Glacial and Syntectonic Sedimentation: the Upper Proterozoic Kingston Peak Formation, Southern Panamint Range, Eastern California

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Glacial and syntectonic sedimentation: The upper Proterozoic Kingston Peak Formation, southern Panamint Range, eastern California

JULIA M. G. MILLER* Department of Geological Sciences, University of California, Santa Barbara, California 93106

ABSTRACT and interpreted as lodgment till or glacioma- INTRODUCTION rine sediment, records the first ice advance. A A sedimentological-stratigraphic study of northward increase in diamictite thickness, The upper Proterozoic Kingston Peak Forma- the upper Proterozoic Kingston Peak Forma- decrease in clast size, and facies change from tion consists of a thick and variable sequence of tion in the southern Panamint Range shows diamictite to argillite and graywacke suggest predominantly clastic sedimentary strata, with that it was deposited under glacial conditions a southern source. Overlying laminated lime- minor carbonate and some extrusive igneous with contemporaneous volcanism and tec- stone marks a transgression. Succeeding rock. Diamictite is very abundant. The forma- tonic activity. Evidence for glaciation rests interbedded sandy limestone, thick-bedded tion is one of numerous upper Proterozoic primarily upon (1) the homogeneity, thick- graywacke, and parallel-laminated siltstone diamictite-bearing sequences which exist on all ness, and lateral extent of two diamictite and sandstone double in thickness over a few continents except Antarctica. Sedimentological units; (2) the facies association of the diamic- kilometres, demonstrating local subsidence studies have shown that many of these se- tite; and (3) presence of striated stones and and renewed terrigenous input. Trough, quences are glaciogenic (for example, Edwards, dropstones within the formation elsewhere in cross-laminated, arkosic sandstone and con- 1984; Link and Gostin, 1981), but the origin of the Death Valley area. In the Panamint glomerate overlain by predominantly massive most of them has been disputed (Schermerhorn, Range, pillowed basalt interbedded with di- diamictite, as much as 190 m thick with a 1974). Problems in their interpretation revolve amictite demonstrates synchronous subaque- locally erosive base, represent glaciofluvial in particular around three issues: (1) the rocks ous volcanism. Lower Kingston Peak units deposits and lodgment till and record the sec- were, in many places, deposited in areas of con- rest on a variable substrate and locally over- ond ice advance. temporaneous tectonism, making it difficult to lap faults, indicating tectonism prior to deposition. Tectonism during Kingston Peak deposition is inferred from abrupt thickness changes and buried faults. Sedimentation was chiefly on a submerged continental platform and locally terrestrial, during a period of incipient rifting. Two ice advances are recorded with associated sea-level fluctuations. The formation thickens northward from 40 to about 1,200 m over -40 km. Initial sediments were fine grained and in basins a few kilometres across; nearby islands provided coarse debris. Overlying sandstone and conglomerate indicate regression. Predominantly massive diamictite, as much as 450 m thick

Figure 1. Map of Death Valley region showing distribution of Kingston Peak Formation (black), pre-Quaternary rocks (shaded), and Quaternary units (blank). AM = Avawatz Mountains, BM = Black Mountains, CDV = Central Death Valley, FM = Funeral Mountains, KR = Kingston Range, PR = Panamint Range, SH = Silurian Hills, SS = southern Salt Spring Hills, TM = Tucki Mountain, MP = Manly Peak quadrangle, TP = Telescope Peak quadrangle.

•Present address: Department of Geology, Vanderbilt University, Nashville, Tennessee 37235.

Geological Society of America Bulletin, v. 96, p. 1537-1553, 20 figs., December 1985.

1537

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JOHNNIE FORMATION 3000 z< NOONDAY DOLOMITE v+p*-. s KINGSTON PEAK m 2000 2 FORMATION < PAHRUMP BECK SPRING DOLOMITE UJo GROUP (T 1000 CRYSTAL SPRING

FORMATION

IGNEOUS AND METAMORPHIC ROCKS

Figure 2. General stratigraphy of the southern Death Valley region. Modified after Goud and others (1969).

isolate glacial influences upon sedimentation; (2) the diamictites are commonly associated intimately with carltonate rocks; and (3) paleomagnetic studies in several cases have shown that demonstrably glacial rocks of this age were deposited at low latitudes (for example, McWil- liams and McElhinny, 1980). This paper aims to demonstrate that both glaciation and faulting took place during deposition of the Kingston Peak Formation. Few, if any, criteria are unique to glaciogenic or syntectonic rocks, and therefore this interpretation is based primarily upon an understanding of the lithofacies and their associations. The case is made that glaciogenic rocks can be recognized through the fades assemblage even when few individual criteria (for example, striated stones) are present. Results come from a sedimentological and stratigraphic study of the Kingston Peak Formation in the southern Panamint Range. Mapping and section descriptions were principally concentrated in the Manly Peak quadrangle (Fig. 1). Many exposures of the formation in the adjacent Telescope Peak quadrangle were studied, as well as selected outcrops elsewhere within the range. The Kingston Peak Formation forms a north- south-trending inelt of outcrops more than 80 km long in the southern Panamint Range. The Kingston Peak Formation was described and mapped in the Manly and Telescope Peak regions by Murphy (1932), Johnson (1957), Lan- phere (1962), Labotka and others (1980), and Albee and others (1981). The formation is also exposed in the areas north, south, and southeast of Death Valley (Fig. 1). It is the youngest formation in the Pahrump Group (Fig. 2). In the Panamint Range, the contact with underlying Beck Spring Dolomite is generally conformable, but locally Beck Spring Dolomite is absent, and elsewhere the contact varies from interfingering

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to unconformable (Labotka and Albee, 1977; r^Ton Labotka and others, 1980). No angular dis- a-alluvium II a n d s I i d e - Quaternary cordance is recognizable at the Kingston Peak- Noonday Dolomite contact, although the QEI Noonday rests on different Kingston Peak units slide breccia in different parts of the Panamint Range, and Cenozoic rnri the two formations interfinger in certain places - Tertiary (Miller, 1983). Little Chief Stock Although referred to in this paper as late QD Proterozoic, the age of the Kingston Peak For- rhyolite, andesite and basalt mation is poorly constrained. In the Panamint Range, the formation unconformably overlies |Khc| metamorphic rocks about 1,800 m.y. old that Cretaceous Hall Canyon Pluton are intruded by quartz monzonite -1,400 m.y. old (Lanphere and others, 1964). Early Cam- Mg brian fossils are present in the upper Wood Mesozoic intrusive Canyon Formation (Palmer, 1971) -2,000 m Mesozoic rocks stratigraphically above. The formation therefore must be between about 1,400 and 570 m.y. old. LEJ Tentative correlations based on the similarities Mesozoic sedimentary between (1) diabase sills in the Crystal Spring and volcanic rocks Formation and in the Apache Group in Arizona (Wrucke and Shride, 1972) and (2) algal struc- m tures in the Noonday Dolomite and some of late Cambrian sedimentary Cambrian - Paleozoic Riphean age in Siberia (P. Cloud, 1983, written rocks commun. and in Wright and others, 1978) nar- row the Kingston Peak age brackets to 1,200 to uP-e 700-800 m.y. In addition, regional correlations Upper Precambrian sedi- in western North America (Christie-Blick and mentary rocks (includes others, 1980) and interfingering with the Noon- Wood Canyon Formation) day Dolomite in the Panamint Range (Miller, 1983) suggest that the age of the formation may be less than 700 m.y. (Armstrong and others, Kingston Peak Formation 1982; Evenchick and others, 1984). Pahrump Mesozoic regional metamorphism has af- •Du Group - Precambrian fected all rocks of the Panamint Range. The Crystal Spring Formation metamorphic grade increases from south to and Beck Spring Dolomite north and east to west, reaching upper amphibolite facies (Labotka and others, 1980). Thermal wb eP-e metamorphism has affected areas close to Meso- qf zoic and Cenozoic plutons. The structure of the : wb World Beater Complex range is dominated by a north-northwest-trend- : qf quartzo-feldspathic gneiss complex ing anticline exposing a core of lower to middle eP-G •" undifferentiated earlier Precambrian Proterozoic igneous and metamorphic rocks (Fig. 3), with intense stretching deformation in places on its steeper western limb (Miller, 1983). Rocks of the Kingston Peak Formation have been locally severely recrystallized and de- Geologic Contact formed; lithologic variation within the formation remains clear, but preservation of sedimen- Fault tary structures is variable. In this study, I was careful to avoid misinterpreting the effects of Slide Plane Mesozoic and Cenozoic deformation.

Location of section, Figs.5, 15. KINGSTON PEAK FORMATION: DESCRIPTION Figure 3. Generalized geologic map of the Manly and Telescope Peak quadrangles, showing location of sections in Figures 5 and 15. Modified after Carlisle and others (1980). Abrupt thickness and facies changes charac- terize the Kingston Peak Formation throughout the Death Valley area. In the Panamint Range, the formation thickens northward from 40 to more than 750 m in the Manly Peak quadrangle; in the northern Telescope Peak quadrangle, a

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total thickness of -1,230 m has been recorded Wildrose submembe' (Labotka and oi:hers, 1980); individual units South Park Mountain Girl submember show local thickriess variations. Because distinct Figure 4. Subdivision of Member lithofacies associations correspond in general to the Kingston Peak Forma- KINGSTON Middle Park submember stratigraphic subdivisions of the formation, the tion as used in this paper, fol- Sourdough Limestone Member stratigraphic nomenclature shown in Figure 4 is lowing Johnson (1957), La- PEAK used here. botka and others (1980), and Surprise Member Carlisle and others (1980). FORMATION Limekiln Spring Member

In the southern Manly Peak quadrangle, in- Limekiln Spring Member terbedded quartzose sandstone, diamictite, and thin-bedded sandstone and siltstone, 150 m thick, form the lowest part of the Kingston Peak ceous unit, and an upper quartzite unit. The The variable character of the base of the Formation (section A in Fig. 5). On the basis of arkosic unit is present oniy locally and is as Limekiln Spring Member is significant. I n many their stratigraphic position and their lithologic much as 100 m thick. It contains breccia, com- places, Limekiln Spring rocks conformably and thickness variations, these rocks are here posed chiefly of Beck Spring Dolomite debris, overlie the Beck Spring Dolomite, and locally assigned to the Limekiln Spring Member de- and dolomite, feldspathic quartzite, arkose, and (for example, in upper Happy and lower Sur- fined by Labotka. and others (1980). A lenticular arkosic conglomerate (Labotka and others, prise Canyons; Fig. 3), the Limekiln Spring breccia, 10 m thick or more, lies with an undu- 1980). In places, there is a gradation from mas- Member interfingers with Beck Spring Dolo- lating basal contact upon older metamorphic sive Beck Spring Dolomite into sedimentary mite. In contrast, the Limekiln Spring Member rocks. It contains angular pebbles, cobbles, and breccia of the Limekiln Spring Member. rests unconformably on Beck Spring Dolomite, boulders of quartzite and gneiss (Fig. 6A). The The thickest and most abundant subdivision Crystal Spring Formation, and lower Protero- overlying sequence of parallel-laminated, very is the argillaceous unit. It is thickest, about 530 zoic rocks in lower Surprise, Pleasant, Coyote fine to fine-grained sandstone and siltstone to 900 m, in western Happy, Surprise, and Hall Canyons, and Goler Wash. Moreover, in lower pinches out abruptly eastward (Fig. 7). Laminae Canyons (Fig. 3; Labotka and others, 1980). Surprise Canyon, the argillaceous unit overlaps are typically 1 to 3 mm thick and normally The dominant lithology is very fine grained mi- a fault which juxtaposes Beck Spring Dolomite graded. Above, massive beds of medium- to caceous sandstone and siltstone (metagraywacke and Crystal Spring Formation (Labctka and coarse-grained quartz arenite and diamictite in and pelitic schist). Conglomerate and breccia others, 1980; Albee and others, 1981). units ranging from 10 cm to 10 m thick (Fig. 8) layers, dolomite interbeds, and lenses of pyritic are interbedded with the fine-grained rocks. A quartz mica schist with anomalous radioactivity Surprise Member few isolated pebbles exist in the thin-bedded (Carlisle and others, 1980; Kettler, 1982) are units. Diffuse bedding, generally shown by vary- present locally. The sandstone and siltstone are Massive or poorly bedded diamictite is char- ing clast abundance, is visible locally in the dia- commonly parallel laminated with some wavy acteristic of the Surprise Member, although this mictite, which contains clasts of quartzite, bed contacts, disturbed bedding, and thick grades northward into argillite and metagray- carbonate, and laminated sandstone and silt- graded beds. Rare isolated clasts of quartzite and wacke. Pillowed metabasalt is interbedded in stone (Fig. 6B). Many beds in this unit are len- granite exist in laminated argillite (Fig. 9), and most sections. Approximately 3 km south of ticular; some wivy bed contacts and rare ripple limestone and calcareous sandstone interbeds Goler Wash, the Surprise Member rests discon- marks are present. A fine- to medium-grained, are present locally. Generally structureless conformably on the Crystal Spring Formation well-sorted quartz arenite with some conglom- glomerate and breccia beds, 20 cm to a few (Miller, 1983) and is only about 35 nc. thick. It erate beds, ~30 m thick, caps the sequence. The metres thick, containing clasts of granite, augen thickens northward to 190 m in Coyote Canyon thick beds are commonly massive, some are gneiss, quartzite, and carbonate, are more com- and to more than 450 m in Redlands and South graded and contain dish structures, and there are mon on the west flank of the anticline. Park Canyons, where the base is not exposed. some fine-grained, parallel-laminated intervals Thin- to thick-bedded quartzite and calcar- An estimated 1,300 m of Surprise Member in with rare ripple marks. Abrupt lateral thickness eous quartzite, 120 to 140 m thick (Labotka upper Hall Canyon probably includes a few and facies changes are characteristic of the and others, 1980), form the uppermost unit of hundred metres of Limekiln Spring Member Limekiln Spring Member. For example, in a the Limekiln Spring Member and exist in most rocks; Labotka and others (1980) reported 880 canyon 2 km south of Goler Wash (Fig. 3), the western sections. Locally, both thinning- and m of Surprise Member in upper Jail Canyon member consists of basal diamictite about 50 m thickening-upward sequences are present, as (Fig. 3). thick overlain by the sandstone and siltstone well as possible sole marks, dish structures, and The lowermost 55 m exposed in the south sequence. starved ripples. Amphibolite and amphibolitic (section A in Fig. 5) comprises in:erbedded In the Telescope Peak quadrangle, Labotka schist are locally intrusive into the lower Lime- quartzose sandstone, conglomerate, and diamic- and others (1980, p. 862) described the Lime- kiln Spring Member. Major- and rare-earth- tite. The sandstone is generally medium grained, kiln Spring Member as "extensively and almost element analyses of these intrusions are similar moderately to well sorted, and massive or exclusively ex]>osed along the western margins to those of pillow lavas in the Surprise Member graded, with some ripple marks, low-angle cross of the anticline." They distinguished three main (Hammond, 1983), suggesting that they are beds, and dish structures. Conglomerate beds units within it: a basal arkosic unit, an argilla- feeders to the lavas. contain pebbles, cobbles, and (rarely) boulders

Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/96/12/1537/3419410/i0016-7606-96-12-1537.pdf by guest on 24 September 2021 800 B Coyote West Redlands West South Park East South Park East Redlands Canyon Canyon Canyon Canyon Canyon

Mountain Girl submember

600 Middle submember m

i'-WH mm 400 «K-'iSiriìpi Surprise Member mm 'J&V-ß,-?'

te kf^ méé

I.V-.b.U'.i-.W. I EXPLANATION 200 1 gli siltstone to fine-grained sandstone

sandstone, fine-to coarse-grained sandstone, locally conglomeratic basalt

breccia

! diamictite arenaceous limestone limestone--parallei laminated dolostone meters no exposure

Figure 5. Stratigraphie sections through the Kingston Peak Formation, Manly Peak quadrangle (locations shown in Fig. 3). For convenience, datum is base of Sourdough Limestone Member.

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of generally subrounded quartzite and s ubangu- lar carbonate. Diamictite is progressively more common up section; in section A (Fig. 5), it constitutes the remaining 35 m of the member. This diamictite unit thickens northward and is particularly not- able for its homogeneity, thickness (as much as more than 450 m) and lateral extent [35 km from south to north). It is generally structureless; bedding, where present, is defined by clast- concentrated and clast-free layers. Inverse to normal and normal graded beds are present locally (Fig. 10), as well as rare sandstone interbeds and lenses which in places show normal grading and channeled bases. Quartzite E nd carbonate clasts predominate. Carbonate boulders a few metres across exist, but most of the clasts are pebble sized; quartzites are rounded to subrounded, and carbonates are subangular. The quartzite-carbonate ratio and the variety of clast types increase up section (Figs. 6C, 6D, 5E, 6F, 11), and there is an over-all decrease in clast size toward the north (Fig. 12). The diamictite matrix is composed typically of rounded to angular quartz and some quartzose sandstone and rare feldspar grains up to a few millimetres across, set in an extremely fine grained, locally calcareous groundmass, which is chiefly biotite, quartz, chlorite, and albite. The extent of recrystalliza- tion restricts speculation as to the nature of the protolith, although the original groundmass must have been rich in clay minerals. Metabasalt, as much as 60 m thick, is present in most sections of the Surprise Member. In the Manly Peak region, it pinches out to the south and east (Fig. 13; Miller, 1983); in places, it is interbedded with diamictite. It is commonly pillowed and amygdaloidal and locally ii; associated with pillow breccia. Interpillow sediment is carbonate and very fine grained quartzite. Some finely laminated layers represent basalt- rich sediments or aquagene tuffs. According to major- and rare-earth-element chemical analyses of two basalts from Happy Canyon (Hammond, 1983), they are tholeiitic in composition.

Figure 6. Pie diagrams showing proportions of various clast types in uinits of the Kingston Peak Formation. A and B = Limekiln Spring Member, Goler EXPLANATION Wash, and Coyote Canyon: A = basal breccia, B = diamictite. C, D, E, and F = diamictite, Surprise Member: C = Lower Surprise Member (that is, l>elow quartzite gneissic rocks level of metabasalt), Manly Peak quadrangle; D = Lower Surprise Member, Telescope Peak quadrangle; E = Upper Surprise Member (that is, above level of metabasalt), Manly Peak quadrangle; F = Upper Surprise Member, Tele- corbonate schist and sandstone scope Peak quadrangle; G = conglomerate, Mountain Girl submembei; H = diamictite, Wildrose submember. N = number of counts made; -100 clasts counted at each locality; only clasts with longest dimension >1 cm included. G granitic rocks • others signifies granitic rocks. Data and collection details in Miller (1983).

Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/96/12/1537/3419410/i0016-7606-96-12-1537.pdf by guest on 24 September 2021 Figure 8. Diamictfte, Limekiln Spring Member, Goler Wash. Hammer is 45 cm long.

Figure 7. View of north side of Coyote Canyon showing Kingston Peak section and lenticularity of Limekiln Spring Member and units within it

Figure 9. Quartzite lonestone in argillaceous unit of Limekiln Spring Member, Pleasant Canyon.

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level of basalt

i 1 1 1 0 20 40 60 80 % total clasts

• quartzite X granitic

A carbonate • other Figure 10. fledded diamictite showing inverse to normal grading, Surprise Member, upper Big Horn Canyon. Scale is Figure 11. Graph showing stratigraphic variation in clast 15 cm long. types and proportions, Surprise Member diamictite, Manly Peak quadrangle only. Approximately 400 m of stratigraphic section is represented. N = number of counts made; sc.« details in Figure 6 caption.

COBBLES ANO BOULDERS

Figure 12. Triangular diagram showing clast sizes in Surprise Member diamictite according to geographic location in Panamint Range. Total north-to-south distance between localities is 33 km. N = number of counts made at each locality; see details in Figure 6 caption.

Localities listed according to geographic location

from south (bottom) to north (top) :

A Surprise Canyon (N=3)

A Happy Canyon (N=4)

O Pleasant Canyon (N=7)

• Redlands Canyon (N=I7) VERY MEDIUM COARSE TO COARSE PEBBLES PEBBLES X Coyote Canyon and Goler Wash (N=7)

In northern parts of the Telescope Peak quad- overlies the Surprise Member and forms a dis- these clasts and the surrounding laminae. The rangle, diamictite exists only at the top of the tinctive marker bed. The lower contact is gener- clastic content of the Sourdough Limestone in- Surprise Member; it is underlain by a hetero- ally sharp, but in two places, limestone is creases up section, and there is a gradational geneous sequence of quartzite, graywacke, interbedded with diamictite. The limestone contact with the overlying South Park Member. schist, conglomerate, and breccia (Fig. 13). thickens and thins without systematic trends, Commonly very fine grained schistose sand- varying between 0.5 and 45 m thick. South Park Member stone, thin- to thick-bedded with some graded The laminae, generally a few millimetres beds and rare isolated pebbles, is interbedded thick, consist of alternations in grain size of cal- Middle Park Submember. This submember with schist. Clasts of carbonate, quartzite, and cite and minor variations in the abundance of thickens toward the north and west and is be- granite are present. fine-grained to very fine grained muscovite and tween 75 and 285 m thick (Figs. 5,13,15). The quartz (Fig. 14). Finely disseminated graphite lower part consists of laminated, arenaceous Sourdough Limestone Member appears to be present in some darker layers. The limestone and calcareous sandstone, with rare laminae are commonly severely folded and de- ripple marks and some soft sediment folds. A persistent laminated limestone bed, named formed, and although most features are tectonic Metagraywacke is interbedded with it; the meta- the "Sourdough Limestone Member," abruptly in origin, the geometry of some folds and low- graywacke is commonly granular and locally angle discontinuities suggests that they were conglomeratic, and it increases in abundance up caused by synsedimentary deformation. The section, where it is interbedded with laminated, limestone contains some lenticular beds and schistose, fine-grained to very fine grained sand- isolated clasts of calcareous silty sandstone; de- stone and siltstone. The graywacke is commonly formation obscures the relationship between structureless, but it contains some graded beds,

NORTH EAST

WEST SOUTH

diamictite

pebbly arkosic sandstone

interbedded sandstone and siltstone with some limestone, conglomerate and diamictite

laminated limestone

V » » ' volcanic rocks

argillite, schist ? no information

BSD Beck Spring Dolomite

CSF Crystal Spring Formation Horizontal scale

Ip-E lower and middle Proterozoîc rocks

Figure 13. Isometric diagram showing facies variation in upper members of Kingston Peak Formation in Panamint Range. Datum is base of Noonday Dolomite, taking level of first carbonate above Mountain Girl submember as Noonday base.

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Figure 14. Even parallel-laminated gray limestone, Sourdough Lime- stone Member, South Park Canyon.

siltstone rip-up clasts, parallel laminae, slump Surprise Wildrose folds, rare ripple marks, possible dish structures, Canyon Canyon and calcareous concretions; locally it has an erosional base. Pebbles in conglomerate beds are mainly quartzite and schist; carbonate clasts are rare. The schistose sandstone and siltstone con- Figure 16. Trough cross-laminated, pebbly, tain pervasive parallel laminae up to a few mil- arkosic sandstone, Mountain Girl siibmem- limetres thick, some wavy bed contacts, graded ber, Middle Park Canyon. Scale is: 15 cm beds, and irregular, probable slump folds. Direc- long. tional current indicators are rare in this submember; a few ripple marks give current directions toward the west. The abundance and stratigraphic positions of the shape of stretched pebbles in conglomerate different lithofacies in the submember vary de- beds shows that the present thickness of the spite an over-all upward-fining trend (Fig. 5). In Mountain Girl submember is approximately eastern Surprise Canyon, the parallel-laminated one-half its original thickness (Miller, 1983). lithofacies dominates (Fig. 15). In northeastern The lower and upper contacts of the Mountain Wildrose Canyon (Fig. 15), diamictite with in- Girl submember are sharp. terbedded conglomerate, breccia with abundant Commonly a darker weathering, more pebbly coarse gray limestone debris, and quartzite over- unit lies below a less pebbly, white quartzite. lie lithofacies similar to southern sections which Conglomerate layers, from 1 to 5 m thick, are here contain a few lonestones. An uppermost more abundant in the lower, darker unit. Crude diamictite is distinct in containing quartzite and upward-fining sequences, as much as -15 m granitic clasts, no carbonate debris, and a coarse- thick, are locally present, and rare, thin (~ 1 m) meters grained matrix with many feldspar granules. It is fming-up sequences exist, but commonly pebbly commonly bedded, locally shows inverse to and nonpebbly levels are intimately and ran- Figure 15. Stratigraphic sections through normal grading, and thins abruptly eastward. domly interbedded. Cobbles and pebbles are the Kingston Peak Formation, Surprise and Mountain Girl Submember. Arkosic sand- almost exclusively composed of quartzite Wildrose Canyons (locations shown in stone, coarse grained, poorly sorted, commonly (Fig. 6G) and are rounded to well rounded, Fig. 3). For explanation of symbols see trough cross-laminated and pebbly, with cobble although in many western sections, they are Figure 5. W = Wildrose submember, MG = conglomerate beds, constitutes the Mountain strongly deformed. Trough cross-laminae, out- Mountain Girl submember, MP = Middle Girl submember. The unit generally thins to- lined by opaque minerals and generally less Park submemlier, SDL = Sourdough Lime- ward the east, from about 40 to 10 m in the than 10 cm high, are the characteristic bedform stone Member, S - Surprise Member. Note northern Manly Peak quadrangle and from throughout (Fig. 16). The orientation of the that recent mapping by M. B. Harding (1984, -130 to 0 m in upper Surprise Canyon (Figs. 5, troughs suggests a dominant paleocurrent direc- written commun.) suggest that the unit desig- 13, 15). These figures provide minimum esti- tion toward the north, but transport directions nated "Middle Park submember" in section G mates of the thinning trends, particularly in are difficult to determine because the rocks are may actually be Surprise Member. western South Park Canyon where a study of deformed (see data in Miller, 1983).

Wildrose Submember. Diamictite at the top laminated limestone. These rocks are interpreted of the Kingston Peak Formation is assigned to as having been deposited in shallow water (see the Wildrose submember. This diamictite is dis- below). This association implies that the Sur- tinct in that it contains gneissic clasts (Fig. 6H). prise Member diamictite was deposited in shal- The types and proportions of clasts vary; locally low water. I propose that the most plausible way carbonate is very abundant, and gneiss is not for this thick, homogeneous diamictite to have present in all places, but gneissic clasts have been deposited in shallow water is by glacial never been seen in diamictites lower in the King- processes. It would be hard to explain the thick- ston Peak section in the Panamint Range. Bed- ness, homogeneity, lateral extent, and facies as- ding in the diamictite is rare and, where present, sociation of the diamictite in a nonglacial setting. defined by different clast concentrations. The Moreover, an interpretation of the over-all facies matrix is similar to that of the Surprise assemblage of these Kingston Peak rocks, given diamictite. below, fits well with a glacial setting. The Wildrose submember crops out discon- Juxtaposition of glaciogenic diamictite with tinuously throughout the Panamint Range; it has carbonate strata (for example, Sourdough Lime- a variable substrate. It is most extensively ex- stone overlying Surprise diamictite) is common posed in upper Pleasant, Happy, and Surprise in upper Proterozoic sequences. Schermerhorn Canyons where it is at least 190 m thick, and in (1974) argued that this close association is evi- the Goler Wash-Coyote Canyon region where dence against glacial conditions during deposi- it is as much as 50 m thick (Figs. 5, 13, 15). tion, whereas Williams (1979) suggested that Detailed mapping in upper Pleasant and Sur- abrupt climatic warming at the close of the gla- prise Canyons has revealed an unconformity cial epoch permitted formation of the carbonate below it (Miller, 1983); the diamictite rests on cap. Carbonate, however, can accumulate in progressively older units farther east, cutting out cold water (Chave, 1967; Leonard and others, at least 115 m of stratigraphie section in 600 m 1981), and cold-water carbonates are associated of horizontal distance. Sharp sedimentary con- with Permian marine glacial rocks in Tasmania tacts with debris from underlying units incorpo- (Rao, 1981). Absence of a terrigenous sediment rated into the diamictite support the evidence supply is a requirement for carbonate accumula- that this is a primary unconformable contact. In tion (Chave, 1967). Transgression following ice upper Happy Canyon, only diamictite is present retreat and melting could cause such a hiatus in in the Kingston Peak Formation (Fig. 13). Clast clastic supply. In addition, warming through in- studies show that Wildrose diamictite overlies solation of resultant expanses of shallow water, Surprise diamictite here, which means that stra- where circulation was restricted, could favor tigraphie section is missing within the Kingston Figure 17. Map showing distribu- carbonate precipitation, and increased biological Peak Formation (Miller, 1983). tion of upper Proterozoic glaciogenic activity may have contributed. This could ex- rocks in western North America. plain the tillite-carbonate association in shelf en- EVIDENCE FOR GLACIATION Modified from Stewart (1972), Ham- vironments (Bjorlykke and others, 1978). A brey and Harland (1981). modern analogue for terrestrial settings may be In the southern Panamint Range, a glacial the association of stromatolitic carbonates and contribution to Kingston Peak sedimentation is sulfate and carbonate evaporites with glacial inferred on the basis of (1) the abundance of sediments in Antarctica (Parker and others, 1981; Walter and Bauld, 1983). diamictite, (2) the facies association of the dia- to 58% of the formation. Homogeneous diamic- mictite, and (3) study and interpretation of the tite units with very rare sandstone interbeds are Glacial conditions during Kingston Peak facies assemblage of the formation as a whole. as much as 250 m thick, and one unit extends 35 deposition elsewhere in the Death Valley region Local isolated stones (lonestones) suggest ice- km from south to north. have also been proposed. Troxel (1967) sug- rafting (Fig. 9). Additional evidence is found in The facies association of the diamictite is crit- gested that Kingston Peak diamictite and graded exposures of the Kingston Peak Formation east ical because diamictite may form in a variety of quartzite beds in the southern Salt Spring Hills of Death Valley, where striated and faceted depositional environments. The thickest and (Fig. 1) were derived from glaciers and redepos- stones and dropstones exist (Hazzard, 1939; most extensive diamictite in the Kingston Peak ited in a marine basin. R. A. Basse (1979, writ- Troxel, 1966; Miller and others, 1981; Miller, Formation of the southern Panamint Range is in ten commun.) favored a glaciomarine setting for 1983) and in the regional occurrence of correla- the Surprise Member. It is interbedded with pil- the formation in the Silurian Hills (Fig. 1), in tive glaciogenic rocks elsewhere in the North lowed volcanic rocks and must therefore have which deposition was predominantly by sedi- American Cordillera. been deposited subaqueously at least in part. ment gravity flows on a prograding deep-water Diamictite constitutes -45% of the Kingston Lack of abundant volcanic debris in the diamic- turbidite fan with some ice-rafting. The Kings- Peak Formation in the southern Panamint tite precludes its derivation from a volcanic ton Peak Formation, moreover, very likely Range (7 stratigraphie sections combined). In source. The diamictite is underlain by quartzose correlates with other diamictite-bearing se- three sections (B, C, E; Fig. 5), it constitutes 54% sandstone and conglomerate and overlain by quences in western North America (Fig. 17;

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Figure 18. Subcrop map of Kingston Peak Formation in southern Panamint Range. BSD = Beck Spring Dolomite, CSF = Crys- tal Spring Formation, pCgn = lower and middle Proterozoic metamorphic and igneous rocks, BHC = Big Horn Canyon, CC = Coyote Canyon, GW = Goler Wash, HC = Hall Canyon, HPC = Happy Canyon, JC = Jail Canyon, PC = Pleasant Canyon, RC = Redlands Canyon, SC = Surprise Canyon, SPC = South Park Canyon, TC = Tuber Canyon, WSC = Warm Spring Canyon.

preceded by erosion and faulting of underlying beds. Around Goler Wash, the base of the Wild- rose submember is conformable in western sections but unconformable in eastern sections less than 2 km away, where Wildrose diamictite rests directly on lower Proterozoic rocks (Fig. 19). This shows that downfaulting of westerly sections preceded erosion and deposition of the diamictite. In northeastern Surprise and Pleasant Canyons, an unconformity exists below the Wildrose diamictite (Miller, 1983), but because this contact is irregular and debris from underlying units is incorporated into the diamictite, it is considered to be due to local erosion. Additional evidence for tectonism contemporaneous with deposition comes from the Kings- ton Range (Fig. 1), where abrupt thickness changes in the upper Kingston Peak Formation exist and where huge blocks of underlying formations are embedded within the formation (Troxel and others, 1977). J. D. Walker and others (1984, written commun.) suggested that Christie-Blick and others, 1980). The glacio- bly upon lower and middle Proterozoic rocks the lower part of the Kingston Peak Formation genic character is well established for several of (Fig. 18). In most of the other parts of the Tele- in the Kingston Range was folded, faulted, and these deposits (for example, in Utah, Christie- scope Peak quadrangle, Kingston Peak rocks weakly metamorphosed before depositiDn of the Blick, 1983; and in northwestern Canada, Eis- overlie the Beck Spring Dolomite; locally the upper part. These observations, coupled with the bacher, 1981; Yeo, 1981), which supports this two formations interfinger, whereas in lower variable internal stratigraphy of the formation in interpretation of the Kingston Peak Formation. Surprise Canyon the contact is unconformable. the Death Valley region as a whole, suggest dep- These relationships show that faulting, and lo- osition in local basins with contemporaneous EVIDENCE FOR cally uplift and erosion, took place prior to tectonic activity. CONTEMPORANEOUS Kingston Peak deposition. In a region affected by active faulting, coarse TECTONIC ACTIVITY Thickness variations between Kingston Peak debris is likely to accumulate by a v.iriety of sections suggest variable subsidence across the processes. The over-all fades assemblage of the Tectonic activity prior to and contemporane- Panamint Range. The argillaceous unit of the Kingston Peak Formation in the southern Pan- ous with deposition of the Kingston Peak For- Limekiln Spring Member is thickest in western amint Range, however, fits best with a glacial mation is implied by (1) a variable substrate to parts of the Telescope Peak quadrangle. The contribution to sedimentation in an area of con- the formation, (2) thickness changes within the Surprise Member thickens northward across the temporaneous tectonism. A similar proposal formation, and (3) local buried faults. range and the Middle Park submember thickens has been made for the depositional environ- In the southern Manly Peak and Telescope northward and westward (Fig. 13). Smaller- ment of the Rapitan Group in northwestern Peak quadrangles, the Kingston Peak Formation scale lenticularity exists in the Limekiln Spring Canada (Eisbacher, 1981; Yeo, 1981). There rests in places disconformably upon the Crystal Member in Coyote Canyon (Fig. 7). and elsewhere, including within the Kingston Spring Formation and elsewhere unconforma- Deposition of the Wildrose submember was Peak Formation southeast of Death Valley

(Miller, 1983), iron-formations are associated during early deposition of the member. One was Jail Canyon, typical Beck Spring Dolomite is with glacial diamictites, and Yeo (1981) sug- in the vicinity of Pleasant and Happy Canyons not present, and limestone at the base of the gested that these iron-rich rocks formed close to and is referred to as "World Beater Dome" Kingston Peak Formation may represent a an area of submarine volcanism and rifting. I (Fig. 3); the other was close to Goler Wash and deeper-water equivalent of the platform propose that faulting during Kingston Peak de- Coyote Canyon. The thickest deposits and there- dolomite. position was associated with continental rifting. fore the deepest depressions lay west of the Overlying fine-grained sedimentary rocks re- structural highs. The one encompassing Surprise cord quiet conditions. The abundance of sulfide INTERPRETATION AND Canyon was probably bounded to the south by minerals and the relatively large amount of free ENVIRONMENTAL SYNTHESIS World Beater Dome, and the Goler Wash- carbon in parts of the argillaceous unit imply Coyote Canyon basin, of unknown northward accumulation in restricted basins under anaer- The lithologic heterogeneity of the Limekiln extent, was probably distinct from a small one obic conditions (Carlisle and others, 1980). Spring Member, coupled with its uneven distri- about 2 km south of Goler Wash. Close to Coyote Canyon and Goler Wash, bution and abrupt lateral thickness and fades Coarse debris at the base of the Limekiln quartzose sandstone and diamictite were subse- changes, shows that deposition took place in Spring Member was locally derived. Near Goler quently interbedded with the fine-grained rocks. local basins, possibly along the faulted edge of a Wash and Coyote Canyon, the debris included I interpret the diamictite as subaqueous mass- larger basin (N. Christie-Blick, 1985, written lower Proteroic gneiss and quartzite, probably flow deposits or as lodgment till. Either glacially commun.). Clasts in Limekiln Spring conglom- from the Crystal Spring Formation, whereas derived debris episodically slumped into the erate and diamictite beds indicate that Beck north of Happy Canyon, Beck Spring Dolomite basin, or oscillation of the ice margin juxtaposed Spring Dolomite, Crystal Spring Formation, debris dominated. There, initial Limekiln Spring till and thin-bedded sediment laid down in quiet and older Proterozoic rocks were being eroded Member deposition was transitional from Beck water (Fig. 20Ai). Lonestones were dropped by simultaneously. This, together with local thin- Spring Dolomite conditions and probably was icebergs. Clasts in the diamictite show that the ning of the lower units, demonstrates that at associated with foundering and faulting of the source region nearby was dominantly lower least two topographic highs existed prior to and western edge of a dolomite platform. North of Pahrump Group rocks. In the Telescope Peak

Section in floor of Above Goler Wash Lotus Mine NW SE

No vertical LKS exaggeration 250 m

250 m

Substrate is : Crystal Spring Formation south of Goler Wash, lower Proterozoic metamorphic rocks in Goler Wash and Coyote Canyon.

Noonday Dolomite Ya W - Wildrose submember -n MP - Middle Park submember Kingston ° Crystal Spring Formation SD - Sourdough Limestone Member ? Peak S - Surprise Member Formation LKS - Limekiln Spring Member — I Lower Proterozoic a metamorphic rocks Figure 19. Generalized stratigraphie cross section to illustrate abrupt lateral thickness changes in Kingston Peak Formation, Goler Wash. Section trends approximately northwest-southeast.

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quadrangle, calm conditions were interrupted at NORTH SOIJTH times by sudden influxes of coarse, locally derived material (Fig. 20B). Breccia and conglomerate beds were deposited by subaqueous mass-flow processes, and some graded beds indicate action of turbidity currents. Lonestones are once again interpreted as ice-rafted dropstones. Quartzose sandstone at the top of the Lime- kiln Spring Member in Coyote Canyon and interbedded conglomerate and sandstone of the basal Surprise Member are similar in texture and sedimentary structures to nearshore shelf sediments affected by periodic storms (Howard and Reineck, 1981) and so are thought to represent deposition in a high-energy nearshore environment (Fig. 20Aii). Dish structures indicate rapid deposition. Clasts in the diamictite and conglomerate are similar, which suggests that diamictite suppliixl the coarse debris. Regression is therefore implied during deposition of upper Limekiln Spring and lower Surprise strata and may have been caused by build-up of a major ice sheet. Farther north (for example, in Happy Canyon), sedimentary structures suggest that the quartzite unit represents submarine fan deposits. Deeper-water conditions persisted there. WEST EAST World Beater Thick diamictite of the Surprise Member is B) Island interpreted as till or waterlaid glaciogenic sediment because of i ts fades associations, as well as its thickness, lateral extent, and homogeneity. This thick diamictite records the first major ice advance during Kingston Peak sedimentation (Fig. 20C). Interliedded pillow lava and brecda record a period of. contemporaneous subaqueous mafic volcanism. At least part of the diamictite was therefore deposited under water, although possibly in melt water beneath ice. Inverse to Figure 20. Two-dimensional sketches illustrating development of Kingston Peak deposi- normal graded beds (Fig. 10) show that some tional region in southern Panamint Range. Ai = lower Limekiln Spring Member, Coyote diamictite was rcdeposited by mass flow. The Canyon-Goler Wash area; Aii = upper Limekiln Spring Member, Coyote Canyon-Goler Wash remainder may be subaqueous or subaerial area; B = argillaceous unit of Limekiln Spring Member, Happy and Surprise Canyons; C = lodgment till or gladomarine sediment. Deposi- Surprise Member; D = Sourdough Limestone Member; E = Middle Park submember; F = tion as lodgmeni: till would imply that ice at Mountain Girl and Wildrose submembers. s.l. denotes sea level. For explanation of symbols, times advanced across the depositional region. see Figure 13. Alternatively, if gladomarine conditions dominated, the homogeneity of the diamictite and scarcity of sandstone and conglomerate in- preted as more distal sediments deposited under known provenance, approximately coincides terbeds would suggest either (1) deposition a quiet-water conditions with some turbidite in- with the time of basalt extrusion. Assumi ng that few kilometres from the ice margin, where ice- fluxes and ice-rafting. the locus of diamictite deposition is related to rafted debris and suspension fall-out dominate Northward thickening of the Surprise Mem- the ice-margin position, then diamictite at the over sediment transported by gladal melt waters ber, the over-all northward decrease in clast size, top of northern Surprise Member sections im- (Boulton and Deynoux, 1981; Andrews and and the northward fades change from diamictite plies that the ice reached its greatest northerly Matsch, 1983) or (2) deposition marginal to a to argillite and graywacke suggest a southern extent near the end of the time represented by polar marine ice sheet or ice shelf where massive source (Figs. 12,13, 20C). Clasts in the diamic- the Surprise Member. diamictite is the dominant lithofades (Anderson tite reveal unroofing in this source area, from Deposition of the Sourdough Limestone and others, 1983). Argillite and graywacke in Beck Spring Dolomite through to basement Member indicates an abrupt hiatus in clastic sed- northern Surprise: Member sections are inter- rocks. The appearance of granitic clasts, of un- iment supply, inferred to have been caised by

NORTH SOUTH setting, on an outer shelf following transgressive events, for upper Precambrian organic-rich laminated limestones in southern Norway that have sedimentary structures very like those of the Sourdough Limestone. Calcareous sandstone interbedded with arenaceous limestone at the base of the Middle Park submember marks renewed terrigenous input into the basin, possibly due to isostatic uplift of the source area. Poorly sorted, imma- ture, graded sandstone beds were deposited by turbidity currents. Subsequently carbonate sed- D) imentation stopped, perhaps due to increased 8.1. water depth, and "background" conditions were represented by tranquil accumulation of parallel-laminated, fine-grained sand and silt (Fig. 20E). Coarse debris in the submember in Wildrose Canyon (Fig. 15) indicates proximity to a sediment source, possibly glacial, that sup- plied predominantly quartzite and granitic material; the bedding in these rocks suggests subaqueous deposition. The usually sharp base to the Mountain Girl submember signifies an abrupt change to shallow-water, high-energy, probably terrestrial conditions. Sedimentary textures and structures are similar to those of braided river and outwash fan, or sandur, deposits (Boothroyd and Ashley, 1975; Reineck and Singh, 1980), which suggests a glaciofluvial setting. The predominance of quartzite clasts probably reflects their resistance in a high-energy setting. Regression may have been due to build-up of a second ice sheet, which deposited the diamictite of the Wildrose submember (Fig. 20F). The diamictite base is locally erosive, and so present-day thickness trends in the Mountain Girl submember may not reflect primary sedimentary trends. Swanson (1982) also has proposed deposition of the Mountain Girl submember in a braided- stream environment. He inferred from paleocurrent and clast-size studies that the source was located west of the Panamint Range. My paleocurrent data suggest a north-south transport direction and a tentative southern source. The rocks are deformed, and so it is difficult to ob- tain reliable paleocurrent data. During rifting, however, local topographic highs and lows could form, and both westerly and southerly transgression due to rapid ice retreat and melting requires tranquil conditions, whereas soft-sedi- source regions could have existed. (Fig. 20D). Rare interbedding of diamictite and ment deformation shows some instability. The Diamictite of the Wildrose submember is limestone shows that slumping or mass flow graphite implies accumulation in an oxygen- interpreted as till, recording a second ice ad- continued locally after limestone deposition depleted environment, and the fine laminae may vance. The variable substrate of the diamictite, began. Sedimentary structures of the limestone represent seasonal fluctuations in sediment coupled with incorporation (in places) of locally are similar to those of basin-margin and upper- supply. There is no evidence to prove whether derived debris, implies deposition as lodgment slope limestones described by Cook and Mullins the limestone formed in marine or fresh water. till by a locally erosive glacier. Rare bedding and (1983). The absence of current-related features Tucker (1983) suggested a similar depositional clast-concentrated layers, particularly around

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Goler Wash and Coyote Canyon, suggest sub- glaciation in Spitzbergen, sea-level rise due to Striated stones and dropstones within the forma- aqueous deposition and winnowing by bottom transgression led to deposition of deep-water tion east of Death Valley support a glacial influ- currents in places. Locally abundant carbonate mud and preceded sea-level fall assodated with ence. No single criterion is diagnostic, however, fragments in the diamictite suggest patchy ero- isostatic rebound. This supports the inferred and the glacial interpretation presented herein sion of a carbonate substrate, whereas the gran- connection between sea level and build-up or incorporates and is based upon knowledge and itic and gneiss ic clasts demonstrate basement melting of ice in this interpretation of the Kings- interpretation of the facies assodations in the rock exposures in the source region. The loca- ton Peak sequence. formation as a whole. tion of this sou rce is unknown, but because the The above depositional scheme (Fig. 20) was In summary, there is evidence for both glada- Wildrose diamictite is absent in many Panamint superimposed upon contemporaneous tectonism tion and contemporaneous faulting in the Kings- Range sections and where present has a variable probably associated with incipient rifting of the ton Peak Formation of the southern Panamint substrate, one might infer that during its deposi- Cordilleran geosyncline. Prior to actual sea-floor Range. Deposition took place during indpient tion the Panamint Range lay close to the ice spreading, tholeiitic volcanism occurs locally continental rifting with local subaqueous volcan- center where erosional processes were active. in continental areas (Keen, 1982) and would be ism. Most sedimentation was on a submerged Interfingering of Wildrose diamictite with represented by the pillowed basalt of the Sur- continental platform with an irregular bathyme- Noonday carbonate strata shows that carbonate prise Member. Stewart and Suczek (1977) sug- try, although there was a terrestrial interlude. deposition began before till deposition termi- gested this scenario for the late Precambrian and Glacial and gladomarine processes dominated. nated. Presumably in some places, glaciers ad- Cambrian development of the western United Two ice advances are recorded but the regional vanced across a carbonate platform, and glacial States. An aulacogen such as the Amargosa au- extent of the glaciation remains uncertain. Sea- retreat, at least ;!n the Panamint Range, was fol- lacogen of Wright and others (1976) could form level fluctuations are inferred as associa ted prin- lowed by shallow-marine conditions of the in such a paleotectonic setting. The timing of this cipally with the accumulation and melting of lower Noonday Dolomite. rifting episode, furthermore may constrain the ice. age of the Kingston Peak Formation; Bond and DISCUSSION others (1983) and Armin and Mayer (1983) ACKNOWLEDGMENTS proposed that rifting began about 600 m.y. ago. A complex fades association, such as that In areas of incipient rifting, regional doming I am very grateful to John Crowell, who sug- described above, would be expected in the gla- may cause uplifts of from 1 to 2 km (Falvey, gested this study and guided, advised, and sup- ciomarine environment. Studies by Anderson 1974), and thus mountainous regions may form ported my work. J. C. Crowell, J. R. Boles, and and others (1980,1983) of sedimentation on the where ice could accumulate. Unequivocally far- A. G. Sylvester criticised an early drift of the Antarctic shelf reveal a complex environment traveled clasts have not been recognized in the manuscript, which was later reviewed by with a paleoslo]3e facing the continent on parts Kingston Peak Formation, implying local (that N. Christie-Blick and C. A. Nelson. The paper of the shelf and an irregular bottom topography. is, alpine) glaciation. The presence of correlative forms part of my Ph.D. dissertation, where addi- Diamictite deposits about 360 m thick exist near glaciogenic rocks elsewhere in the western Cor- tional details can be found. Numerous col- the Ross Ice Shelf (Barrett, 1975). It is uncer- dillera, however, may imply continental-scale leagues assisted in valuable discussions; in both tain, however, whether the late Proterozoic gla- gladation (Fig. 17). the field and the lab. I also thank my field assist- ciation in western North America was local or The paleolatitude of the Kingston Peak For- ants. The research was funded by National continental in extent; possibly gladomarine en- mation is unknown. Paleomagnetic studies in Science Foundation Grant EAR 77-C6008 to vironments in places such as southeast Alaska the Death Valley area were unsuccessful because John Crowell, and I acknowledge financial sup- provide better modern analogues. There sedi- of a Mesozoic overprint (M. O. McWilliams, port from the University of California and Sohio mentation by tide-water glaciers takes place in 1980, written commun.). The age of the forma- Petroleum Company. fjords (Powell, 1981). tion is poorly constrained, and it is therefore Sea-level fluctuations, inferred from the sedi- hard to know which regional paleolatitude map mentary facies, are in this study interpreted as to use. If the formation is 600 or 700 m.y. old, REFERENCES CITED primarily due to build-up and melting of ice. In then Irving's (1979) maps place eastern Califor- Albee, A. L., Labotka, T. C., Lanpheie, M. A., and McDowell. S. D., 1981, nia at paleolatitudes of approximately 20° and Geologic map of the Telescope Peak Quadrangle: U.S. Geological Sur- this environment of active faulting, however, vey Map GQ-1532. tectonically induced sea-level changes could 10°, respectively, at those times. Anderson, J. B„ Kurtz, D. D„ Domack, E. W„ and Balshaw, K. M„ 1980, Glacial and glacial marine sediments of the Antarctic continental shelf: occur. Local changes caused by uplift or down- Journal of Geology, v. 88, no. 4, p. 399-414. Anderson. J. B„ Brake, C„ Domack, E„ Myers, N„ and Wri|;ht, R., 1983, drop of fault blocks would be difficult to distin- CONCLUSIONS Development of a polar glacial-marine sedimentation model from Ant- arctic Quaternary deposits and glaciological information, in Molnia, guish from glacio-eustatic effects. In a glacial B. F., ed., Gladomarine sedimentation: New York, Ilenum Press, environment, there is a complex interplay be- Even in an area where few individual sedi- p. 233-264. Andrews, J. 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