The Sedimentary Record 2000; Shen and Schidlowski, 2000). Due to The - endemic biotas and facies control, it is diffi- cult to correlate directly between siliciclas- Transition in the tic- and carbonate-dominated successions. This is particularly true for the PC-C boundary interval because lowermost Southern , USA Cambrian biotas are highly endemic and Frank A. Corsetti James W.Hagadorn individual, globally distributed guide Department of Science Department of are lacking (Landing, 1988; Geyer and University of Southern Amherst College Shergold, 2000). Los Angeles, CA 90089-0740 Amherst, MA 01002 Determination of a stratigraphic bound- [email protected] [email protected] ary generates a large amount of interest because it provides scientists with an oppor- ABSTRACT:The Precambrian-Cambrian boundary presents an interesting tunity to address a variety of related issues, stratigraphic conundrum: the trace used to mark and correlate the base of the including whether the proposed boundary Cambrian, pedum, is restricted to siliciclastic facies, whereas position marks a major event in Earth histo- biomineralized fossils and chemostratigraphic signals are most commonly obtained ry. Sometimes the larger-scale meaning of from carbonate-dominated sections.Thus, it is difficult to correlate directly between the particular boundary can be lost during many of the Precambrian-Cambrian boundary sections, and to assess details of the the process of characterization. This is timing of evolutionary events that transpired during this interval of time.Thick demonstrated in a plot of PC-C boundary sections in the White-Inyo region of eastern California and western Nevada, USA, papers through time (Fig. 2): an initial contain mixed siliciclastic-carbonate lithofacies, and therefore promote correlation “ rush” to publish on the boundary between these classic, well-studied lithologic end-members.An integrated occurred after the formation of the working stratigraphic approach was applied to the White-Inyo succession, combining group on the PC-C boundary in the early lithologic, paleontologic, and chemostratigraphic data, in order to address the 1970s; papers trailed off though the 1980s, temporal framework within the basin, and to facilitate worldwide correlation of the and plummeted after the GSSP was ratified boundary. Results from the southern Great Basin demonstrate that the negative by the International Union of Geological δ13C excursion that is ubiquitous in carbonate-dominated successions containing Sciences (IUGS) in 1992 (Rowland and small shelly fossils occurs within stratigraphic uncertainty of the first occurrence of Corsetti, 2002). As our understanding of T. pedum.This global geochemical marker thus provides a link with the primary this interval of Earth history grows, we biostratigraphic indicator for the Precambrian-Cambrian boundary. focus more on the “bigger picture” issues (e.g., evolution and diversification of the Metazoa), and focus less on the “boundary INTRODUCTION the GSSP (Gehling et al., 2001). issues.” However, we will inevitably seek tie The Precambrian-Cambrian (PC-C) transi- Approximately 70% of all PC-C boundary points with which to link fossils from silici- tion records one of the most important successions are siliciclastic (Landing, 1994). clastic sections to the geochemical and cli- intervals in the history of , because it However, many carbonate successions mate-change data from carbonate-dominat- encompasses the appearance and diversifica- around the world have been more intensely ed sections so that we can improve our tion of metazoans, the invasion of the infau- studied because they record the advent of understanding of this critical interval. nal realm, the advent of widespread biomineralization and easily Mixed siliciclastic-carbonate successions and , as well as dramatic isotopic obtainable δ13C chemostratigraphic records become crucial in the search for stratigraph- and atmospheric changes (Lipps and Signor, (summarized in Kaufman et al., 1997; ic tie points. Although a number of impor- 1992; Bengtson, 1994; Knoll and Carroll, Shields et al., 1997; Bartley et al., 1998; tant lower Cambrian sections containing 1999; Bottjer et al., 2000; Knoll, 2000; Shields, 1999; Corsetti and Hagadorn, mixed siliciclastic-carbonate successions are Babcock et al., 2001; Fig. 1). Here we draw a distinction between the PC-C transition, represented by the post-glacial terminal through the early Cambrian (ca. 600-520 Ma), and the PC-C boundary, a chronostratigraphic boundary represented by a point in rock (Global Standard-strato- type Section and Point, or GSSP) in the , Newfoundland, section (Landing, 1994). The GSSP section is com- posed predominantly of siliciclastics (Narbonne et al., 1987), and the fossil cho- sen to coincide with the boundary, Figure 1. Summary of pertinent features associated with the PC-C transition (data compiled principally Treptichnus (or Phycodes) pedum, is restricted from Droser and Bottjer, 1988; Crimes, 1992; Droser et al., 1999, 2002; Knoll and Carroll, 1999; to siliciclastic facies. T. pedum recently has McIlroy and Logan, 1999), demonstrating the biospheric changes represented in this interval. SSFs: been demonstrated to occur ~ 4 m below small shelly fossils. Arrow denotes the first appearance of vertically-oriented .

4 | May 2003 The Sedimentary Record GEOLOGIC BACKGROUND From the time of Walcott (1908), the thick, superbly exposed, and highly fossiliferous Lower Cambrian strata from the southwest- ern United States (Figs. 3, 4, cover photo) have proved instrumental for understanding the Cambrian biotic explosion, and have even been suggested for a potential basal Cambrian stratotype (Cloud, 1973). Proterozoic—lower strata in the southern Great Basin were deposited on a thermally subsiding trailing margin created Figure 2. PC-C boundary publications through through rifting of the Laurentian in Figure 3. A. Map showing distribution of four time (constructed by searching GEOREF for the (e.g., Stewart, 1966, interfingering facies successions that span the ‘Precambrian-Cambrian,’ ‘Proterozoic- 1970; Stewart and Suczek, 1977; Armin PC-C interval in the southern Great Basin; suc- Cambrian,’ and ‘Neoproterozoic-Cambrian’ in and Mayer, 1983; Bond et al., 1985). cessions become progressively thicker to the the title). Neoproterozoic-Cambrian strata in the northwest, the offshore direction (after Nelson, southwestern United States thicken from 1978; Corsetti et al., 2000; Fedo and Cooper, known (e.g., Mongolia, Brasier et al., 1996; southeast to northwest, and can be grouped 2001). B. Shaded area represents the approxi- mate PC-C outcrop belt in the southern Great Olenik uplift, , Knoll et al., 1995; into four distinct but interfingering succes- Basin (after Stewart, 1970); the Mt. Dunfee Mackenzie Mountains, northwestern sions: Craton, Craton Margin, Death Valley section was offset to its present position by post- , Narbonne and Aitken, 1995; (proximal-shelf), and White-Inyo (proxi- Cambrian transtensional faulting. southern Great Basin, Corsetti and mal- to mid-shelf) successions (Stewart, Hagadorn, 2000), not all of these contain 1970; Nelson, 1976, 1978; Mount et al., ous with respect to earliest Cambrian guide the PC-C boundary. Also, not all the sec- 1991; Corsetti and Hagadorn, 2000; Fedo fossils (e.g., Signor and Mount, 1986). tions contain an appropriate juxtaposition and Cooper, 2001; Fig. 3). An erosional dis- , which are important guide fossils of carbonate- and trace-fossil-rich siliciclas- conformity removed the PC-C boundary in Lower Cambrian sections in the Great tic strata. Thick, relatively complete, well- interval in the Craton and Craton Margin Basin (e.g., Nelson, 1976; Palmer, 1981, exposed, and easily accessible successions in successions (Fedo and Cooper, 1990, 2001). 1998; Hollingsworth, 1999), make their the southern Great Basin contain siliciclastic This sequence boundary is traceable from first appearance well above this interval units and the boundary-marking fossil, T. the Craton Margin through the Death (Hollingsworth, 1999). pedum, in association with carbonate units Valley succession to the White Inyo succes- recording a complete δ13C chemostrati- sion, and probably represents the “Sauk I” White-Inyo Succession graphic profile (Corsetti and Kaufman, disconformity (Palmer, 1981). The bound- In ascending order, the White-Inyo 1994; Corsetti et al., 2000; Corsetti and ary interval resides below this unconformity Succession consists of the Wyman Hagadorn, 2000; Hagadorn and Waggoner, where incision was limited. The Death Formation, Reed Dolomite, Deep Spring 2000). The southern Great Basin sections Valley succession records both appropriate Formation, Campito Formation, Poleta provide an excellent opportunity to com- and iso- Formation, Harkless Formation, and the pare results from a variety of stratigraphic tope data (Corsetti and Hagadorn, 2000). Mule Spring (Nelson, 1962; Fig. approaches that have emerged as useful for However, the sections are relatively thin and 4). The White-Inyo Mountains have been correlating potential and bound- the carbonates from which the δ13C record the focus of intense PC-C boundary study, aries within the Cambrian (e.g., Geyer and was recovered are particularly thin. The but the paucity of earliest Cambrian fossils Shergold, 2000). White-Inyo succession is thickest, but, until has been problematic (e.g., Cloud and now, has been considered poorly fossilifer- Nelson, 1966; Taylor, 1966; Alpert, 1977;

Figure 4. Generalized lithostratigraphic columns for the PC-C transition interval in the southern Great Basin (after Nelson, 1962, 1976; Stewart, 1970; Fedo and Cooper, 2001). Whereas the Lower Cambrian portion is well constrained and correlated between the intervals, correlations between Neoproterozoic strata are less well con- strained. Base of the Sauk I Sequence removes some of the Neoproterozoic-Lower Cambrian interval in more proximal (Craton Margin) settings. The Death Valley succession contains a Neoproterozoic glacial-cap-carbonate succession, but no known correlatives exist in the White-Inyo succession. Fossil symbols represent first occurrences of key taxa.

May 2003 | 5 The Sedimentary Record

Figure 5: A. Mountain in the Inyo Range, the fication; periodic emergence is indicated. Helminthoidichnites formation exceeds 3000 meters in Overall, sedimentary stacking patterns, sedi- on bed sole, Wyman thickness (Nelson, 1962). The mentary structures, and facies associations Formation, south of section primarily represents shal- suggest that each member represents a shal- Hines Ridge, low marine deposition. The base lowing-upward parasequence. Sharp discon- Andrews Mountain, of the formation is not exposed, formities divide the members (but see California (scale so the nature of any underlying Mount et al., 1991). The Campito, Poleta, bar=1 cm incre- contact in not known (Nelson, Harkless (and ), and Mule ments). B. Domal 1962). The Reed Dolomite rests Spring formations record similar shallow , unconformably on the Wyman at marine, mixed-siliciclastic carbonate strata Middle Deep Spring Formation, Mt. most localities and is divided into (e.g., Moore, 1976; Mount and Bergk, Dunfee, Nevada three members: the Lower 1998), and have similar sedimentary ori- (knife ~8 cm long). Member, Hines Tongue, and the gins. C. Packstone lag bed Upper Member. The Lower The White-Inyo succession contains a composed mostly of Member is characterized by number of body and trace fossils. We have Cloudina riemkeae coarsely-crystalline pink dolo- identified bed-parallel tubular trace fossils, (across middle of stone with cross-bedded oolitic including Helminthoidichnites and photo), Lower Deep horizons, and minor domal stro- (Fig. 5A), in the Wyman Formation; we Spring Formation, matolite horizons. This suggests cannot falsify the hypothesis that some of Mt. Dunfee, subtidal to intertidal marine dep- these are body fossils. The Hines Tongue of Nevada (field of osition. The Hines Tongue is a the Reed Dolomite contains a depauperate view ~32 cm wide). D. Close-up of area southward-thickening siliciclastic suite of bed-parallel trace fossils, such as shown in Fig. 5C unit consisting of hummocky- Helminthoidichnites, Planolites, and showing C. riemkeae crossbedded sandstone and minor Torrowangea, and the Upper Member con- debris (field of view siltstone with minor carbonate tains packstones of the body fossil Cloudina. ~5 cm wide). E. interbeds. Thus suggests deposi- Carbonates of the Lower and Middle Treptichnus pedum, tion below normal wave base but Members of the Deep Spring Formation Upper Deep Spring above storm wave base. The contain Cloudina (in skeletal lags and isolat- Formation, Andrews Hines Tongue is thickest in the ed occurrences; Figs. 5C, D). These fossils Mountain, Hines Ridge area of the Inyo were initially identified as Cambrian small California (field of Range, and thins dramatically to shelly fossils (Signor et al., 1983) but were view ~9 cm wide). the north in the White subsequently reinterpreted as the F. and , Upper Mountains and Esmeralda Neoproterozoic Cloudina (Grant, 1990). It Deep Spring County, Nevada. The Upper remains unclear whether all of the forms Formation, Hines Member is characterized by mas- reinterpreted as Cloudina are, in fact, Ridge, California sive dolostones. Minor karstifica- Cloudina or whether some are small shelly (field of view ~9 cm tion is present at the contact with fossils. Siliciclastics of the Middle Member wide). the overlying Deep Spring also contain rare examples of Cloudina and Formation at some localities. bed-parallel trace fossils, including Planolites The Deep Spring Formation is and Plagiogmus. Treptichnus pedum (Fig. formally divided into the Lower, 5E), which delineates the PC-C boundary, Middle, and Upper Members, occurs near the top of the Middle Member Nelson, 1976, 1978; Mount et al., 1983; each consisting of a siliciclastic-carbonate in the Mt. Dunfee area and at the base of Signor et al., 1983; Gevirtzman and Mount, couplet (Gevirtzman and Mount, 1986; the Upper Member in the White 1986; Signor and Mount, 1986; Droser and Mount et al., 1991). The siliciclastic half- Mountains; in the latter case, T. pedum is Bottjer, 1988; Corsetti and Kaufman, 1994; cycle of each member contains green, ripple associated with a moderately diverse ichno- Fritz, 1995; Hagadorn and Bottjer, 1999; cross-laminated siltstones, and fossil assemblage (including Cruziana and Hagadorn et al., 2000). Because the PC-C with hummocky cross-stratification, indi- , Fig. 5F). The Campito boundary paradigm has changed over the cating deposition in relatively shallow water Formation contains trilobites characteristic last three decades, the inferred position of above storm wave base. The boundary of the and zones (see the boundary in the succession has changed between the siliciclastic and carbonate half- Hollingsworth, 1999), abundant trace fos- as well. New fossil evidence (Fig. 5) is con- cycle is transitional at most localities. The sils, and limited archaeocyathid bioherms sistent with the position of the boundary. carbonate half-cycle is commonly character- (Nelson, 1976, 1978). More comprehensive biostratigraphic infor- ized by rhythmically interbedded carbonate mation is contained in the cited references. wackestone and siliciclastic-rich siltstone, δ13C CHEMOSTRATIGRAPHY The Wyman Formation consists of crossbedded oolite, and intraclastic grain- Faunal data are broadly useful for correla- interbedded mudrock, siltstone, and stone; a high-energy, shallow-water deposi- tion across the PC-C interval in the south- , with lensoidal oolitic, pisolitic, tional environment is indicated. The top of ern Great Basin, but δ13C chemostratigra- and oncolitic carbonate layers that increase each carbonate half-cycle is commonly phy provides another important technique in number upsection. Near Andrews dolomitized, and often shows minor karsti- for constraining intrabasinal and interre-

6 | May 2003 The Sedimentary Record

Figure 6. point useful for correlations between silici- Integrated clastic-dominated sections and carbonate- chemostratig- dominated sections. raphy and In addition to providing a tool for biostratigra- chronostratigraphic work, secular variation phy for the in the δ13C record can be used to address PC-C inter- issues of basin scale. For example, if we use val in the the 13C record as a chronostratigraphic southern δ Great Basin tool, there is a progressive omission of the 13 (data from δ C record in the onshore direction. The Corsetti and most complete isotopic and stratigraphic Kaufman, records are present in the most offshore sec- 1994; Corsetti and Hagadorn, 2000 and references therein; this study). The δ13C record is most complete at tions. This trend is not unexpected. the Mt. Dunfee section (the most offshore section), where T. pedum occurs in the upper part of the Middle However, previously it was not possible to Deep Spring Formation. The d13C record is progressively less complete towards the craton. Stromatolites occur determine the magnitude of stratal omission in the White-Inyo succession in association with the δ13C nadir. using available lithostratigraphic or bios- tratigraphic information. gional correlations. The Neoproterozoic- the Death Valley succession, and this poten- Cambrian δ13C record has been relatively tially resolves the question. GLOBAL IMPLICATIONS well characterized and includes many posi- The relative synchronicity of the first Integrated biostratigraphic and chemostrati- tive and negative excursions (e.g., Magaritz appearance of T. pedum and the negative graphic information from the southern et al., 1991; Brasier et al., 1994, 1996; δ13C excursion in the southern Great Basin Great Basin demonstrate that the first Strauss et al., 1992; Corsetti and Kaufman, can be further tested by comparing samples occurrence of T. pedum, the trace fossil used 1994; Shields, 1999; Corsetti et al., 2000; from the thinner Death Valley succession to to correlate the PC-C boundary, co-occurs Montanez et al., 2000) reflecting secular samples from the much thicker, carbonate- with the ubiquitous negative carbon isotope variation and recognizable globally. rich White-Inyo succession. High-resolu- excursion recorded in carbonate-dominated Although most δ13C data are recovered from tion sampling for carbon isotope successions around the world. It is beyond carbonate dominated successions, it is possi- chemostratigraphy was conducted though the scope of this paper to correlate between ble to analyze organic-rich siliciclastic suc- the Deep Spring Formation at multiple sec- all the carbonate- and siliciclastic-dominat- 13 cessions for δ C org. To be effective, this pro- tions across the basin, in concert with bios- ed section because endemism, hiatuses, and cedure requires that the analyzed section did tratigraphic sampling (Fig. 6). Most of the diagenesis complicate the global picture. not experience significant heating, and that Lower Deep Spring Formation, where Using the trace fossil and chemostratigraph- rules out many sections from serious consid- Cloudina is present, shows a positive iso- ic records from the Great Basin as a bridge, eration (e.g., Strauss et al., 1992). Thus, topic excursion (to ~+4‰ PDB). The however, it appears that the first occurrence robust δ13C data from siliciclastic-dominat- excursion is progressively omitted in the of small shelly fossils was relatively synchro- ed sections have remained elusive. A carbon onshore direction, and reaches only ~+2‰ nous with the first appearance of T. pedum. isotope reference curve does not exist for the in more onshore sections. A negative excur- If we ignore potential facies control on the PC-C interval, but broadly similar sion, commonly down to ~-5‰, is recorded first appearance of T. pedum in the Mt. chemostratigraphic patterns exist among from the top of the Lower Member through Dunfee section, it could be argued that many PC-C sections (Shields, 1999). the middle of the Middle Member. small shelly fossils just barely predate T. Ignoring low amplitude variations, the Cloudina also occurs in this interval. The pedum because the first small shelly fossils major δ13C trends include: 1, a latest negative excursion is most pronounced in appear in association with relatively negative Neoproterozoic major positive carbon iso- offshore sections, where isotopic composi- δ13C values (Knoll et al., 1995). Given the tope excursion (slightly older than 548 Ma; tions plummet to ~-7‰. Curiously, the iso- relatively small amount of stratigraphic Grotzinger et al., 1995), associated with topic nadir is associated with unusually uncertainty, the debate regarding the choice Cloudina, simple horizontal trace fossils, abundant and thrombolite of trace fossils vs. small shelly fossils as the and -type fossils; followed by 2, a development (Oliver and Rowland, 2002). stratotype marker is, in our view, rendered pronounced negative carbon isotope excur- At Mt. Dunfee, which represents the most moot. The PC-C transition is well calibrat- sion nearly coincident with the PC- C offshore section, δ13C values rise to near ed (Bowring et al., 1993; Grotzinger et al., boundary, at ca. 543-542 Ma (Bowring et 0‰, then return to mildly negative values 1995), and the duration of the negative al., 1993; Grotzinger et al., 1995). The pre- beneath the Middle-Upper Deep Spring excursion is constrained to less than one cise position of the negative excursion with contact. This excursion is missing from the million . This implies that phosphatic respect to the paleontologic marker of the other, less complete sections in the onshore biomineralization and vertically-oriented boundary was unclear for a number of direction. T. pedum occurs in association burrowing developed quickly and nearly years, although it was commonly assumed with this return to negative δ13C values. The synchronously (probably in less than one that the negative excursion coincided with Upper Deep Spring Formation records a million years). Interestingly, the δ13C and the boundary horizon. Corsetti and positive excursion to ~+2‰. Thus, the pres- trace fossil biostratigraphic records from the Hagadorn (2000) demonstrated that T. ence of T. pedum in association with the Mt. Dunfee area closely match the hypo- pedum does in fact occur within one nega- negative excursion is verified in the White- thetical, composite reference section pro- tive- δ13C shift of the boundary horizon in Inyo succession, and it provides a global tie- posed by Shields (1999).

May 2003 | 7 The Sedimentary Record

CLOUD, P.E., 1973, Possible stratotype sequences for the basal Paleozoic infaunal ecology and evolution during the Proterozoic-Cambrian CONCLUSION in : American Journal of Science, v. 273, p. 193-206. transition: Palaios, v. 14, p. 58-72. Stratigraphic sections in White-Inyo CLOUD, P.E., and NELSON, C.A., 1966, -Cryptozoic and MONTANEZ, I.P., OSLEGER, D.A., BANNER, J.L., MACK, L.E., and related transitions; new evidence: Science, v. 154, p. 766-770. MUSGROVE, M., 2000, Evolution of the Sr and C isotope composi- Mountains, California-Nevada, provide a CORSETTI, F.A., AWRAMIK, S.M., PIERCE, D.L., and KAUFMAN, A.J., tion of Cambrian oceans: GSA Today, v. 10, no. 5, p. 1-7. 2000, Using chemostratigraphy to correlate and calibrate unconfor- MOORE, J.N., 1976, Depositional environments of the Lower Cambrian well-exposed and easily accessible PC-C mities in Neoproterozoic strata from the southern Great Basin of the and its stratigraphic equivalents, California and boundary interval through a mixed silici- United States: International Geology Review, v. 42, p. 516-533. Nevada: Brigham Young University Research Studies, Geology Series, CORSETTI, F.A., and HAGADORN, J.W., 2000, Precambrian-Cambrian v. 23, p. 23-38. clastic-carbonate succession. In this succes- transition; Death Valley, United States: Geology, v. 28, p. 299-302. MOUNT, J.F., and BERGK, K.J., 1998, Depositional sequence stratigraphy 13 of Lower Cambrian grand cycles, southern Great Basin, U.S.A: sion, δ C chemostratigraphy has been com- CORSETTI, F.A., and KAUFMAN, A.J., 1994, Chemostratigraphy of Neoproterozoic-Cambrian units, White-Inyo Region, eastern International Geology Review, v. 40, p. 55-77. bined with biostratigraphy to provide well- California and western Nevada; implications for global correlation MOUNT, J.F., GEVIRTZMAN, D.A., and SIGNOR, P.W., III, 1983, constrained correlations, and these correla- and faunal distribution: Palaios, v. 9, p. 211-219. Precambrian-Cambrian transition problem in western North CRIMES, T.P., 1992, Changes in the trace fossil biota across the America; Part I, Tommotian fauna in the southwestern Great Basin tions have application for correlating Proterozoic-Phanerozoic boundary: Journal of the Geological Society and its implications for the base of the Cambrian : Geology, v. 11, p. 224-226. between siliciclastic- and carbonate-domi- of London, v. 149, p. 637-646. DROSER, M.L., and BOTTJER, D.J., 1988, Trends in depth and extent of MOUNT, J.F., HUNT, D.L., GREENE, L.R., and DIENGER, J., 1991, nated successions globally. The ubiquitous bioturbation in Cambrian carbonate marine environments, western Depositional systems, biostratigraphy and sequence stratigraphy of United States: Geology, v. 16, p. 233-236. Lower Cambrian Grand Cycles, southwestern Great Basin, in Cooper, 13 J.D., and Stevens, C., eds., Paleozoic paleogeography of the Western negative δ C excursion near the base of the DROSER, M.L., GEHLING, J.G., and JENSEN, S., 1999, When the worm United States; II, SEPM Pacific Section Book 67, p. 209-226. Cambrian is confirmed to coincide with the turned; concordance of Early Cambrian ichnofabric and trace-fossil record in siliciclastic rocks of South : Geology, v. 27, p. 625- NARBONNE, G.M., and AITKEN, J.D., 1995, Neoproterozoic of the first occurrence of T. pedum in multiple sec- 628. Mackenzie Mountains, northwestern Canada: Precambrian Research, v. 73, p. 101-121. tions across the southern Great Basin. From DROSER, M.L., JENSEN, S., GEHLING, J.G., MYROW, P.M., and NARBONNE, G.M., 2002, Lowermost Cambrian Ichnofabrics from NARBONNE, G.M., MYROW, P.M., LANDING, E., and ANDERSON, M.M., the time of Walcott to the present , the the , Newfoundland: Implications for 1987, A candidate stratotype for the Precambrian-Cambrian bound- Cambrian Substrates: Palaios, v. 17, p. 3-15. ary, Fortune Head, Burin Peninsula, southeastern Newfoundland: Canadian Journal of Earth Sciences, v. 24, p. 1277-1293. Neoproterozoic-Cambrian succession in the FEDO, C.M., and COOPER, J.D., 1990, Braided fluvial to marine transi- southwestern United States continues to tion; the basal Lower Cambrian , southern NELSON, C.A., 1962, Lower Cambrian-Precambrian succession, White- Marble Mountains, , California: Journal of Inyo Mountains, California: Geological Society of America Bulletin, provide important data on one of the most Sedimentary Petrology, v. 60, p. 220-234. v. 73, p. 139-144. NELSON, C.A., 1976, Late Precambrian-Early Cambrian stratigraphic and interesting intervals in Earth history. FEDO, C.M., and COOPER, J.D., 2001, Sedimentology and sequence stratigraphy of Neoproterozoic and Cambrian units across a craton- faunal succession of eastern California and the Precambrian- margin hinge zone, southeastern California, and implications for the Cambrian boundary, in Moore, J.N., and Fritsche, A.E., eds., early evolution of the Cordilleran margin: Sedimentary Geology, v. Depositional environments of lower Paleozoic rocks in the White- ACKNOWLEDGMENTS 141-142, p. 501-522. Inyo Mountains, Inyo County, California: SEPM, Pacific Section, Los Angeles. We are indebted to S.W. Awramik, L.E. FRITZ, W.H., 1995, Esmeraldina rowei and associated Lower Cambrian trilobites (1f fauna) at the base of Walcott’s Waucoban Series, south- NELSON, C.A., 1978, Late Precambrian-Early Cambrian stratigraphic and Babcock, D.J. Bottjer, J.D. Cooper, M.L. ern Great Basin, U.S.A: Journal of , v. 69, p. 708-723. faunal succession of eastern California and the Precambrian- Cambrian boundary: Geological Magazine, v. 115, p. 121-126. Droser, S.Q. Dornbos, C.M. Fedo, J.S. GEHLING, J.G., JENSEN, S., DROSER, M.L., MYROW, P.M., and NARBONNE, G.M., 2001, Burrowing below the basal Cambrian GSSP, OLIVER, L., and ROWLAND, S.M., 2002, Microbialite reefs at the close of Hollingsworth, G.B. Langille, S.A. Leslie, Fortune Head, Newfoundland: Geological Magazine, v. 138, p. 213- the Proterozoic Eon: The Middle Member Deep Spring Formation at 218. Mt. Dunfee, Nevada, in Corsetti, F.A., ed., Proterozoic-Cambrian of the Great Basin and Beyond, SEPM Pacific Section Book 93, p. 97- L.B. McCollum, J.F. Mount, C.A. Nelson, GEVIRTZMAN, D.A., and MOUNT, J.F., 1986, Paleoenvironments of an 122. A.R. Palmer, M.N. Rees, S.M. Rowland, B. earliest Cambrian (Tommotian) shelly fauna in the southwestern Great Basin, U.S.A: Journal of Sedimentary Petrology, v. 56, p. 412- PALMER, A.R., 1981, Subdivision of the Sauk Sequence. U.S. Geological Runnegar, R.A. Shapiro, J.H. Stewart, B. 421. Survey, Open-File Report 81-743, p. 160-162. PALMER, A.R., 1998, A proposed nomenclature for the stages and series Waggoner, and G.J. Wiggett for collegial GEYER, G., and SHERGOLD, J., 2000, The quest for internationally recog- nized divisions of Cambrian time: Episodes, v. 23, p. 188-195. for the Cambrian of : Canadian Journal of Earth Sciences, v. 35, p. 323-328. discussions, advice, and data. A.J. Kaufman GRANT, S.W.F., 1990, Shell structure and distribution of Cloudina, a potential index fossil for the terminal Proterozoic: American Journal ROWLAND, S.M., and CORSETTI, F.A., 2002, A brief history of research provided geochemical analyses and aided in of Science, v. 290-A, p. 261-294. on the Precambrian-Cambrian boundary in the southern Great Basin, in Corsetti, F.A., ed., Proterozoic-Cambrian of the Great Basin and GROTZINGER, J.P., BOWRING, S.A., SAYLOR, B.Z., and KAUFMAN, A.J., data interpretation. We also thank the Beyond, SEPM Pacific Section, Book 93, p. 79-85. 1995, Biostratigraphic and geochronologic constraints on early - White Mountain Research Station mal evolution: Science, v. 270, p. 598-604. 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