbctTbc
To
Tda
Tcp
Taa Tba Tsg Tm Tbci
Tci
Tdvt Tov
Tbc
Tbc
Tmpi
Tmd
?
?
?
? ?
?
?
M I N E R A LM O U N T A I N S
42
65
6
P
B
(On map)?
(Shown vertical orinclined on cross section)
?
(Map)
?
(Cross section)
?
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