Ingersoll 1983

8/14/2019 Ingersoll 1983

1/18

i l ie Ai i ic i ic i in \ .MHi , i ( ' [ i o f Puiu i lc uni ( iL 'o lop is Is l l i il l c l ii i\ 6^ , N,K ^(J i iK I9 i ) , l> I 125-1 14: , 71 igs,. 6 Tablos

Petrofacies and Provenance of Late MesozoicForearc Basin, Northern and Central California^

RAYMOND V. INGER SOLL'

ABSTRACT

Data from the Great Valley G roup (sequence) representthe most complete information regarding sandstonepetrology of sediment derived from a magmatic arc. Thisinformation is useful in documenting tectonic and magmatic events within the arc and related terranes, and formsthe basis for the establishment of petrostratigraphic unitsfor mapping and correlation. Sandstone and conglomer

ate compositions are controlled by changes in provenance,many of which were basinwide and synchronous. Clay-mineral composition is controlled primarily by burialmetamorphism. Careful attention to sample collection,sample preparation, and petrographic techniques is essential for uniform results. Seven petrographic parameters(P/F, Lv/L , M, Q p/Q , Q, F, and LUsted in decreasingimportance to petrofacies discrimination) define eightpetrofacies (Stony Creek, Flatina, Lodoga, Grabast,Boxer, Cortina, Los Gatos and Rumseylisted in approximate order of decreasing age).

The Upper Jurassic-Lower Cretaceous petrofacies(Stony Creek, Flatina, and Lodoga) contain higher lithiccontents (supracrustal sources), whereas the Upper Cretaceous petrofacies (especially the Rumsey) contain higherproportions of plutoniclastic components (quartz, feldspar, and micas). The proportion of potassium-feldsparincreases from near zero in the Upper Jurassic to nearly50% of all feldspars in the uppermost Cretaceous.

The lower part of the Great Valley Group (Upper Jurassic and Lower Cre taceous) contains significant quantitiesof sedimentaclastic and metamorphiclastic materialeroded from accreted and deformed terranes ("tectonichighlands") formed by the arc-arc collision (Nevadanorogeny) that occurred prior to initiation of theFranciscan-Great Valley-Sierra Nevada arc-trench system. The Klamath Mountains area provided a major proportion of this detritus. Ophiolite and serpentinite detrituswas deposited locally near the base of the Great ValleyGroup as a result of deform ation along the east side of thegrowing Franciscan subduction complex. Volcaniclasticdetritus was fed into the entire forearc basin as magma-

Copyright 1983. The American Association of Petroleum Geologists. Allrights reserved.

'Manusc riptreceived, July 14,1982; accepted, December 16,1982.^Department of Geology, University of New M exico, Albuquerque, New Mex

ico 87131; present address, D epartment of Earth and Space Sciences, University of California, Los Angeles, California 90024.

I thank the following for help and advice during various parts of this study: S.B. Bachman, A. Basu, P. F. Bertucci, T. J. Bornhorst, W. R. Dickinson, S. G.Franks, S. A. Graham, D. G. Howell, C. F. Mansfield, R. W. Ojakangas, L. A.

Raymond, E. I. Rich, and R. A. Schweickert. Financial assistance was provided by NSF Grant D ES72-01728 A02 and by the Research Allocations Committee of the University of New M exico.

tism increased in the Sierra N evada area during the Cretaceous . As the volcanic cover was stripped off,plutoniclastic and metamorphiclastic detritus from theunderlying batholithic terranes was provided in abundance to the forearc basin. Crustal components were more"continental" in the southern Sierra Nevada and more"oceanic" in the northern Sierra Nevada, as demonstratedby the higher proportions of metamorphiclastic detritusand by the more felsic nature of volcaniclastic detritus to

the south. By the m iddle of the Late Cretaceous, extensivebatholithic terranes provided potassium-feldspar-richarkosic detritus to the entire forearc basin. By the Paleo-gene, arc magmatism had migrated eastward sufficientlythat deeper levels of the California part of the arc wereexposed by erosion, tectonic activity decreased in theforearc basin, and the basin was filled to sea level in mostparts.

INTRODUCTION

The late Mesozoic and P aleogene history of the forearcbasin of northern and central California (Fig.1) has beenreconstructed using stratigraphic, structural, petrologic,sedimentologic, and tectonic data in combination withactualistic models for arc-trench systems (e.g., Ingersoll,1978a, 1979a, 1982; Dickinson and Seely, 1979; Ingersolland D ickinson, 1981). Subduction-accretion, arc magm atism and forearc sedimentation initiated in the Late Jurassic (Tithonian, Fig. 2), following arc-arc collision(Schweickert and Cowan, 1975). During the latest Jurassicand all of the C retac eou s, the G reat Valley was the site of adeep forearc basin, within which the Great Valley Groupaccumulated (Great Valley sequence of Bailey et al, 1964;Ingersoll and Dickinson, 1981; Ingersoll, 1982). By thePaleogene, the forearc basin had filled to near sea levelthroug hout most of the Great Valley area (Dickinson et al,1979b) and subduction had been terminated sequentiallyby the northw ard m ovement of the Mendocino triple junction during the Neogene (Atwater, 1970). The upper Mesozoic strata filling the forearc basin record the history of themagmatic arc (Dickinson and Rich, 1972; Ingersoll,1978b; M ansfield, 1979), as well as the history of erosionof the crust on top of which and within which the arcformed. Sandstone petrology, in combination with conglomerate petrology and clay m ineralogy, provides the primary m ethod of determining the provenance of the GreatValley Gr oup , and hence the history of the magm atic arcand related features.

This paper is the produc t of years of work on the petrology of the Great Valley Group. This is the first study thathas involved the application of uniform methods by a sin-

1125

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11 2 6 Late Mesozo ic Forearc Ba sin, California

4IN2 0 W

S A N F R A N C I S C O \

0 20 40 60 80 100 kmI 1 1 1 U__l

SAN A N D R EA S FA U LT S Y S T E M

I I CENOZOIC SEDIMENTS AND VO LCA NIC S

1 = 1 F RA N CIS C AN A N D R E L A T E D R O CK S

\-i; : GREAT VALLEY GROUP

I I I I K L A M AT H - S I E R R A N E V A D A - S A L I N i A

IG N EO U S A N D M E TA M O R P H I C T E R R A N E S

I I SOW

FIG. 1Location map of northern and central California, showing principal components of late Mesozoic arc-trench system andgeographic locations. Great Valley includes both Sacramento and San Joaquin Valleys. Sierra Nevada igneous and metamorphic ter-ranes represent roots of magmatic arc, and Franciscan Complex represents highly deformed subduction complex formed landward oftrench. Great Valley Group is primarily Upper Cretaceous in San Joaquin Valley and is Upper Jurassic through Upper Cretaceous inSacramento Valley. Exposures of Lower Cretaceous and Upper Jurassic along west side of San Joaquin Valley are not discussed in thispaper (see Mansfield, 1979). Small outcrops of uppermost Cretaceous that nonconformably overlie Sierra Nevada basement alongeast side of Sacramento Valley are too small to show at this scale. Great Valley Group lies nonconformably on Klamath basement nearRedding. C oast Range oph iolite underlies Great Valley Group at other surface locations along west side of Great Valley (after Inger-soll, 1978a)

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Raym ond V. Ingersol l 1127

gle operator to rocks encompassing the entire age span(Tithonian throu gh Maestrichtian) and the entire length ofthe Great Valley (Sacramento and San Joaquin Valleys). Itis both a refinement of previous work, especially that ofDickinson and Rich (1972), Ingersoll (1978b), and Mansfield (1979), and a contribution of new data and insights

from areas not previously studied in detail. The petrologicdata represent the most complete information available onsandstone petrology from any forearc basin. In addition,the present study demonstrates the usefulness ofthe petro-facies concept both for provenance-tectonic reconstructions and for stratigraphic-correlation studies.

PREVIOUS WORK

Vertical stratigraphic variations in sandstone composition within the Great Valley Group have formed the basisfor stratigraphic mapping, provenance inferences, andpaleotec tonic recon struction s for several years (e.g.. Schilling, 1962;Ojakangas,1968;Gilbert and Dickinson, 1970;Swe and Dickinson, 1970; Rich, 1971; Dickinson andRich, 1972; Perkins, 1974; Ingersoll, 1978a, b, 1979b;Mansfield, 1979). Stratigraphically extensive petrofaciesbased on inferred original sandstone co mposition m ay beused to define petrologic intervals equivalent to formations (Dickinson and Rich, 1972). "Petrofacies" is usedhere in the more restricted sense expressed first by Mansfield (1971), based on detailed sandstone composition,rather than in the broader sense of Weller (1958), which issynonymous with "lithofacies," as most commonly usedtoday. In my usage, petrofacies is one type of lithofacies,and petrostratigraphy is one type of lithostratigraphy.

In general, sandstone composition is controlled by thefollowing factors: provenance, transportation, deposi-tional environment, and diagenesis (Suttner, 1974). However, sandstone composition of the Great Valley Group iscontrolled primarily by provenance, as demonstrated bythe immaturity of the detritus (both compositionally andtexturally), the close linkage between source areas andbasin, the lack of correlation between composition anddepositional environment, and the lack of destruction bydiagenesis of the key components (Ingersoll, 1978b).Thu s, in the GreatValley Grou p, transportation and depositional environment app ear to have been unimportant indetermining sandstone composition. The effects of diagenesis may be removed mentally by careful petrographic

work based on an understanding of thetypes of alterations(Dickinson et al, 1969; Ingersoll, 1978b).Studies of conglomerate petrology (e.g., Perkins, 1974;

Bertucci, 1980; Seiders, 1983) contribute additional data,and broadly confirm petrofacies and p rovenance interpretations based on sandstones. Such studies are especiallyuseful for correlating petrographic parameters to sourcerock types. However, conglomerates are not ubiquitouswithin the Great Valley Group, and they are much moretime-consuming to study in detail than are related sandstones (Dickinson and Rich, 1972).

Studies of clay mineralogy within the Great ValleyGroup (e.g., Ojakangas, 1968; Clark and Bond, 1978)

indicate that burial depth and depositional facies con trolclay-mineral types; therefore, clays are not useful as

L AT E J U R A S S I C -C R E TA C E O U S

TIME SCALEPETROFACIES

FIG. 2Radiometrictime scale usedin present study, and stratigraphic relations of eiglit petrofacies. Diagonallines denote general absence or paucity of strata. After Ingersoll (1979a); vanHinte (1976a, b).

provenance-determined petrofacies indicators. However,the roughly equal amounts of illite, chlorite, and m ontmo-rillonite are consistent with mid-latitude deposition andvolcanic provenance (Clark and Bond, 1978).

Techniques of detailed petrographic work on gray-wackes and arkoses (term s used in the broadest sense) wereoutlined first by Dickinson (1970). Subsequently, severalstudies have expanded on this work, and modified nomen

clature and procedures (e.g., G raham et al, 1976; Stewart,1976,1977,1978; Ingersoll, 1978b; Dickinson and Suczek,1979; Dickinson et al, 1979a; Ingersoll and Suczek, 1979;Ma nsfield, 1979; M oore , 1979). These studies involvesand and sandstone from a wide variety of tectonic settings, but all of the studied areas have in common rapiddeposition in tectonically active basins, resulting in thickaccumulations of compositionally and texturally immature sandstones.

SAMPLING

The Upper Cretaceous part of the Great Valley Group

was sampled extensively and studied petrographically byIngersoll (1976, 1978b). Sample locations can be found in

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1128 Late Mesozoic Forearc Basin, California

Table 1. Data Used In Present Study

S a m p l eN u m b e r

75-3775-3875-4175-6075-6575-10375-10475-11275-11475-11675-11975-12075-121

75-12575-12975-13175-13275-15775-16375-17775-17975-18175-18575-18775-188784-27784-29M C - 1 0

D P C - 6D P C - 7D P C - 9A P - 2 6 - 7J-22-3JA-10-6

75-5175-5975-14175-14375-14475-16475-17475-18075-18275-18475-19175-19275-19475-195

74-3574-3674-39

74-4174-70

Q

36

45

35

45

47

3941

33

37

37

3939

32

43

35

30

33

42

44

4346

38

39

40

39

48

41

34

374648

47

39

46

33

3137

38

35

44

43

40

4332

40

45

39

30

38

22

26

5235

Q F L %

Q m

35

42

34

44

46

3841

31

35

34

37

3831

41

34

29

33

42

43

42

45

38

39

3938

47

40

32

3744

44

44

38

43

32

29

35

37

34

43

4037

41

31

3944

39

29

37

21

24

5134

F

42

32

43

43

36

42

42

23

26

19

23

2018

36

21

26

40

40

40

4737

42

38

4536

43

51

49

433330

33

42

33

36

3437

39

39

37

37

33

42

53

41

43

4042

42

3927

3035

L

22

2322

13

17

19

18

4437

44

3841

50

21

44

44

27

18

16

1017

20

23

1625

10

8

17

1921

22

20

20

20

31

35

26

22

26

20

2028

1515

1912

2128

21

39

47

1830

Lt

23

26

23

13

19

2018

46

39

47

40

43

5122

45

46

27

18

17

11

18

20

23

1625

11

9

19

2022

26

23

2124

32

37

28

24

27

21

2330

17

16

2014

2129

22

40

50

1931

F R M W %

M

6

11

11

20

8

11

19

10

4

7

1712

1512

214

22

6

10

13

8

13

6

12

7

8

7

11

76

3

8

8

8

9

7

10

11

8

10

69

88

11

17

14

11

6

3

7

97

P/F

41

48

46

52

49

52

73

70

59

71

67

58

52

64

93

50

52

62

56

4641

43

45

5147

52

59

51

4241

59

62

59

61

63

7954

56

54

7054

50

5081

61

73

77

75

72

71

68

7360

Lv/L Qp/Q

RUMSEY

56

6079

84

78

7987

55

42

38

51

4532

48

47

45

6179

78

5740

5367

6061

56

49

69

5972

58

61

65

80

3

61

1

3

30

7

7

9

64

4

3

3

5

0

1

2

22

01

11

2

2

5

14

87

3

8

LOS GATOS

44

5337

51

49

39

3832

41

35

44

46

2531

5

65

5

3

2

6

6

33

2

3

01

CORTINA

69

73

74

6674

3

6

9

11

MYBP

84

82

74

74

73

82

82

76

76

80

77

77

77

77

75

74

74

72

76

737077

71

73

73

82

82

84

757680

73

7884

88

82

86

86

85

83

8687

85

89

83

85

8889

88

87

86

8885

D

360

360

365

515

495

180

180

105

105

110

125125

125

130

240

325

325

485

555

415415

425

430

445

445

290

280

290

360360

360

165

165165

575

525

385

385

385

555

410420

435

430

460

460

450450

150

150

150

145115

QpLvmLsm%

OP

4

11

2

2

6

6

0

5

6

7

64

2

5

34

0

3

5

85

02

32

910

9

17

15

14

515

5

56

8

4

4

11

7

86

4

10

01

5

3

5

32

Lvm

54

5377

82

7374

87

53

39

36

484332

46

4544

61

77

74

5338

5366

5860

51

44

63

5867

50

53

62

68

42

5035

46

47

38

33

30

3833

42

41

25

31

65

71

71

6473

Lsm

42

3621

16

20

19

13

43

5557

4653

6649

52

53

39

20

21

40

5847

32

38

38

40

46

28

4126

35

33

3317

53

45

59

45

50

58

55

63

55

61

54

49

7568

30

26

24

3326

LmLvLs%

Lm

38

3319

14

18

13

8

35

48

54

4048

6141

44

35

24

15

13

3544

36

29

28

29

34

40

22

298

25

33

32

15

55

4355

48

47

53

53

62

51

57

54

50

6957

26

2322

2120

Lv

56

60

79

84

78

7987

55

42

38

514532

4847

45

6179

78

5740

5367

60

61

56

49

69

5972

58

61

65

80

44

5337

51

49

39

3832

41

35

44

46

25

31

69

73

74

6674

Ls

6

7

2

2

4

8

5

10

107

987

11

920

16

5

10

816

114

1210

1011

9

1320

17

6

35

1

58

1

5

8

96

88

1

4

612

6

4

4

136

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Raymo nd V. Ingersoll 1129

Table I ((Ontinued)


74-7174-7474-7674-10374-10574-10675-875-1175-3675-8475-8575-8775-9075-9375-957 5 - 9 7 A75-97B75-9975-10275-13575-137784-18784-19M C - 4M C - 8NC-1NC-2NC-3NC-4NC-6

NC-7NC-8NC-9NC-15D-18-6F-18-3J-22-20

Q303428273425344143292631282822

282125403536494527463534303539

41353736353929

QFLO/o

Q m

293328243323313842282429262519

251823393334444226453333293438

40343634343827

F

505053422742403938464938434037

293135393940323141374041443940

35373937513846

L

201619313933262019252532293241

434840212624202532172625262621

24282427152325

Ll

211620344036292320272733313544

465143222726242833172727272722

25292529152527

F R M W ' t ^

M

664453644233342

324957446754556

6745

1086

J

P/1

616862585851645846585156505248

474662686966605569568463656568

63646266696365

1 A 1

837679847786707160768180737776

727170925050575481736153626661

48475161768573

Up Q

412

114

1178366489

11

111310236975134331

4337246

MVBI '

878687888688868486888888888482

828282838583848489868686868687

88888889828688

D

110135130354030

220220360

0005

1515

252525

180230230300305290290315315315315315

315315315310165165160

QpLvmLsmVo

Qp

6349388

146664776

756448

18114145341

6359566

Lvm

787476777480646156727677687172

676765894846474878725851606361

44454856727968

Lsm

162420142213272538221819252123

272728

74746364118273744373338

49524735231425

LmLvLsVo

Lm

16201612175

252323147

12186

12

1815105

3934273513232738232826

38473628221323

Lv Ls

83 176 579 584 477 786 970 571 660 1776 981 1280 873 977 1776 12

72 1171 1470 2092 350 1150 1557 1754 1181 673 461 1253 962 1566 661 13

48 1547 751 1461 1176 285 273 4

BOXER

74-174-474-2574-2774-2874-3074-3374-4474-4574-46'74-50

74-5474-5674-5974-6274-6474-6674-6874-69

74-7274-77

26214221363335353340252637262031303129

3138

22174219353032333138232635241628282926

2838

28303745303231292925293227263429273238

3036

4649213434353536383546

4337494640433732

3925

50532136353838384037484339515042464035

4226

1184467645442454253

46

64688279776988717880656257796592788268

8087

84798490887672746480919187718778708177

7447

16160

103897659067

19109S

10

102

95939095959089908995949490899389898989

8988

165170215165165150150145145145145135130100100100100115115

120130

8606378655506487669

74

77748485867166696075879181698173667670

6945

1520169

12222525351999

13281220281821

2351

7141055

192223311566

1122

914221419

2242

84798490887672746480919187718778708177

7447

9765756356323738855

411

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6/18


hihl i ' I l ( ( inl iruu'd)


74-84

74-8974-9274-9374-957 4 - K M )75-175-17

75-1875-35A75-35B75-78A75-78B75-8277-76784-6784-7784-8784-12N C - I ON C - 1 2N C - 1 4

75-4675-4975-5075-52

75-53

75-5575-57

75-14075-14975-15275-15975-16675-16875-16975-17075-172SL-3

77-7777-7877-7977-8177-8277-8477-8577-8677-87

77-89C77-89F77-9077-9177-92

77-9377-9477-95

Q31

363938342937292632432019463934263230342431

2826423033

253532282638232831272824

5333312929404840434630463042

384159

QFl.ff/

9 m

27

333334312736272329411817443228232927322027

2525402629

203430262434222529252521

3328201124342023271918371332

303857

I_

35

303029364142323233354042303032283035312736

2832372322

332830333039292231313522

1323198

383398

1888

281034

223734

I)

1

34

343133303021384235234039243234463834354833

4442214745

423739394323475138423754

3444506433274252394662256124

40217

1,1

38

373737333222414538244241263940494138375237

4742235149

473940404627495340444056

5449618238327169557474357735

48258

1 R M W ' o

M

4

173235213521634434414

711459

710774

11666572

22206702224509

519

P 1

58

768461656486537768926872758177798667848588

8170886669

706560605982797263616551

7889899783849347847185789583

828486

1 \ 1

85

905082748060858858667877626255516551614955

U P (.

12

81411954

101384

10104

1818128

127

1611

G R A B A S T

2439585141

333226494027183639343348

1124

1512

19456995987

1011

P L AT I N A

45333544243263

253146

183927

183810

3815356217146043386040205625

2182

N n HI'

95

928791889288939387879494889895929292959291

9589919494

928989888894949089898989

117123124125125125126126126128128125126125

125124123

1)

55

5050454535

21515515536036025251025

310315315310310315310

570575575520525

525525385390395560555400405405405405

2520201515101055

-5-5

155

10

101010

Qpl

.Qp__

9

815129467877558

1815669679

71898

104445

13256475

3710182213184125303716272231

171317

AIllL

1 Mi l

77

824272677656798254627473575147486146574650

2238534738

303125473824183436333046

28292935212737

237

95

133119

15339

s i l l " ' ( )

Ism

13

104316241938141139322122353138463244374741

7161394454

606571495763806157636350

3460534467552273335479604850

685474

L i i i

L m

9

93813131229

54

3923141224

832422138273833

7560294651

596769445562775750606640

2248134373339

95404475384941

273276

\\ 1.;

L,v

85

905082748060858858667877626255516551614955

2439585141

333226494027183639343348

45333544243263

253146

183927

183810

^'0..

Ls

6

1135

139

111083

118

111430137

1411131312

11

1327

81475

1148

1161

12

332051123

3428

37

4219441132

553014

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Raym ond V. Ingersoll 1133

/

/

5/ *','r.-

m-

FIG. 3Sample locations for lower GreatValley Group, Sacramento Valley. Solid line outlines Upper Jurassic-Lower Cretaceous outcrops, as shown on California Division of Mines andGeology state map sheets. Lines on left and top show arbitrarybase line and direction along which distances were measured.Afew samples in north have negative distances. Sample locationsfor Upper Cretaceous outcrops aregiven by Ingersoll (1976).

ings remained flexible as successive groupings were run.Stratigraphic and geographic positions were used looselyto constrain the movement of samples between groups(i.e., samples were moved freely to stratigraphically andgeographically neighboring groups, but were not movedto distant grou ps). Previous petrofacies g roups were combined (e.g., Grabast and Studhorse of Ingersoll, 1978b,

and M ansfield, 1979, were combined into one petrofacies,the Grabast of the present study), and a new petrofaciesgroup was defined (Platina). High-lithic and low-lithicvariants (e.g., Dickinson and Rich, 1972; Ingersoll, 1978b)were combined into single groups, thus decreasing theimportance of QFL percentages in petrofacies discrimination and increasing the importance of the other parameters. Interestingly, but not surprisingly, the ratio ofplagioclase to total feldspar (P/F) is the most importantfactor in discriminating the petrofacies. Bailey and Irwin(1959) first noted the stratigraphic significance ofpotassium-feldspar content in their pioneering study ofthe Franciscan Complex and the Great Valley Group in

northern California. The ratio of volcanic lithics to totalunstable lithics (Lv/L) is the second most important discriminating p arameter.

Several other parameters were tried before choosingthese seven. Of most interest, polycrystalline quartz (Qp)was added to the un stable lithics to form a total-lithics category, and QmFLt (Table 2) percentages were calculated.No significant change in petrofacies discriminationresulted; therefore, QFL percentages were retained asdefining param eters. The ratio of polycrystalline quartz tototal quartz (Qp/Q) was added as a seventh parameter(Dickinson and Rich, 1972, and Ingersoll, 1978b, usedonly six parameters) because of the high polycrystalline-quartz content of the lower Sacramento Valley petrofacies. Previous work (Dickinson and Rich, 1972) hadmisidentifled much of this fine-grained material as felsicvolcanics, a distinction that is difficult to make withoutproperly stained thin sections (W. R. Dickinson, personalcommun., 1979).

Once the petrofacies groupings had been established,means, standard deviations, and correlation coefficientswere calculated from all the data using a stepwise-regression-analysis program (UCLA BMD02R, revised12/24/75). In addition, super petrofacies were constructed for the Sacramento Valley, San Joaquin Valley,lower petrofacies (Upper Jurassic and Lower Cretaceous),and upper petrofacies (Upper Cretaceous). These fourgroups, along with the T otal group (all samples) were analyzed in the same m anner as the petrofacies.

The stratigraphic and geographic distributions of theeight petrofacies are show n in Figures2 an d 4. Some of theboundaries are time-transgressive and interfingering indetail, but the broad correspondence between stratigraphic position and petrofacies is clear. The southernboundary of the Platina petrofacies is not controlled bystratigraphic position, but apparently represents a lateralchange in source terranes from primarily Klamath provenance (Platina) to primarily northern Sierra Nevada provenance (Stony Creek and Lodoga). Undoubtedly, thispetrofacies boundary is gradational and is not precisely

defined locally. The lateral boundaries between the UpperCretaceous Sacramento Valley (Boxer and Cortina) and

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R a y m o n d V. Ingersoll 1135

SACRAMENTO

00

>>-LU

SACRAT^ENTO

00

Q:

>-LiJ

a:

DALINGA

^

tP

FIG. 4Generalized map showing geographic locations of outcrops of eight petrofacies. Fine lines denote outcrops; heavy lines showpetrofacies boundaries. Base map from Jennings (1977). Dashed horizontal lines indicate area of overlap between north part of map(left) and south part of map (right).

A possible regional unconformity (Peterson, 1967) andgeneral quiescence of plutonism in the Sierra Nevada during much of Lodoga deposition (Evernden and Kistler,1970) support this contention. The Huntington Lakeintrusive epoch (Early Cretaceous) affected sandstone

compositions more in the San Joaquin Valley than in theSacramento Valley (Ingersoll, 1978b; Mansfield, 1979).

The Boxer petrofacies (Cenomanian and Turonian)includes two contrasting types (quartzose and lithic variants) that fall into discrete fields on a QFL plot, but which

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Table 3. Means and Standard Deviations for Soven Parameters of Kighl Great Valley Petrofacies(Numbers of Samples Shown in Parentheses)

Parame te r

QFL

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R a y m o n d V. I n g e r s o l l 11 3 7

Table 4. Means and Standard Deviations for Seven Parameters of hour Super Petrofacies and TOTAL (iroiip(Numbers of Samples Shown in Parentheses)

Parameter

QFL% Q

QFL

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1138 Late Mesozoic Forearc Basin. California

Up Lm

RUMSEY-JONCl- '

OSGATO

rORTIN '-

BOXFRR .

GRABAS

F

(d)

UPRGVG.

PLATINRUMSEY-\ LODOGA

. \ STONCR BOXERR. '

ODRTIN

G R A B A & ,

OSGATO: \ A ,

1, RUMSEY-^,

Y GRABAS CORTIN^^

P\ ATIN

LOUOGA

QA,

yiOTAL

i \ ' ' VLOWGVG "v ^ V \- . J > \ \

(q)

UPRG\A3

TOTAL - . \ . y

(hi Qp

SJQVAI

'f:'--\-; - -TOTAL

VSACVAL TOTAL-

SACVAL

'L Lvm'^

# / \ \

vSJQVAL W / )S A C V A L - J ^ ^ X

/ V_Lsm Lv^ ^ L s

FIG. 7 Triangular plots of QFL (left), QpLvmLsm (center), and LmLvLs (right) for eight petrofacies (top row), TOTAL, upper(UPRGVG), and lower (LOWGVG) super petrofacies (middle row), and TOTAL, Sacramento (SACVAL), and San Joaquin(SJQVAL) super petrofacies (bottom row). See Table 2 for explanation ofterminology. See Ingersoll and Suczek(1979) for discussionof statistical significance of fields of variation determined by standard deviations.See text for discussion of plots.

son, 1975), coupled with the eastward migration of theSierra Nevada arc during the Cretaceous (Evernden andKistler, 1970; Dic kin son , 1973; Inge rsoll , 1978a, b,

1979a). The lowest occurrence of significant amounts ofpotassium-feldspar in the Great Valley Groupis within theLodoga petrofacies, which also contains the lowest occurrence of significant quantities of monocrystalline quartzand increased phyllosilicates (increased plutoniclasticdetritus).

North-south variations of petrofacies are illustrated inFigure 7 (g, h, i). These plots prim arily reflect th e contra stin crust ("continental" to the south and "oceanic" to thenorth), within which and on top of which the late Mesozoic magmatic arc was constructed (Burchfiel and Davis,1972; Kistler and Peterman, 1973; Ingersoll, 1978b). TheSan Joaquin petrofacies contain higher percentages of

plutoniclastic and metamorphiclastic detritus, whereas theSacramento petrofacies contain more volcaniclastic and

sedimentaclastic (supracrustal) detritus. These conclusions are supported by the positive correlation coefficientsrelating southerly distance to Qm, M , and Lm (Table5) for

the uppe r part of the sequenc e, and by the increasingly fel-sic nature of volcanic lithic fragments to the south (Ingersoll, 1978b). Correlations among most of thesecomponents for the lower petrofacies are insignificant,but correlation between Lv and distance is positive,reflecting distance from nonvolcanic sources in the Klam-aths. Sub-Upper Cretaceous petrofacies a re mostly absentin the San J oaq uin Valley (see Mansfield, 1979, for summary of the few data tha t exist), so that com parison of theSan Joaquin and Sacramento petrofacies is affected byage differences.

In summary, prior to the Late Cretaceous, primarilysedimentaclastic and metamorphiclastic detritus was

derived from the Klamath area, whereas primarily volcaniclastic detritus was derived from the Sierra Nev ada east of

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Raym ond V Ingersol l 1139

Table 5. Correlation Coefficients Between Distance and Age, and the I'elrographic Parameters for Four Super Petrofacies andTOTAL (.roup*

Petrofacies '

S A C VA L

SJOVAL

UPRGVG

LOWGVG

TOTAL

Disl .

**Age'

D- 0 . 3 7

M Y B P

D

0.18M Y B P

D

- 0 . 1 6M Y B P

D

- 0 . 0 1M Y B P

D- 0 . 4 6

M Y B P

Q

0.12

- 0 . 2 7 -

0,02

- 0 . 6 7 -

0.27

- 0 . 4 7 -

- 0 . 2 2 -

- 0 . 4 2 -

0.14

- 0 . 3 0 -

Q F L %

Q m F

0.30 0 .33-

- 0 . 5 3 - 0 . 5 5

0 . 0 1 - 0 . 11

- 0 . 7 2 - 0 . 5 1

0.28 0 .05-

- 0 J 2 - 0 . 1 5

-0 .02 0 .18

-0 .47 0 .01

0.32 0 .36-

- 0 . 5 6 - 0 . 5 8

l.

- 0 . 3 1 -

0.56

0.05

0.66

- 0 . 2 2 -

0.42

0 .06 -

0.30

- 0 . 3 4 -

0.58

Lt

-0 .38

0.64

0.06

0.69

-0 .23

0.45

-0 .08

0.31

- 0 . 4 0

0.66

FRMW" ' .

M

0.27

- 0 . 5 0

0.12

- 0 . 2 9

0.38

- 0 . 5 2

- 0 . 0 5

- 0 . 4 6

0.46

- 0 . 5 3

P/F 1

- 0 . 2 4

0 6 8 -

0.53

0.69-

- 0 . 0 6 -

o.y0.15

0.20

- 0 . 3 4 -

0 .71 -

A / L Q p / Q

0 , 1 4 - 0 . 3 5

-0.31 0.73

0,07 0.10

-0 .75 0 .65

- 0 . 6 2 - 0 . 2 6

0.09 0.52

0 . 3 8 - 0 . 1 7

0.32 0.43

- 0 . 1 2 - 0 . 4 1

-0 .21 0 .75

QpL.vmLsrr

Qp Lvm

- 0 . 3 9 0 . 1 9 -

0 . 5 5 - 0 . 3 8

0.08 0.07-

0 . 3 5 - 0 . 7 7

- 0 . 1 2 - 0 . 5 9

0.21 0.06-

- 0 . 4 6 0 . 4 5 -

0 .04 0 .31-

- 0 . 4 3 - 0 . 0 5

0 . 5 9 - 0 . 3 0

1%

Ls m

-0.05

0.21

- 0 . 0 9

0.71

0.62

- 0 . 1 0

-0 .27

- 0 . 3 6

0.24

0.10

LmLvLsi?^

Lm

0.03

- 0 . 1 2 -

- 0 . 0 2

0 .77 -

0 .65 -

- 0 . 0 6

- 0 . 2 9

- 0 . 4 2

0 .38 -

- 0 . 2 0 -

Lv

0 .14 -

-0 .31

0 .07 -

- 0 . 7 5 -

- 0 . 6 2 -

0 .09 -

0 .38 -

0.32

- 0 . 1 2 -

-0 .21

'o

Ls

-0 .27

0.54

-0 .19

-0 .21

-0 .17

-0 .04

-0 .10

0.17

-0 .38

0.56

'Cor relation coefficients are underlined if absolute value is greater than cutoff (2/vn )"S AC VA L = Sacramento Valley; SJQVAL = SanJo aquin Valley; UPRGVG = upperGreat Valley Group; LOWGVG = lower Great Valley Group; TOTAL ^ all

samples,^Correlations between distance and age for eacfi group.

the Sacramento Valley. During the Late Cretaceous, vol-caniclastic detritus was contributed by the entire SierraNevada arc, with greater amounts of metamorphiclasticdetritus in the south; plutoniclastic detritus increased withtime.

There are other interesting correlations d emon strated inTable 5. However, interpretation of m any of these correlations is complicated by the fact tha t many of the variablesare linked either ma thema tically or geologically. Of specialconcern is the fact that distance (increasing southward)and age (m.y. before present) are negatively correlated forthe SACVAL and TOTAL g roups . This correlation is dueto the lack of sub-Upper Cretaceous petrofacies in the SanJoaquin Valley as well as to better exposure of Upper Cretaceous petrofacies at the south end of the SacramentoValley than at the north end. T herefore, some correlationsin these two groups are artifacts of this samphng biasrather than being geologically significant. This problem

does not exist for the other three grou ps in Table5, as demonstrated by the lack of significant correlation betweendistance and age.

The primary way in which the present petrofacies differfrom those of Dickinson and Rich (1972) is in the recognition that the lower petrofacies (Stony Creek, Platina, andLodoga) contain significant proportions of nonvolcanicdetritus (Ingersoll, 1979b). !n addition, the Platina pe trofacies is newly defined as a sepa rate entity. Dickinson an dRich (1972) mentioned that petrologic characteristics atthe north end of the Sacramento Valley did not fit easilyinto the petrofacies subdivisions to the south. Theyincluded all of the sediments at the north end of the valley

in their Lodoga petrofacies, even though the bo ttom of thesection is significantly older than the lower Lodoga to the

south. Discriminant analysis suggests that the northernsandstones (primarily locally derived from underlyingmetam orphic terranes) are distinct enough from both theStony Creek and Lo doga petrofacies to warrant establishment of a new petrofacies. The Platina differs from theother two petrofacies in having higher Qp and Lm (primarily metasedimentary; Fig. 7b, c). However, as mentioned, the boundary between the Platina and the othertwo petrofacies is gradational and possibly intertonguing(Fig. 4). The Stony Creek and Lodoga become more vol-caniclastic in nature to the south (Table 5).

Recognition of significant quantities ofQp, Ls, and Lsm(sedimentaclastic and metamorphiclastic detritus) withinthe three lower petrofacies is supported by studies ofUpper Jurassic and Lower Cretaceous conglomerates(e.g., Bertucci, 1980; Seiders, 1983). Dickinson and Rich(1972) noted that chert was the predom inant clast type inthese conglom erates, without explaining the apparent lack

of voluminous chert in their sandstones. D etailed study ofthe paleontology of some of the chert clasts in the conglomerates confirms that source areas included bothKlamath and northern Sierra Nevada Triassic-Jurassicterranes (Bertucci, 1980; Seiders et al, 1979) which consisted of accreted "tectonic high lands" (intraoceanic arcs,subduction complexes, and related features) and locallyformed continental-margin arc terranes. These terraneswere accreted to North America an d/o r deformed primarily during the Late Jurassic during arc-arc coUision (Sch-weickert and Cowan, 1975; Irwin, 1981; Schweickert,1981; Ingersoll, 1982), the classic Nevadan orogeny Thus,when the late Mesozoic subduction regime was initiated in

the Tithonian, significant terranes of nonvolcanic rockprovided much of the detritus to the base ofthe Great Val-

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1140 Late Mesozoic Forearc B asin, California

ley Gro up . These sedimentaclastic and metamorphiclasticsediments resemble suture-derived detritus more than arc-derived detritus (e.g., Graham et al, 1976; Ingersoll andSuczek, 1979). This is demonstrated best by the fact thatthe Platina (and to a lesser degree, the Stony Creek andLodoga) overlaps the "mixed magmatic arcs and subduc-

tion complexes" and "suture belts" fields of Figure 6 ofIngersoll and Suczek (1979) (compare to Figure 7b, c ofthis paper). In contrast, all of the other petrofacies plotwithin or very close to the "magmatic arc" fields. Thisobservation has fundamental significance regardingpaleotectonic reconstructions of Ca lifornia in the Jurassicbecause the abundance of suture-derived detritus in thelower Great Valley Group is consistent with Schweickertand Cowan's (1975) model. Prior to the identification ofthis detritus, a major problem with the model of arc-arccollision during the Nevadan orogeny was the scarcity ofsubduction- and suture-related detritus in the Sierran foothills, where it "should" be (R. A. Schweickert, personalcom mu n., 1981). The present results suggest instead thatmost of this detritus accumulated in the newly formedforearc basin (Great Valley) west and south of the suturebelts.

Bertucci (1980) has suggested that Tithonian andValanginian conglomerates within the Stony Creek Formation are fundamentally different, with the former primarily consisting of chert-argillite assemblages and thelatter primarily consisting of volcaniclastic detritus. Mypoint co unts agree with his cobble counts w hereverwe collected the same units. However, Bertucci studied only oneValanginian conglomerate (Bidwell Point lens), whereas 1point-counted several Valanginian sandstones. TheBidwell Point lens apparently is unique within the StonyCreek Form ation, representing an unusually pure volcanicprovenance. Sandstones both above and below this unitconsist of the more common mixtures of volcanic, sedimentary, and metamorphic provenances. My point countsdelineate other sandstone and conglomerate units withvolcaniclastic components as significant as the BidwellPoint lens, but they are minor in volume. None of thecounted parameters shows a systematic differencebetween Tithonian and Valanginian, and all fall within theStony Creek pe trofacies, even though there are significantlocal variations in com position.

Local occurrences of "basaltic san dston es," detrital ser-pentinite, and other ultramafic sediments and volcanicswithin the base of the Great Valley Gro up (Dickinson an dRich, 1972) probably were derived locally from the underlying Co ast R ange op hiolite (Bailey et al, 1970; Ho pso n etal , 1981). Some of the "bas altic sands tones" were countedduring the present study and were found to consist of mixtures of probably locally derived basaltic detritus withprobably distantly derived "normal" Stony Creek detritus. Even where mafic volcanics are the dominant clasttype, the sandstones have Stony Creek characteristics.Bertucci (1980) demonstrated that Kimmeridgian(?) breccias at the base ofthe Great Valley Gro up consist of ophiolite detritus. Also, McLaughlin and Pessagno (1978)suggested that th e "basaltic sa nds tone ," pillow lavas, dia

base, an d breccias within the Great Valley Group and theCoast Range ophiolite all had common sources.

Also of local significance are detrital and protrusive ser-pentinites within the Stony Creek Formation (e.g.,Carlson, 1981a, b). Some Stony Creek sandstones nearthese protrusions (of Late Jurassic through Early Cretaceous age?) contain significant proportions of detrital ser-pentinite mixed with the dominant distantly derived

"typic al" Stony Creek detritus. It can be difficult to recognize this serpentinite detritus, especially with the highdegree of burial metamorphism that the Stony Creek hasexperienced. Most of the serpentinite clasts were countedas Lv and/or Lvm because they are altered ultramafic ormafic igneous rocks. Some were counted as M if they consist of coarse-grained single serpentine crystals or flakes.Extrabasinal ophiolite detritus (primarily from the Klam-aths and northern Sierra Nevada) shows up mostly as Lv,Qp, P, an d Ls. Presumably, serpentinite weathered rapidlyand could not be transported very far, so that Klamath-derived serpentinite probably is rare in the Great ValleyGroup. This conclusion is supported by the fact that significant quantities of identifiable detrital serpentinite havebeen recognized only in locations near known local serpentinite profusions.

Significant correlation coefficients were used to separate(negative) or group together (positive) various parameters

Table 6. Parameter Associations forTOTAL Group

Qm-F-K-M-LmF-K-Lv-LvmLt-Q-Qp-Lsm-LsM-Lm-Lsm

(plutoniclastic-metamorphiclastic)(volcaniclastic)(sedimentaclastic)(metamorphiclastic)

(Table 6) . The resulting groupings delineate the dom inantsource rock types for the Great Valley Group. Othergroupings are possible and some parameters may standalone in certain provenance settings (e.g., Lv may be theonly significant param eter co ntributed by certain volcanicprovinces). However, the groupings in Table 6 are suggested as the primary source types for the Great ValleyGroup as a whole. Potassium-feldspar probably wasderived from both plutonic and volcanic settings, whereasplagioclase does not show up in any of the groups, probably because it was ubiquitous in all source areas at alltimes. However, interpretation of correlation coefficientsbetween ratios, such as P/ F and Q p/Q ,is tentative, as discussed by Ingersoll (1978b). The associations in Table 6seem to be the best estimates for major source rock typesbased on statistically determined correlations and geologicreasoning.

CONCLUSIONS

The present study demonstrates the usefulness ofdetailed sandstone petrography in stratigraphic, provenance, and paleotectonic studies. The late Mesozoic andPaleogene magmatic-arc history is preserved within theGreat Valley Group and related strata, and magmatic-

tectonic events (many of which are basinwide) controlpetrostratigraphic characteristics.

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Raym ond V. Ingersoll 1141

The lower part of the Great Valley Grou p (Upper Jurassic and Lower Cretaceous) contains significant quantitiesof sedimentaclastic and metamorphiclastic materialeroded from accreted and deformed terranes ("tectonichighlands") formed by arc-arc collision (Nevadan orogeny) that occurred prior to initiation of the Franciscan-Great Valley-Sierra Nevada arc-trench system. TheKlamath Mountains area provided a major proportion ofthis detritus. Ophiolite and serpentinite detritus wasdeposited locally near the base of the Great Valley Groupas a result of deformation along the east side of the growing Franciscan subduction complex. Volcaniclastic detritus was fed into the entire forearc basin as magmatismincreased in the Sierra Nevada a rea during the Early C retaceo us. As the volcanic cover was stripped off, plutoni-clast ic and metamorphiclast ic detr i tus from theunderlying batholithic terranes was provided in abundance to the forearc basin . Crustal compon ents were more"continental" in the southern Sierra Nevada and more

"oceanic" in the northe rn Sierra Nevada, as dem onstratedby the higher proportions of metamorphiclastic detritusand by the m ore felsic nature of volcaniclastic detritus tothe south . By the middle of the L ate Cretaceous, extensivebatholithic terranes provided K-feldspar-rich arkosicdetritus to the entire forearc b asin. By the Paleogene, arcmagmatism had migrated eastward sufficiently that theCalifornia part of the arc was eroded to deep levels, tectonic activity was lessened in the forearc basin, and thebasin filled to sea level in most p art s.

The data presented here represent the most completedocumentation of the history and erosion of any mag-matic arc. Th e late Mesozo ic arc-trench system of Califor

nia may be used as a norm for comparison with othersystems because it is so thoroughly studied. However, thelocal history of any basin and related source areas must beunderstood on its own terms also , as demo nstrated by thepresent study. Speculations con cerning m agmatic-arc evolution in general must await additional detailed analysis ofother arc-derived sediments.

R E F E R E N C E S C I T E D

Atwater, T, 1970, Implications of plate tectonics for the Cenozoic tectonic evolution of western North America: GSA Bulletin, v. 81, p.3513-3535.

Bailey, E. H., and W. P. Irwin, 1959, K-feldspar content of Jurassic andCretaceous graywackes of northern Coast Ranges and SacramentoValley, California: A AP G Bulletin, v.43 , p. 2797-2809.

and D . L. Jone s, 1964, Franciscan and related rocks, andtheir significance in the geology of western Californ ia: CaliforniaDivision of Mines and Geology Bulletin 183, 177 p.

M. C . Blake, Jr., and D. L . Jones , 1970, On-land M esozoic oceanic crust in California Coast Ranges: U.S. Geological Survey Professional Paper 700-C, p.C70-C81.

Bertucci,P. F., 1980, Petrology and proven ance of Upper Jurassic-LowerCretaceous Great Valley Sequence conglomerate, northwestern Sacramen to Valley, California: Master's thesis. University of California,Davis, 143 p .

Burchfiel, B. C , and G. A. Davis, 1972, Structural framework and evolution of the southern part of the Cordilleran orog en, western UnitedStates: American Journ al of Science, v. 272, p. 97-118.

Carlson, C , 1981a, Sedimentary serpentinites of the Wilbur Springsareaa possible Early Cretaceous structural and stratigraphic linkbetween the Franciscan complex and the Great Valley sequence: Master's thesis, Stanford University, 105 p.

1981b, Upwardly mobile melanges, serpentinite prolusions andtransport of tectonic blocks in accretionary prisms: GSA Abstractswith Programs, v. 13, p. 48.

Clark, M. S., and G. C. Bond,1978, Clay mineralogy ofthe Upper Jurassic to Cretaceous section of the Great Valley sequence exposed atPutah Creek, in J. C. Kramer, ed.. Geologic guide to the northernCalifornia C oast Ranges Sacramento to Bodega Bay: Annual Field

Trip Guidebook of the Geological Society of Sacramento, 1978, p,115-129.

Dickinson, W. R., 1970, Interpreting detrital modes of graywacke andarkose: Jo urn al of Sed imentary Petrology, v. 40, p. 695-707.

1973, Widths of modern arc-trench gaps proportional to pastduration of igneous activity in associated magmatic arcs: Journal ofGeophysical Research, v. 78, p . 3376-3389.

1975, Potash-depth (K-h) relations in continental margin andintra-oceanic magmaticarcs: Geology, v. 3, p. 53-56.

and E. 1. Rich, 1972, Petrologic intervals and petrofacies in theGreat Valley Sequence, Sacramento Valley, California: GSA Bulletin,V. 83, p. 3007-3024.

and D. R. Seely, 1979, Structure and stratigraphy of forearcregions: AAPG Bulletin, v. 63, p. 2-31.

and C . A. Suczek, 1979, Plate tectonics and sandstone compositions: AA PG Bulletin, v. 63, p. 2164-2182.

K.P. Helmold, a n d j . A.S tein, 1979a, Mesozoiclithic sandstonesin central Oregon: Journal of Sedimentary Petrology, v. 49, p. 501-516.

R. V. Ingersoll, and S. A. Graham, 1979b, Paleogene sedimentdispersal and paleotectonics in northe rn Ca lifornia: GSA Bulletin, v.90 , Part I, p. 897-898; Part II, p. 1458-1528.

R. W. Ojakangas, and R. J. Stewart,1969, Burial metamorphismof the late M esozoic Great Valley sequence, Cache Creek, California:GSA Bulletin, v. 80, p. 519-525.

R. V. Ingersoll, D. S. Cow an, K. P. Helmold, and C. A. Suczek,1982, Provenance of Franciscan graywackes in coastal California:GSABulletin, V. 93,p .95- l07.

Evernden, J. F., and R.W. Kistler, 1970, Chronology of emplacement ofMesozoic batholithic complexes in California and western Nevada:U.S. Geological Survey Professional Pa per623, 42 p.

Gazzi, P., 1966, Le arenarie del flysch sopraeretaceo deH'Appeninnomodenese; correlazioni con il flysch di M onghid oro: M ineralogica etPetrograph ica A cta, v. 12, p. 69-97.

Gilbert, W. G., and W. R. Dickinson, 1970, Stratigraphic variations insandstone petrology. Great Valley sequence, central Cahfornia Coast:GSA Bulletin, v. 81, p. 949-954.

Graham, S. A., R. V. Ingersoll, and W. R. Dickinson, 1976, Commonprovenance for lithic grains in Carboniferous sandstones from Ouachita Mountains and Black Warrior basin: Journal of SedimentaryPetrology, v. 46, p. 620-632.

Hopson, C. A., J. M. Mattinson, and E. A. Pessagno, Jr., 1981, CoastRange ophiolite, western California,in W. G. Erns t, ed., Geotectonicdevelopment of C alifornia: Englewood Cliffs, New Jersey, Prentice-Hall, Inc., p. 418-510.

Ingersoll, R. V., 1976, Evolution of the Late C retaceous forearc basin ofnorth ern and central California: PhD thesis, Stanford U niversity, 200P-

1978a, Paleogeography and paleotectonics of the late Mesozoicforearc basin of northe rn and central California,in D. G. Howell andK. A. McDougall, eds., Mesozoic paleogeography of the westernUnited States: SEPM Pacific Section, Pacific Coast PaleogeographySymposium 2 , p. 471-482.

1978b, Petrofacies and petrologic evolution of the Late Cretaceous forearc basin, northern and central California: Journal ofGeology, v. 86, p. 335-352.

1979a, Evolution of the Late C retaceous forearc basin, north ernand central California: GSA Bulletin, v. 90, pt. 1, p. 813-826.

1979b, Petrofacies and proven ance of the lower part of the GreatValley Sequence, Sacramen to Valley, California: G SA A bstracts withPrograms, v. 11, p. 85-86.

1982, Initiation an d evolution ofthe Great Valley forearc basin ofnorthern and central California, U.S.A.,in J. K. Leggett, ed.,Trench-forearc geology: sedimentation and tectonics on modern andancient active plate margins: Geological Society of London Special

Publication 10, p. 459-467.and Dickinson,W. R., 1981, Great Valley Group (sequence). Sac-

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1142 Late Mesozoic Forearc B asin, California

rame nto Valley, California, in V. Frizzell, ed., Upper M esozoic Franciscan rocks and Great Valley sequence, central Coast Ranges,California: Annual Meeting Pacific Section SEPM Field Trips I and4, p. 1-33.

- and C. A. Suczek, 1979, Petrology and provenance of Neogenesand from Nicobar and Bengal fans, DSDP Sites211 and 218: Journal of Sedim entary Petrology, v. 49, p . 1217-1228.

Irwin, W. P., 1981, Tectonic accretion of the Klamath Mountains,in

W,G. Ernst, ed., Geotectonic development of California: EnglewoodCliffs, N ew Jersey, Prentice-Hall, Inc ., p. 29-49.

Jennings, C . W., 1977, Geologic map of C alifornia: C alifornia Divisionof M ines and Geology, scale,1:750,OOO.

Kistler, R. W., and Z . E. Pete rman ,1973, Variations in Sr, Rb, K, N a, andinitial Sr /S r* ' in Mesozoic granitic rocks and intruded wall rocks incentral Ca lifornia: G SA B ulletin, v. 84, p. 3489-3511.

Mansfield, C . E, 1971, Stratigraphic variation in sandstone petrology ofthe Great Valley Sequence in the southern Coast Ranges west ofCoalinga, California: GSA Abstracts with Programs, v. 3, p. 157.

1979, Upper Mesozoic subsea fan deposits in the southern DiabloRange, California: record of the Sierra Nevada magmatic arc: GSABulletin, v. 90, pt. I, p. 1025-1046.

McLaughlin, R. J., and E. A. Pessagno, Jr., 1978, Significance of agerelations above and below Upper Jurassic ophiolite in The Geysers-

Clear Lake region, California: U.S. Geological Survey Journal ofResearch, v. 6, p . 715-726.Moore, G. R, 1979, Petrography of subduction zone sandstones from

Nias Island, Indonesia: Journal of Sedimentary Petrology, v. 49, p.71-84.

Ojakangas, R. W., 1968, Cretaceous sedimentation, Sacramento Valley,California : GS A B ulletin, v. 79, p. 973-1008.

Perkins, M. E., 1974, Geology and petrology of the East Bay outlier ofthe late M esozoic Great Valley Sequence, Alameda County, California; M aster's thesis. University of Ca lifornia, Berkeley,120 p.

Peterson, G. L., 1967, Lower Cretaceous stratigraphic discontinuity innorthern California a nd Orego n: AAP G Bulletin, V. 51 , p. 864-872.

Pettijohn, F. J., P. E. Potter, and R. Siever, 1972, Sand and sandstone;New York, Springer-Verlag, 618 p.

Rich, E. I., 1971, Geologic map of the Wilbur Springs quadrangle,Colusa and Lake Counties, California: U.S. Geological Survey Mis

cellaneous Geologic Investigations Ma p1-538.Schilling, F. A., Jr., 1962, The Upper Cretaceous stratigraphy of the

Pacheco Pass quadrangle, California: PhD thesis, Stanford University, 153 p.

Schweickert, R. A .,1981, Tectonicevolution of the SierraNevada range,in W. G. Ernst, ed., Geotectonic development of California: Englewood Cliffs, New Jersey, Prentice-Hall, Inc., p.87-131.

and D. S. Cowa n, 1975, Early Mesozoic tectonic evolution of thewestern Sierra Nevada, California: GSA Bulletin, v. 86, p. 1329-1336.

Seiders, V. M., 1983, Correlation and provenance of upper Mesozoicchert-rich conglom erate of California: GSA Bulletin, v. 94.

E. A. Pessagno, Jr., and A. G. Harris, 1979, Radiolarians andconodonts from pebbles in the Franciscan assemblage and the GreatValley sequence of the California Coast Ranges: Geology, v. 7, p. 37-40.

Stewart, R . J., 1976, Turbidites of the A leutian abyssal plain: m ineralogy,provenance, and c onstraints for Cenozoic motion of the Pacific plate:GSA Bulletin, v. 87, p. 793-808.

1977, Neogene turbidite sedimentation in Komandorskiy basin,western Bering Sea: AAP G Bulletin, v.61, p. 192-206.

1978, Neogene volcaniclastic sediments from Atka basin, Aleutian Ridge: AA PG Bulletin, v. 62, p. 87-97.

Suttner, L. J., 1974, Sedimentary petrograp hic provinces: an evaluation:SEPM Special Publication21 , p. 75-84.

Swe, W., and W. R. Dickinson, 1970, Sedimentation and thrusting of lateMesozoic rocks in the Coast Ranges near Clear Lake, California:GSA Bulletin, V.81 , p. 165-187.

Van der Plas, L ., and A . C. Tobi, 1965, A chart forjudg ing the reliabilityof point counting results: American Jo urnal of Science, v.263, p. 87-90.

van Hinte, J. E ., 1976a, A Jurassic time scale: AA PG Bulletin, v. 60, p.489-497.

1976b, A Cretaceous time scale: AAPG Bulletin, v. 60, p. 498-516.

Weller, J. M., 1958, Stratigraphic facies differentiation and nomenclature: AA PG Bulletin, v. 42, p. 609-639.

Zuffa, G. G., 1980, Hybrid arenites: their composition and classification: Jou rnal of Sedimentary Petrology, v. 50, p. 21-29.

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