Department of Defense
Legacy Resource Management Program
PROJECT 07-349
Constructing a Regional Historical Context for
Terminal Pleistocene/Early Holocene
Archaeology of the North-Central Mojave Desert
Jack Meyer, Jeffrey Rosenthal, Brian F. Byrd, and D. Craig
Young, Far Western Anthropological Research Group
May 2011
This document is unclassified and may be released to the public.
Constructing a Regional Historical
Context for Terminal Pleistocene/
Early Holocene Archaeology of the
North-Central Mojave Desert
Step 1: Paleoenvironmental Landscape Reconstruction
By:
Jack Meyer, M.A., Jeffrey Rosenthal, M.A.,
Brian F. Byrd, Ph.D., and D. Craig Young, Ph.D.
Far Western Anthropological Research Group
With a contribution from:
Manuel R. Palacios-Fest, Ph.D.
Terra Nostra Earth Sciences Research
May 2011
Submitted to:
Department of Defense
Legacy Resource Management Program
Project 07-349
Cooperative Agreement Contract No.
W912DY-07-02-0042 (W31RYO72277563)
TABLE OF CONTENTS
ABSTRACT ............................................................................................................................................... 1
ACKNOWLEDGEMENTS ....................................................................................................................... 3
1. INTRODUCTION ............................................................................................................................... 4
2. OVERALL PROJECT GOALS AND DESIGN ..................................................................................... 6
3. REGIONAL NATURAL AND CULTURAL CONTEXT ..................................................................... 9
Modern Setting .......................................................................................................................................... 9
Mojave Desert ........................................................................................................................................ 9
Northwest Mojave Desert ....................................................................................................................... 9
Paleoenvironment .................................................................................................................................... 11
Paleoclimate in Global Perspective ....................................................................................................... 11
Mojave Desert Paleovegetation ............................................................................................................. 12
Mojave Desert Paleolandscape .............................................................................................................. 13
Archaeological Context ............................................................................................................................ 16
Western North America ....................................................................................................................... 16
Great Basin and the Intermountain West ............................................................................................. 18
Mojave Desert ...................................................................................................................................... 18
4. FIELD INVESTIGATIONS AND NEW DATA ON THE TERMINAL PLEISTOCENE/
EARLY HOLOCENE .............................................................................................................................. 21
Research Approach ................................................................................................................................... 21
Field Investigation Methods and Analytical Studies .................................................................................. 21
Inflow Record Sampling ....................................................................................................................... 22
Lake Level and Outflow Record Sampling ............................................................................................ 22
Soil and Strata Designations and Descriptions ...................................................................................... 24
Radiocarbon Dating and Regional Database Compilation .................................................................... 24
Micro-Invertebrate Sampling and Analysis ........................................................................................... 25
Project Results .......................................................................................................................................... 25
Inflow Records ..................................................................................................................................... 25
China Lake Basin Lake Level Records ................................................................................................... 50
China Lake Outflow Records ............................................................................................................... 57
5. PALEOHYDROLOGY AND LANDSCAPE HISTORY IN THE NORTHWESTERN MOJAVE
DESERT DURING THE PLEISTOCENE/HOLOCENE TRANSITION ............................................. 61
Hydrological History of Lower Owens River and Local Drainages ........................................................... 61
Lake Level History ................................................................................................................................... 64
Terrestrial Landform History ................................................................................................................... 67
Comparison with Regional Records.......................................................................................................... 67
Searles and Owens Lake Basins ............................................................................................................. 68
Other Mojave Desert Records .............................................................................................................. 69
Conclusions ............................................................................................................................................. 73
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6. CONCLUSION AND OUTLINE FOR STEP 2 ................................................................................. 74
Implications for Early Human Settlement and Site Preservation ............................................................... 74
Step 2 – Historical Context ...................................................................................................................... 74
REFERENCES ......................................................................................................................................... 76
APPENDICES
Appendix A.
Appendix B.
Appendix C.
Appendix D.
Geological Sample Locality Stratigraphic Descriptions.
Radiocarbon Laboratory Dating Results and Methods.
Regional Radiocarbon Dating Compendium.
Micro-Invertebrates from the China Lake Basin Environs by Dr. Manuel R. Palacios-Fest.
LIST OF FIGURES
Figure 1. Regional Map Showing the Project’s Main Federal Land-Managing Agencies
in Relationship to the Mojave Desert and Great Basin. ............................................................................ 5
Figure 2. Map of Mojave Desert Showing the Project’s Main Federal Land-Managing Agencies. ................... 7
Figure 3. Map of Indian Wells Valley and China Lake Basin Environs. ........................................................ 10
Figure 4. Map of Mojave Desert showing Pleistocene Lakes, including those associated
with Owens River and Mojave River Systems. ....................................................................................... 14
Figure 5. Pleistocene Pluvial Lake Connections Along the Owens River Drainage System. ........................... 15
Figure 6. Landscape Features and Geological Sample Locations in the China Lake Environs. ....................... 23
Figure 7. Distribution of Radiocarbon Dates from this Study....................................................................... 28
Figure 8. Index Map Showing Location and Extent of Detailed Maps for Geological Sample Localities. ...... 29
Figure 9. Rose Valley Landscape Features and Sample Loci. ......................................................................... 31
Figure 10. Rose Valley Alluvial Landforms and Stratigraphy. ....................................................................... 32
Figure 11. Alluvial Stratigraphy of Selected Rose Valley Loci........................................................................ 33
Figure 12. Indian Wells Canyon Inset Terrace and Sample Locus. ............................................................... 36
Figure 13. Indian Wells Canyon Sample Locus. ........................................................................................... 37
Figure 14. Indian Wells Canyon Terrace Alluvial Stratigraphy. .................................................................... 38
Figure 15. Little Dixie Wash Landscape Features and Sample Loci............................................................... 39
Figure 16. Little Dixie Wash Alluvial Terrace and Strata. ............................................................................. 40
Figure 17. Alluvial Stratigraphy of Selected Little Dixie Wash Loci. ............................................................. 42
Figure 18. Little Dixie Wash Alluvial Fan and Cobble Ridge Loci. ............................................................... 43
Figure 19. Sample Locus and Terminal Pleistocene and Holocene Deposits along Dove Springs Wash. ....... 46
Figure 20. Dove Springs Wash Sample Locus and Alluvial Strata. ................................................................ 47
Figure 21. Dove Springs Wash Alluvial Stratigraphy. ................................................................................... 48
Figure 22. Geologic Deposits and Former Lake Contours in Indian Wells Valley. ........................................ 51
Figure 23. Prominent Lake Features and Former Shorelines in China Lake Basin......................................... 53
Figure 24. Landforms and Deposits in the China Lake Basin. ...................................................................... 54
Figure 25. Alluvial Stratigraphy of Core 9 from the China Lake Basin.......................................................... 55
Figure 26. Landscape Features and Sample Locus in Salt Wells Valley-China Lake Outlet. .......................... 58
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Figure 27. Landforms and Lake Features in Salt Wells Valley-China Lake Outlet......................................... 59
Figure 28. Elevational Cross Section of Little Dixie Wash Showing Inset Position
of Terminal Pleistocene/Earliest Holocene Terrace. ............................................................................... 62
Figure 29. Radiocarbon Record of Lake Level and Landscape Changes in the China Lake Basin Area. ......... 63
Figure 30. Lake History Based on the Age, Nature, and Elevation of Radiocarbon-Dated Samples............... 65
Figure 31. Elevation of Former Shore Lines and Lake Levels in Relation to Modern Topographic
Features and Selected Prehistoric Sites ................................................................................................... 66
Figure 32. Radiocarbon Dates Relevant to the Lacustrine History of the Lower Owens River System. ......... 70
Figure 33. Radiocarbon Dates Relevant to the Lacustrine History of the Mojave River System
and Other Enclosed Basins. ................................................................................................................... 71
Figure 34. Radiocarbon Dates from Terrestrial Spring, Marsh, “Black Mat,” and other
Wetland Deposits in the Mojave Desert................................................................................................. 72
LIST OF TABLES
Table 1. Summary of Field Investigations by Geological Sample Locality. .................................................... 22
Table 2. Radiocarbon Geological Sample Dating Results for this Study. ...................................................... 26
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ABSTRACT
The well-known early archaeology at Naval Air Weapons Station (NAWS) China Lake in east-central
California currently lacks strong historical context, making stewardship, determinations of eligibility for the
National Register of Historic Places, and management of these cultural resources, as required by Section 110 of
the National Historic Preservation Act, a difficult task for all federal agencies. This is in part because the earliest
sites are difficult to accurately date within the Terminal Pleistocene or Early Holocene (15,000 to 8,000 years
ago). They are also thinly spread over vast tracts of land, leaving the regional context for understanding their
significance equally thin and poorly understood.
This study, funded by the Department of Defense Legacy Resource Management Program (Project 07349, Cooperative Agreement Contract Number W912DY-07-02-0042 [W31RYO72277563]) takes a regional,
multi-agency approach to build a strong and comprehensive context by partnering NAWS China Lake with
contiguous and nearby federal land-managing agencies in the Mojave Desert, including the Fort Irwin National
Training Center (NTC), the National Park Service (Death Valley National Park and Mojave National Preserve),
and the Bureau of Land Management (BLM). The project is multi-disciplinary, using a global perspective and
paleoenvironmental context. The results are designed to substantially aid National Register determinations of
eligibility by identifying current data gaps and systemizing data collection. As such, it will facilitate developing
and tailoring future research designs for early site management. By examining sites associated with the earliest
occupations in the region, the project will also aid Native Americans, inclusive of designated Tribal Historic
Preservation Officers at Mojave Desert Tribes, in understanding their cultural history.
This report presents Step 1 of the study—a paleoenvironmental landscape reconstruction of the
Terminal Pleistocene/Early Holocene in the north-central Mojave Desert. Specifically, the investigations focused
on the ancient hydrology and geomorphology of the China Lake Basin area, which was once part of the extensive
Owens River pluvial lake system that extended from Mono Basin to Death Valley. Situated fully on NAWS
China Lake, the basin has the highest concentrations of Terminal Pleistocene/Early Holocene archaeology in the
Mojave Desert. As such, it is the ideal setting to investigate the timing and nature of early human settlement in
the Mojave Desert and assess how world-wide climatic changes associated with the Pleistocene/Holocene
transition impacted early prehistory in western North America.
The extent that ancient lakes and wetland habitats were critical to the earliest occupants of the Mojave
Desert remains uncertain and much debated. This is largely because the pluvial history of Lake China remains
poorly understood, inferred mainly from lacustrine records obtained from nearby contexts such as Owens and
Searles lakes. The current study gathered new, independent geological data directly from the China Lake Basin
environs to reconstruct the Terminal Pleistocene and Early Holocene paleoenvironment. This included previously
undocumented geologic stratigraphic records of the Pleistocene/Holocene transition in local washes emanating
from the adjacent Sierra Nevada, inflow records along the Owens River channel leading to China Lake, within
the China Lake Basin itself, and at the China Lake overflow channel.
Step 1 of the project—reconstructing the paleoenvironment during the Pleistocene/Holocene transition
(15,000-8000 cal BP)—was an unqualified success and provides a firm foundation for creating a strong historical
context for the early archaeological sites in this region (which will be carried out in Step 2 of the project). This
new paleoenvironmental reconstruction provides a strong and compelling three-stage geomorphic and
hydrological transition between 15,000 and 8,000 years that documents the demise of pluvial conditions and the
deterioration in effective moisture. Pleistocene pluvial lake levels declined and China Lake and Searles lake basins
became hydrologically separated by ~13,400 cal BP. China Lake, however, persisted until just after 13,000 cal BP.
Subsequently, localized wetland habitats flourished as high groundwater levels and spring discharge continued to
deliver surface flows to local washes and the China Lake Basin area. These wetland habitats largely disappeared by
~9000 cal BP as groundwater levels dropped, and alluvial fan deposition increased. This newly developed
hydrological record from the NAWS China Lake area facilitates better understanding of the greater Mojave
Desert and southwestern Great Basin, indicating that region-wide climatic shifts from the Terminal Pleistocene
through the Early Holocene were responsible for these patterns. The timing of these changes coincides well with
Constructing a Regional Historical Context for Terminal
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evidence from Greenland ice cores, demonstrating that geomorphic changes in the Mojave Desert during the
Pleistocene/Holocene transition represent threshold responses to world-wide climate change.
As such, these results provide a firm foundation for conducting Step 2 and successfully completing the
overall project objectives. This entails creating a strong historical context for understanding the archaeology of the
Terminal Pleistocene and Early Holocene. This will strengthen stewardship, provide a consistent and rigorous
basis for determinations of eligibility for the National Register of Historic Places, and greatly assist in the
management of these cultural resources, as required by Section 110 of the National Historic Preservation Act.
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ACKNOWLEDGEMENTS
This project was funded by the Department of Defense (DoD) Legacy Resource Management Program
(Project 07-349, Cooperative Agreement Contract No. W912DY-07-02-0042 [W31RYO72277563]). The study
was administered by the US Department of the Army Corps of Engineers, Engineering and Support Center,
Huntsville; managed by the DoD Legacy Resource Management Program; and carried out by Far Western
Anthropological Research Group. The aim of the DoD Legacy Resource Management Program is to provide
resources for protecting, enhancing, and conserving natural and cultural resources on DoD lands through
stewardship, leadership, and partnership. The DoD Legacy Resource Management Program proposal was written
by Brian Byrd and Amy Gilreath and submitted by Naval Air Weapons Station (NAWS) China Lake for Fiscal
Year 2007 funding.
A number of individuals provided important support and assistance in making the project a success.
Without the hard work and persistence of Michael Baskerville (Cultural Resources Manager, NAWS China Lake)
and Kish LaPierre (Cultural Resources staff, NAWS China Lake) this project would not have been possible. They
were instrumental in obtaining environmental and Explosive Ordnance Disposal (EOD) clearance to explore the
installation’s geomorphology and to conduct paleoenvironmental coring on the installation. We also greatly
appreciate Rod Snodgrass at EOD for providing us with safe passage to various locations on the installation. Russell
Kaldenberg (prior Cultural Resources Manager, NAWS China Lake) played an important role in ensuring the
project proposal was well-supported. Robert Couch (Applied Research Associates) graciously provided copies of
core logs as well as other information regarding cores he had obtain previously in the China Lake Basin. We also
appreciate and thank US Geological Survey geologist, Angela Jayko, for sharing field notes and radiocarbon dates
from the Rose Valley area.
Cecilia Brothers (Cultural Resource Management Specialist) of the DoD Legacy Resource Management
Program served as Legacy Project Lead. Ms. Brothers, along with Pedro Morales (Natural Resources Management
Specialist) of the DoD Legacy Resource Management Program provided invaluable support which is greatly
appreciated. They secured a contract and funding vehicle for Far Western to conduct this investigation, managed
the project, and graciously obtained time extensions when needed.
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1. INTRODUCTION
This multi disciplinary project is designed to provide a new historical context for the poorly understood
Terminal Pleistocene/Early Holocene archaeology in the Mojave Desert of east-central California. The project is
funded by the Department of Defense (DoD) Legacy Resource Management Program (Project 07-349,
Cooperative Agreement Contract No. W912DY-07-02-0042[W31RYO72277563]). The study was
administered by the US Department of the Army Corps of Engineers, Engineering and Support Center; managed
by the DoD Legacy Resource Management Program; and carried out by Far Western Anthropological Research
Group. The aim of the Legacy Resource Management Program is to provide resources for protecting, enhancing,
and conserving natural and cultural resources on DoD lands through stewardship, leadership, and partnership.
This study takes a regional multi-agency approach that partners NAWS China Lake with contiguous
and nearby federal land-managing agencies, including the Fort Irwin National Training Center (NTC), Death
Valley National Park, the Mojave National Preserve, and the Bureau of Land Management (BLM), along with
Native American Tribes (Figure 1). The results will have direct military benefits by aiding stewardship,
determinations of eligibility for the National Register of Historic Places, and management of these early sites
throughout the arid west.
The project consists of two main components: 1) a paleoenvironmental reconstruction of the dynamic
ancient landscape during the Terminal Pleistocene and Early Holocene (15,000 to 8,000 years ago); and 2)
construction of a GIS-derived diachronic model of early settlement in paleoenvironmental context (based in large
part on re-analysis of existing archaeological material using new dating methods). Owing to the scale of the project,
funding was only provided for Step 1: reconstructing Mojave Desert pluvial lake histories and hydrological regimes
at the end of the Ice Age. A subsequent proposal will be submitted for funding Step 2 of the project.
This report presents the results of Step 1 of the project and consists of six chapters. Chapter 2
summarizes the overall project goals and design, while Chapter 3 provides a brief environmental and cultural
background for the study area. Chapter 4 presents the approach, fieldwork, and laboratory results for the
paleoenvironmental investigations. In Chapter 5, these results are placed in broader contexts and a Terminal
Pleistocene/ Early Holocene paleoenvironmental reconstruction is presented. The report concludes in Chapter 6
with a brief discussion of the approach that will be taken in Step 2 of the study.
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OREGON
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Figure 1. Regional Map Showing the Project’s Main Federal Land-Managing Agencies
in Relationship to the Mojave Desert and Great Basin.
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2. OVERALL PROJECT GOALS AND DESIGN
The Mojave Desert and the Great Basin have perhaps the most extensive archaeological records for early
human occupation in North America. This record is largely comprised of small surface scatters of archaeological
material, typically represented by distinctive early flaked stone artifacts often referred to as characteristic of the
Clovis and Paleo-Indian archaeological complexes. This early occupation began near the end of the last Ice Age, a
period of time referred to as the Terminal Pleistocene/ Early Holocene (between 15,000 and 8,000 years ago).
NAWS China Lake has long been recognized as having one of the largest concentrations of early prehistoric
cultural material (e.g., Davis and Palaqui 1978), even exceeding the impressive archaeological assemblage
associated with the margins of Pleistocene Lake Mojave in the Mojave National Preserve (e.g., Campbell and
Campbell 1937). At NAWS China Lake, these archaeological sites are concentrated in the low-lying China Lake
Basin. Yet throughout the west, the regional context for understanding the significance of these resources remains
poorly developed and not well understood. This makes National Register evaluations, stewardship, and
management of the earliest sites challenging and often unsystematic.
This study takes a regional perspective toward building a strong historical context for understanding
Terminal Pleistocene/ Early Holocene archaeology of the Mojave Desert (Figure 2). This broad-based approach
encompasses 5,000 square miles, and includes the jurisdiction of numerous federal land-managing agencies
(including the Fort Irwin NTC, the BLM, Death Valley National Park, and the Mojave National Preserve).
Such a broad-scale approach is appropriate because early inhabitants of the arid west were mobile huntergatherers who may have traversed across large tracts of land each year. Thus, a small-scale study would only
encompass a limited piece of extensive settlement systems, and makes it difficult to appreciate the full range of
early human/land interplay.
In addition, these small, mobile bands of hunters-gatherers typically focused on infrequent (sporadic) but
very rich environmental settings within the desert. As the last Ice Age ended, substantial global climatic changes
took place, including unprecedented warming and cooling events that significantly impacted rainfall patterns, the
landscape, and its flora and fauna. Indeed the climate changed and fluctuated on an amplitude and with a
frequency that nature has not approached since. Desert lakes, a distinctive aspect of the Pleistocene pluvial
ecosystem, dried up during this period of dramatic climatic change. Probably the most prominent Pleistocene
pluvial system was the series of linked lakes that began with Owens River flowing into Owens Lake on the east side
of the Sierra Nevada, which then overflowed into Lake China (on NAWS China Lake), then into Lake Searles
(partially on NAWS China Lake), then into Lake Panamint, and finally continued to its terminus at Lake Manly
(in Death Valley National Park). Given that the ancient (paleo-) environment of the region was very different than
today, it is necessary to gather data to reconstruct its precise character. This broad regional perspective will allow us
to identify productive environmental settings at different points in time at the end of the Ice Age.
The earliest archaeology in the west (especially well-represented at NAWS China Lake and Fort Irwin
NTC) can only be understood in a broad regional context that takes into account a rapidly changing
paleoenvironment. Therefore, this project takes a multi-disciplinary, global perspective toward reconstructing
hydrological regimes and pluvial lake histories at the end of the Ice Age (Step 1), and the nature and spatial
distribution of the Terminal Pleistocene/Early Holocene archaeological record within this regional ecological
context (Step 2). The project also capitalizes on recent insights into the global climate, such as from the
Greenland ice cores, and employs innovative and new methods and analytical tools to comprehensively examine
large-scale archaeological patterns.
This report concerns Step 1 of the project, developing a paleoenvironmental reconstruction for the
region. Surprisingly, the pluvial history of ancient China Lake has never been rigorously studied, despite its rich
early archaeological record. The approach we have taken has been to gather new independent data from geological
localities on the ancient hydrology of China Lake Basin (including inflow sources, the basin itself, and its
output/overflow history). With these results, the history of the region’s ancient lakes and the timing of pluvial
conditions can be reconstructed. This model can then be compared and contrasted with existing reconstructions
Constructing a Regional Historical Context for Terminal
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Figure 2. Map of Mojave Desert Showing the Project’s Main Federal Land-Managing Agencies.
Constructing a Regional Historical Context for Terminal
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of the pluvial history of the Mojave River system, which terminated at Pleistocene Lake Mojave (in the Mojave
National Preserve). These results will provide new insight on how dramatic global climatic changes at the end of
Pleistocene impacted paleoenvironments in the Mojave Desert and the timing and scale of these changes.
The paleoenvironmental baseline will then provide a foundation for subsequent Step 2, which will
include analysis of pollen from alluvial cutbanks, cores, and packrat middens to refine reconstructions of ancient
plant communities in the region; re-analysis of Terminal Pleistocene/ Early Holocene archaeological materials;
and the synthetic integration of paleoenvironmental and archaeological results through GIS spatial modeling.
Completion of Step 2 will result in a new and appropriate historical context for the Terminal
Pleistocene/Early Holocene archaeology of the Mojave Desert. The final product will aid in National Register
eligibility determinations by identifying current data gaps, and greatly assist in the development and tailoring of
research designs for future Section 106 and Section 110 efforts at Early sites. This will, in turn, facilitate
management decisions for desert land managers, assist SHPOs and THPOs (such as the Big Pine Paiute and
Shoshone Timbisha tribes), and greatly benefit the military mission of both NAWS China Lake and Fort Irwin
NTC, as well as at nearby Marine Corps Air Ground Combat Center (MCAGCC) 29 Palms.
The project is scaled to the regional level, and puts NAWS China Lake at the lead in a multi-agency
consortium that includes contiguous and nearby federal land-managing agencies. The use of a multi-disciplinary,
global perspective and employment of innovate laboratory techniques allows NAWS China Lake to take a
leadership role in managing early archaeology in the Mojave Desert. The final product will fill some existing data
gaps, provide clarity on remaining information needs, and summarize current knowledge concerning Terminal
Pleistocene/ Early Holocene sites. As a result, the funding will aid Early site NRHP eligibility determinations; and
assist land managers throughout the arid west, western states’ SHPOs, and Mojave Desert THPOs in addressing
future National Historic Preservation Act Sections 106 and 110 needs.
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3. REGIONAL NATURAL AND CULTURAL CONTEXT
This chapter provides a brief contextual overview that sets the stage for our investigation of Terminal
Pleistocene and Early Holocene human adaptations. Initially, the modern setting is summarized; then prior
paleoenvironmental reconstructions are discussed. Finally, the archaeological record is reviewed with special
emphasis on normative perspectives and lacunae in our understanding of regional adaptive trends.
MODERN SETTING
Mojave Desert
The study area falls within the Mojave Desert, and the four main federal land-holding agencies involved
in the project are well-distributed across this region (see Figure 2). The Mojave Desert extends east from the Sierra
Nevada, Tehachapi, San Bernardino, and San Gabriel mountains to the Colorado River, and south from Death
Valley to near the northern edge of the Salton Trough. As such, it falls mainly within California, with the
northeastern portion extending into southernmost Nevada.
The Mojave Desert is part of the greater southern Basin and Range physiographic province, and is
generally considered a subdivision of the larger Great Basin within intermountain western North America. The
Basin and Range province is characterized by multiple, roughly parallel, fault-block, and volcanic mountain
ranges separated by broad valleys. Within this province, the Mojave Desert is a transition between the high, cold
desert-steppe of the Great Basin to the north, and the low, hot, Colorado and Sonoran deserts to the south and
southeast. In general, the region is typified by large alluvial fans emanating from steep mountain ranges and playas
in valley bottoms.
The Mojave Desert climate is characterized by very low rainfall, high temperatures, extreme intra-daily
variation in temperature, and periodic high winds (Thompson 1929:69). In contrast to the Great Basin farther
north, the Mojave is considered a hot desert, with maximum winter temperatures averaging about 15 °C (60 °F)
and summer temperatures averaging between about 35 and 39 °C (96 and 102 °F).
Rainfall is sporadic, and any single locality can go years without measurable precipitation (Major 1977).
Rainfall in the region includes winter (October through April) precipitation from storms eastward from the Pacific,
and summer rainfall (May through September) driven by Sonoran monsoonal storms originating to the south
(Bryson 1957). The months with the most precipitation include November through February and July through
August. The majority of annual rainfall, however, occurs in winter, between December and March. This is unlike
the Colorado Desert to the south, where as much as half of annual precipitation derives from summer monsoons.
Surface water is rare, save for the occasional spring or rare pools left after winter storms and summer monsoons.
The greater Mojave Desert biome is composed of a mosaic of different plants adapted to xeric desert
conditions (Barbour and Major 1988). Though generally lacking diversity, it includes species commonly found in
both the Great Basin and the Sonoran Desert. Elevation, temperature, sediments, geology, slope, and other factors
result in different vegetation communities within the greater Mojave Desert biome. Creosote-dominated
vegetation communities, however, are the most pervasive in the region.
Northwest Mojave Desert
This project is focused on the China Lake Basin within NAWS China Lake in the northwestern portion
of the Mojave Desert. The basin falls within Indian Wells Valley, an enclosed hydrological sink extending a
maximum of 55 miles north-south and 30 miles east-west (Figure 3). Rose Valley and the China Lake Basin, both
of which are referred to frequently in this report, are subsets of Indian Wells Valley. The valley is a downdropped, bedrock basin, in-filled with as much as 6,200 feet of lacustrine and alluvial sediments. Elevations range
from 2,150 feet above mean sea level (amsl) on the China Lake playa to about 3,000 feet amsl at the top of the
alluvial piedmont rimming the valley. Reaching elevations above 8,000 feet, the Sierra Nevada Mountain Range
Constructing a Regional Historical Context for Terminal
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Figure 3. Map of Indian Wells Valley and China Lake Basin Environs.
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lies immediately to the west, while the Coso Range lies to the north, and the Argus Range to the east. The El Paso
Mountains and Black Hills separate Indian Wells Valley from Fremont Valley to the south, the latter separated
from the Antelope Valley farther southwest by the Rand Mountains, Rosamond Hills, and Bissel Hills. Each of
the basins in the northwestern Mojave is distinguished by a valley-bottom playa. These include the playas at
China Lake and Airport Lake in Indian Wells Valley, Koehn Lake in Fremont Valley, and Rogers, Buckhorn, and
Rosamond lakes in Antelope Valley.
Aridity in the northwestern Mojave Desert is mainly a product of its southern latitude and position east
of the Sierra Nevada and Peninsular ranges. Due to the north-south orientation of these mountain ranges,
prevailing westerly winds are cooled as they rise to overcome the mountain crests, causing them to release heavy
moisture. This results in high amounts of rain and snow on the windward, west-facing slopes of the Sierra and
Peninsular ranges, but creates a rain shadow on the eastern side.
Typically, between 3.0 and 6.5 inches of rain fall occurs each year in Indian Wells Valley (as measured at
NAWS China Lake’s Weather Station). Higher elevations surrounding the valley receive light snowfall from
November through April, generally dissipating within a few days. Springs and small seeps provide the primary
surface water in the valley, but during rare periods of intense rain, the playa of China Lake Basin holds up to
several inches of water. Any number of ephemeral drainages originating in the Sierra Nevada, Argus ranges, and
ranges to the south deliver surface flows to China Lake Basin, although, these too are rare. In fact, not a single
perennial stream currently exists within Indian Wells Valley.
The hot, arid China Lake Basin and Indian Wells Valley fall within the Mojave Creosote bush scrub
formation (Küchler 1976). This desert scrub vegetation includes extensive tracts of Creosote Bush Scrub, Saltbush
Scrub, and Alkali Sink plant communities, the latter associated with the dry lake-bed playas. Creosote bush
(Larrea tridentata) tends to form large homogenous tracts, frequently with its principle associate burrobush
(Ambrosia dumosa), in the coarse, well-drained soils on the valley bottoms, alluvial piedmonts, and surrounding
slopes to an elevation of around 3,500 feet amsl (Holland and Keil 1990; Silverman 1996). Saltbush Scrub
communities occur primarily on the low-lying desert plains adjacent to the ancient lake-bed playa and are
primarily composed of members of the goosefoot family (Chenopodiaceae). Allscale (Atriplex polycarpa) is the
most common species in Indian Wells Valley, forming uniform tracts along the edges of China Lake playa. Alkali
Sink Scrub occurs in the highly saline zone surrounding the playa and is transitional between the Saltbush Scrub
community and the barren salt flats of the former lake bed. Common species within the Alkali Sink community
include desert holly (Atriplex hymenelytra), allscale, and saltgrass (Distichlis spicata).
A variety of species of passerine and raptorial birds, joined periodically by migratory waterfowl drawn by
the few perennial springs and infrequent playa lakes, occur in the region. Small mammals are also common in the
valley including ground squirrels (Spermophilus spp.), pocket mice (Prognathus spp.), woodrats (Neotoma spp.),
black-tailed jackrabbit (Lepus californicus), and desert cottontail (Sylvilagus audubonii). Coyote (Canis latrans),
desert kit fox (Vulpes macrotis), badger (Taxidea taxus), ringtail cat (Bassariscus astutus), bobcat (Lynx rufus), and
mountain lion (Felis concolor) are the principle carnivores. Mule deer (Odocoileus hemionus) and desert bighorn
sheep (Ovis canadensis nelsoni) are also known to occupy higher elevations in this region.
PALEOENVIRONMENT
Paleoclimate in Global Perspective
Environmental conditions in the past were different than they are today. During the Late Pleistocene and
Early Holocene, the climate was generally cooler and periodically much wetter. Recent high-resolution proxy
climate data from annually layered ice cores, particularly in Greenland and Antarctica, have refined our
understanding of how changes in climate affected the globe during the Late Pleistocene and Early Holocene
(Alley 2000; Alley et al. 2003; Charles 1998). A tight chronology of events at less than the decade level of
resolution are now available that chart the magnitude and timing of climatic events (Grachev and Severinghaus
2005; Severinghaus and Brook 1999; Severinghaus et al. 1998; Steffensen et al. 2008; Taylor et al. 1997). These
developments in global paleoclimate reconstruction provide an opportunity to more tightly link varied lines of
paleoenvironmental evidence (including lake cores, site pollen, geoarchaeology, and archaeological information),
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reconcile contradictory aspects of earlier reconstructions, and more accurately assess the role of climate change in
prehistoric occupation trends during this time frame. Results are briefly summarized below. All dates throughout
this report are referred to in calibrated years before present, rather than radiocarbon years, unless otherwise noted.
Calibrated ages are a more accurate reflection of the true timing and length of past events, and allow correlation
with high resolution paleoclimate records developed from annualized phenomena (e.g., varve counts, growth
increments) and radiocarbon dates developed from different kinds of carbonate fractions (e.g., wood, tufa,
mollusk shell).
Global climatic changes were both rapid and extreme during the Late Pleistocene and Early Holocene
(Severinghaus and Brook 1999; Severinghaus et al. 1998; Grachev and Severinghaus 2005; Steffensen et al.
2008). At the height of the last glacial maximum, 22,000 cal BP, it was much colder and drier than today (at least
five to seven °C). During this period of climatic change and fluctuation, there were two remarkable events when
temperature increased rapidly and dramatically. The first event occurred about 14,600 ± 300 cal BP, marking the
start of the Bølling climatic regime (Severinghaus et al. 1998), and the second took place 11,570 ± 10 cal BP at
the onset of the Preboreal era (Severinghaus and Brook 1999). During both events, mean annual temperature
increased globally, and in Greenland where the most detailed information has been obtained, it increased 9 ± 3 °C
(16 ± 5 °F). Each of these climate events occurred within one or two decades, in other words, less than one
generation (Severinghaus and Brook 1999; Severinghaus et al. 1998). This global warming trend, ultimately
marking the end of the last Ice Age, was slowed and partly reversed during a cooler interval between 12,900 and
11,570 cal BP termed the Younger Dryas. It should also be noted that the transition to the Younger Dryas took
place over a 100-year period, considerably slower than the Bølling and Preboreal rapid warming events
(Severinghaus et al. 1998; Severinghaus and Brook 1999; Taylor et al. 1997).
The implications of these high amplitude global events on local environmental sequences and human
adaptations have yet to be fully realized as it takes time to re-examine existing information and gather new data.
Overall, the northward retreat of ice sheets at the end of the Pleistocene in the northern hemisphere led to a
northward shift in the jet stream and a change in the distribution of storm systems. However, the impact of these
rapid warming events and the intervening Younger Dryas cold interval on global circulation patterns, rainfall, and
vegetation is increasingly the subject of research in a variety of settings world-wide, including the Great Basin
(e.g., Madsen 1999). There are also emerging indications that the nature and scale of paleoenvironmental changes
may have varied greatly between regions within North America (e.g., Meltzer and Holliday 2010).
The causal factors underlying these rapid changes in global climate (both the two rapid warming events
and the somewhat slower cooling reversal) remain obscure. Recently, there has been much speculation regarding
the causes of the Younger Dryas cooling episode. Probably the most controversial interpretation is that this
cooling event was precipitated by an extraterrestrial impact (such as a comet or meteorite) and directly brought
about the demise of the Pleistocene megafauna (e.g., Firestone et al. 2007). In North America, 34 species of
Rancholabrean megafauna went extinct, including ten species that were larger than a ton in average weight.
Notable species were Pleistocene horse, camel mammoth, mastodon, dire wolf, American lion, sloth, and tapir.
This ET theory has been met with enthusiasm (Kennet et al. 2008), cautious interest (Haynes 2008; Faith and
Surovell 2009), and skepticism (Gill et al. 2009; Surovell et al. 2009). Most notably, there have been questions
raised regarding whether there is indeed evidence of a large extraterrestrial impact event and whether a number of
these species had already gone extinct prior to the Younger Dryas.
Mojave Desert Paleovegetation
Late Pleistocene and Early Holocene proxy paleoclimatic and paleoenvironmental records (especially
geomorphic, pollen, and packrat midden analyses) provide a dynamic diachronic picture of Mojave Desert
paleoenvironments (Drover 1979; Enzel et al. 1992, 2003; Enzel and Wells 1997; Koehler and Anderson 1998;
Koehler et al. 2005; Tchakerian and Lancaster 2002; Spaulding 1990; Wells and Anderson 1998; Wells et al.
1989; Wells et al. 2003; West et al. 2007).
During the Late Pleistocene (between about 25,000 and 12,000 years ago) semiarid-to-arid conditions
also prevailed in the northwestern Mojave Desert due to the rainshadow of the Sierra Nevada. Much cooler
temperatures than today, however, made effective precipitation much higher. As a result, Pinyon-juniper
Constructing a Regional Historical Context for Terminal
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woodland was widespread at elevations between about 1,000 and 1,800 meters (3,280 and 5,900 feet); and
Juniper woodland was dominant below 3,000 feet (Spaulding 1990; Minnich 2007). In Death Valley, Utah
Juniper and Whipple yucca (Yucca whipplei) thrived in an area today dominated by Mojave Desert scrub (Wells
and Woodcock 1985).
Koehler et al. (2005) notes that the rare occurrence of pinyon north of latitude 36° N (immediately
north of the China Lake Basin) during the Late Pleistocene is characteristic of a paleoecotone that bisected the
northern Mojave at this time. North of this latitude, Juniper-steppe with an understory of cold-adapted shrubs is
characteristic of relatively cold winter temperatures, whereas the common occurrence of pinyon and Whipple
yucca, and the rare presence of steppe shrubs south of 36° N, is consistent with milder winters.
Recently, Gill et al. (2009) has argued that Terminal Pleistocene megafauna extinctions had a profound
effect on ancient vegetation patterns. In addition, Gill et al. (2009) assert that the demise of these “keystone
megaherbivores” began well prior to the Younger Dryas. In eastern North America, their extinction led to a rise in
hardwood forest and ultimately more extensive forest fires. Although the precise implications for the Mojave
Desert are uncertain, undoubtedly rapid vegetation changes and novel plant associations lacking modern analogs
characterized the Terminal Pleistocene.
At the end of the Pleistocene, vegetation began to shift toward modern geographic patterns (Koehler and
Anderson 1998; Koehler et al. 2005; Wigand and Rhode 2002). Initially, the distribution of pinyon pine greatly
decreased, and desert thermophiles migrated northward. By about 11,650 years ago (the start of the Holocene)
climate warmed enough to classify the region as a hot desert, and that much of the region was dominated by
species typical of the modern upland Mojave Desert community (<1,300 meters). These included juniper,
wolfberry, cliffrose, and desert almond. Though Middle Holocene (starting around 8,000 years ago) climates are
now seen as substantially more variable than Antevs’ (1948) initial conception of a warm, dry Altithermal, it
appears that the Holocene warming and drying trend continued during this period. This helped foster the
evolution of modern, xerically adapted vegetation communities.
Mojave Desert Paleolandscape
Clearly, climate, hydrology, and vegetation were significantly different before about 15,000 years ago,
during the Late Pleistocene than after. Runoff from surrounding mountains was of an order of magnitude greater
than today, and greater effective moisture allowed lakes to retain substantial amounts of water. At times during
the Late Pleistocene, large lakes were widespread in the Great Basin. Within the Mojave Desert, the most
extensive was the Owens River system (Figure 4). At its maximum, this was a 450-kilometer-long network of
interconnected lakes and rivers that originated at Lake Russell in Mono Basin, flowed into Owens Lake on the
east side of the Sierra Nevada, which then overflowed into Lake China (on NAWS China Lake), then into Lake
Searles (partially on NAWS China Lake), then into Lake Panamint, and finally continued to its terminus at Lake
Manly in Death Valley National Park (Benson et al. 1990, 1996, 1997, 1998; Gale 1914; Garrett 1991; Grayson
1993; Smith 2010).
The Mojave River drainage also carried regular, if not perennial, flows during the Late Pleistocene,
forming a series of associated lakes (Enzel et al. 1989; Tchakerian and Lancaster 2002; Wells et al. 2003). This
long river has its origins in the San Bernardino Mountains in the Transverse range along the southern edge of the
Mojave Desert. During this pluvial period associated with higher precipitation and major flood events, a series of
Pleistocene lakes were formed at the lower reaches of this system. These included, starting upstream, Lake Manix,
Cronese Lake, and Lake Mojave. Lake Mojave encompassed modern playas of Soda Lake and Silver Lake, of
which the former lies within the Mojave National Preserve.
During the Pleistocene, the Owens River system drained almost the entire eastern Sierra front, from
Mono Lake to China Lake, and extended well into the Mojave Desert through Searles Valley and Panamint
Valley before ending in Death Valley (Figure 5). When Owens Lake reached its outlet at an elevation of about
1,145 meters (3,756 feet), it overflowed to Rose Valley which, in turn, overflowed into Indian Wells Valley and
Constructing a Regional Historical Context for Terminal
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Figure 4. Map of Mojave Desert showing Pleistocene Lakes, including those associated
with Owens River and Mojave River Systems.
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4500
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Note: Adapted from Smith & Street-Perrott (1983).
Figure 5. Pleistocene Pluvial Lake Connections Along the Owens River Drainage System.
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China Lake. China Lake would in turn overflow into Searles Valley when it reached an elevation of between
about 665 and 670 meters (2,180 and 2,200 feet) or approximately ten to 16 meters (53 to 33 feet) in depth
(Benson et al. 1990; Gale 1914; Rosenthal et al. 2001; Smith and Street-Perrott 1983; Warren 2008). Searles
Lake then had to fill to a depth of approximately 172 meters (564 feet) before it coalesced with the waters of
China Lake to form pluvial Lake Searles. This lake rose until it reached its sill with Panamint Valley where it
would have been almost 200 meters deep (656 feet), maintaining a surface elevation of 690 meters (2,264 feet).
By the Late Pleistocene, however, the paleo-Owens River only connected the intermediate basins of Owens,
China, Searles, and Panamint lakes (Smith and Street-Perrott 1983); today the river terminates at the nearly dry
lakebed of Owens Lake.
As the hydrologic “gatekeeper,” the Owens River system, and Owens Lake in particular, has been most
extensively studied via a series of lake cores (Benson 2004; Benson et al. 1996; Benson et al. 1997; Phillips 2008;
Phillips et al. 1996) and descriptive and chronological analysis of littoral environments and neotectonics (Bacon et
al. 2006; Orme and Orme 2008). Several studies have also focused on stratigraphy of Lake Searles, providing
reconstructions of this pluvial lake’s history (Ramírez de Bryson 2004; Smith 1979, 2010; Smith and StreetPerrott 1983; Benson et al. 1990).
Based on these studies, two contrasting models now exist for the Owens River system. One
reconstruction has its origins at Lake Searles and is consistent with prevalent lake-level reconstructions elsewhere
in the Great Basin (Madsen 1999). This model tends to correlate high lake levels with cold intervals (such as the
Younger Dryas). In contrast, a newer model proposed by Benson et al. (1997), drawing on recent Owens Lake
coring, aims to link the results with global climate patterns (see also Benson et al. 2003). They argue that Late
Pleistocene cold intervals were dry and, hence, lake levels were lower, while warm intervals were wet with
correspondingly high lake levels. There is also considerable difference of opinion regarding when precisely, if at
all, Owens Lake and China Lake may have overflowed during the Terminal Pleistocene/Early Holocene (Benson
et al. 1997; Bacon et al. 2006; Smith 2010). Surprisingly, no comprehensive study of pluvial Lake China has been
undertaken. As such, reconstruction of Terminal Pleistocene/ Early Holocene environmental conditions and lake
level timings in the China Lake Basin have had to rely on conflicting proxy data from the immediately upstream
basin (Owens) and the immediately downstream basin (Searles) (e.g., Basgall 2007; Byrd 2007; Giambastiani
2008; Rosenthal et al. 2001; Warren 2009).
ARCHAEOLOGICAL CONTEXT
Western North America
For many years, the Paleoindian culture referred to as Clovis was considered to reflect the first human
group to enter and populate the New World (e.g., Haynes 1969; Jelinek 1992). These big game hunters were
thought to have crossed the Berring land bridge bringing with them a blade-based tool kit (with strong affinities
to the Upper Paleolithic of the Old World) that included distinctive Clovis spear points (large concave-base
lanceolate points with a long thinning flake at the base, referred to as fluting) (Collins 1999; Haynes 2002).
Traveling through an opening in the ice sheets, it is thought that these ancient people “blitzkrieged” through the
Americas around 13,500 to 12,800 cal BP, possibly decimating the last of the Pleistocene megafauna.
Clovis sites are best documented in the southwest and the Great Plains (Haynes 2002). The distinctive
Clovis adaptive strategy then gave way to the Folsom culture (dated between about 12,900 and 11,900 cal BP),
also represented by wide-ranging, mobile hunters and gatherers who periodically exploited large game (especially
bison) and retained the fluting technology, albeit on smaller and thinner projectile points (Fiedel 1992). By the
start of the Early Holocene, at least in the Great Plains, Folsom was replaced by the Plano culture (postdating
around 11,900 cal BP) that had more varied point forms, all of which were unfluted and typically had
rectangular bases.
The Clovis-first perspective has fallen out of favor in recent years owing in part to newly documented
sites in South America that appear to predate Clovis (Madsen 2004), and recent results from Texas on an
archaeological assemblage (referred to as the Buttermilk Creek Complex) that stratigraphically underlies and
predates a Clovis occupation horizon (Waters et al. 2011). Currently there is considerable agreement that humans
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entered the New World via multiple migrations using both coastal and inland routes (Erlandson et al. 2007a).
Most scholars view this as a post-glacial maximum process (after 21,000 cal BP), although some have argued for
pre-glacial maximum incursions as well (Madsen 2004). In short, the Clovis-first paradigm has given way to a
multifaceted perspective on entry into the New World. Conventional thinking now embraces the likelihood that
some groups entered in pre-Clovis times, and that other populations with different technologies and adaptive
strategies than Clovis may have occupied North America during the Terminal Pleistocene.
These new perspectives have spurred archaeologist to explore fresh ideas for the initial occupation in
western North America. For example, Erlandson and others (2007b) have elaborated on the coastal migration
route model. They refer to it as “the Kelp highway,” that entailed travel by boat, exploiting this corridor’s highly
productive marine resources. This route to South America, of course, may have entailed landings by paleocoastal
hunter-gatherers along California’s ancient shoreline, which would have been situated westward of the modern
shoreline, and in most places is now inundated. A single date of about 13,200 to 12,900 cal BP on skeletal
remains from Arlington Springs (CA-SRI-173) on the northern Channel Islands off the southern California coast,
has lent credence to this perspective (Johnson et al. 2002).
Despite the demise of the Clovis-first paradigm, new research continues to enhance our understanding of
the Clovis complex. Waters and Stafford (2007) recently conducted a new high-precision dating program, and
their results indicate that the Clovis complex persisted for a much shorter time span than previously estimated—
perhaps only 300 years (from around 13,000 to 12,700 cal BP—11,050 to 10,800 radiocarbon years before
present [RCYBP]). If correct, this implies that either Clovis populations or Clovis technology rapidly spread
across an extensive portion of North America. This short chronology, however, has not been fully accepted (Beck
and Jones 2010; Haynes et al. 2007).
It has long been recognized that classic Clovis sites have not been documented in California (e.g.,
Moratto 1984). Indeed, with the exception of human skeletal remains from the Arlington Springs site, no
stratified site in California has been dated to the Clovis time frame (13,500 to 12,800 cal BP). Fluted points are
also infrequently encountered in California, generally as isolated surface finds (Dillon 2002; Rondeau et al. 2007).
The two most prominent concentrations of fluted points occur near Tulare Lake in the southern San Joaquin
Valley and in China Lake Basin (Davis and Panlaqui 1978; Hopkins 1991). Moreover, scholars have recently
stressed that labeling all fluted points in California as Clovis is inappropriate since these projectiles rarely fall
within the morphological or metric range of fluted points well-documented at actual Clovis sites in the Southwest
and the Great Plains (e.g., Byrd 2006; Dillon 2002; Rondeau 2006; Rondeau et al. 2007). Instead, California
fluted points are typically smaller and thinner, and it has been suggested that they should be referred to under the
more general rubric of “fluted” or “concave-base” points; a tacit recognition that they may well post-date the age
of Clovis (Basgall 1998).
The recent proposition (Firestone et al. 2007) that the Younger Dryas cooling episode and the demise of
the North America Racholabrean megafauna was caused by an extraterrestrial impact has drawn considerable
archaeological interest. Haynes (2008) has recently concurred that a major perturbation took place at the start of
the Younger Dryas cold interval, circa 12,900 cal BP. The start of the Younger Dryas is marked by the widespread
appearance of a black, organic-rich layer, and Clovis sites and Pleistocene megafauna (except the bison)
stratigraphically underlie these “black mats.” As such, Haynes (2008) cautiously revives Martin’s (1967) notion
that Clovis populations may have contributed to or caused the demise of Pleistocene megafauna.
Other scholars have gone so far as to suggest that this extraterrestrial event at the start of the Younger
Dryas (around 12,900 cal BP) caused a major human population disruption in California. Kennett et al. (2008)
assert that this event led to large-scale wildfires and the extinction of pigmy mammoths on the northern Channel
Islands. Both Jones (2008) and Kennett et al. (2008) also argue that early human occupation (contemporaneous
with Clovis) was then disrupted for 600 to 800 years, after which (around 12,200 cal BP) a “large-scale
colonization” took place. Supporting evidence for both early occupation episodes is limited to two dates from two
sites (i.e., one date from each time segment). This “disruption” hypothesis is not, however, supported by evidence
from other parts of western North America (Beck and Jones 2010; Meltzer and Holliday 2010). For example,
Meltzer and Holliday (2010), drawing on an extensive database of dated sites in the Great Plains and southwest,
Constructing a Regional Historical Context for Terminal
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document a continuous sequence of occupation that begins well prior to the Younger Dryas and continues
through the end of the Pleistocene. Indeed, the bulk of Pleistocene sites in this area date to the Younger Dryas.
Great Basin and the Intermountain West
The demise of the Clovis-first model has led Great Basin scholars to reassess the nature of Terminal
Pleistocene occupation (e.g., Beck and Jones 1997), and the relationship between pluvial lakes and early
occupation trends (Adams et al. 2008; Pinson 2008). Recently, Beck and Jones (2010) have argued that the
earliest intermountain west sites (those in the Great Basin and on the Columbian Plateau) were not represented
by Clovis complex assemblages with their characteristic blade technology and fluted points. In fact, no Clovis
assemblage sites have been dated or documented. Instead, stemmed point assemblages represent the earliest
occupation episodes. They muster a total of 29 radiocarbon dates from 11 localities with stemmed points
including 17% that date to the Bølling-Allerød (contemporaneous with the Clovis complex) and 83% which date
to the Younger Dryas (most of which fall within the early part). As such, “Western Stemmed” point assemblages
originated in the Terminal Pleistocene and are considered to be nearly as early, if not contemporaneous, with the
Clovis complex of the Great Plains and the southwest.
Besides having different forms of projectile points, these Western Stemmed assemblages are also
differentiated from Clovis complex assemblages by having: 1) flake rather than blade blanks for projectile points;
2) side struck rather than end struck flake blanks for bifaces; 3) points typically made from fine-grained volcanics
rather than chert; and 4) have an additional tool type—crescents (typically bifacially retouched, often with one
steep-side)—considered to be a marker of littoral adaptations (Beck and Jones 2010:97-100). Similar to
California, fluted points are typically found in surface contexts in this region and based on statistical analysis are
significantly smaller than fluted points from Clovis sites (Beck and Jones 2010:Table 4). As such, Beck and Jones
(2010) argue that intermountain west fluted points most likely post-date the Clovis complex and are
contemporaneous with Folsom occupation in the Great Plains. This is consistent with the earliest dates from
Clovis sites which they argue occur in the southern Great Plains (Texas); a subsequent northwest migration
accounts for later dates in the northern Great Plains (Colorado).
Beck and Jones (2010:81) further suggest that “…initial colonization of the intermountain region most
likely involved groups moving inland from the Pacific coast carrying a non-Clovis technology, which was already
in place by the time Clovis technology arrived.” Although evidence of Terminal Pleistocene stemmed points is
lacking near the coast, they suggest that a likely migration route for coastal groups was up the Columbia River
onto the plateau and then into the Great Basin.
Mojave Desert
The flurry of new perspectives on the Terminal Pleistocene record in surrounding regions has yet to
significantly impact long-held views on the Mojave Desert archaeological record. A brief review is provided below.
Possible Early Assemblages
Periodically, assertions have been made that humans occupied the Mojave Desert as early as 40,000 years
ago, and these claims generally focus on sites with heavily weathered surface material that lack the formal shaping
characteristic of finished tools (see Moratto 1984:29-73 for a detailed review). These “pre-projectile point” sites
have often been referred to as the Malpais complex, and the absence of diagnostic tools and dating evidence has
led most archaeologists to discount assertions of very early occupation episodes (Sutton et al. 2007).
Most scholars believe that the earliest occupation in the Mojave Desert began considerably later, in the
Terminal Pleistocene (e.g., Moratto 1984). There are, however, no sites with radiocarbon assays on cultural
material that date to the Pleistocene. Infrequent fluted and non-fluted concave-base points are considered to fall
within this time frame (Basgall 1988; Basgall and Hall 1991; Byrd 2006, 2007; Rondeau et al. 2007; Sutton et al.
2007:234; Warren and Phagan 1988). These are most often recovered in isolated or mixed contexts, with the
most extensive documented in China Lake Basin (Basgall 2004, 2005, 2007; Byrd 2006, 2007; Davis and
Panlaqui 1978; Rondeau et al. 2007). There is also considerable difference of opinion whether or not fluted
lanceolate points should be referred to as Clovis points and therefore representative of the Clovis complex (which
Constructing a Regional Historical Context for Terminal
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Far Western
is tightly dated to between 13,500 and 12,800 cal BP), or instead subsumed within the Great Basin Concave Base
point series (Basgall 1995; Byrd 2006; Sutton et al. 2007; Warren 2008). The loose and inconsistent use of the
term Clovis in the Mojave Desert, at times being used to refer to all fluted points and to possible post-Clovis
complex time segments of the Pleistocene (between 12,800 and 11,600 cal BP), has hindered advances in
understanding the early record.
Overall, little is known about Terminal Pleistocene human occupation in the Mojave Desert; the nature
of land-use, subsistence, and the organization of technology remains poorly defined, as do basic temporal
parameters. While it is widely assumed that fluted and unfluted concave-base points in the Mojave Desert date to
the Terminal Pleistocene, this has never been demonstrated radiometrically or chronostratigraphically. Recent
obsidian hydration efforts provide a basis for constructing a relative time sequence, but hydration-age conversions
remain poorly resolved, particularly for the earliest time periods (e.g., Basgall 1991; Rosenthal 2010). These
efforts do indicate that fluted and unfluted concave-base points most likely predate stemmed points in the Mojave
Desert (e.g., Basgall 1988; Gilreath and Hildebrandt 1997; Gold et al. 2007; Meyer et al. 2010:Table 12;
Rosenthal 2010). They also provide a basis for linking site assemblages with similar obsidian hydration profiles
(but lacking diagnostic points) to a relative time sequence of projectile points (e.g., Byrd 2006, 2007).
Lake Mojave Assemblages
Lake Mojave Assemblages represent the earliest well-recognized and spatially extensive archaeological
occupation horizon in the Mojave Desert. The Lake Mojave Period is named in reference to the pioneering work
of Elizabeth Campbell (Campbell et al. 1937) along the margins of Pleistocene Lake Mojave, whose southern
portion lies within the Mojave National Preserve. Lake Mojave archaeological assemblages include stemmed Lake
Mojave and Silver Lake projectile points, crescents, pressure-flaked bifaces, flake-based tools, and percussionflaked cores (Basgall and Hall 1992, 1994a, 1994b; Basgall 1991, 1993; Basgall et al. 1988; Byrd 2006, 2007;
Byrd and Berg 2007; Eerkens et al. 2007; Sutton et al. 2007; Warren 1967, 1984, 1986). Flaked stone
technology focused on using non-obsidian fine-grained volcanics and metavolcanics and ground stone is also now
recognized as an integral aspect of the artifact assemblages (Basgall 1993; Basgall et al. 1988; Basgall and Hall
1994b; McGuire and Hall 1988). Sites are especially well-documented on Fort Irwin and NAWS China Lake as
well as near Lake Mojave.
Warren and his colleagues have argued that Lake Mojave Period settlements were mainly concentrated
along lake shores, and produced artifact assemblages reflecting heavy emphasis on hunting with only a minor
indication of plant processing (Warren 1967, 1984, 1986; Warren and Crabtree 1986; Warren et al. 1984;
Warren and Schneider 2003). Subsequent research by Basgall and Hall (1992) in contrast, has documented Lake
Mojave sites in a wider range of habitats with artifact and faunal assemblages indicative of a more generalized
adaptation (Basgall 1993; Basgall et al. 1988).
Lake Mojave assemblages are generally believed to date to the Early Holocene (11,600 to 8000 cal BP),
and possibly slightly earlier. However, only a handful of radiocarbon dates on cultural material have been
obtained, all of which fall in the Early Holocene (Basgall 1993:Table 3.1). Thus, no Lake Mojave sites have
produced evidence for Pleistocene-age occupation contemporaneous with early Western Stemmed point sites
elsewhere in the Great Basin and on the Columbia plateau (Beck and Jones 2010).
The subsequent Pinto Period, defined by the presence of Pinto points with characteristic shoulders and
bifurcated bases (Basgall and Hall 1992; Harrington 1957; Vaughan and Warren 1987), has traditionally been
considered to date to the Middle Holocene (circa 8000 to 4400 cal BP). However, recent dating results on shell
beads from six sites dominated by Pinto points all produced Early Holocene-age dates (Fitzgerald et al. 2005).
Moreover, most of the results (seven of 11 samples) predate 9000 cal BP, raising questions regarding earlier
estimates for the time span of both the Pinto and Lake Mojave periods (Basgall and Hall 1994a, 2000; Fitzgerald
et al. 2005; Schroth 1994).
Spatial analyses and obsidian hydration readings suggest that Western Stemmed Tradition points are
temporally later than concave-base points in the Mojave Desert (Basgall 1993:47; Basgall and Hall 1991; Meyer
et al. 2009:Table 17; Rosenthal et al. 2001; Rosenthal 2010). Such is not the case for Pinto points; they co-occur
Constructing a Regional Historical Context for Terminal
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with stemmed points at many sites and their obsidian hydration readings overlap significantly with those of
stemmed points (Rosenthal 2010).
In short, strong evidence for the timing of the origins and end of the Lake Mojave Period is lacking. It is
conceivable that it has its origins in the Terminal Pleistocene and its demise prior to the end of the Early
Holocene. Moreover, it is possible that other assemblages may have overlapped temporally with Lake Mojave
Period assemblages.
Evidence from the China Lake Basin Environs
As discussed, few localities in the Mojave Desert evince substantial human occupation during the
Terminal Pleistocene, when colonizing populations are thought to have first settled most of North America and
extinct megafauna still roamed the landscape. China Lake Basin, however, appears to be a major exception to this
trend. Although radiometric and chronostratigraphic evidence is lacking, the Pluvial Lake China area harbors a
number of small, discrete surface assemblages which have produced either diagnostic tools or potentially early
obsidian hydration readings, hinting at persistent human occupation during the Terminal Pleistocene.
Distinguished mainly by fluted and basally thinned concave-base projectile points and Coso obsidian
hydration readings averaging greater than about 15.0 microns, at least 14 separate surface sites or site loci in the
basin may date to the Terminal Pleistocene (e.g., Basgall 2004; Byrd 2006:Table 12; Byrd 2007:Table 17). China
Lake Basin also contains numerous localities where the fossil remains of large herbivores, including elephantidae,
bison, camelids, and equous have been found (Fortsch 1978). These remains are often spatially convergent with
the earliest archaeological residues (e.g., Basgall 2005; Davis and Panlaqui 1978). Currently, the surficial context
of these finds makes behavioral associations between extinct megafauna and early human hunters, unconvincing
(c.f., Basgall 2005:5-2; Davis and Panlaqui 1978; Moratto 1984:70).
China Lake Basin and the broader Indian Wells Valley also harbor extensive evidence for Lake Mojave
assemblages (Basgall 2004, 2005; Byrd 2006, 2007; Rosenthal et al. 2001). These surface sites are represented
mainly by Coso obsidian hydration readings, averaging between about 15.0 and 11.0 microns, and tool
assemblages including large projectile points of the Western Stemmed Tradition (e.g., Silver Lake and Lake
Mojave forms), domed unifacial “scrapers” or cores, chipped-stone crescents, and various other bifacial and
minimally modified tools. These assemblages are found widely in the basin. In contrast, post-Lake Mojave Period
occupation is rare in China Lake Basin (Basgall 2005:108-109; Rosenthal et al. 2001:74).
Why this comparatively small basin harbors such a high concentration of Terminal Pleistocene/Early
Holocene archaeological sites, and numerous other larger and better-studied basins in the Mojave Desert do not,
is an important problem; the answer to which may lead to a better understanding of the earliest human
adaptations in western North America. Undoubtedly, the answer will be greatly aided by gaining a better handle
on local paleoenvironmental conditions.
While aspects of the paleoenvironment have been reasonably well studied in adjoining lowlands such as
Owens Valley, we know little about the local environment in China Lake Basin during the Terminal Pleistocene/
Early Holocene. Lake histories remain poorly resolved and continue to be the subject of much speculation (e.g.,
Basgall 2004, 2005; Byrd 2006, 2007; Giambastiani 2008; Rosenthal et al. 2001; Warren 2008). Furthermore,
little is known about other types of environments that may have existed in the larger Indian Wells Valley during
the transition from the Pleistocene to the Holocene. Archeologists have suggested that lake-side marshes, spring
seeps, wet meadows, and other riparian settings were likely present in the valley bottom (e.g., Basgall 2004; Davis
and Panlaqui 1978; Rosenthal et al. 2001; Warren 2008), but little direct evidence of these types of mesic habitats
has been forthcoming. Understanding the environment in China Lake Basin and Indian Wells Valley during this
period is critical for identifying the types of plant and animal foods that may have attracted early foraging groups;
determining where in the basin those resources are likely to have existed; and distinguishing how climate changes at
the end of the Pleistocene may have influenced human economic and technological developments during the
Holocene.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
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4. FIELD INVESTIGATIONS AND NEW DATA ON THE
TERMINAL PLEISTOCENE/EARLY HOLOCENE
This chapter consists of three main sections. First, we briefly outline the research approach taken to gain
new insight into the Terminal Pleistocene/Early Holocene transition in the north-central Mojave Desert. Then
we summarize the nature of our field investigations and the analytical methods that were employed. Finally, we
present the results of our field investigations, highlighting the salient aspects of the new geomorphic records that
were documented during this study. This substantive section is divided into three main parts structured to
facilitate new insight into the paleoenvironmental history of the China Lake Basin: the inflow records, the lake
basin records, and the overflow records.
RESEARCH APPROACH
Despite considerable research on the hydrological and paleoenvironmental records of Owens Lake and
Searles Lake, the fluvial history of these interconnected basins during the Pleistocene/ Holocene transition is still a
subject of significant disagreement (c.f., Bacon et al. 2006; Benson et al. 1990; Orme and Orme 2008; Smith
2010). This has, in part, fueled debate about the nature of early human occupation in this region and the extent
to which lacustrine and/or some other types of mesic environments were the focus of early subsistence economies
in the Mojave Desert (c.f., Basgall 1993; Basgall and Hall 1994; Byrd 2006, 2007; Rosenthal et al. 2001; Sutton
et al. 2007; Warren 1967, 1984, 1986, 2008). The lack of consensus regarding the Owens and Searles records has
resulted in conflicting interpretations about the timing of lacustrine high stands at China Lake and the antiquity
of early human occupation in the basin, much of which lies well below the lake’s outflow sill (i.e., below
maximum lake level; e.g., Rosenthal et al. 2001; Warren 2009).
Because Indian Wells Valley (inclusive of Rose Valley and the China Lake Basin) is the main
hydrological link between Owens Valley and Searles Valley, paleohydrologic and geomorphologic records from
this area provide the most direct means of resolving discrepancies in the interpretation of the hydrologic record of
the lower Owens River system and the nature and timing of early human occupation in this region. As a result, a
main goal of the current effort was to generate new primary data on the paleohydrology and landscape history of
Indian Wells Valley during the period between 15,000 and 8000 cal BP. This was done through a program of
focused field and laboratory work combined with a literature search and broad synthesis of existing information
from Indian Wells Valley/China Lake Basin and the wider Mojave Desert.
FIELD INVESTIGATION METHODS AND ANALYTICAL STUDIES
To better understand the fluvial history of China Lake and the lower Owens River system, field work
focused on identifying geomorphic records related to the timing of water inflow, water outflow, and lake level
fluctuations within China Lake Basin. At various times in the past, China Lake Basin and the larger Indian Wells
Valley received surface water inflow from two primary sources: the Owens River through Rose Valley; and local
washes and streams, particularly those with large watersheds draining the eastern Sierra Nevada (St.-Amand
1986). To assess the contribution of these drainages during the Terminal Pleistocene and Early Holocene, we
examined natural and mechanical exposures along the Owens River system in Rose Valley, and all major washes
entering Indian Wells Valley from the eastern Sierra Nevada and El Paso Mountains. No substantial drainages
enter China Lake Basin from the White Hills and Coso Range to the north or the Argus Range to the east.
Fieldwork included several facets. Initially, wide-ranging field inspection of the inflow, lacustrine basin,
and overflow areas was conducted to better understand surface manifestations of the geomorphic record and to
identify localities for detailed study and sampling. Then 15 inflow alluvial sample localities were subjected to
detailed investigations (Table 1; Figure 6). These included six in Rose Valley (northwest of China Lake Basin),
seven in the southwest portion of Indian Wells Valley (one in Indian Wells Canyon and six along Little Dixie
Wash), and one locality immediately southwest of the valley in Dixie Wash. Then coring took place at seven
localities near the margins of China Lake Basin. Finally, surface samples were collected in two locations in the
general overflow area. These efforts, along with analytical methods, are summarized below. It should be noted
Constructing a Regional Historical Context for Terminal
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that the sample locations that were studied during these field investigations are entirely comprised of geological
field localities—none were archaeological sites.
Table 1. Summary of Field Investigations by Geological Sample Locality.
SETTING
LOCALITY
UTM EAST a UTM NORTH a LOCALITY TYPE
NUMBER
OF C-14
DATES
NUMBER OF
INVERTEBRATE
SAMPLES (PRESENT) b
Rose Valley, Inflow
Rose Valley flat
417934
3984967
Alluvial section 1
Rose Valley, Inflow
Cinder flat
418765
3981771
Alluvial section 1
Rose Valley, Inflow
Dead Chevy
415058
3984307
Alluvial section 1
Rose Valley, Inflow
Lava end
416269
3985690
Alluvial section 3
2 (0)
Rose Valley, Inflow
North Pit
415295
3991136
Alluvial section 2
1 (1)
Rose Valley, Inflow
South Pit
416035
3990462
Alluvial section 2
2 (0)
Indian Wells Canyon, Inflow 418471
3948131
Alluvial section 3
Little Dixie Wash, Inflow
Locus 1
422956
3935635
Alluvial section 2
2 (1)
Little Dixie Wash, Inflow
Locus 3
422592
3935262
Alluvial section 5
5 (1)
Little Dixie Wash, Inflow
Locus 4
421761
3935245
Alluvial section 3
3 (0)
Little Dixie Wash, Inflow
Locus 5
420471
3934298
Alluvial section 2
Dove Springs Wash
Locus 5771
408904
3918620
Alluvial section 2
3 (2)
China Lake Basin
Core 9
434038
3955277
Core
2
2 (0)
China Lake Basin
Couch et al.(2004) Core SB01 423635
3961800
Core
3
2 (0)
China Lake Basin
Couch et al. (2004) Core SB05 437475
3944908
Core
1
4 (4)
China Lake Basin
China Lake tufa knoll
445330
3950497
Surface
1
Overflow Area
Salt Wells Valley, outlet beach 447540
3949962
Surface
1
1 (1)
a
b
Notes: NAD 83 Zone 11; One additional sample was obtained from Little Dixie Wash locality 2. It contained ostracodes identical to those from
localities 1 and 5. Nine other samples from Couch et al. (2004) cores TTIWV-SB08, -SB10, and -SB28, and one sample from Core 8 retrieved during
the current study, were also analyzed for micro-invertebrates. These samples remain undated and are of little analytical utility (see Appendix D).
Inflow Record Sampling
In Rose Valley we documented and sampled alluvial strata at six separate geological localities in the central
and southern part of the valley trough. Five of the sample loci were located near the main valley axis where evidence
of the former Owens River channel is still visible (North and South Borrow Pits, Lava End, Rose Valley Flat, and
Cinder Flat). The sixth locality was an isolated playa in the southwest part of the valley (Dead Chevy Flat).
Most of the stream channels draining the eastern Sierra Nevada and El Paso Mountains into the Indian
Wells Valley were found to lack exposed deposits of appropriate age. We were, however, able to identify and
sample nine localities that had small isolated alluvial terraces dating to the Terminal Pleistocene/Early Holocene.
These sample localities were situated within three separate drainages emanating from the eastern slope of the
Sierra. These include Indian Wells Canyon (1 locality) and Little Dixie Wash (seven localities), which drain into
Indian Wells Valley/ China Lake Basin, and Dove Springs Wash (one locality), which drains southeast through
Red Rocks Canyon into Koehn Lake Basin (Figure 6).
Lake Level and Outflow Record Sampling
As part of our evaluation of the inflow and outflow history of China Lake Basin, we combined an
examination of lake shore features visible on the surface with a coring program in the central and northwest parts
of Indian Wells Valley. Lake features such as beach deposits, barrier ridges, strand lines, wave-cut platforms, and
calcareous tufa formations occur throughout China Lake Basin, offering direct evidence of the existence of former
lake stands at different elevations (Couch et al. 2004; Davis 1975; Davis and Panlaqui 1978; Gale 1915; Kunkel
and Chase 1969; Lee 1913; Moyle 1963; St.-Amand 1986). In an effort to determine the age and altitude of
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
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Sample Localities
China Lake Basin (683 m, 2240 ft)
Major Roads
Rivers
Waterbodies
Military Bases
Parks
Counties
Owens
Lake
Sa
C
lt
k
ree
Cos
395
INYO COUNTY
ang
us R
Arg
oR
e
20
Death Valley
e
ang
Haiwee
Reservoir
Kilometers
10
0
0
10
Miles
20
rgosa R
ive
y
nge
r
t Ra
lley
t Va
DEATH
VALLEY
NATIONAL
MONUMENT
eR
Slat
Southern Sierra Nevada
Ama
n
ami
n
ami
NAWS China Lake
North Range
alle
th V
Dea
Pan
Pan
Rose
Valley
e
ang
Sea
rles
China Lake
Basin
e
Vall
Indian Wells Canyon
h
duc
t
y
Ridgecrest
as
ue
W
ixie
Lit
tl
eD
e
L os Ang
Aq
les
dR
Re
o
as
lP
Little Dixie Wash
NAWS China Lake
South Range
ns
tai
un
o
M
Fort Irwin
k
oc
E
on
ny
Ca
14
Dove Springs Wash
Koehn
Lake
(Dry)
KERN COUNTY
SAN BERNARDINO COUNTY
Figure 6. Landscape Features and Geological Sample Locations in the China Lake Environs.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
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Far Western
particular lake stands, we examined and documented several such features in portions of the NAWS China Lake.
Examination and documentation of these lake-related features also focused on upper Salt Wells Valley and Poison
Canyon which forms the hydrological conduit between China Lake and Searles Basin. This examination was
focused in the Main Magazines and Ordnance T & E areas within NAWS China Lake and down-stream
localities in Poison Canyon. At two geological localities, samples were collected and dated.
As part of the coring effort, we sampled seven geological locations in China Lake Basin and along the
former Owens River fan in Indian Wells Valley. Sediments were recovered in cores from depths between about
two and 13 meters (~6 and 45 feet) below ground surface using a 4-inch diameter hollow-stem auger. Five cores
(3 through 7) on the Owens River fan were found to contain stratified alluvial deposits of terrestrial origin, but
lacked datable material and evidence of lacustrine deposition (note: access precluded drilling at locations originally
designated as cores 1 and 2). The two cores (Core 8 and 9) recovered along the margins of China Lake Basin
recorded a sequence of terrestrial and lacustrine deposits. Of these, further study focused on Core 9 because it
contained the most detailed and unambiguous record of lake and distal fan deposition.
Alluvial and lacustrine deposits previously recovered in select cores from Indian Wells Valley/China Lake
Basin (Couch 2003) were also examined and five stratigraphic samples from two of these earlier cores (SB-1 and
SB-5) were radiocarbon dated, and several samples were subjected to ostracode analysis. These samples, however,
are excluded from further consideration because the results proved stratigraphically inconsistent and largely
irrelevant (too old) for the current study.
Soil and Strata Designations and Descriptions
Stratigraphic units (strata) recorded in cores and cut-bank exposures were identified on the basis of
physical composition, superposition, relative soil development, and/or textural transitions (i.e., upward-fining
sequences) characteristic of discrete depositional cycles. Each exposed stratum was assigned a Roman numeral (I,
II, III, etc.) beginning with the oldest or lowermost stratum and ending with the youngest or uppermost stratum.
Buried soils (also called paleosols), representing formerly stable ground surfaces, were identified on the basis of
color, structure, horizon development, bioturbation, lateral continuity, and the nature of the upper contact with
the overlying deposit, as described by Birkeland et al. (1991), Holliday (1990), Retallack (1988), and Waters
(1992), among others. Detailed descriptions of sample localities are provided in Appendix A.
Master horizons describe in-place weathering characteristics and are designated by upper-case letters (A,
B, C), and are preceded by Arabic numerals (2, 3, etc.) when the horizon is associated with a different stratum
(i.e., 2Cu); number 1 is understood but not shown. Combinations of these numbers and letters indicate the
important characteristics of each major stratum and soil horizon; they are consistent with those outlined by
Birkeland et al. (1991), Schoeneberger et al. (1998), and the United States Department of Agriculture Soil Survey
Staff (1998).
Radiocarbon Dating and Regional Database Compilation
For this study, geological samples were submitted for radiometric analysis to Beta Analytic Inc. (BETA)
in Miami, Florida, or the National Ocean Sciences Accelerator Mass Spectrometry Facility (NOSAMS) at the
Woods Hole Oceanographic Institution in Massachusetts. All radiocarbon dates reported here (unless otherwise
indicated) were calibrated to calendar (solar) years before present (cal BP) according to Stuiver and Reimer (1993)
using the CALIB version 6.01 program and intcal04.14c dataset (Reimer et al. 2004) to compensate for secular
variations in the cosmic output of radiocarbon over time; by convention, zero years before present (0 BP) equals
1950 AD. The radiocarbon-dating methods and laboratory sample sheets are provided in Appendix B along with
the results.
To compensate for regional reservoir effects of old or dead carbon, following the findings of Lin et al.
(1998), a correction factor of 330 years was subtracted from all conventional dates obtained on carbonate
materials (i.e., tufa, oolites, CaCo3) and freshwater bivalve shells. All dates were then calibrated using the
terrestrial dataset for the northern hemisphere. No correction factor was applied to dates on ostracodes or
freshwater gastropod samples (e.g., Pigati 2002; Pigati et al. 2004). Individual dates are identified by their original
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
24
Far Western
lab number and reported as the calculated median probability intercept, while error ranges are reported at the 2sigma (95%) confidence interval.
A total of 36 new dates were obtained for this study on geological samples of algal tufa (carbonate),
freshwater gastropod shell, organic sediment (peat, soil), and plant remains (roots, pine needle). Dating results
and additional information about the new samples are reported in the following sections and presented in Table 2
and summarized in Figure 7.
A regional database of 576 radiocarbon dates from more than 163 separate localities in the Mojave
Desert and immediately adjacent regions (e.g., the Owens Valley) was also compiled from published and
unpublished sources. The database (Appendix C) includes information on location, elevation, provenience, and
stratigraphic context; obtained whenever possible from the primary sources.
In all, we compiled 224 dates (36.6%) from 69 localities in the Indian Wells Valley/China Lake Basin
and adjoining areas (Dove Springs Wash, Rose Valley, Searles Valley), and 388 dates from 97 other localities in
the Mojave Desert. About three-quarters of the total sample (n=469 or 76.6%) date to between 17,000 and 7000
cal BP, and are relevant for the current study of the Terminal Pleistocene/ Early Holocene transition.
Micro-Invertebrate Sampling and Analysis
A total of 38 geological sediment samples from China Lake Basin (n=20), Dove Springs Wash (n=3),
Little Dixie Wash (n=12), and Rose Valley (n=3) were analyzed for micro-invertebrates and mollusks by Dr.
Manuel R. Palacios-Fest (Appendix D). Only 11 of the samples contained ostracodes or mollusk shells. In
addition, 24 valves of the ostracode species Ilyocypris bradyi from two localities (Dove Springs Wash and North
Borrow Pit) were used to conduct stable isotope (δ13C and δ18O) analysis at the Environmental Isotope
Laboratory of the University of Arizona. A complete description of methods and results of the micro-invertebrate
and mollusk analyses are presented in Appendix D.
PROJECT RESULTS
This discussion is divided into three parts. First, inflow records are presented, organized by drainage.
Then Lake Level records are considered. Finally, the China Lake overflow records are discussed. The location and
extent of detailed maps for each sample locality are presented in Figure 8.
Inflow Records
This section includes a discussion of the Rose Valley geological localities followed by consideration of
those localities situated further to the southwest that drain the eastern Sierra Nevada (Indian Wells Canyon, Little
Dixie Wash, and Dixie Wash). This is followed by a synthesis of the inflow history during the Terminal
Pleistocene and Early Holocene.
Rose Valley Locality
As the main conduit for water flow between Owens and China lakes, geomorphic evidence from Rose
Valley is critical for understanding the fluvial history of these adjacent lake basins. Rose Valley ranges in elevation
from about 1,067 meters (~3,500 feet) amsl at its northern end, about 78 meters (~256 feet) below the Owens
Lake outflow sill, to about 1,036 meters (~3,400 feet) amsl at its southern end, and about 1,200 meters (~3,937
feet) above the China Lake outflow sill. The valley’s long axis trends from northwest to southeast and is relatively
small; about 18.5 kilometers (11.5 miles) in length and ten kilometers (~6.2 miles) in width. It is bounded on the
west by faults along the base of the eastern Sierra Front Range (dominantly granitic rocks), and on the east by
faults at the base of the Coso Range and Darwin Hills (dominantly volcanic rocks). Outcrops of Pliocene
rhyodacite occur at the northern end of the valley, and Pleistocene basalt flows (e.g., Little Lake and Red Hill)
outcrop at its southern end (Duffield and Bacon 1981; Duffield and Smith 1978; Jayko 2009).
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
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Far Western
Beta-237061
Beta-249418
Beta-249419
Beta-259414
Beta-259415
Beta-259416
Beta-260150
Beta-260151
Beta-260152
Organic (black mat)
165
9410
100 -24.5 10372 10656 10887
Beta-260153
Organic (black mat)
180
8120
100 -23.1
8703
9065
9321
Beta-260154
Organic sediment
50
6770
100 -22.2
7458
7627
7797
Beta-260155
Soil (SOM)
Soil (SOM)
Shell (gastropod)
Soil (SOM)
Soil (SOM)
Organic sediment
90
300
175
198
270
427
9720
9750
10000
9610
10120
9690
100
50
60
50
60
50
-24.1
-24.5
-11.6
-25.3
-25.6
-26.3
10742
11088
11262
10766
11590
11067
11097
11190
11486
10944
11746
11123
11289
11250
11722
11167
11988
11225
Beta-260156
Beta-272225
Beta-272226
Beta-272227
Beta-272228
Beta-280679
Organic sediment
1064
14610
50
-24.6 17501 17780 18026
Beta-280680
Soil (SOM)
Soil (SOM)
Carbonate (tufa)
Organic sediment
155
268
1
255
9930
10450
11440
8790
40
40
50
40
-25.2 11235 11324 11410
-25.5 12202 12387 12549
4.6 12773 13000 13138
-25.0 9627 9811 9939
Beta-280681
Beta-280682
Beta-280683
Beta-280684
Organic sediment
470
11560
50
-25.9 13276 13395 13567
Beta-280685
INY, Rose Valley, Lava end
26
INY, Rose Valley, Lava end
INY, Rose Valley, Lava end
INY, Rose Valley, Chevy flat
KER, Indian Wells Canyon
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
KER, China Lake, Core 9
KER, China Lake, Core 9
Far Western
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
SBR, China Lake, tufa knoll
INY, Rose Valley, north pit
INY, Rose Valley, south pit
LABORATORY
NO.
270
8790
40
nr
9627 9811 9939
5258 16250 80 -25.5 19215 19416 19583
6371 12160 70 -27.4 13788 14008 14224
3079
180
40 -22.8 131
176
230
3201 >Mod. na -22.4
5700 >Mod. na -21.9
15
7320
80 -23.7 7994 8129 8323
70
9180 100 -22.8 10184 10369 10588
60
4440
80 -23.0 4867 5074 5295
UPPER
2-SIGMA
Soil (SOM)
Organic sediment
Soil (SOM)
Organic sediment
Plant (parts)
Plant (pine needle)
Organic sediment
Organic sediment
Organic sediment
CAL BP
(MED. PROB.)
Profile IK-01, 2Ab buried fan/terrace
Bore Hole TTIWV-SB01
Bore Hole TTIWV-SB01
Bore Hole TTIWV-SB05
Bore Hole TTIWV-SB05
Bore Hole TTIWV-SB05
Auger 2, Rose Valley Flat
Auger 4, Cinder Flat
Column Sample, Lava End; 2Ab
horizon below Cartago soil
Column Sample, Lava End; black
mat below Cartago soil
Column Sample, Lava End; black
mat below Cartago soil
Lava End Rose Valley Flat; 2Ab
horizon below Cartago soil
Auger 7, Dead Chevy Flat, 2Ab
Profile IK-01, 3Ab soil near base of cutbank
Locality 1, cutbank along west side of wash, 2Ab
Locality 1, cutbank along west side of wash, 2Ab
Locality 1, cutbank along west side of wash, 3Ab
Core 9, 6Cg, pale olive silty clay, distal fan,
slough, or playa above coarse beach deposit
Core 9, 11Cg, olive gray near-shore
sand below coarse beach deposit
Local 4, Auger 1, T-3(?) terrace, 3Ab horizon
Local 4, Auger 1, T-3(?) terrace, 7Ab horizon
Algal tufa on granitic knoll W of lake outlet
RV-NCTP-3Cu Strat. II, within
coarse channel facies
RV-SCTP-4Ob Strat. II, lower playa, east side
LOWER
2-SIGMA
KER, Indian Wells Canyon
KER, China Lake, Core SB01
KER, China Lake, Core SB01
KER, China Lake, Core SB05
KER, China Lake, Core SB05
KER, China Lake, Core SB05
INY, Rose Valley flat
INY, Rose Valley, Cinder flat
INY, Rose Valley, Lava end
±
12C/13C
MATERIAL DATED
14C CRY BP
CONTEXT AND DESCRIPTION
CM
COUNTY, LOCALITY, LOCUS
MEAN DEPTH
Constructing a Regional Historical Context for Terminal
Pleistocene/Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
Table 2. Radiocarbon Sample Dating Results for this Study Listed by Lab Number.
SBR, Searles, Salt Wells Valley
LABORATORY
NO.
UPPER
2-SIGMA
CAL BP
(MED. PROB.)
LOWER
2-SIGMA
±
12C/13C
MATERIAL DATED
14C CRY BP
CONTEXT AND DESCRIPTION
CM
COUNTY, LOCALITY, LOCUS
MEAN DEPTH
Constructing a Regional Historical Context for Terminal
Pleistocene/Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
Table 2. Radiocarbon Sample Dating Results for this Study Listed by Lab Number continued.
27
Beach sand, marl, Anodonta and snail shells
Shell (gastropod)
1
11550 50 -8.0 13267 13387 13537 Beta-280686
on wave-cut bedrock platform
KER, Indian Wells, Little Dixie Local 4, Auger 1, T-3(?) terrace, 5Ab horizon
Soil (SOM)
210 10510 50 -25.6 12375 12473 12610 Beta-280734
KER, Indian Wells Canyon
Profile IK-01,
Organic sediment
373 10240 50 -24.8 11758 11984 12142 Beta-280735
6Ob, thin peaty layer near base
KER, Dove Springs Wash
DSW-L#5771-5Ab Strat. X (IX in field)
Soil (SOM)
107
4230
40 -23.4 4685 4753 4861
Beta-280993
KER, Indian Wells, Little Dixie Fan Local 5, left bank, 3Ab, flaketool in 3Cu
Soil (SOM)
233
6990
40 -23.2 7718 7827 7882
Beta-281207
KER, Indian Wells, Little Dixie Fan Local 5, left bank, 4Ab, below flaketool
Soil (SOM)
285
6340
40 -23.2 7168 7273 7331
Beta-281208
KER, Dove Springs Wash
DSW-L#5771-5Ab Strat. X
Plant (roots)
107 >Mod. na -21.3
OS-79559
KER, Dove Springs Wash
DSW-L#5771-13Ab Strat. I, basal unit
Soil (SOM)
440 10300 60 -25.4 11953 12102 12393
OS-79560
KER, Indian Wells, Little Dixie LDW-L#2-2Ab Strat. II, east bank
Plant (roots)
35 >Mod. na -20.4
OS-79561
KER, Indian Wells, Little Dixie LDW-L#2-3ABkb Strat. I, east bank
Plant (roots)
55 >Mod. na -26.2
OS-79562
KER, Indian Wells, Little Dixie LDW-L#3-4Ab Strat. IV, with snails, west bank Soil (SOM)
263 10000 55 -24.9 11263 11482 11717
OS-79563
KER, Indian Wells, Little Dixie LDW-L#3-6Ab Strat. II, west bank
Soil (SOM)
320 10100 55 -25.5 11399 11697 11844
OS-79564
KER, Indian Wells, Little Dixie LDW-L#3-7Ab Strat. I, basal unit, west bank
Soil (SOM)
350 10500 60 -25.7 12369 12454 12598
OS-79565
INY, Rose Valley, north pit
RV-NCTP-3Cu Strat. II, channel facies, north Plant (roots)
255 >Mod. na -13.1
OS-79566
INY, Rose Valley, south pit
RV-SCTP-4Ob Strat. II, lower playa, east side Plant (roots)
470 >Mod. na -12.7
OS-79567
INY, Rose Valley, north pit
RV-NCTP-2Ab Strat. III, north wall
Soil (SOM)
75
985
45 -22.0 788
883
971
OS-79583
KER, Indian Wells, Little Dixie LDW-L#3-3Ab Strat. V, with snails, west bank Soil (SOM)
203
9440
95 -25.2 10479 10703 11099
OS-79584
KER, Indian Wells, Little Dixie LDW-L#3-5Ab Strat. III, weak soil, west bank Soil (SOM)
298 10100 110 -25.1 11271 11688 12058
OS-79585
KER, Dove Springs Wash
DSW-L#5771-8Ab Strat. VI, with snails
Plant (roots)
223 >Mod. na -24.5
OS-79586
INY, Rose Valley, south pit
RV-SCTP-3Ab Strat. III, upper playa, east side Soil (SOM)
210
9980
55 -24.1 11250 11447 11645
OS-79587
Notes: Samples Beta-259414, -259415, -259416, 249418 and -249419 were obtained from cores previously reported by Couch (2004) and were stored at the core repository at
UC Bakersfield when accessed for the current project. We assume based on the modern dates, that Samples Beta-259414, -259415, -259416 were contaminated with recent
organics at some point following collection. Samples OS-79559, -79561, -79562, -79566, -79567, -79586 are modern root fractions. A miscommunication with the radiocarbon
laboratory resulted in analysis of these modern contaminants, rather than the organic sediment (SOM) fraction intended.
Far Western
KER, China Lake, Core 9
INY, Rose Valley, south pit
SBR, Searles, Salt Wells Valley
SBR, China Lake, tufa knoll
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
KER, Dove Springs Wash
KER, Indian Wells Canyon
KER, Indian Wells, Little Dixie
Figure 7. Distribution of Radiocarbon Dates from this Study.
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
Locality or Locus
INY, Rose Valley, south pit
KER, Indian Wells, Little Dixie
KER, Indian Wells Canyon
KER, China Lake, Core 9
INY, Rose Valley, Dead Chevy
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
INY, Rose Valley, Lava end
INY, Rose Valley, Cinder flat
KER, Indian Wells Canyon
INY, Rose Valley, north pit
INY, Rose Valley, Lava end
INY, Rose Valley flat
KER, Indian Wells, Little Dixie
INY, Rose Valley, Lava end
KER, Indian Wells, Little Dixie
INY, Rose Valley, Lava end
KER, Dove Springs Wash
0
1,500
3,000
4,500
6,000
7,500
9,000
10,500
12,000
13,500
15,000
16,500
18,000
INY, Rose Valley, north pit
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
HOLOCENE
PLEISTOCENE
cal BP (Median Probability, 2-Sigma Range)
28
Far Western
so R
ang
e
INYO COUNTY
us R
Arg
Haiwee
Reservoir
e
ang
Pan
n
ami
Fig. 9
eR
Slat
Southern Sierra Nevada
lley
t Va
Fig. 22
e
ang
Fig. 23
Sea
rles
China Lake
Basin
e
Vall
Wash
y
Fig. 26
t le
Dix
ie
Fig. 12
ue
Lit
Ridgecrest
duc
t
Fig. 15
L
les
n ge
os A
Aq
El
Pa
so
ta
un
Mo
ins
d
Re
C
ck
Ro
Fig. 19
n
yo
an
Koehn
Lake
(Dry)
0
Kilometers
5
10
14
0
5
Miles
10
SAN BERNARDINO COUNTY
KERN COUNTY
Figure 8. Index Map Showing Location and Extent of Detailed Maps for Geological Sample Localities.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
29
Far Western
A complex series of Pleistocene- and Holocene-age alluvial fans coalesce around the valley margins to
form sloping aprons along its eastern and western sides. Recent alluvial deposits are more localized and largely
restricted to the lowest-lying portions of the valley floor (Jayko 2009). All six geological localities reported below
occur within these recent deposits and are inset below higher and older fan remnants originating at the base of the
eastern Sierra (Figure 9). Distinctive natural features within the valley include a relatively young volcanic cinder
cone (Red Hill), a paleo-waterfall carved into basalt by the Owens River channel (Fossil Falls), and a spring-fed
body of water known as Little Lake, all located in the southern part of the valley. Paleoenvironmental records
indicate a meadow, salt grass marsh, and shallow ponds existed at Little Lake between about 5800 and 3200 cal
BP, suggesting the water table was nearly 13 meters lower then than at present (Mehringer and Sheppard
1978:165).
Borrow Pit Loci
The north and south borrow pits are situated near the center of Rose Valley about 1.25 kilometers
(~0.78 miles) and 0.4 kilometers (0.25 miles) due north of Gill Station/Coso Road, and roughly 1.1 kilometers
(0.7 miles) and 1.6 kilometers (1.0 mile) due east of State Route 395, both respectively (Figure 9). The pits lie
about 0.8 kilometers (0.5 miles) apart within the relatively flat valley-axis alluvial unit of Jayko (2009). Both pits
have irregularly cut sloping-side walls that expose alluvial deposits from a few meters to several meters below the
original ground surface (Figure 10). Each was excavated by Caltrans in the 1960s to extract sand and gravel
deposited by the lower Owens River and alluvial fans emanating from the eastern Sierra.
South Borrow Pit
In the south pit, a six-meter-thick, vertically stratified sequence of channel, floodplain, lacustrine/paludal,
and eolian deposits is exposed along the eastern side. The basal stratum (Stratum I-5Cu) consists of coarse sand
that grades downward into rounded to subrounded gravel and cobbles with sorting and bedding that clearly
represent the bed load of a formerly active stream or river channel (Figure 11). This stratum is overlain by a thin
layer of dark organic-rich silt (Stratum II-4Ob, or black mat 1) that marks a transition from high-energy to lowenergy depositional conditions. A radiocarbon date from Stratum II (11,560 ± 50 BP, or 13,395 cal BP, Beta280685) indicates this transition occurred during the Terminal Pleistocene.
Above these strata lies a relatively thick deposit of light-colored silt loam (Stratum III-3Cu) with a very
prominent dark organic-rich horizon in the upper 0.5 meters (Stratum IV-3AOb, or black mat 2; Figure 11). The
uniform fine-grained texture, light lower and dark upper horizons, and presence of mesic-adapted snails indicate
this stratum was deposited in a shallow lake or wetland setting, as noted by Jayko (personal communication
August 2010). A sample of the 3OAb horizon of Stratum III submitted for this study yielded a radiocarbon date
of 9980 ± 55 BP, or 11,447 cal BP (OS-79587), and a nearly identical date of 10,000 ± 40 BP, or 11,473 cal BP
(WW-4519) was obtained by Jayko (personal communication August 2010) on a second sample from the same
horizon. This evidence confirms the presence of lacustrine/paludal (marsh) environments in Rose Valley during
the transition from the Terminal Pleistocene to Early Holocene.
The prominent upper black mat is abruptly overlain by a fining-upward deposit of loam and loamy sand
of mixed alluvial and eolian origins in which a weakly developed soil has formed (Stratum V-2Ab/2Cu).
Overlying this is a deposit (Stratum VI) of pale brown coarse sand that contains a poorly sorted mixture of gravel
and cobbles whose origin can be attributed to a combination of alluvial and eolian processes within the valley axis
(Figure 11).
North Borrow Pit
The north pit contains a sequence of vertically stratified channel, floodplain, and eolian deposits that
were exposed in a five-meter-thick section on the pit’s northeastern side. Here, the basal stratum (Stratum I4Cu4) consists of coarse sand with weakly sorted and poorly bedded subangular to well-rounded gravel and
cobbles that appear to be an alluvial fan deposit (Figure 11). This stratum is overlain by a relatively thin layer of
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
30
Far Western
North Borrow Pit (1031 m, 3383 ft)
South Borrow Pit
Coso Junction
L
O
S
S E
R O
A
N
G
E
U E D U C T
A Q
E
U
U G O N
T
R
N Y
P O
C A
E Y
L L
VA
S
L E
S E
395
Lava End
Rose Valley Flat
Dead Chevy
R E D
H I L L
1182 m, 3877 ft
Cinder Flat
F O S S I L
FA L L S
L
T
I T
L
E
L A K E
C A
N
YO
L I T T L E
L A K E
958 m, 3143 ft
N
Legend
0
Kilometers
1
2
Sample Loci
0
1
Miles
2
Figure 9. Rose Valley Landscape Features and Sample Loci.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
31
Far Western
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
3AOb 11,447 cal BP
(OS-79587)
4Ob 13,395 cal BP
(Beta-280685)
3Cu3 9811 cal BP
(Beta-280684)
2Ab 5050 cal BP
(Beta-260152)
3Ob1, 3Ob29065 cal BP,
10,656 cal BP
(Beta-260154,
Beta-260153)
Middle Holocene Alluvial
Fan Deposits Overlying
Early Holocene Black
Mats in Pauludal Deposit
at Lava End Locus
Red Hill
32
Channel Deposit Below Black Mat
(4Ob) in South Borrow Pit
Black Mat (3AOb) in Paludal
Deposit, South Borrow Pit
Far Western
Overview of South Borrow Pit Locus to Northeast
Organic Silt (3Cu) in Alluvial
Fan Deposit, North Borrow Pit
Overview of North Borrow Pit Locus to Northwest
Lava End Sample Location Rose Valley,
Inyo County, View to South
Lava End Sample Location Rose Valley, Inyo County,
View to Northeast
Figure 10. Rose Valley Alluvial Landforms and Stratigraphy.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
SOUTH BORROW PIT
STRATUM
LAVA END
AC - Very pale brown
coarse sand,
gravel, and cobbles
VI
AC - Pale brown sand
V
X
1
IV
1
2Ab - Light brownish-gray
V
2Cu - Light yellowish-brown
sandy loam
10,000 ± 40 BP, or
11,473 cal BP
(WW-4519)
NORTH BORROW PIT
2
X
3AOb - Dark gray
organic-rich
silt loam
(black mat 2)
IV
8120 ± 100, or
9065 cal BP
(Beta-260154)
9410 ± 100, or
10656 cal BP
(Beta-260153)
III
2
II
I 2.2
X
X
A - Very pale brown
silty clay
II
2Ab - Pale loamy sand
6770 ± 100, or 7627 cal BP
(Beta-260155)
4440 ± 80, or 5074 cal BP
(Beta-260152)
2CU - Light yellowish-brown
coarse sand
3Cu1 - Light gray silt
I
3AOb1 - Gray sitly clay (black mat 4)
3Cu2 - Light gray silt
3AOb2 - Dark gray silty clay (black mat 3)
3Cu3 - Light gray silt
4Cu - Pale brown fine sand
5Cu - Very pale brown
coarse sand
HISTORIC GROUND SURFACE
(Capped by 2.0 meters of artificial fill)
A - Brown sandy loam
0
0
0
0
9980 ± 55 BP, or
11,447 cal BP
(OS-79587)
DEAD CHEVY FLAT
HORIZON - Description
IV
Cu1 - Light yellowish-brown
silty clay
Cu2 - Sand
985 ± 45 BP,
1
X
2Ab - Yellowish-brown
sand
9720 ± 100,
or 11097 cal BP
(Beta-260156)
or 883 cal BP
(OS-79583)
Cu - Pale brown silt laminated/bedded
1
X
2Ab - Grayish brown sandy
loam
III
2Cu1 - Brown sandy loam
2Cox - Dark yellowish-brown
coarse sand and gravel
2
2
2Cu2 - Poorly sorted small/large
gravel and cobbles lag deposit
2.5
II
8790 ± 40 BP,
9811 cal BP
(Beta-280684)
33
3
X
3
III
3Cu3 - Brown to light gray fine well
sorted sand
4Cu4 - Weakly sorted and poorly bedded coarse sand
and gravel, small/medium
cobbles. Sub-angular
to well rounded
3Cu - White silt loam
I
4
4
11,560 ± 50 BP, or
13,395 cal BP
(Beta-280685)
X
II
5
4Ob - Very dark grayish-brown
organic-rich silt (black mat 1)
5Cu - Brown fine to coarse sand, rounded
to subrounded gravel and cobbles,
well sorted and bedded, coarsening downward
5
I
Note: Depth in Meters
6
Far Western
Figure 11. Alluvial Stratigraphy of Selected Rose Valley Loci.
fine, well-sorted sand containing a dark organic silt lens that pinches out to the west (Stratum II-3Cu3), marking
a transition from high-energy to lower-energy depositional conditions. A date from the silt lens of 8790 ± 40 BP,
or 9811 cal BP (Beta-280684) indicates that this transition occurred during the Early Holocene.
Three species of micro-invertebrates (two ostracodes and one mollusk) occurred in the 3Cu Horizon
(see Appendix D, Table 5). The ostracodes Ilyocypris bradyi and Fabaeformiscandona acuminata suggest a dilute,
spring source. F. acuminata’s salinity tolerance is below 1,000 milligrams L-1 total dissolved solids (TDS)
(Forester et al. 2005) implying that the sample location is close to the water source (see Appendix C, Table 4).
Two mollusk specimens of Tryonia sp. were also identified in the sample (see Appendix C, Table 7). The genus
Tryonia is known to prefer low-to-moderate salinity (1,000-2,000 milligrams L-1 TDS; Sharpe 2002, 2003;
Appendix D, Table 6).
Five valves of I. bradyi were analyzed for carbon and oxygen isotopes. As discussed in the Results section
of Appendix D, the δ18O value obtained from the 3Cu samples are the most positive obtained from the China
Lake region suggesting either arid conditions prevailed during the Early Holocene or rainfall was more seasonal
(e.g., monsoons; Appendix D, Table 8).
The sand lens is abruptly overlain by an erosional lag deposit of poorly sorted small-to-large gravel and
cobbles (Stratum III-2Cu2) that fines-upward into a sandy loam in which a weakly developed soil has formed
(Stratum III-2Ab/2Cu1). The mixed nature of Stratum III likely reflects the influences of both alluvial and
eolian processes. A date of 985 ± 45 BP or 883 cal BP (OS-79583) from the 2Ab horizon provides a minimum
age for Stratum III, and a maximum age for the deposit of alluvial silt and sandy loam that overlies it (Stratum
IV-A/Cu). Finally, this section is overlain by about 2.0 meters of artificial fill derived from the borrow activities
(see Figure 11).
Neighboring Geological Localities—Dead Chevy Flat, Cinder Flat, Rose Valley Flat, and Lava End
Other Early Holocene dates were obtained from buried soils and organic black mats identified in small
surface playas elsewhere in the valley. At Dead Chevy Flat to the southwest of the borrow pits (see Figure 9), a
buried soil (2Ab) that formed on a fan deposit of coarse sand and gravel (Stratum I-2Cox) provided a date of
9720 ± 100 BP, or 11,097 cal BP (Beta-260156). This buried soil was overlain by light-colored, fine-grained
playa deposits (Stratum II in Figure 11).
In the valley axis at the Lava End locality (see Figure 9), a six-stratum sequence was identified in which
coarse and fine sand (Stratum I-6Cu and Stratum II-5Ab) is overlain by two vertically stratified organic black
mats (Stratum III-3AOb1 and 3AOb2), both formed in silty clay (see Figure 11). The lower 3Ob2 mat is dated
at 9410 ± 100 BP, or 10,656 cal BP (Beta-260153), and the upper 3Ob1 mat dates to 8120 ± 100, or 9065 cal
BP (Beta-260154). Overlying black mat 4 is a fining-upward deposit of coarse-sand to loamy sand that contains
some internal sorting and bedding, consistent with an alluvial origin (Stratum IV-2Ab/2Cu). A weakly developed
soil that formed in the upper part of Stratum V yielded radiocarbon dates of 6770 ± 100, or 7627cal BP (Beta260155) and 4440 ± 100, or 5074 cal BP (Beta-260152), indicating it is Early-to-Middle Holocene in age. Above
this lies a moderately indurated, pale brown sand deposit that is probably eolian in origin (see Figure 11).
Dates similar to those from black mat 3 and 4 at Lava End were obtained at nearby Cinder Flat and Rose
Valley Flat. Thin, organic-rich buried soils (2Ab Horizons) at these localities yielded dates of 9180 ± 100, or
10,369 cal BP (Beta-260151) and 7994 ± 80, or 8129 cal BP (Beta-260150), respectively (see Figure 9; not
depicted in Figure 11 or elsewhere).
Eastern Sierra Drainages
Indian Wells Canyon
Situated on the western side of Indian Wells Valley, this geological locality occurs in the lower part of
Indian Wells Canyon about 8.5 kilometers (~5.3 miles) west-northwest of the town of Inyokern, and about 2.9
kilometers (~1.8 miles) west of State Route 14 along Indian Wells Canyon Road; about 100 meters due south of
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
34
Far Western
the gravel road (Figure 12). The exposed section lies along the canyon’s south side where a north-flowing wash
meets the east-west oriented canyon bottom at an elevation of about 1,000 meters (3,280 feet) amsl; roughly 340
meters (1,115 feet) above the floor of China Lake Basin. At this point, the wash is deeply incised through an
isolated alluvial terrace that is set against the surrounding granitic bedrock. Incision during the late Holocene has
removed a 20-meter-long segment of the terrace, exposing a five meter vertical sequence of 11 alluvial strata along
the eastern side of the wash. These strata rest upon steep granitic hill slopes (Stratum I) that are weathered and
truncated by erosion (Figure 13).
The basal alluvial stratum (Stratum I-9Cox) is an erosional lag deposit consisting of coarse granitic sand
and small subangular-to-subrounded gravel with iron-oxide mottling throughout (Figure 14). This is overlain by
a very thin organic mat of dark grayish-brown sandy clay loam (Stratum II-8Ob) that marks a transition from
erosional to depositional conditions. This lower mat is covered by a deposit of very fine well-sorted sand that is
either alluvial or eolian in origin, or both (Stratum III-7Cu1/7Cu2). Above this is a poorly sorted and bedded
channel deposit composed of oxidized sand and gravel (Stratum IV-6Cox) that fines upward into sandy loam
containing another thin organic mat at the top (Stratum IV-6Ob). A date of 10,240 ± 50 BP, or 11,984 cal BP
(Beta-280753) obtained on this mat confirms it is Terminal Pleistocene in age. This upper mat is buried by a
deposit of fine oxidized sand that is massive and probably eolian in origin (Stratum V-5Cox). Capping this
stratum is a 20-centimeter thick layer of dark grayish-brown loamy sand that contains a very weakly developed
soil (Stratum VI-4Ab).
A deposit of oxidized alluvial sand overlies Stratum VII, which fines upward into loamy sand containing
a moderately developed soil (Stratum VII-3Ab/3Cox). A date of 9750 ± 50 BP, or 11,190 cal BP (Beta-272225)
obtained on the 3Ab horizon indicates it is Early Holocene in age, and that underlying strata (VI and VII) mark
the transition from the Terminal Pleistocene to the Early Holocene.
This soil is buried by a deposit of poorly sorted and well-bedded alluvial sand that grades into grayishbrown loamy sand. It is distinguished by a moderately developed soil that contains some flaked stone debitage of
Coso obsidian (Stratum VIII-2Ab/2Cu). A sample of the 2Ab Horizon yielded a date 8790 ± 40 BP, or 9811 cal
BP (Beta-237061) demonstrating that it is also Early Holocene-age. This former land surface is covered by about
80 centimeters of brown loamy sand that lacks any obvious soil development (Stratum IX-AC), suggesting it was
probably deposited during the Late Holocene (<4000 cal BP).
Little Dixie Wash
Little Dixie Wash is the largest of the three drainages exiting the eastern Sierra Nevada, where alluvial
records from the Terminal Pleistocene/Early Holocene are stored. This geological locality is situated in the
southwestern part of Indian Wells Valley about 11 kilometers (~6.8 miles) southwest of the town of Inyokern,
and about 6.3 kilometers (~3.9 miles) southeast of the intersection of State Route 14 with State Route 178
(Freeman Junction); more than eight kilometers (five miles) east of the Sierra Nevada Front range (Figure 15).
The wash drains from southwest to northeast directly into China Lake Basin and is the main internal drainage for
that part of Indian Wells Valley. The portion of the wash examined for this study ranges in elevation from about
860 to 830 meters (2,821 to 2,723 feet) amsl, which is more than 160 meters (~525 feet) above the basin floor,
and about one-half the elevation of the Indian Wells Canyon locality. The wash channels runoff from Freeman
Canyon, Cow Heaven Canyon, Sage Canyon, Peak Horse Canyon, and Bird Spring Canyon.
The medial portion of Little Dixie Wash contains alluvial terraces that are inset several meters or more
below the surface of a broad and highly dissected alluvial fan that emanates from Freeman Canyon to the west
(Figure 16). Immediately to the east, a basalt flow—part of the El Paso Mountains—rises more than 95 meters
(~315 feet) above the channel (Figure 15). In this section of the wash, the channel is incised through the inset
alluvial terrace (T2 terrace) for 2.8 kilometers (~1.75 mile), creating a series of natural bank exposures about one
to three meters above the channel bottom. Four sections containing stratified alluvial deposits exposed in the inset
terrace were sampled on the western bank of the wash (Localities 1, 3, 4, 5; Figure 15). In addition, two isolated
deposits of exceptionally large cobbles were identified within this segment, each forming a ridge on either side of
the wash.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
35
Far Western
1450 m, 4757 ft
Athel Ave
Inse
t
Ter
rac
e
Indi
an W
ell
an
Indian Wells Canyon
(989 m, 3,244 ft)
14
sC
yo
Rd
ES AQUEDUCT
EL
n
I N
D
I A
N
W
E L
L S
VA
L L
E Y
G
L OS AN
Bow Ave
St Louis Ln
Legend
0
Kilometers
0.5
1
Sample Locus
Inset Terrace
0
0.5
Miles
1
Figure 12. Indian Wells Canyon Inset Terrace and Sample Locus.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
36
Far Western
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
Indian Wells Canyon Sample Locus and Indian Wells Valley in Distance (east)
Strata Exposed in Incised and Inset Alluvial Fan Terrace to Southeast
37
2Ab 9811 cal BP
(Beta-237061)
Far Western
Radiocarbon-Dated Strata within Alluvial Fan Terrace
Figure 13. Indian Wells Canyon Sample Locus.
STRATUM
HORIZON - Description
0
AC -
IX
8790 ± 40, or 9811 cal BP
(Beta-237061)
1
X
Brown loamy sand
2Ab - Grayish-brown loamy sand, contains
Coso obsidian debitage
VIII
2Cu - Light gray sand, poorly sorted, well bedded
2
9750 ± 50, or 11,190 cal BP
(Beta-272225)
X
VII
3Ab - Dark gray loamy sand
3Cox - Brown sand, prominent
oxidization throughout
3
VI
4Ab - Dark grayish-brown loamy sand
V
5Cox - Light olive-brown fine sand, well sorted
10,240 ± 50, or 11,984 cal BP
(Beta-280753)
X
IV
4
III
II
I
6Ob - Dark gray sandy loam, organic rich (black mat)
6Cox - Strong brown sand, poorly sorted and bedded,
oxidation nearly continuous
7Cu1 - Brown very fine sand, well sorted
7Cu2 - Brown very fine sand, well sorted, oxidization throughout
8Ob - Dark grayish-brown sandy clay loam, organic rich (black mat)
9Cox - Strong brown sand, oxdidation throughout
Note: Depth in Meters
Figure 14. Indian Wells Canyon Terrace Alluvial Stratigraphy.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
38
Far Western
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
Locus 1
T1
T2
Locus 4
Locus 3
R
oa
d
Acti ve Wash
Figure 28
Transect
T3 - Older Fan
C
an
yo
n
T1
T2?
Locus 2
ed
R
oc
k
T1
T3 - Older Fan
R
H
F R
E E
M A
N
G
L
W
U
T1
39
C
H
WA
S H
Fan
T1
T3 - Older Fan
L
IT
E
TL
D I X
I E
Fan
T2
T1
East Cobble Ridge
A S
T1
Fan Locus 5
Black Butte Basalt
929 m, 3047 ft
West Cobble Ridge
Sample Loci
Early Holocene Fan
Terrace 3, Older Pliestocene Fan
Active Wash
Terrace 1, Late Holocene
Terrace 2, Terminal Pleistocene-Earliest Holocene
Black Butte Basalt
Far Western
Figure 15. Little Dixie Wash Landscape Features and Sample Loci.
Feet
1,000
0
0
200
Meters
2,000
400
T2
3Ab - 10,703 cal BP
(OS-79584)
2Ab 10,944 cal BP,
11,486 cal BP
on soil, snail
(Beta-272227,
Beta-272226)
4Ab - 11,482 cal BP
(OS-79563)
3Ab 11,746 cal BP
(Beta-272228)
5Ab - 11,688 cal BP
(OS-79585)
6Ab - 11,697 cal BP
(OS-79564)
7Ab - 12,454 cal BP
(OS-79565)
Radiocarbon-Dated Black Mats and
Paludal Deposits at Locus 3 (2-m tape for scale)
Radiocarbon-Dated Black Mat (3Ab) and
Paludal Deposit (2Ab) at Locus 1
Stratigraphic Section Exposed at Locus 3
Stratigraphic Section Exposed at Locus 1
Older Alluvial Fan
Sierra Nevada
Inset Terrace
Older Alluvial Fan
Inset Terrace
Overview of Inset Alluvial Terrace at Locus 3 to the West
Overview of Inset Alluvial Terrace at Locus 1 to the North
Figure 16. Little Dixie Wash Alluvial Terrace and Strata.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
40
Far Western
Alluvial Terrace Stratigraphy (Loci 1-4)
The basal stratum (Stratum I-7Ab/7Cu) is an alluvial deposit consisting of fine sand and small roundedto-subrounded gravel that gradually fines upward into grayish-brown silty clay, displaying moderate soil
development (Figure 17). This stratum was exposed at the base of the Locus 3 cutbank, and was identified in an
auger boring at Locus 4 (see Figure 15). The 7Ab horizon proved to be Terminal Pleistocene in age as verified by
nearly identical dates of 10,500 ± 60 BP or 12,454 cal BP (OS-79565) from Locus 3, and 10,450 ± 40 BP or
12,387 cal BP (OS-79565) from Locus 4.
Overlying this stratum is a silty clay alluvial deposit that displays a light brownish-gray lower portion and
a gray upper portion (Stratum II-6Cu and 6Ab, respectively), with a few small iron-oxide mottles present in both
horizons. The 6Ab horizon represents a moderately developed soil that produced a Terminal Pleistocene date of
10,100 ± 55 BP or 11,697 cal BP (OS-79564), which corresponds to a date of 10,160 ± 60 BP or 11,746 cal BP
(Beta-272228) on the 3Ab horizon at Locus 1 (Figure 17). At Locus 3 this stratum is capped by an alluvial
deposit of light brownish-gray silt loam with common iron-oxide mottles that fines upward into grayish-brown
silty clay with fewer mottles and weak soil development (Stratum III-5Cox and 5Ab, respectively). A sample of
the 5Ab horizon produced a date of 10,100 ± 110 BP or 11,688 cal BP (OS-79585), nearly identical to the age of
the underlying 6Ab horizon.
Lying above Stratum III is alluvial sediment deposited in a paludal environment (see Appendix D).
This deposit consists of a light brownish-gray silty loam that fines upward into grayish-brown silty clay, on
which is formed a weakly developed soil containing small gastropod shells (Stratum IV-4Cu and 4Ab,
respectively). This stratum is Early Holocene in age based on a date of 10,000 ± 50 BP or 11,482 cal BP (OS79563) on the 4Ab horizon, corresponding closely with dates of 10,000 ± 60 BP or 11,486 cal BP (Beta272226) and 9610 ± 50 BP or 10,944 cal BP (Beta-272227) from the 2Ab horizon at Locus 1 (see Figure 16
and Figure 17). At Locality 3, Stratum IV is covered by another deposit of alluvial and paludal sediment
composed of light yellowish-brown loamy sand that fines upward into light grayish-brown silty clay (Stratum
V-3Cu and 3Ab, respectively). The upper portion of this stratum displays a weakly developed soil containing
small gastropod shells. A date of 9440 ± 95 BP or 10,703 cal BP (OS-79584) from the 3Ab horizon verifies
that this deposit was formed during the Early Holocene.
Stratum V is overlain by a light gray silty clay loam alluvial deposit with a moderately developed ped
structure and some powdery calcium carbonate coatings (Stratum VI-2Bwb). Immediately above this fine-grained
stratum is a thick deposit of coarse sand and small-to-large gravel formed by the complex interplay of alluvial fan
and eolian processes (Stratum VII-A/Cu).
Micro-Invertebrates
Two loci within Little Dixie Wash were sampled and analyzed for micro-invertebrates (LDW-Locus #3
and LDW Locality #4). Ostracodes and mollusks were only identified at LDW-Locus #3 (see Appendix D, Table
3). Three dilute-water, spring-related ostracode species were identified in the 4Ab Horizon of Locality 4,
including Fabaeformiscandona acuminata, Eucypris meadensis, and Cypridopsis okeechobei. This assemblage suggests
water salinity did not exceed 1,000 milligrams L-1 TDS (Forester et al. 2005). In addition, four aquatic
gastropods occurred in the same horizon: Pseudosuccinea columella, Helisoma (Carinifex) newberryi, Gyraulus
parvus, and Fossaria parva (see Appendix D, Figure 2c). All four species tolerate a wide range of salinity and can
occur in a variety of environments from swamps to streams (Sharpe 2002, 2003; see Appendix D, Table 6).
Alluvial Fan Stratigraphy (Locus 5)
As the southernmost (upstream) geological locality along the wash, a vertical sequence of six alluvial strata
was documented south of the present confluence of Freeman Gulch and Little Dixie Wash at Locus 5 (see Figure
15). This sequence is part of an alluvial fan that is inset within the gulch below much older deposits of the
Freeman Fan (Figure 18). Attention to this locus was sparked by the discovery of a chert-formed flake-tool
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
41
Far Western
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
UPSTREAM
DOWNSTREAM
SOUTH
NORTH
FAN LOCUS 5, WEST BANK
LOCUS 3, WEST BANK
0
Cu - Pale brown sand, small to
medium subangular to
rounded gravels
VI
1
Aeolian (Dune) Deposits
0
Cu - Same as above
2Bwb - light gray silty clay loam
42
X
3Ab - Brown sandy clay loam
IV
3Cu - Brown sandy loam, chert uniface
flaketool near base of horizon
6340 ± 40,
or 7273 cal BP
(Beta-281208) on soil
X
3
III
4Ab - Light brownish-gray silty clay loam,
common iron oxide mottles in upper
5-10 cm
4Cu - Light brownish-gray coarse sand to sandy
loam, 20 cm layer of fine sand at lower
contact
5Ab - Light brownish-gray sandy clay loam
II
I
5Cox - Light brownish-gray loamy sand
4
6Ab - Light yellowish-brown sandy loam,
common oxide mottles
6Cu - Light yellowish-brown coarse sand,
and poorly sorted gravel
2
X
X
V
10,100 ± 110,
or 11,688 cal BP
(OS-79585)
10,100 ± 55,
or 11,697 cal BP
(OS-79564)
10,500 ± 60 BP,
or 12,454 cal BP
(OS-79565)
X
X
IV
III
3Ab - Light grayish-brown silty clay
with snails
Cu - Light yellowish-brown,
fine to medium sand,
well sorted
1
9610 ± 50,
or 10,944 cal BP
(Beta-272227) on soil
10,000 ± 60,
or 11,486 cal BP
(Beta-272226) on snail
X
2
3
II
4Ab - Grayish brown silty clay with
snails
4Cu - Light brownish-gray silt loam
X
X
5Ab - Grayish brown silty clay
5Cox -Light brownish-gray silt loam
X
X
6Ab - Gray silty clay
10,160 ± 60,
or 11,746 cal BP
(Beta-272228) on soil
2Ab - Gray sandy loam,
few snail shells
II
2Cu - Light brownish-gray sandy
clay loam, few powdery
CaCo3 filaments
3Cu - Light yellowish-brown loamy
sand
10,000 ± 55,
or 11,482 cal BP
(OS-79563)
X
I
3
3Ab - Gray silty clay, few oxidization
mottles
3Cox - Light yellowish-brown,
sandy loam, common
oxidization mottles
6Cu - Light brownish-gray silty clay
I
X
X
7Ab - Grayish-brown silty clay
3.7
Hand Auger
2Ab - Brown sandy clay loam
A - Yellowish-brown
loamy sand
III
1
9440 ± 95,
or 10,703 cal BP
(OS-79584)
Cinega and Floodplain Deposits
V
6990 ± 40,
or 7827 cal BP
(Beta-281207) on soil
0
VII
VI
2
LOCUS 1, WEST BANK
A - Light yellowish brown sand
with small to large gravel
150 cm transition to fine sand and
small gravels
7Cu - Fine sand and small gravel
5.2
Note: Depth in Meters
Figure 17. Alluvial Stratigraphy of Selected Little Dixie Wash Loci.
Far Western
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
3Ab 7827 cal BP
(Beta-281207)
3Cu
4Ab7273 cal BP
(Beta-281208)
Chert Flake Tool Exposed in 3Cu Horizon at Locus 5
View of Flake Tool (L-R top, side, bottom)
Imbricated Clasts
in West Cobble Ridge
43
Angular and Rounded Clasts
in East Cobble Ridge
Stratigraphic Section Exposed at Fan Locus 5
Linear Arrangement of Cobbles at West Ridge to Northeast
Sierra Nevada
Older Alluvial Fan
Freeman
Gulch
Inset Holocene Fan
Far Western
Overview of Inset Holocene Fan at Locus 5 to Southwest
Overview of West Cobble Ridge to Northwest
Figure 18. Little Dixie Wash Alluvial Fan and Cobble Ridge Loci.
Overview of East Cobble Ridge to Northeast
protruding from the cut-bank within the wash (see Figure 17); the only in situ prehistoric tool identified during
this study. Since similar artifacts are typically associated with Terminal Pleistocene/ Early Holocene cultural
assemblages in the Mojave Desert (e.g., Basgall 1993), an effort was made to bracket the artifact’s age by obtaining
radiocarbon dates from overlying and underlying deposits.
The lower four strata (Stratum I-IV) at Locus 5 consist of coarse sand that fine upward into sandy loam
(Stratum I), sandy clay loam (Stratum II and IV), or silty clay loam (Stratum III), each with weakly developed
soils formed in the stratum’s upper portion (see Figure 17). The presence of a few small angular to subrounded
gravel in Stratum I, II, and IV, and the small-to-medium angular to subrounded gravel in Stratum III are typical
of an alluvial fan deposit. Iron-oxide mottles also occur in the Ab horizons of Stratum I and III, and the lower
part of Stratum II (5Cox horizon).
The artifact was found about five centimeters above the contact of Stratum III and IV within the lower
3Cu horizon of Stratum IV at a depth of about 2.7 meters below ground surface (see Figure 17 and Figure 18). A
radiocarbon date of 6340 ± 40 BP or 7223 cal BP (Beta-280208) was derived from the 4Ab horizon of Stratum
III underlying the artifact, and the overlying 3Ab horizon of Stratum IV gave a slightly older date of 6990 ± 40
BP or 7827 cal BP (Beta-280208), indicating that some older carbon was probably reworked or redeposited into
Stratum IV. Despite the age reversal, this artifact was probably deposited sometime between about 7,800 and
7,200 years ago, or roughly, at the end of the Early Holocene.
Overlying the lower four strata is an alluvial fan deposit of sandy clay loam displaying a weakly developed
soil (Stratum V-2Ab; presumably Middle Holocene), capped by a coarse sand with small to medium subangular
to rounded gravel formed by alluvial and eolian processes (Stratum VI-Cu; Middle or Late Holocene?). The latter
stratum lacks evidence of soil development (see Figure 17). No black mats, organic-rich soils, mesic-adapted
snails, or paludal-like deposits occur within the alluvial fan sequence exposed at Locus 5.
Cobble Ridge Loci
Two isolated deposits of small boulders and large cobbles were also identified along the edges of the
wash, each forming a distinctive ridge or berm (see Figure 18). The most downstream of these was identified on
the eastern side of the wash about 585 meters (1,919 feet) southwest of Locus 4 at an elevation of about 850
meters (2,790 feet). The other is evident on the western side of the wash about 370 meters (1,214 feet) southwest
of Locus 5 at an elevation of about 864 meters (2,836 feet); approximately 1.4 kilometers (~0.87 miles) upstream
from the eastern cobble ridge (see Figure 15).
The eastern (downstream) ridge is well exposed in a 1.5- to 3.0-meter vertical section that parallels the
wash over a distance of about 20 meters. The long axis of the ridge is oriented from the southwest to the northeast
and slopes in the same general direction (see Figure 18). The deposit overlies truncated volcanic bedrock and is
dominated by large angular-to-subangular basalt cobbles (30 to 90 centimeters in diameter) that are smaller
toward the bottom of the deposit (i.e., coarsens upwards). The lower portion contains a small percentage of
granitic gravel and small cobbles that are generally rounded-to-well-rounded (see Figure 18). The gravel, cobbles,
and boulders lie clast-to-clast with very little fine-grained matrix present.
The western (upstream) ridge parallels the wash over a distance of more than 55 meters (>180 feet),
standing about 1.5 to 2.5 meters above the base of the wash (see Figure 18). The long axis of the ridge is oriented
from the northwest to southeast and slopes slightly in that same direction. Only partially exposed in profile, the
deposit overlies truncated granitic bedrock and is dominated by large rounded-to-subrounded granitic cobbles (40
to 100 centimeters in diameter) that are imbricated and mainly clast-to-clast, with granitic sand and gravel filling
the interstices (see Figure 18).
As the formation of similar boulder/cobble ridges normally results from high-energy flood events, the
presence of these deposits suggest the amount of runoff, rate of stream flow, and erosive power within Little Dixie
Wash was exponentially greater on one or more occasions. These event-related deposits are probably related to
initial down-cutting and erosion of the older fan deposits, prior to emplacement of the Terminal
Pleistocene/Early Holocene inset terrace.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
44
Far Western
Dove Springs Wash
The Dove Springs Wash geological locality lies about 5.1 kilometers (~3.1 miles) northwest of the
intersection of State Route 14 and the entrance to Red Rocks State Park, and 1.8 kilometers (1.1 miles) due west
of State Route 14; about 3.6 kilometers (~2.2 miles) southwest of Little Dixie Wash (Figure 19). At an elevation
of about 908 meters (2,980 feet) amsl, the exposed section in Dove Springs Wash occupies a central position
along the drainage between the headwaters at about 1,830 meters (~6,000 feet) amsl and the basin of Koehn (dry)
Lake, where it terminates at about 576 meters (1,890 feet) amsl; approximately 12.8 kilometers (~8 miles) to the
southeast (Figure 19). A series of discontinuous alluvial terraces lie inset along the wash several meters or more
below the surrounding landscape of highly eroded and deeply dissected Miocene- to Pleistocene-age alluvial and
volcanic deposits (Miller and Amoroso 2007). The exposed sections correspond to the Latest Pleistocene and
Holocene young alluvial fan deposits mapped (Qyw4) by Miller and Amoroso (2007).
The Dove Springs Wash geological locality consists of a 200-meter (~656-foot) long cutbank extending
along the north side of the wash in which a sequence of 13 alluvial strata is exposed in a 4-meter-high (~13.1foot) vertical section (Figure 20). These correspond to the dark bands of “lignitic sand” described by
paleontologist David Whistler from the San Bernardino County Museum (Whistler 1990, 1994). A date of
12,642 cal BP (Beta-18449) from a conifer branch collected in a soil near the base of the wash (Whistler locality
5775) indicated that Terminal Pleistocene, and possibly Early Holocene, deposits were present at this location.
The occurrence of a single chalcedony flake from the dated stratum identified by Whistler (1994) may provide
evidence for human use of this locality during the Terminal Pleistocene.
Alluvial Stratigraphy
The basal stratum, which was only partially exposed at this locus, is an alluvial deposit consisting of sandy
loam and a few (~10%) small rounded-to-subrounded gravels (Stratum I-13Ab) displaying a moderately
developed, very dark gray soil (Figure 21). Organics from this soil yielded a Terminal Pleistocene date of 10,300 ±
60 BP, or 12,102 cal BP (OS-79560). The 2-sigma confidence interval from this date does not overlap with the
date of 12,642 cal BP reported by Whistler (1994) from the basal deposit. Thus, it is not clear if both dates are
from the same stratum, as Whistler’s (1994) sample originated from an exposure several hundred meters downstream. In the exposure examined for the current study, the deepest soil is buried by an alluvial deposit composed
of pale red volcanic sand and gravel (Stratum II-12Cu), which fines upward into sandy loam. A moderately
developed, very dark, grayish-brown soil formed in the upper portion of this stratum (Stratum II-12Ab).
Above this lies a fine alluvial sand with a few iron-oxide mottles that grades upward into silty clay
displaying a weakly developed grayish-brown soil (Stratum III-11Cox and 11Ab, respectively). This is overlain by
a silty clay with a few iron-oxide mottles in the lower portion and a moderately developed dark gray soil in the
upper part (Stratum IV-10Cox and 10Ab, respectively). Capping the soil is a thin deposit of coarse sand that
grades abruptly into loamy sand with a very weakly developed grayish-brown soil (Stratum V-9Cu and 9Ab,
respectively), probably marking a very short period of surface exposure (Figure 21).
Overlying this is a paludal deposit of fine-to-loamy sand with a very weakly developed grayish-brown soil
near the upper contact (Stratum VI-8Cu and 8Ab, respectively). Freshwater snail shells, like those identified at
Little Dixie Wash, were present throughout this stratum (Figure 21). Covering Stratum VI are two relatively
thick alluvial strata composed of fine-to-coarse sand with weakly developed, light-colored soils at the top of each
(Stratum VII-7Ab/7Cu and Stratum VIII-6Ab/6Cu, respectively), representing episodes of increased stream flow
and channel aggradation.
These units underlie another paludal deposit of coarse sand that fines upward into sandy clay loam with a
moderately developed dark grayish-brown soil, containing saline-tolerant ostracodes and a few very small
freshwater snail shells (Stratum IX-5Cu and 5Ab, respectively; see Appendix D). A date of 4230 ± 40 BP or 4753
cal BP (Beta-280993) was derived on organic sediment from the 5Ab horizon, indicating a Middle Holocene-age
for this paludal environment.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
45
Far Western
U
C
T
Qya/Tr
E
D
Qyw2
Q
U
w1
Qy
E
S
A
Qyw3
A
N
G
E
L
Qya 1-3
Q
L
O
S
Qyw 1-3
yw
Qya
4
Qyw3Qyw3
14
Qyw1
Qya3
Qyw4
Dove Springs Wash (908 m, 2979 ft)
Qyw3 Qyw4
Qya3
w4
Qy
Qyw3
Qy
w4
Qya 1-3
Qyw2
Qyw2
Qyw4
Qya
Qya
Qya 1-3
Qyw3
Qya 1-3
Qya4
Qyw3
Qya
Qya 1-3
w4
Qy
Qyw4
Qya
Qya4
Qya
Qya
w4
Qy
Qyw2
w3
Qy
Qyw4
Qyw3
Qya4
Qyw 1-3
Qya
Qya/Tr
Qyw4
Qya
Qyw2Qyw4
Qyw4
Qyw3
Qya Qyw2
Qya3
Qyw4Qyw3
Qya
Qyw2
Qyw3
Qya
Qyw 1-3
Qyw2
Qya
Qyw 1-3
Sample Locus
Geologic Unit (Miller and Amoroso 2007)
Qyw1, Youngest wash deposits (Holocene)
Qyw2, Younger wash deposits (Holocene)
Kilometers
Qyw3, Young wash deposits (Holocene)
0
0.25
Qyw 1-3 (Holocene)
Qya 1-3 (Holocene)
0
0.25
Qya3, Young alluvial fan deposits (Holocene)
Miles
Qya4, Young alluvial fan deposits (Holocene and Latest Pleistocene)
Qyw4, Young wash deposits (Holocene and latest Pleistocene)
Qya, Young alluvial fan deposits, undifferentiated (Holocene and Latest Pleistocene)
0.5
0.5
Figure 19. Sample Locus and Terminal Pleistocene and Holocene Deposits along Dove Springs Wash.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
46
Far Western
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
5Ab 4753 cal BP
(Beta-280993)
47
Freshwater Snail Shell Exposed in Cut Bank
Overview of Dove Springs Sample Locus to Northeast
3 meters b.s.
12Ab
Far Western
13Ab 12,102 cal BP
(OS-79560)
Overview of Dove Springs Sample Locus to Southeast
Black Mats and Paludal Deposits at Sample Locus
Black Mats and Paludal Deposits Exposed Downstream
Figure 20. Dove Springs Wash Sample Locus and Alluvial Strata.
WHISTLER LOCAL 5771
STRATUM
HORIZON - Description
0
Ap - Artificial fill
XIII
A - Brown loamy sand
Cu - Pale brown sand
2Ab - Brown loamy sand
XII
2Cu - Pale brown fine sand
3Ab/Cu - Grayish-brown loamy sand, pale brown coarse sand
XI
4Ab/Cu - Grayish-brown loamy sand, pale brown fine sand
X
4230 ± 40 BP, or 4753 cal BP
(Beta-280993)
1
X
5Ab - Dark grayish-brown sandy clay loam with ostracodes
IX
5Cu - Very pale brown coarse sand
6Ab Light brownish-gray coarse sand
VIII
6Cox - Very pale brown coarse sand
7Ab - Brown sandy loam
VII
2
7Cu - Pale yellow fine to coarse sand
8Ab - Grayish-brown loamy sand
Snails Present
VI
8Cu - Light brownish-gray fine sand
V
9Ab/Cu - Grayish-brown loamy sand, very pale brown coarse sand
10Ab - Dark grayish silty clay
IV
10Cox - Light yellowish-brown silty clay
11Ab - Grayish-brown silty clay
III
3
11Cox - Light brown grayish fine sand
12Ab - Very dark grayish-brown sandy loam
12Cu - Pale red coarse sand
II
4 Meters
10,300 ± 60 BP, or 12,102 cal BP
(OS-79560)
X
13Ab - Very dark gray sandy loam
I
Figure 21. Dove Springs Wash Alluvial Stratigraphy.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
48
Far Western
Above Stratum IX are three additional alluvial strata (Stratum X, XI, and XII), each consisting of coarseto-fine sand and loamy sand with relatively thin, weakly developed soils, ranging from brown to dark grayishbrown in color (see Figure 21). At the present surface of the sampled exposure is an artificial fill deposit from a
dirt access road constructed along the northeastern side of the wash.
Micro-Invertebrates
Samples from three isolated horizons were analyzed for micro-invertebrates, including the 5Ab, 8Ab, and
13Ab Horizons. The latter sample was found not to contain micro- or macro-invertebrates. The 5Ab Horizon
contained an abundant ostracode record (dry mass of 2.6 specimens per gram of sediment). Four species were
identified including Eucypris meadensis (the most abundant), Ilyocypris bradyi, Fabaeformiscandona acuminata, and
Cypridopsis vidua (see Appendix D, Figure 2b). Eucypris meadensis is a dilute-water, spring-related species and
Ilyocypris bradyi is a spring- and stream-related species (see Appendix D, Table 4). Dominance of Eucypris
meadensis indicates salinity did not exceed 1,000 milligrams L-1 TDS (Forester et al. 2005).
Ten valves of I. bradyi, in two batches of five shells each, were analyzed for carbon and oxygen
isotopes. As discussed in the Results section of Appendix D, it is inferred that these values indicate low
evaporation during deposition of the 5Ab horizon. The stable isotope signature is consistent with the dilutewater inference from micro-invertebrates.
Two ostracode and three mollusk species were identified from the older 8Ab Horizon including I. bradyi
and E. meadensis accompanied by the gastropods Physa virgata and Tryonia sp. and the clam Pisidium casertanum.
Dilute waters hosted this faunal association. Salinity did not exceed 2,000 milligrams L-1 TDS, the maximum
tolerance for Tryonia sp., but more likely was close to 1,000 milligrams L-1 TDS, the maximum tolerance for E.
meadensis (Forester et al. 2005; Sharpe 2002, 2003).
The stable isotope analysis of ten valves of I. bradyi from the 8Ab Horizon yielded δ13C and δ18O
values similar to those from the 5Ab Horizon. Like the latter horizon, it is inferred that the δ18O values in
Horizon 8Ab reflect low rates of evaporation (Appendix D, Table 8). The stable isotope signature is consistent
with the dilute-water inference from micro-invertebrates.
Summary of Terminal Pleistocene/Early Holocene Inflow Conditions
Alluvial strata preserved in Rose Valley, Indian Wells Valley, and Dove Springs Wash provide a record of
successive landscape changes and related surface flows from the Terminal Pleistocene to Early Holocene. The
record begins prior to the formation of the lower black mat in the South Borrow Pit in Rose Valley, around
13,400 cal BP. This mat lay upon coarse-grained sand, gravel, and cobble deposits that were sorted and bedded
within an active channel, under high-energy fluvial conditions not recorded in later-dating deposits exposed in
this section. We interpret these fluvial deposits as bed-load of the former Owens River channel, suggesting
significant water flow shortly before 13,500 to 13,600 years ago, based on the upper 2-sigma range of the
associated radiocarbon date.
In contrast, basal deposits from eastern Sierra Nevada drainages were consistently found to date between
about 12,600 and 12,000 cal BP, and thus post-date the interval of high-energy bed-load and channel activity in
Rose Valley. Further, all of the Terminal Pleistocene/ Early Holocene alluvial deposits identified in drainages
emanating from the Sierra Nevada represent discontinuous terraces set within older fans. An absence of earlier
alluvial terrace deposits in these drainages implies that erosional processes (i.e., channel incision and lateral
migration) prevailed prior to 12,600 cal BP, precluding deposition and storage of sediment. High-energy cobble
ridges (not dated) bordering the channel of Little Dixie Wash may be further evidence of this erosive interval.
When the lower Owens River and Sierra drainage records are viewed together, it appears that surface
runoff and stream flows were generally greater between about 13,600 and 12,600 cal BP, with high-energy flows
and erosive conditions persisting no later than about 12,600 to 12,400 cal BP in most of the studied drainages. A
shift in the depositional regimen occurred toward the end of the Pleistocene (between roughly 12,600 and 11,500
cal BP), allowing fine-grained sands, silts, and clays to accumulate in large and small drainages alike. This interval
is marked by multiple short depositional pulses, each separated by intervening periods of landform stability and
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
49
Far Western
soil formation. The lowest alluvial strata at Dove Springs Wash, Little Dixie Wash, and Indian Wells Canyon,
record an initial episode of deposition between about 12,600 and 12,300 cal BP, followed by a more stable period
between about 12,300 and 12,000 cal BP. This cycle was followed by another depositional pulse centered
between about 12,000 and 11,800 cal BP, and a stable period at the end of the Pleistocene between about 11,800
and 11,500 cal BP. This latter interval corresponds to the formation of organic-rich horizons (i.e., soil, peat, and
black mats) and habitats supporting freshwater snails.
These same general conditions persisted well into the Early Holocene. After another pulse of deposition
around 11,200 cal BP, organic-rich horizons and mesic habitats supporting freshwater snails once again appeared
between about 10,900 and 10,400 cal BP in Rose Valley and Little Dixie Wash. This suggests that effective
moisture during the first millennia of the Holocene was at least as high as the last millennium of the Pleistocene.
Yet, despite persistent wet conditions, the fine-grained nature and sequential pulsing of deposition in the local
drainages imply only periodic, low-energy surface flows in the lower Owens River system and eastern Sierra
drainages. This, in turn, indicates there were likely no significant or sustained sources of inflow into China Lake
during the Terminal Pleistocene/ Early Holocene transition.
China Lake Basin Lake Level Records
Indian Wells Valley is a topographic basin bounded by the Sierra Nevada on the west, the Argus Range
on the east, the Coso Range on the north, and the El Paso Mountains and Rademacher Hills on the south (see
Figure 8). The basin is structurally controlled by a series of mostly active faults including the Sierra Nevada
Frontal Fault to the west, the Airport Lake and Argus Range faults to the east, the Little Lake Fault to the northnorthwest, and the Inyokern Fault to the south (Figure 22; Roquemore 1981; Zbur 1963). The valley floor lies
between 792 and 656 meters (2,600 and 2,154 feet) amsl, and is covered mainly by a series of broad coalescing
Pleistocene-age pediments and Holocene-age alluvial fans that generally slope from west to east and from south to
north across the valley. Outcrops of Pliocene-age lacustrine deposits (White Hills) have been uplifted and faulted
along the valley’s northern side, separating China Lake Basin from the internally fed basin of Airport Lake. On
the northwestern side of the valley, the White Hills are partly overlain by Pleistocene basalt flows (e.g., Little
Lake) that form prominent flat-topped ridges adjacent to the former channel of the lower Owens River (Duffield
and Bacon 1981; Duffield and Smith 1978; St.-Amand and Roquemore 1979; Zbur 1963).
Today, Indian Wells Valley has no perennial streams (Kunkel and Chase 1969; Moyle 1963; St.-Amand
1986). China Lake Basin is distinguished by a dry playa that lies along the southeastern side of Indian Wells
Valley; it represents the lowest point on the valley floor (655 meters or 2,154 feet amsl). China Lake Basin is the
primary depocenter for water and sediment transported by the lower Owens River system through Rose Valley.
When water filled the basin in the past, it then overflowed southeast through a narrow canyon in the Argus Range
and into Salt Wells Valley and Poison Canyon until reaching the Searles Valley basin; a drop of about 176 meters
(~577 feet) overall.
The present elevation of the sill or topographic divide between China Lake and Searles basins is about
670.5 meters (2,200 feet) amsl according to USGS digital elevation model data. Others have variously placed it at
667.5 meters (2,190 feet) amsl (Dutcher and Moyle 1973; Kunkel and Chase 1969; Smith 1979), 668.7 meters
(2,194 feet) amsl (Lee 1913), and 665 meters (2,181 feet) amsl (Smith and Street-Perrott 1983); a difference of
5.5 meters (18 feet). With such discrepancies, it is interesting to note that a well hole placed within the basin’s
outlet identified about 12.5 meters (41 feet) or more of “windblown sand” immediately overlying bedrock, with
“no water-laid material” reported (Kunkel and Chase 1969:31). This means the bedrock sill lies at an elevation of
about 658.4 meters (2,160 feet) amsl, or only about 1.8 meters (~6 feet) above the south playa low point. This
suggests that overflow and lake levels were partly controlled by a “soft sill” of windblown sand and/or a beach
barrier ridge that was likely breached and rebuilt more than once by lake transgressions and regressions.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
50
Far Western
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Basalt (Tb)
Landslide Deposits (Ql)
Goler Formation (Tg)
Black Mountain Basalt (Qbb)
Ricardo Formation (Tr)
Dune Sand (Qds)
Old Dune Sand (Qos)
Old Lacustrine Deposits (Qol)
Old Lake Shore Deposits (Qls)
Older Fan Deposits (Qof 3)
Older Fan Deposits 2 (Qof 2)
Older Fan Deposits 3
Older Alluvium (Qoa)
Playa Deposits (Qp)
Sand and Interdune Deposits (Qsp)
Unnamed Volcanic Rocks (Qv)
Younger Alluvium (Qya)
Younger Fan Deposits (Qyf)
Basement Complex (pTu)
City
Transect
Fault (Ludington et al. 2005)
Elevation Contour
Major Roads
km 0
County Line
Military Base
mi 0
2.5
2.5
5
5
Figure 22. Geologic Deposits and Former Lake Contours in Indian Wells Valley.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
51
Far Western
Lake Core Stratigraphy (Core 9)
Situated within the NAWS China Lake Charley Range, Core 9 was placed about 6.8 kilometers (4.2
miles) northwest of Armitage Airfield (Figure 23). This is about 3.4 kilometers (2.1 miles) northwest of the Range
Access Road and Snort Access Road intersection, and about 55 meters (180 feet) west of Range Access Road
(UTM zone 11, 434038E, 3955277N, WGS 84). The core was positioned west of the present China Lake playa
in the dune and inter-dune playa zone (Figure 24) at an elevation of about 669.6 meters (2,197 feet) amsl, which
is just below the modern sill level, and within the area defined as Stake 19 for archaeological purposes by Emma
Lou Davis (Davis 1975; Davis and Panlaqui 1978).
Core 9 contained a vertically stratified sequence of lacustrine and terrestrial deposits that extended about
10.7 meters (35 feet) in depth below the surface of a small inter-dune playa (Figure 24). The lower six meters
(~20 feet) of the core contain lacustrine sediments that record a transition from higher/deeper to lower/shallower
lake levels. At the base of this sequence is a stratum of greenish-gray (gleyed) sandy clay loam, likely deposited
subaqueously in a relatively deep lake (Stratum I-12Cg). Above this is an olive-gray (gleyed) deposit of coarse sand
that fines upward into very fine sand (Stratum II-11Cg). This deposit formed in a shallower lake, signaling an
overall lowering of water levels (Figure 25). A date of 14,160 ± 50 BP, or 17,780 cal BP (Beta-280680) obtained
on organics from this stratum indicates the deposit is Late Pleistocene in age.
Stratum II is overlain by a gray-to-olive-gray (gleyed) deposit that coarsens upwards from very fine sand
to sandy loam (Stratum III-10Cg1 and 10Cg2); again formed in a lacustrine setting. These facies are capped by a
60-centimeter thick deposit of moderately sorted and bedded coarse sand and small-to-medium, subangular-torounded gravel (Figure 25), which formed along the shore of a former lake (Stratum IV-9Cu). The top of the
beach deposit lies 7.6 meters below surface at an elevation of about 662.2 meters (2,172 feet) amsl. Above this is a
layer of light gray sandy loam which appears to be lacustrine sand, weakly cemented by gypsum (Stratum V-8C).
The sand underlies another layer of light gray sand that contain a few moderately sorted and bedded, small-tomedium, subangular-to-rounded gravel, and a few thin layers of black sand (Stratum VI-7C). The Stratum VI
sands may have accumulated near shore—perhaps related to a prograding Owens River delta—but in deeper
water than the coarse sand lenses associated with Stratum IV. Lacustrine sediments in Core 9 terminate at an
elevation of about 665.3 meters (2,181 feet) amsl and do not appear to contain carbonates as no effervescence was
observed when exposed to a ten percent solution of hydrochloric acid.
Capping the lacustrine sequence is a 4.5-meter (~15-foot) thick sequence of terrestrial alluvial and eolian
deposits (Figure 25). The base of this sequence is initiated by a pale olive (gleyed) silty clay alluvial deposit with
subangular blocky structure and a few hard nodules of calcium carbonate (CaCo3) near the top (Stratum VII6Cg). The gleying and fine-grained texture suggests a slough or playa setting for this stratum. Organics obtained
from the 6Cg horizon yielded an Early Holocene date of 9690 ± 50 BP, or 11,123 cal BP (Beta-280679).
Above is another slough or playa deposit of white sandy clay loam with weak soil development that is
infused with calcium carbonate (CaCo3), which effervesces violently when exposed to hydrochloric acid (Stratum
VIII-5Akb). This soil is buried by light olive-grey silty-clay displaying weak soil development and containing a
few hard calcium carbonate (CaCo3) nodules that effervesce strongly when exposed to hydrochloric acid (Stratum
IX-4Akb); again formed within a slough or playa.
The slough and playa deposits are overlain by a deposit of pale yellow medium-to-coarse sand that fines
upward into light olive-brown silt with weak soil development formed by a combination of alluvial and eolian
processes (Stratum X-3Cu and 3Ab, respectively). The soil is covered by a layer of strongly effervescent pale
yellow sand of eolian origin (Stratum XI-2Cu; interval between 1.52 and 2.13 meters not recovered) that fines up
into light yellowish-brown silt. This deposit displays weak soil development and contains soft calcium carbonate
(CaCo3) nodules that are also strongly effervescent (Stratum XI-2Akb). The sequence is completed by very pale
brown loamy sand that grades into very pale brown silt (Stratum XII-Cu and A, respectively), both strongly
effervescent. This stratum forms the present inter-dune playa surface (Figure 24 and Figure 25).
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
52
Far Western
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
Wave Cut (686 m, 2,250 ft)
Wave Cut (686 m, 2,250 ft)
R
ach
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Core 3
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Core 9
(669m, 2197ft)
395
Kern County
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Maximu m Hol
Core 6
Core 5
San Bernardino County
Inyo County
Core 4
km 0
Contour
Beach Features
Far Western
Inyokern
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1
2
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LT
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LONE
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LS
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178
Ridgecrest
Figure 23. Prominent Lake Features and Former Shorelines in China Lake Basin.
13,000 cal BP
(Beta-280683)
Sorted, Bedded Beach Sand and Gravel, ~8 to 9 m, Core 9
(Strata IV)
Algal Tufa Exposed on Granitic Bedrock
Knoll to Southeast
Dune and Interdune Playas in Core 9 Area to Southwest
Honeycomb Formations on Bedrock Knoll to Northwest
683 m (2,240 ft) amsl
670 m (2,200 ft) amsl
Two Proiminent Shorelines on Knoll Near Outlet to Southwest
China Lake Playa from Bedrock (Tufa) Knoll to Northwest
Figure 24. Landforms and Deposits in the China Lake Basin.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
54
Far Western
CORE 9
Depositional
Environment
STRATUM
HORIZON - Description
669.6 Meters (2,197 Feet) amsl
0
A - Very pale brown (10YR7/3, dry) silt
XII
Cu - Very pale brown (10YR7/3, dry) loamy sand
1
2Akb - Light yellowish-brown (2.5Y6/3, dry) silt
No Recovery
XI
2
Alluvial and
Aeolian Deposits
2Cu? - Pale yellow (2.5Yy/3, dry) sand
3Ab - Light olive-brown (2.5Y5/3, dry) silt
3Cu - Pale yellow (2.5Y7/3, dry) medium to
coarse sand
X
Terrestrial
3
4Akb - Light olive-grey (5Y6/2, dry) silty clay
IX
VIII
5Akb - White (5Y8/1, dry) sandy clay loam
4
VII
6Cg - Pale olive (5Y8/1, dry) silty clay
X
9690 ± 50, or
11,123 cal BP
(Beta-280679)
5
7Cu - Light gray (2.5Y7/2, dry) sand with few
moderately sorted and bedded, small-tomedium, subangular to rounded gravel,
and few thin lenses of black sand
6
VI
Beach and
Near-Shore
Lacustrine
Deposits
7
8C - Light gray (2.5Y7/1, dry) sandy loam
V
8
9Cu - Various color fine to coarse sand,
small-to-medium subangular to rounded
gravels, moderately sorted and bedded
Lacustrine
IV
9
10Cg1 - Olive gray (5Y5/2, dry) sandy loam
III
10Cg2 - Gray (5Y5/1, dry) very fine sand
Near-Shore Facies
10
14,610 ± 50, or
17,780 cal BP
(Beta-280680)
II
Off-Shore Facies
I
11Cg - Olive gray (5Y5/2, dry) very fine sand,
coarse sand in lower 5 cm
X
10.67
Meters
12Cg - Greenish-gray (5GY6/1, dry) sandy clay loam
Figure 25. Alluvial Stratigraphy of Core 9 from the China Lake Basin.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
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Far Western
Beach, Shoreline, and Lake Features
At least two and possibly three wave-cut strand lines can be seen encircling a steep bedrock knoll on
China Lake Basin’s southeast side. The knoll and strand lines are similar to, or the same as, those pictured by Lee
(1913:405). The knoll lies immediately south of Lark Seep, northwest of the intersection of Water and Knox
Roads, and reaches a maximum elevation of about 700 meters (2,300 feet) amsl (see Figure 23). The highest
strand line forms a subtle notch that surrounds the top of the knoll at about 695 meters (2,280 feet) amsl. Lower
down the knoll is a conspicuous strand line at about 683 meters (2,240 feet) that coincides with the presence of a
light-colored deposit of sediment and the absence of bedrock surface outcrops. The most prominent and recent
looking of the three strand lines is a narrow terrace of beach sand and gravel at an altitude of about 670 meters
(2,200 feet) amsl near the base of the bedrock knoll (see Figure 24). The elevations of all three features correspond
with those of other suspected shoreline features previously reported in Searles and China Lake Basins (Davis
1975; Davis and Panlaqui 1978; Kunkel and Chase 1969; Moyle 1963; Smith 1979; St.-Amand 1986), while the
lowest wave-cut strand line lies at the same elevation as the modern outflow sill.
A little more than 1.7 kilometers (1 mile) northeast of this knoll is a smaller bedrock knoll, located
northwest of the intersection of Knox and Magazine roads, and about 400 meters (1,314 feet) northwest of the
basin sill and outlet channel (see Figure 23). An examination of the knoll top revealed that calcareous algal tufa
deposits were attached to the bedrock at an elevation of about 665.5 meters (2,183 feet) amsl, and that lakeshore
wave-action had created extensive honeycomb patterns within the bedrock (see Figure 24). Tufa of this type
forms when lime-secreting algae colonize zones where sunlight regularly penetrates below the surface of a lake
(Scholl 1960). The tufa produced a date of 11,440 ± 50 BP, or 13,000 cal BP (Beta-280680; reservoir correction
applied). As this locality lies about five meters below the modern outlet, the associated date suggests a lake stood
below the sill level during the Terminal Pleistocene.
At Basalt Ridge on the basin’s northern side (see Figure 23), tufa deposits occur near the ridge top at
about 680.9 meters (~2,234 feet) amsl and are discontinuous and consist of conglomerates that contain numerous
basalt gravel and cobbles. The elevation of these deposits correlates with the intermediate strand line (683 meters
amsl) identified on the bedrock knoll near the basin’s outlet. Davis (1978) obtained dates of 15,650 cal BP and
13,710 cal BP (UCLA-1911A, UCLA-1911B,) on tufa from this general location, suggesting that a coalesced lake
existed above the China Lake Basin outflow sill as recently as 13,700 cal BP.
Lake Level History
Basal lacustrine deposits from Core 9 indicate that a relatively deep lake existed in that location before
about 18,000 cal BP during the last glacial maximum. Given the depth below surface of these fine-grained
lacustrine deposits (660.8 meters amsl; Stratum II and III), the associated high stand, probably correlated with the
683- or 695-foot shorelines evident at the outlet knoll. The appearance of near-shore beach deposits in Core 9
after 17,780 cal BP indicates that the lake began to contract around that time. Dates on Anodonta shell of 14,390
± 70, or 17,504 cal BP (Beta-220692) and 13,130 ± 80, or 15,939 cal BP (Beta-220691) from the basin’s eastern
side confirm the presence of a lake, at least periodically, from about 17,500 to 16,000 cal BP (Byrd 2007). Basalt
Ridge tufa deposits suggest the lake attained a level of as much as 680.9 meters (~2,234 feet) amsl by 15,650 cal
BP and again by 13,710 cal BP. If these dates are correct, they likely correlate with lacustrine deposits of Stratum
VI, in Core 9, representing a higher stand following deposition of the lower beach deposits sometime after 17,780
cal BP (i.e., Stratum IV).
Lake levels dropped to at least the 670-meter (2,200 feet) sill level by 13,000 cal BP, as marked by the
formation of algal tufa of this age on bedrock near the outlet at an elevation of about 666 meters (~2,186 feet)
amsl. By the Early Holocene, the lake had dropped well below the 665-meter level based on a date of 11,123 cal
BP from the basal alluvial/eolian sequence (beginning at 665.3 meters amsl) above the lacustrine sands in Core 9.
The age of this capping deposit suggests the underlying fine-grained lacustrine sediments date older than 11,123
cal BP. However, since the upper lake deposits remain undated, the lacustrine record could be substantially older
than the age of the capping deposit. As no evidence was found in Core 9 to indicate that the lake ever again rose
to the 665-meter level, China Lake seems not to have reached its outflow sill after about 13,000 cal BP.
Constructing a Regional Historical Context for Terminal
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North-Central Mojave Desert, Step 1
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Far Western
China Lake Outflow Records
Except for a few rounded bedrock knolls (e.g., Lone Butte), the narrow canyon forming China Lake’s
outlet consists of steep and rugged bedrock slopes. The canyon floor is partially filled with dune sand and alluvial
sediments, and does not have a continuous channel or dominant wash exposed at the surface.
Two prominent wave-cut strand lines encircle bedrock knolls in the canyon (Figure 26). The highest of
these lies at about 683 meters (2,240 feet) amsl, or the same elevation as the laterally extensive shoreline found in
China Lake Basin (Figure 27). A prominent beach ridge is associated with this shoreline on the northern side of
Lone Butte where it extends northward over a distance of about 190 meters (~623 feet) to an elevation of about
659 meters (~2,163 feet) amsl. Composed mainly of gravel and cobbles, the ridge measures about 46 meters
(~150 feet) across at its widest point, and is elevated some four to five meters (13 to 16 feet) above the
surrounding land surface (Figure 27).
A less conspicuous shoreline feature is situated at about 654 meters (2,147 feet) amsl. This shoreline is
associated with a smaller barrier-type beach ridge on the northern side of Lone Butte, extending in a northeast
direction for about 127 meters (~417 feet; Figure 26). Measuring about 16 meters (~50 feet) across at its widest
point, this ridge consists mainly of gravel, and is elevated at least one to two meters (2.9-5.8 feet) above the
surrounding land surface (Figure 27). Given its elevation below the sill of China Lake Basin, the lower shoreline
and beach ridge appear to represent a recessional stand of Lake Searles.
Another beach deposit was identified at a slightly lower elevation of 652 meters (2,140 feet) amsl on a
wave-cut bedrock platform perched above the canyon floor about 1.6 kilometers (~1 mile) west-southwest of
Lone Butte (UTM Zone 11, 447540E, 3949962N, WGS 84; Figure 26). This deposit consists of lacustrine marl
overlain by beach sand that contains freshwater snail (Helisoma Carinifex newberryi) and mollusk (Anodonta sp.)
shells (Figure 27). A date of 11,550 ± 50 BP or 13,387 cal BP (Beta-280686) from one of the snail shells
establishes the age of the beach as Terminal Pleistocene.
Salt Wells Valley and Poison Canyon
As the connecting link between China Lake and Searles Lake basins, Salt Well Valley and Poison Canyon
contain outcrops of lacustrine and shoreline deposits that lie below the 670-meter (2,200-foot) sill level of China
Lake. Smith (2009) has mapped the age and extent of these deposits, and various studies have obtained
radiocarbon dates on shells, lacustrine marl, carbonates, and rock varnish from the area (Benson et al. 1990;
Couch 2003; Dorn et al. 1990; Garcia et al. 1993; Hildebrandt and Darcangelo 2006; Kaldenberg 2006; Lin et
al. 1998; Ramirez de Bryson 2004; Smith 2009). Radiocarbon dates from these deposits record sustained stands
of Lake Searles that are proxy evidence for outflow from China Lake Basin (Smith 2009).
Nine Anodonta shells from this area yielded dates ranging between 16,645 and 13,556 cal BP (Beta211389, Beta-211387), with an overall mean age of 14,400 cal BP (Hildebrandt and Darcangelo 2006;
Kaldenberg 2006). These samples were recovered between elevations of about 640 and 587 meters (2,100 and
1,926 feet) amsl (average of 625 meter, 2,050 feet), with most or all derived from surface or reworked contexts.
Eleven dates on marl and carbonate from Salt Wells Valley and Poison Canyon range between about 15,800 and
12,347 cal BP, resulting in a mean of 13,717 cal BP (Couch 2003; Lin et al. 1998; Ramirez de Bryson 2004). All
but one of these samples is from elevations of 590 to 575 meters (1,936-1,886 feet) amsl, or about 581 meters
(1,906 feet) amsl, on average.
Shell samples from Salt Wells Valley and Poison Canyon are generally older and regularly found about
44 meters (144 feet) higher in elevation than the marl and carbonate samples. This relationship is consistent with
shells occurring in shallow near-shore positions, and marl and carbonates forming in deeper off-shore positions of
the lake. The age and elevation of these samples suggest a large and/or deep lake was established in the canyon
more than 16,000 years ago and based on the youngest shells dates, may have persisted at relatively high levels up
to at least 13,500 years ago. The size/depth of the lake appears to have declined substantially after about 13,300
cal BP, as younger dates have only been obtained from one sample of marl and one sample of carbonate at low
elevations within the canyon. This data implies that water levels had dropped below the China Lake sill and
created two separate lake basins after about 13,300 years ago.
Constructing a Regional Historical Context for Terminal
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Far Western
L at
e Plei
ene
stocen
e Sh
eli
ne
(6
m
ore
li
,2
ne
China Lake Naval
Weapons CTR
Sh
or
83
Term
i n al Plei
st
oc
(6
Re c
683 m
ess
70
i
on
a l Sh
o re
li n (
e 65
4
670 m
M
ag
az
i
m
,2
2 00
1 46
)
Lower Barrier Beach
Upper Barrier Beach
R
4m
65
ne
f t)
d
0 mm
67 83
6
654 m
m, 2
0f
t)
ft
683
m
24
Beach-Shell deposit on wave-cut platform
(652 m, 2,140 ft)
Dune sand
Outlet Canyon
ON
TR
Outlet Channel
A
ER
AT
W
PI
L
PE
E
IN
LO
NE
BU
TT
E
m
4
65
670 m
683 m
Sample Locus
Landscape Features
Elevation Contour
Beach Barrier
0
0
Meters
200
1,000
Feet
400
2,000
Figure 26. Landscape Features and Sample Locus in Salt Wells Valley-China Lake Outlet.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
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58
Far Western
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
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Lower Beach Ridge
59
Marl, Shells, and Beach Sand on Wave-Cut
Bedrock Platform at 654 m (2,147 ft) amsl to
Northeast (above); Date of 13,387 cal BP
(Beta-280686) on Small Snail (far right)
13,387 cal BP (Beta-280686)
Upper and Lower Beach Barrier Ridges to North (above);
Tufa Near Top of Upper Ridge at 683 m (2,240 ft) amsl (right)
683 m (2,240 ft) amsl
654 m (2,147 ft) amsl
Far Western
Two Prominent Shorelines on Bedrock Knoll to Northwest
Prominent Shorelines on Hillsides of Salt Wells Valley to East toward Searles
Figure 27. Landforms and Lake Features in Salt Wells Valley-China Lake Outlet.
China Lake’s Outlet History
Stratigraphic and radiocarbon evidence show there was a large and deep lake within Salt Wells Valley and
Poison Canyon more than 15,000 years ago. This lake probably stabilized at or around 683 meters (2,240 feet)
amsl (China and Searles coalesced), as marked by extensive shoreline features at that altitude. The lake likely
maintained itself at relatively high levels until about 13,500 cal BP, after which the number of radiocarbon-dated
shells in Salt Wells Valley declines. Searles Lake dropped rapidly between about 13,500 and 13,400 cal BP, until
it temporarily stabilized at about 654 meters (2,147 feet) amsl, some 16 meters (52.4 feet) below the sill of China
Lake. Evidence of this recessional stand includes an extensive shoreline, a barrier beach ridge, wave-cut bedrock
platform, and beach deposit with shells dating to about 13,390 cal BP (Beta-280686), all of which occur within
three meters (9.8 feet) or less of the 654-meter (2,147-foot) shoreline. The near absence of marl and carbonate
deposits and freshwater shells dating less than 13,300 cal BP suggest that Searles Lake fell rapidly after this time
and has not since returned to Salt Wells Valley or upper Poison Canyon. The history of lake level and landscape
changes is discussed further in Chapter 5.
Constructing a Regional Historical Context for Terminal
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5. PALEOHYDROLOGY AND LANDSCAPE HISTORY IN THE NORTHWESTERN MOJAVE
DESERT DURING THE PLEISTOCENE/HOLOCENE TRANSITION
The current study documents a three-part geomorphic and hydrological transition, reflecting
deterioration of effective moisture conditions around the time of the Pleistocene/Holocene transition in the
northwestern Mojave Desert. This sequence is marked first by the decline in lake levels and hydrological
separation between the lake basins of China Lake and Searles. Following this interval, groundwater continued to
be delivered to these valleys in pulses, supporting localized wetland habitats in medial channel positions and
around spring seeps. After 10,000 cal BP, groundwater levels dropped, formerly wet locations dried, and a
widespread re-activation of alluvial fan deposition occurred across the northwestern Mojave Desert.
HYDROLOGICAL HISTORY OF LOWER OWENS RIVER AND LOCAL DRAINAGES
Between about 18,000 and 13,500 cal BP, China Lake Basin received substantial and often sustained
inflows from the lower Owens River and other local drainages, resulting in high lake stands. Deposition of deepwater lacustrine sediments (Core 9), freshwater Anodonta shells, tufa deposits, and related shoreline features, offer
compelling proof of high water levels in China Lake and Searles basins during this time period (details provided in
next section). Surface flows from Owens River are confirmed by coarse-grained channel deposits (i.e., cobbles and
gravels) along the river in Rose Valley, dating just prior to 13,400 cal BP. In the South Borrow Pit, fine-grained
silt and an organic-rich black mat rest immediately above Owens River channel deposits and indicate that active
water flow slowed or stopped and the depositional regime changed sometime around 13,400 cal BP (Figure 29).
It remains possible that the lower Owens River continued to flow after this time, as the active channel could have
shifted away from the sample locality. However, stratigraphic records from several other locations in Rose Valley
dating to the Early Holocene and later reveal only coarse alluvial fan or fine-grained distal fan/playa deposits in
axial positions once occupied by the lower Owens River.
Comparatively high surface water flows prior to 13,000 cal BP in the Indian Wells Valley region is also
supported by the terrace sequence and stratigraphic records preserved in local washes. No later than 12,600 cal
BP, alluvial deposits began to accumulate as discrete and discontinuous inset terraces in the medial and lower
reaches of the largest drainage systems, including Little Dixie and Dove Springs washes. These deposits now form
the first terrace (T2) above the active channels and fill erosional voids carved into older and higher distal fan
deposits (Figure 28). The position of these terraces suggests that the dominant fluvial process prior to about
12,600 cal BP was lateral channel migration and erosion. The absence of older terrace deposits in these inset
positions indicates that local run-off may have been substantially higher before this time. By 12,600 cal BP, the
competency of these drainages had declined and they were no longer capable of evacuating even fine-grained
sediments.
Between about 12,600 and 10,500 cal BP, water discharge into some local washes appears to have been
regular, but episodic, reflected by similar sequences of stratified sands, silts and organic-rich horizons preserved as
inset terraces at Little Dixie Wash, Dove Springs Wash, and Indian Wells Canyon. Groundwater and/or effective
moisture conditions supported mesic habitats colonized by freshwater gastropod and ostracode species, formation
of soils and organic-rich layers (black mats), and the episodic deposition of paludal (spring or marsh) sediments.
At least three cycles of deposition are recorded during the Terminal Pleistocene/Early Holocene (Figure 29). The
first two depositional pulses occurred between 12,600 and 12,300 cal BP, and between 12,000 and 11,800 cal
BP. The latter interval coincides with the appearance of freshwater mollusks and formation of organic-rich
horizons in Little Dixie Wash. In the South Borrow Pit in Rose Valley, deposition of more than two meters of
fine silt loam is recorded along the lower Owens River channel after 13,400 cal BP, but before 11,400 cal BP,
when an organic rich mat developed. At this same time, formation of spring mats dated between 11,540 and
11,270 cal BP is evident at the Basalt Ridge locality in China Lake Basin (Basgall 2004) and an organic mat
developed in Indian Wells Canyon, dated to about 11,200 cal BP. The Early Holocene brought a repeat of this
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
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Transect shown in Figure 15
847
NORTHWEST
SOUTHEAST
845
841
839
T-3
Older Pleistocene
Fan Deposit
837
T-2
Middle Holocene
Alluvial and
Aeolian Deposits
coarse
sand and
gravel
T-1
Locus 3
Active Wash
Deposit
Terminal PleistoceneEarliest Holocene
Alluvial Deposits
835
T-3
Little Dixie Wash
coarse sand
and gravel
Older Pleistocene
Pliestocene
Fan Deposit
Elevation in Meters (amsl)
843
fine sand
and gravel
EXAGGERATED VERTICAL SCALE
833
0
100
200
300
400
500
600
700
800
Distance in Meters (NW to SE)
Figure 28. Elevational Cross Section of Little Dixie Wash Showing Inset Position
of Terminal Pleistocene/Earliest Holocene Terrace.
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
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Far Western
cal BP (Median Probability, 2-Sigma Range)
HOLOCENE
2
4
6
8
0
2
4
6
8
17,500
Owens River Inflow
China-Searles Coalesced
16,500
63
0
18,500
17,500
PL EISTOCENE
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
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CHINA LAKE BASIN AREA
18,500
16,500
15,500
15,500
14,500
14,500
China-Searles Separate
13,500
13,500
12,500
12,500
YO U N G ER D R YAS IN T ER VAL
Lakes Recede
and Dessicate
11,500
11,500
10,500
10,500
Terrestrial
Alluvium
9,500
9,500
8,500
8,500
7,500
7,500
6,500
6,500
ke
La
sin
Ba
s
n
lai
dp
oo es
Fl nag
nd rai
sa lD
an ria
l F st
via erre
lu
Al m T
fro
les
ar
Se
let
ey ut
all O
s V on
ell any
W
lt n C
Sa iso
Po
e
ak
aL
in
Ch
Far Western
Figure 29. Radiocarbon Record of Lake Level and Landscape Changes in the China Lake Basin Area.
Number of Dates
(N=90; Median Probabilties at 200-Year Intervals)
pattern as a depositional pulse after about 11,200 cal BP was again followed by the emergence of habitats
supporting freshwater mollusks and the development of organic-rich horizons by about 10,700 cal BP in Little
Dixie Wash. Deposition of fine-grained, clay-rich silts dated between 10,600 and 9065 cal BP at the Lava End
locality in Rose Valley also reflect comparatively high ground-water flows into the Early Holocene.
Physical evidence of surface water at this time, however, is not widespread but largely limited to specific
drainage segments where hydrologic conditions permitted the formation of braided channel systems (cienegas)
and near-level inset alluvial terraces composed of only very fine-grained sands, silts, and clays. Much of the water
in these settings was likely supplied by local springs and other groundwater sources fed and recharged in part, by
non-local sources at higher elevations in the Sierra, such as the upper South Kern River; an important source of
ground water in southern Indian Wells Valley (Guler and Tyne 2004, 2006; Ostdick 1997). These conditions
began around the on-set of the Younger Dryas, but continued well into the Early Holocene.
After about 10,500 cal BP, the number of groundwater-related deposits declined substantially,
presumably due to warmer and drier conditions characteristic of the Middle and Late Holocene in the
northwestern Mojave Desert. However, a brief period of moist conditions during the Middle Holocene is
recorded at Dove Springs Wash, where ostracode-rich, fine-grain paludal deposits (Stratum X-5Ab) date to 4753
cal BP (Beta-280993); the only such example post-dating 10,400 cal BP identified during this study.
LAKE LEVEL HISTORY
China Lake Basin appears to have received substantial input from the lower Owens River and other local
washes, up to about 13,400 cal BP. A prominent wave-cut shoreline and related features at an elevation of about
683 meters (2,240 feet) amsl in China Lake Basin, and lacustrine deposits in Salt Wells Valley, Poison Canyon,
and the larger Searles Lake Basin dated between about 16,000 and 15,000 cal BP (Figure 30), indicate that waters
from China and Searles basins merged to form a relatively stable and sustained lake (Figure 31). We estimate the
Terminal Pleistocene lake to have covered an area roughly 272 square kilometers and include a water volume of
about 3.8 million cubic meters. Bivalve shells in upper Salt Wells Valley dated between 14,035 and about 13,955
cal BP occur below the 670-meter elevation (although the precise context and elevation of these dated shells
remains unknown; Kaldenberg 2006), suggesting declining waterlevels and separation of the two lake basins. By
13,700 cal BP, a coalesced lake reformed and stabilized well above the modern China Lake sill (670.6 meters,
2,200 feet) at an elevation of no less than 681 meters (2,234 feet) amsl, based on a dated tufa sample from the
Basalt Ridge in China Lake Basin (Davis and Panlaqui 1978).
Lake levels appear to have fallen at least 11 meters (36.1 feet) to the elevation of the China Lake Basin
outflow sill (670.6 meters; 2,200 feet amsl), between about 13,700 and 13,400 cal BP and China and Searles
lakes separated (Figure 30). Evidence for this rapid decline comes from a date of 13,390 cal BP on freshwater
Helisoma sp. shell associated with a beach deposit in upper Salt Wells Valley, at an elevation of 654 meters (2,147
feet) amsl, and a date of 13,000 cal BP from algal tufa situated just below the outflow sill in China Lake Basin, at
an elevation of 666 meters (2,186 feet) amsl. The decline in depth recorded for China and Searles lakes correlates
almost precisely with evidence from the lower Owens River channel indicating that high-energy surface flows
stopped by 13,400 cal BP. The separate lakes stabilized long enough to form a prominent set of shoreline features
at the sill elevation in China Lake Basin (670.6 meters; 2,200 feet amsl) and in upper Salt Wells Valley at an
elevation of about 654 meters (2,147 feet) amsl (see Figure 27). We estimate this lake stand to have covered an
area roughly 160 square kilometers with a water volume of 1.03 million cubic meters—about 75% less volume
and 60% less area than the coalesced high stand.
China Lake receded below the 665 meter (2,182 feet amsl) elevation sometime between 13,000 and
11,100 cal BP (Figure 30), based on dated alluvial fan deposits in Core 9, at an elevation of 665 meters, and the
algal tufa formed near the outflow sill, at an elevation of 666.3 meters (2,186 feet). A continuous sequence of
alluvial fan deposits in Core 9, above the 665 meter elevation, and radiocarbon dates on buried soils obtained by
Davis (Davis and Panlaqui 1978) at her Stake 1 locality, and by Basgall (2004) at Basalt Ridge, indicate China
Lake did not reach or exceed the sill level after 12,000 to 11,000 cal BP (Figure 30). Any high-water stands within
Constructing a Regional Historical Context for Terminal
Pleistocene/ Early Holocene Archaeology of the
North-Central Mojave Desert, Step 1
64
Far Western
685
China-Searles Coalesced
Basalt Ridge
Soil
670
Stake 1
“flaggy sandstone”
with artifacts
665
Basalt Ridge
Tufa
Spring
Sediment
Deposits
hummock
?
Stake 1
Soil
ak
Core 9
aL
n
i
h
6Cg
C
Tufa
Knoll
Stake 1
?
660
Searles Lake
675
China Lake
Sill
e
Elevation in Meters (sample mean)
680
Anadonta
Core 9
11Cg
?
655
?
?
Modern
Playa
?
Anadonta
650
Beach/Shell Deposit in Outlet
645
?
640
7,000
Marl
8,000
9,000
10,000
11,000
12,000
13,000
Anadonta*
3 Anadonta*
Anadonta*
14,000
15,000
16,000
17,000
18,000
Distance in Meters (NW to SE)
Above China Lake
At or Below China Lake
At or Below Searles Lake
Inferred China Lake Level
Inferred Searles Lake Level
Note: *Precise Elevations and Context Unknown (Represents Minimum Elevation).
Figure 30. Lake History Based on the Age, Nature, and Elevation of Radiocarbon-Dated Samples.
Constructing a Regional Historical Context for Terminal
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Far Western
675
670
670.6 m—Terminal Pleistocene Lake
665
665 m—Maximum Holocene Lake
modern playa
Holocene Beach Barrier Ridges and Berms
680
KER-SBR County Line
682.75 m—Late Pleistocene Lake
KER -6669
685
KER -6659, -6660
690
Stake 19 (Davis 1975, 1978); Core 9 (this Study)
NAWS Fenceline
Henry “Kill” Site
(Davis 1975, 1978)
695
Elevation in Meters (amsl)
EAST
Flightline Road
Stake 1 and 24 (Davis 1975, 1978)
WEST
700
660
Note: Vertical Scale Exaggerated
28,000
26,000
24,000
22,000
20,000
18,000
16,000
14,000
12,000
10,000
8,000
6,000
4,000
2,000
0
655
Distance in Meters (along Transect 1)
Figure 31. Elevation of Former Shore Lines and Lake Levels in Relation to Modern Topographic
Features and Selected Prehistoric Sites
Constructing a Regional Historical Context for Terminal
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the basin during the remainder of the Holocene would have resulted in a maximum water depth of no greater
than ten meters (33 feet), based on the elevation of the modern playa at 655 meters (2,149 feet) amsl. This would
have resulted in a lake roughly 97 square kilometers in size, with a water volume of just 377,000 cubic meters—
90% less volume and 75% less area than the Late Pleistocene high stand.
Beach berms and barrier ridges along the eastern side of China Lake Basin (see Figure 23 and Figure 31),
occur at an elevation of roughly 662 meters (2,172 feet) amsl and appear to have been formed during brief
Holocene transgressions or represent recessional features, post-dating 13,000 cal BP, based on the dated tufa
sample at an elevation of about 666 meters (2,186 feet) amsl. Preliminary photon-stimulated-luminescence dating
of the beach ridges is consistent with this interpretation, suggesting these features formed sometime between
about 8,000 and 13,000 years ago (Berger in Giambastiani 2008), during the Terminal Pleistocene/ Early
Holocene.
TERRESTRIAL LANDFORM HISTORY
Between about 10,400 and 9800 cal BP, a substantial shift in depositional regimes is apparent across
Indian Wells Valley and the broader northwestern Mojave Desert, represented by the accumulation of coarsegrained alluvial fan deposits which now form extensive piedmonts along valley margins. In fan-head positions,
these Holocene-age deposits are set below Pleistocene-age fan surfaces, but mantle the older deposits toward the
valley bottom. This period of fan rejuvenation follows an extended interval of landscape stability during the
Terminal Pleistocene/ Early Holocene, represented by widespread stratigraphic unconformities marked by buried
soils dating to this time period.
Holocene-age deposits form modern fan surfaces bordering local washes and immediately overlie finegrained sediments deposited as inset terraces during the Terminal Pleistocene/ Early Holocene at Little Dixie
Wash and Indian Wells Canyon. Along Little Dixie Wash, younger fan deposits also extend onto the distal
portions of older fans, forming a continuous apron across both surfaces (see Figure 28). Dates from inset terraces
at Little Dixie Wash localities 1 and 3 indicate fan progradation began after 10,900 to 10,700 cal BP. This is
consistent with a stratified alluvial fan sequence identified at the confluence of Freeman Gulch and Little Dixie
Wash at Locality 5 (see Figure 15), which began forming before ~7800 and 7200 cal BP.
In Indian Wells Canyon, fan aggradation began sometime after 11,190 cal BP, but before 9810 cal BP,
based on a date from the uppermost loamy sand stratum and one from a buried soil formed on the overlying
coarse-grained fan deposit. On the piedmont bordering the western side of Indian Wells Valley, Young (2007)
reported a date of 10,246 cal BP (Beta-237063) from a buried soil capped by coarse fan deposits, while at the
Basalt Ridge locality in China Lake Basin, Basgall (2004) reported a date of 9360 cal BP (Beta-170209) from a
buried soil, also capped by coarse, distal fan/and or eolian deposits. Just south of Indian Wells Valley, in the
Koehn Lake Basin (the outflow to Dove Springs Wash), Early Holocene fan rejuvenation is also marked by a
buried soil dated to 10,640 cal BP (Beta-255187; Young 2009).
In Rose Valley, alluvial fan deposits began accumulating about 9800 cal BP in the North Borrow Pit, and
in the South Borrow Pit after 11,775 cal BP, while buried soils formed on distal fan/playa deposits at Dead Chevy
Flat, Cinder Flat, and Rose Valley Flat are dated 11,097, 10,370, and 8130 cal BP, respectively. At Little Lake just
to the south of Cinder Flat, alluvial fan deposits capped a buried soil at the Stahl site (INY-182) dated 9600 cal BP
(Schroth 1994), further suggesting fan aggradation was widespread in Rose Valley during this time period.
Combined, these records suggest that a prolonged period of alluvial fan stability during the Terminal
Pleistocene/Early Holocene was interrupted, beginning in the Early Holocene, by widespread fan rejuvenation
and deposition. Younger-dating buried soils in some of these same fans (e.g., Young 2007), indicate that
punctuated fan deposition has been the dominant geomorphic process in the northwestern Mohave Desert
through the Holocene.
COMPARISON WITH REGIONAL RECORDS
Up to about 13,400 cal BP effective precipitation and Sierra Nevada run-off was sufficient to maintain
high-energy surface flows through the lower Owens River channel to China Lake Basin. These inflows
Constructing a Regional Historical Context for Terminal
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periodically resulted in a coalesced lake between China Lake and Searles Basins. After this time however, surface
flows through the lower Owens River stopped and China and Searles lakes declined rapidly. The two lakes
eventually separated, when water levels dropped below the China Lake Basin outflow sill by 13,400 cal BP. For
some period of time the lakes remained at elevations approaching the outflow sill (~670 meters amsl), but by
11,100 cal BP, China Lake had dropped below 665 meters amsl.
Searles and Owens Lake Basins
The lacustrine record for China Lake presented here corresponds reasonably well with the reported
sequence of high and low lake stands in the adjoining and inter-connected basins of Owens and Searles Lakes.
However, interpretations of the mechanisms responsible for Terminal Pleistocene/Early Holocene lake level
fluctuations in Owens and Searles basins are currently at odds. A recent study by Bacon et al. (2006) concluded
that Owens Lake probably stopped overflowing to Rose Valley and China Lake Basin after 15,500 cal BP. The
record from Searles Basin reported by Smith (2009) and others (e.g., Benson et al. 1990; Smith and Street-Perrott
1983), identify substantial evidence for lake stands in Searles Basin up to about 12,900 cal BP (ca. 11,000
RCYBP) attributing this to sustained input from the Owens River via outflow from Owens and China Lake
(Smith 2009:81-83). Despite differences in the interpretation of the source of water in put, calibrated radiocarbon
dates from these interconnected basins demonstrate that intervals of high and low lake levels largely correspond
from the Terminal Pleistocene into the Early Holocene.
In Searles Basin, Smith (2009:Figure 39) recognizes a high stand at about 18,700 cal BP (15,500
RCYBP) followed by declining lake levels between about 18,200 and 16,600 cal BP (15,500-13,500 RCYBP),
similar to a decline in China Lake levels after 17,780 cal BP (14,610 RCYBP) as evinced by beach deposits below
the outflow elevation in Core 9. Owens Lake is also inferred to be nearly dry during this period (Bacon et al.
2006:Figure 3). Subsequently, the Searles lake record suggests a coalesced lake formed in China Lake and Searles
Basins at around 15,500 cal BP, reflected in the China Lake Basin by off-shore lacustrine deposits above the beach
sands in Core 9 (Stratum VI, 7Cu), and tufa deposits at Basalt Ridge dated 15,650 cal BP. This high stand is also
consistent with Bacon et al.’s (2006:Figure 3) suggestion that water levels in Owens Lake rose to the sill level and
overflowed into the lower Owens River channel about 15,500 cal BP.
Smith (2009:75, Figure 39) indicates Searles Lake rose once again between 13,900 and 12,900 cal BP
(12,000-11,000 RCYBP), when it coalesced with China Lake. We believe that Smith (2009:Table 5) based the
youngest age of the final transgression on a radiocarbon date of 10,900 RCYBP or 12,500 cal BP obtained on
tufa reported by Garcia et al. (1993) from an elevation of 689 meters (2,261 feet) amsl in Searles Basin. Uraniumseries dating of this same sample provided a much older date of 17,000 RCYBP (Garcia et al. 1993; Smith
2009:Table5), however, suggesting the tufa may relate to an earlier high stand. Lin et al. (1998) re-sampled tufa
deposits from this same location and generated a date of 12,070 ± 100 RCYBP or 13,900 cal BP, very similar to
the date and elevation of the last high stand recognized in China Lake Basin. This final coalesced lake is
represented at an elevation of 681 meters amsl by a second Basalt Ridge tufa, dated 13,700 cal BP (11870 ± 120
RCYBP). Evidence developed for the current study indicates lake levels declined precipitously in China Lake and
Salt Wells Valley after this date, closely matching a decline of more than 20 meters in Owens Lake dated about
13,200 cal BP (Bacon et al. 2006:Table 3, Figure 3) and extremely low lake levels in Searles basin after 12,900 cal
BP (Smith 2009:75).
To the extent that the Searles and China Lake records agree that a coalesced lake persisted in these basins
until just before 13,400 cal BP, current information suggests this high stand could not have been the result of
overflow from Owens Lake. According to Bacon et al. (2006) Owens Lake last spilled into the lower Owens River
much earlier (ca. 15,500 cal BP). If true, evidence for high-energy surface flows in the lower Owens River channel
and high lake levels in China Lake and Searles Basins after 15,000 cal BP derive solely from Sierran run-off into
Rose Valley and Indian Wells Valley. However, it remains an open question whether local drainages alone could
cause China and Searles lakes to coalesce, without input from Owens Lake and the larger Owens River watershed
(e.g., Smith 2009:83). Even if run-off into Rose Valley and Indian Wells Valley after 15,000 cal BP was sufficient
to cause a unified lake stand, equal, if not larger, amounts of water would be expected to enter the upper Owens
River from the Sierra, potentially causing Owens Lake to rise and spill over (e.g., Smith 2009:83). Unfortunately,
Constructing a Regional Historical Context for Terminal
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channel deposits in the lower Owens River bed dated to before 13,400 cal BP cannot be directly attributed to
overflow from Owens Lake, yet their presence indicates high-energy surface flows through Rose Valley continued
during the Terminal Pleistocene, a phenomenon not recorded in stratigraphic records after this time.
All dates from Searles Basin after about 12,000 cal BP (~10,200 RCYBP) are associated with the Upper
Salt deposit, and represent a desiccated or dry lake (Smith 2009:Table 10). While radiocarbon dates from
lacustrine-related deposits (e.g., tufa, marl, oolites, bivalves, gastropods, and organic sediments) in Searles Basin,
suggest an intermittent lake may have persisted there until about 11,000 cal BP (Figure 32), a coalesced lake
could not have extended into China Lake Basin. Radiocarbon-dated buried soils at elevations between 666 and
667 meters amsl (Davis and Panlaqui 1978), spring mats at an elevation of 674 meters (Basgall 2004), and
alluvial fan deposits at 665 meters in Core 9, demonstrate that if a lake was present in China Lake Basin after
13,000 cal BP, it lay well below the basin’s outflow sill at 670 meters amsl. These records further suggest that any
Holocene lake in China Lake Basin was likely no greater than about ten meters deep, supporting Benson et al.’s
(1990) contention that “lakes did not form in the Searles Lake Basin during the Holocene as the result of spill
from the Owens Lake Basin” (Benson et al. 1990:270).
Other Mojave Desert Records
Radiocarbon evidence from several other lake basins in the Mojave Desert corresponds well to the China
Lake record reported here. With the exception of the Mojave River system (e.g., Silver Lake, Soda Lake, Afton
Canyon, and Mojave River), virtually all dated samples indicate that vestigial pluvial lakes in this region were gone
by about 11,000 cal BP (Figure 32 and Figure 33). As the Mojave River system has its headwaters in the
Peninsular Ranges of western California (see Figure 4), this drainage appears to have continued to receive extralocal surface flows periodically up to about 10,000 cal BP, and occasionally thereafter (Wells et al. 2003).
However, the last sustained high stand at Lake Mojave occurred during the Lake Mojave II Period, which ended
about 13,000 cal BP (11,400 RCYBP). This is almost precisely the same time as the last period of high lake stands
recognized in China Lake Basin and Searles Basin. Most other lake basins in the Mojave Desert (e.g., Coyote
Lake, Bristol Lake, Koehn Lake, Panamint Valley, Death Valley), appear to have also dried by about 13,000 cal
BP (Figure 32 and Figure 33), roughly corresponding to the beginning of the Younger Dryas. Radiocarbon
evidence suggests some of these basins may have periodically held water later in time, but none of the dated
samples evince persistent lake stands after 11,000 cal BP (Figure 32 and Figure 33).
Overall, effective moisture in the wider Indian Wells Valley region appears to have remained
comparatively high after 13,000 cal BP resulting in the formation of spring seeps and minor, episodic, surface
flows in the lower Owens River channel, some local washes, and in China Lake Basin, probably fed by local and
extra-local sources of ground water. This period does not appear to have been uniformly wetter. Rather, the
geomorphic record suggests brief periods of higher effective moisture, which largely ended in the China Lake
region by 9000 cal BP. This correlates with the Intermittent Lake III Period at Lake Mojave (Wells et al. 2003),
14
dated between 13,000 and about 9800 cal BP (11,400 to 8700 C BP).
Depositional pulses of fine-grained sediments and the development of organic-rich horizons between
12,600 and about 8000 cal BP recorded in Rose Valley and local washes, correlate almost precisely with similar
ground-water records from black mats and other fluvial deposits (Unit E) reported by Quade et al. (2003) from
western Nevada in the eastern Mojave Desert (Figure 34). Isolated spring deposits from China Lake Basin dated
between 11,400 and 11,200 cal BP (Basgall 2004) and at Rogers Ridge in Nelson Basin at Fort Irwin dated
between 9200 and 8800 cal BP (Jenkins 1985), are also indicative of this period of higher groundwater discharge
during the Early Holocene. While wetter conditions persisted as late as 8000 cal BP in some locations, a
comparison of regional records (Figure 34) shows that the most sustained period of elevated groundwater
discharge correlates almost precisely with the end of the Younger Dryas (ca. 12,000 to 11,600 cal BP).
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Constructing a Regional Historical Context for Terminal
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Figure 32. Radiocarbon Dates Relevant to the Lacustrine History of the Lower Owens River System.
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Constructing a Regional Historical Context for Terminal
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Constructing a Regional Historical Context for Terminal
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Figure 34. Radiocarbon Dates from Terrestrial Spring, Marsh, “Black Mat,” and other
Wetland Deposits in the Mojave Desert.
An abrupt shift in geomorphic processes is characteristic of the final phase of the Pleistocene/Holocene
transition in Indian Wells Valley. Beginning after about 10,400 cal BP, an extended period of landscape stability
was interrupted by depositional cycles recorded in numerous alluvial fans across this region. Harvey et al. (1999),
McDonald et al. (2003), and Miller et al. (2010) have previously recognized this phenomenon elsewhere in the
Mojave Desert, attributing it to shifts in climate and vegetation associated with the Pleistocene/Holocene
transition. Declines in vegetative cover at the beginning of the Holocene, combined with a shift from mainly
winter to summer (monsoonal) precipitation, appear to be responsible for these widespread geomorphic changes
(Harvey et al. 1999; McDonald et al. 2003; Miller et al. 2010). An isotopic record from ostracodes recovered in
basal alluvial fan deposits in Rose Valley (see Appendix D) supports the notion that greater seasonal rainfall from
increased monsoonal activity, as opposed to simply vegetation shifts, are responsible for these widespread
depositional responses (McDonald et al. 2003).
CONCLUSIONS
Analysis of the geomorphic and hydrologic records of surface water inflows and lake level histories in
Indian Wells Valley document a three-part shift during the Terminal Pleistocene and Early Holocene that
strongly correlates with other geomorphic and fluvial information from the central and eastern Mojave Desert.
Similarities in these records indicate that effective moisture during the Terminal Pleistocene/Early Holocene in
the Mojave Desert was higher than anytime since. Pluvial lakes in China and Searles Basins reached high stands at
the height of the glacial maximum (ca. 20,000 cal BP), in concert with other pluvial lakes in the Mojave Desert
(e.g., Lake Manly, Lake Mojave, etc.). Lake levels appear to have fluctuated until about 13,000 cal BP, coincident
with the onset of the Younger Dryas. Occasional lake stands may have occurred after that time in the larger basins
of the Mojave Desert (e.g., Searles Lake) or those fed by extra-local water sources (e.g., Owens Lake and Lake
Mojave) If a lake was present in China Lake Basin during the Holocene, it could have only been intermittent, and
did not reach above 665 meters amsl, far below the outflow sill to Searles Basin at 670 meters. Groundwaterrelated deposits including organic-rich black mats, dating between about 12,600 and 10,000 cal BP, are preserved
in several drainages entering China Lake Basin, and are consistent with region-wide evidence for high
groundwater levels and increased spring discharge during the Terminal Pleistocene and first part of the Holocene.
Terminal Pleistocene/ Earliest Holocene stratigraphic and paleoenvironmental records identified by this
study have established a firm foundation for future archaeological research in the China Lake area. The pluvial
lake history of China Lake Basin is much better resolved based on this synthesis, adding clarity to the conflicting
interpretations drawn from adjacent lake basins. The pluvial system was in substantial decline by the beginning of
the Clovis Period (ca. 13,500 to 12,900 cal BP), but a lake persisted in China Lake Basin through much of this
interval. After 13,000 cal BP, around the beginning of the Younger Dryas, groundwater was the primary source
for surface flows throughout Indian Wells Valley and elsewhere in the Mojave Desert, expressed mainly as isolated
spring seeps and as wetlands in inset terrace positions along major washes and streams. Former lake basins appear
to have periodically held water through this interval, but well below previous high stands. A rapid decline in
effective precipitation during the Early Holocene is marked by widespread alluvial fan deposition in the Mojave
Desert, most likely related to periodic summer monsoons.
Constructing a Regional Historical Context for Terminal
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6. CONCLUSION AND OUTLINE FOR STEP 2
Step 1 of the DoD Legacy Program study “Constructing a Regional Historical Context for Terminal
Pleistocene/Early Holocene Archaeology of the North-Central Mojave Desert” is now complete. The objective of
this initial step was to reconstruct the paleoenvironment during the Pleistocene/Holocene transition (15,0008000 cal BP). This investigation was an unqualified success and provides a firm foundation for creating a strong
historical context for early human occupation in the northern Mojave Desert (which will be carried out in Step 2
of the project). This paleoenvironmental research identified and dated a three-stage geomorphic and hydrological
transition tied to deterioration in effective moisture. Initially, Pleistocene pluvial lake levels declined, and China
Lake and Searles lake basins became hydrologically separated by 13,400 cal BP. China Lake, however, persisted
until just after 13,000 cal BP. Subsequently, localized wetland habitats flourished as high groundwater levels and
spring discharge continued to deliver surface flows to local washes and the China Lake Basin area. These wetland
habitats largely disappeared by ~9000 cal BP as groundwater levels dropped, and alluvial fan deposition increased.
IMPLICATIONS FOR EARLY HUMAN SETTLEMENT AND SITE PRESERVATION
Each of the paleoenvironmental changes described above almost certainly had an effect on the
subsistence economies of early foraging groups and the location and preservation of archaeological sites from the
Terminal Pleistocene and Early Holocene. Notably, sites in China Lake and Searles Basins dating to pre-Clovis
and Clovis time segments (15,000 to 13,000 cal BP) should occur above the Terminal Pleistocene lake high
stand, at elevations greater than 670 to 680 meters amsl. In contrast, post-Clovis age sites from the Younger Dryas
Terminal Pleistocene and Preboreal Early Holocene (13,000 to 10,500 cal BP) should be much more widely
distributed and will likely occur below the prior lake high stand on the valley floor. Archaeological deposits from
the Late Pleistocene (i.e., Pre-Clovis and Clovis intervals) and Terminal Pleistocene/ Early Holocene are also
expected to occur along the lower Owens River channel and other local washes where surface water flows persisted
and localized wetland habitats developed. As surface water flows declined in the Early Holocene, sites from this
time period are expected to cluster near active spring seeps and close to the China Lake playa where near-surface
groundwater created periodic playa lakes and associated wetland habitats attractive to early foraging groups.
However, widespread alluvial fan activation beginning in the Early Holocene may have buried many
archaeological deposits from the Pleistocene-Holocene transition. Such buried sites are expected to occur where
Holocene-age distal fans intersect former lake margins and overtop older fan remnants adjacent to major washes,
particularly those draining the eastern Sierra Nevada. Finally, we would anticipate a very different settlement
distribution in the latter portion of the Early Holocene (after 9000 to 8000 cal BP) and into the Middle
Holocene, as groundwater levels declined and wetland habitats disappeared from valley basins and Sierra-fed
streams,, and only the most productive springs continued to provide surface water flows.
STEP 2 – HISTORICAL CONTEXT
Paleoenvironmental results, just described, provide a firm foundation for conducting Step 2 and
successfully completing the overall project objectives. This entails creating a strong historical context for
understanding the archaeology of the Terminal Pleistocene and Early Holocene. This will strengthen stewardship,
provide a consistent and rigorous basis for determinations of eligibility for the National Register of Historic
Places, and greatly assist in the management of these cultural resources, as required by Section 110 of the National
Historic Preservation Act. As discussed in the proposal, Step 2 will entail reconstructing Terminal
Pleistocene/Early Holocene plant and animal communities to understand fluctuations in resource potential, and
re-examining Terminal Pleistocene/Early Holocene archaeological sites within the north-central Mojave Desert to
reconstruct changing land-use patterns.
To accomplish these objectives, Step 2 will be comprised of four elements. First, the nature of local
habitats will be reconstructed across this three-stage Terminal Pleistocene/Early Holocene transition. This is
necessary since rapid climate change at the end of the Pleistocene created novel plant and animal co-associations
Constructing a Regional Historical Context for Terminal
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North-Central Mojave Desert, Step 1
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that lack modern analogs. This habitat reconstruction will concentrate on identifying the range of available food
resources and their relative abundance at various points in time. Ancient plant communities will be reconstructed
based on pollen identification and analysis from alluvial sections, cores, and possibly packrat middens. Changes in
the type and abundance of animal resources (large and small fauna as well as extinct megafauna) will be derived
from a synthetic, temporal analysis of a large body of existing paloenotological data in the region.
Next, new analysis of existing Terminal Pleistocene/Early Holocene archaeological site collections within
the north-central Mojave Desert will be conducted using modern methods and techniques. First, we will focus on
dating assemblages. This analysis will capitalize on our recent success in distinguishing discrete artifact scatters
dating to different temporal segments within the Terminal Pleistocene/Early Holocene using new obsidian
hydration methods (e.g., Byrd 2006, 2007, 2010; Byrd et al. 2010; Rosenthal 2010). Previously, most obsidian
artifacts from Early sites were considered unsuitable for obsidian hydration dating owing to extensive surface
weathering; new techniques that obtain readings from small cracks created during initial manufacture have
overcome this obstacle. Fortunately, the extensive Terminal Pleistocene/Early Holocene archaeological record in
the north-central Mojave region (especially at NAWS China Lake and Fort Irwin NTC) has an abundance of
obsidian artifacts from the nearby, well-studied Coso Volcanic field. By combining obsidian hydration results
from flakes and formed artifacts, with diagnostic projectile points and their hydration readings, sites can be
classified by age and in relationship to our three-stage paleoenvironmental reconstruction.
Subsequently, sites within each temporal segment will be analyzed from a functional and technological
standpoint. This will include consideration of site and assemblage size, raw material reliance, and variation
between tool types (focusing on variation in the relative emphasis on chert, obsidian, and other coarser-grained
volcanic rocks), flaked stone reduction strategies (especially biface and core reduction), and the range and relative
emphasis on particular tool types (such as different types of scrapers and crescents). These insights into
manufacturing traditions and tool kits will form a basis for inferring site function, resource emphasis, and
potential historical relationships to other cultural complexes in California and the intermountain west (e.g., Beck
and Jones 2010; Graf and Schmidt 2007; Fitzgerald et al. 2005; Madsen 2004).
Step 2 will conclude with the construction of a GIS-linked data base that presents regional patterns in site
distribution at different points in time. New archaeological and paleoenvironmental data will be integrated into a
GIS-derived diachronic model of early human settlement. This model will highlight diachronic trends in regional
site distribution patterns. The overall results will fill data gaps, provide a basis for systematizing data collection,
identify areas where buried archaeological sites of specific ages may be located, and result in a new and appropriate
historic context for evaluating Terminal Pleistocene/Early Holocene sites in the north-central Mojave region.
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APPENDIX A
GEOLOGICAL SAMPLE LOCALITY STRATIGRAPHIC DESCRIPTIONS
Appendix A: Indian Wells Canyon, Right (East) Bank
Depth (cm)
Horizon
Description
Brown (10YR 5/3; dry) loamy sand, massive to single grain structure, stratified, 10 to 25%
gravels, soft consistency, and clear smooth lower contact.
Grayish brown (10YR 5/2, dry) loamy sand, massive to weak fine subangular blocky structure,
10 to 25% gravels, soft to slightly hard consistency, contains flaked stone debitage, and
gradual smooth lower contact.
0-80
AC
80-120
2Ab
120-220
2Cu
Light gray (10YR 7/2, dry) sand, massive to single grain structure, 10 to 25% gravels and few
angular cobbles, loose to soft consistency, poorly sorted, well bedded, and abrupt smooth
lower contact.
220-240
3Ab
Dark gray (10YR 4/1, dry) loamy sand, massive to weak fine subangular blocky structure, 10 to
25% gravels, slightly hard consistency, and clear smooth lower contact.
240-320
3Cox
Brown (7.5YR 4/3, dry) sand, 10 to 25% gravels, massive to single grain structure, soft
consistency, prominent oxidization throughout, and abrupt smooth lower contact.
320-350
4Ab
350-370
5Cox
370-375
6Ob
375-425
6Cox
425-435
7Cu1
435-445
7Cu2
Brown (7.5YR 5/3, dry) very fine sand, massive to single grain structure, soft consistency, well
sorted, continuous oxidization throughout horizon, abrupt smooth lower contact.
445-446
8Ob
Dark grayish brown (10YR 4/2, dry) sandy clay loam, massive to weak fine granular structure,
>10% small gravels, soft consistency, and abrupt smooth lower contact.
>446
9Cox
Strong brown (7.5YR 5/6, dry) sand, massive to single grain structure, 10 to 25% gravels, loose
to soft consistency, continuous oxidation throughout horizon.
Dark grayish brown (10YR 4/2, dry) loamy sand, massive structure, 10 to 25% gravels, soft to
slightly hard consistency, and abrupt smooth lower contact.
Light olive brown (2.5YR 5/4, dry) fine sand, massive to single grain structure, soft consistency,
well sorted, discontinuous oxidization patches near upper and lower contacts, and abrupt
smooth lower contact.
Dark gray (10YR 4/1, dry) sandy loam, weak medium platy structure, >10% gravels, soft
consistency, and clear smooth lower contact.
Strong brown (7.5YR 5/6, dry) sand, massive to single grain structure, 50 to 75% gravels, loose
consistency, poorly sorted and bedded, nearly continuous oxidation throughout horizon, abrupt
smooth lower contact.
Brown (7.5YR 5/3, dry) very fine sand, massive to single grain structure, soft consistency, well
sorted, clear smooth lower contact.
Appendix A: Little Dixie Wash, Locus 1, Left (West) Bank
Depth (cm)
Horizon
Description
Yellowish brown (10YR 6/4; dry) loamy sand, weak fine to very fine granular structure, >10%
small to medium subangular and subrounded gravels, soft consistency, and gradual lower
contact.
0-40
A
40-170
Cu
Light yellowish brown (2.5Y 6/3; dry) fine to medium sand, single grain structure, >10% small
gravels, loose consistency, well sorted, and abrupt smooth lower contact.
170-200
2Ab
Gray (10YR 6/1, dry) sandy loam, strong to moderate fine to medium granular to subangular
blocky structure, hard consistency, few snail shells, common small abandoned root holes,
clear smooth lower contact.
200-250
2Cu
Light brownish gray (2.5Y 6/2; dry) sandy clay loam, weak medium to coarse subangular
blocky structure, hard consistency, few powdery CaCo3 filaments on ped faces, and abrupt
smooth lower contact.
250-280
3Ab
Gray (2.5Y 5/1, dry) silty clay, strong fine to medium angular blocky structure, very hard
consistency, few oxidization mottles, few CaCo3 nodules, few small root holes, clear smooth
lower contact.
280-305
3Cox
0-170
A/Cu
170-195
2Bwb
195-210
3Ab
210-260
3Cu
260-265
4Ab
265-295
4Cu
Light brownish gray (2.5Y 6/2; dry) silty loam, weak coarse subangular blocky structure, slightly
hard consistency, common mica flecks, and abrupt smooth lower contact.
295-300
5Ab
Grayish brown (10YR 5/2, dry) silty clay, strong fine to medium subangular blocky structure,
hard consistency, few oxidization mottles, abrupt smooth lower contact.
300-310
5Cox
Light brownish gray (2.5Y 6/2; dry) silt loam, moderate medium to coarse subangular blocky
structure, common oxidization mottles, abrupt and smooth lower contact.
310-330
6Ab
Gray (2.5Y 5/1, dry) silty clay, strong fine to medium subangular blocky structure, hard to very
hard consistency, few small oxidization mottles in root holes, clear smooth lower contact.
330-340
6Cu
Light brownish gray (2.5Y 6/2; dry) silty clay, moderate coarse subangular blocky structure,
hard consistency, few small oxidization mottles in root holes, and abrupt smooth lower contact.
340-370
7Ab
Grayish brown (10YR 5/2, dry) silty clay, strong medium to coarse angular blocky to prismatic
structure, hard to very hard consistency, and few small oxidization mottles in root holes.
Light yellowish brown (2.5Y 6/4; dry) sandy loam, massive structure, slightly hard to hard
consistency, common abandoned root holes and oxidization mottles, and clear smooth lower
contact.
Light yellowish brown (2.5Y 6/3; dry) sand, single grain structure, 10 to 25% small to large
gravels, loose to soft consistency, and abrupt wavy lower contact.
Light gray (10YR 7/2, dry) silty clay loam, moderate fine to medium subangular blocky
structure, hard consistency, some CaCo3 coatings on ped faces and root holes, abrupt smooth
lower contact.
Light grayish brown (10YR 6/2, dry) silty clay, strong fine to medium subangular blocky
structure, hard consistency, contains small snail shells, clear smooth lower contact.
Light yellowish brown (2.5Y 6/3; dry) loamy sand, massive structure, slightly hard consistency,
and abrupt smooth lower contact.
Grayish brown (2.5Y 5/2, dry) silty clay, strong fine to medium subangular blocky structure,
hard consistency, contains small snail shells, clear smooth lower contact.
Appendix A: Dixie Wash, Fan Locus 5, Left (West) Bank
Depth (cm)
Stratum
Horizon
Description
0-193
VI
Cu
193-220
V
2Ab
220-245
IV
3Ab
245-275
IV
3Cu
275-295
III
4Ab
Light brownish gray (2.5Y 6/2; dry) silty clay loam, moderate medium subangular blocky
structure, hard consistency, common iron oxide mottles in upper 5-10 cm, and a clear smooth
lower contact.
295-350
III
4Cu
Light brownish gray (2.5Y 6/2; dry) coarse sand to sandy loam, massive to single grain structure,
10-25% small to medium angular to subrounded gravels, slightly hard consistency, 20 cm layer
of fine sand at abrupt smooth lower contact.
350-364
II
5Ab
Light brownish gray (2.5Y 6/2; dry) sandy clay loam, weak fine subangular blocky structure, hard
to very hard consistency, few root holes, and a clear smooth lower contact.
364-380
II
5Cox
Light brownish gray (2.5Y 6/2; dry) loamy sand, massive structure, >10% small gravels, soft
consistency, and an abrupt smooth lower contact.
380-398
I
6Ab
Light yellowish brown (2.5Y 6/3; dry) sandy loam, weak to moderate fine granular structure,
slightly hard consistency, common iron oxide mottles, and a clear smooth lower contact.
298->420
I
6Cu
Light yellowish brown (2.5Y 6/3; dry) coarse sand, single grain structure, >10% small angular to
subrounded gravels, loose consistency, poorly sorted, and an abrupt smooth lower contact.
Pale brown (10YR 6/4; dry) sand, massive to single grain structure, 10-25% small to medium
subangular to rounded gravels, loose to soft consistency, and an abrupt smooth lower contact.
Brown (10YR 5/3, dry) sandy clay loam, moderate fine to medium subangular blocky structure,
soft to slightly hard consistency, and an abrupt smooth lower contact.
Brown (10YR 5/3, dry) sandy clay loam, moderate medium subangular blocky structure, hard
consistency, and an abrupt smooth lower contact.
Brown (10YR 5/3, dry) sandy loam, massive structure, <10% small rounded gravels, hard
consistency, and an abrupt smooth lower contact. Chert scraper found in situ near base of this
horizon.
Appendix A: Dove Springs Wash, Left (Northeast) Bank, Whistler Local 5771
Depth
(see figure)
Horizon
A
Description
Brown (10YR 5/3; dry) loamy sand, massive structure, 10 to 25% small to large subrounded to rounded gravels,
soft consistency, and clear smooth lower contact.
Cu
Pale brown (10YR 6/2, dry) sand, single grain structure, 10 to 25% small to large subrounded to rounded poorly
sorted upward fining gravels, loose consistency, and abrupt wavy lower contact.
2Ab
Brown (10YR 5/3; dry) loamy sand, weak medium subangular blocky structure, soft consistency, and clear smooth
lower contact.
2Cu
Pale brown (10YR 6/2, dry) very fine sand, massive structure, soft consistency, and abrupt wavy lower contact.
3Ab
3Cu
4Ab
4Cu
5Ab
5Cu
Grayish brown (10YR 5/2; dry) loamy sand, weak fine subangular blocky structure, soft consistency, and abrupt
smooth lower contact.
Pale brown (10YR 6/2, dry) medium to coarse sand, massive to single grain structure, moderately sorted, loose
consistency, and abrupt smooth lower contact.
Grayish brown (10YR 5/2; dry) loamy sand, weak medium subangular blocky structure, soft consistency, and clear
smooth lower contact.
Pale brown (10YR 6/2, dry) very fine sand, massive structure, well sorted, soft consistency, and abrupt smooth
lower contact.
Dark grayish brown (10YR 4/2; dry) sandy clay loam, moderate fine to medium subangular blocky structure, soft
consistency, and clear smooth lower contact.
Very pale brown (10YR 7/3, dry) medium to coarse sand, single grain structure, poorly sorted, loose consistency,
and clear smooth lower contact.
6Ab
Light brownish gray (10YR 6/2; dry) loamy sand, >10% small subrounded to rounded gravels, weak medium
subangular blocky structure, slightly hard consistency, and clear smooth lower contact.
6Cox
Very pale brown (10YR 7/3, dry) medium to coarse sand, massive to single grain structure, poorly sorted, soft to
slightly hard consistency, and abrupt smooth lower contact.
7Ab
7Cu
8Ab
8Cu
9Ab
9Cu
Brown (10YR 5/3; dry) sandy loam, weak medium subangular blocky structure, soft consistency, and clear smooth
lower contact.
Pale yellow (2.5Y 7/3, dry) fine to coarse sand, massive to single grain structure, well sorted and bedded, soft
consistency, and abrupt smooth lower contact.
Grayish brown (10YR 5/2; dry) loamy sand, weak fine subangular blocky structure, soft consistency, and abrupt
smooth lower contact.
Light brownish gray (10YR 6/2, dry) loamy very fine sand, massive structure, well sorted, soft to slightly hard
consistency, and clear smooth lower contact.
Grayish brown (10YR 5/2; dry) loamy sand, weak fine subangular blocky structure, soft consistency, and clear
smooth lower contact.
Very pale brown (10YR 7/3, dry) medium to coarse sand, massive to single grain structure, poorly sorted, loose
consistency, and abrupt smooth lower contact.
10Ab
Dark gray (10YR 4/1; dry) silty clay, strong medium to coarse subangular blocky structure, hard consistency,
common oxidized mottles in small to medium root holes, and clear smooth lower contact.
10Cox
Light yellowish brown (2.5Y 6/3, dry) silty clay, weak medium subangular blocky structure, hard consistency,
common oxidized mottles in small to medium root holes, and clear smooth lower contact.
11Ab
Grayish brown (10YR 5/2; dry) silty clay, strong medium to coarse subangular blocky structure, slightly hard to
hard consistency, few oxidized mottles in root holes, and clear smooth lower contact.
11Cox
Light brownish gray (2.5Y 6/2, moist) fine sand, <10% small subrounded to rounded gravels, massive to single
grain structure, soft to slightly hard consistency, few oxidized mottles in root holes, and abrupt smooth lower
contact.
12Ab
Very dark grayish brown (10YR 3/2; moist) sandy loam, >10% small subrounded to rounded gravels, moderate
fine subangular blocky structure, soft to slightly hard consistency, few oxidized mottles, common small root holes,
and clear smooth lower contact.
12Cu
Pale red (2/5YR 7/3, dry) medium to coarse sand, >10% small subrounded to rounded gravels, massive to single
grain structure, slightly hard consistency, and clear smooth lower contact.
13Ab
Very dark gray (10YR 3/1; dry) sandy loam, 10% small gravels, weak granular structure, and hard consistency.
Appendix A: Core 9—Charley Range, West of Flight Line Road
Depth (cm)
Horizon
0-46
A
46-91
Cu
91-152
2Akb
152-213
213-268
2Cu?
268-287
3Ab
287-305
3Cu
305-381
4Akb
381-396
5Akb
396-457
6Cg
457-756
7Cu
756-762
8C
762-914
9Cu
914-930
10Cg1
930-994
10Cg2
994-1061
11Cg
1061-1067
12Cg
Description
Very pale brown (10YR 7/3, dry) silt, weak fine to medium subangular blocky structure, slightly hard
consistency, very few fine root hole, strongly effervescent with HCL (~5% CaCO3), and a clear smooth
lower contact.
Very pale brown (10YR 7/3, dry) loamy sand, massive to single grain structure, loose consistency,
strongly effervescent with HCL (~5% CaCO3), and an abrupt smooth lower contact.
Light yellowish brown (2.5Y 6/3, dry) silt, weak fine subangular blocky structure, slightly hard consistency,
common soft CaCO3 masses, and violently effervescent with HCL (>10% CaCO3).
no recovery
Pale yellow (2.5Y 7/3, dry) sand, massive to single grain structure, loose consistency, strongly
effervescent with HCL (~5% CaCO3), and an abrupt lower contact.
Light olive brown (2.5Y 5/3, dry) silt, weak fine subangular blocky structure, soft consistency, few fine root
holes, noneffervescent with HCL, and an abrupt lower contact
Pale yellow (2.5Y 7/3, dry) medium to coarse sand, single grain structure, loose consistency, and a clear
lower contact.
Light olive grey (5Y 6/2, dry) silty clay, moderate fine subangular blocky structure, slightly hard
consistency, few fine root holes, few hard CaCO3 nodules near upper contact, strongly effervescent with
HCL (~5% CaCO3), and an abrupt lower contact
White (5Y 8/1, dry) sandy clay loam, moderate fine subangular blocky structure, hard consistency,
violently effervescent with HCL (>10% CaCO3), and an abrupt lower contact
Pale olive (5Y 6/3, dry) silty clay, moderate fine subangular blocky structure, hard consistency,
noneffervescent with HCL, few small hard CaCO3 nodules in upper 5cm, and an abrupt lower contact.
Light gray (2.5Y 7/2, dry) sand, single grain structure, <10% small to medium subrounded to water worn
gravels, loose consistency, moderately sorted and bedded with few thin layers of black sand, and an
abrupt lower contact.
Light gray (2.5Y 7/1, dry) sandy loam, massive structure, hard consistency, noneffervescent with HCL,
weakly cemented with gypsum, and a clear lower contact.
Various color fine to coarse sand, single grain structure, <10% small to medium subangular to rounded
gravels, loose consistency, noneffervescent with HCL, moderately sorted and bedded with few thin black
sand layers, and an abrupt smooth lower contact.
Olive gray (5Y 5/2, dry) sandy loam, massive structure, slightly hard consistency, noneffervescent with
HCL, and an abrupt lower contact.
Gray (5Y 5/1, dry) very fine sand, single grain structure, loose consistency, noneffervescent with HCL,
coarse sand in lower 5cm, and an abrupt lower contact.
Olive gray (5Y 5/2, dry) very fine sand, single grain structure, loose consistency, noneffervescent with
HCL, coarse sand in lower 5cm, and an abrupt lower contact.
Greenish gray (5GY 6/1, dry) sandy clay loam, massive structure, slightly hard consistency,
noneffervescent with HCL, and an abrupt lower contact.
Appendix A: Descriptions of Cores 3, 4, 5, 6, 7, and 8
CORE
Core 3
Depth (cm)
0-91
91-229
Core 4
Depth (cm)
0-152
152-168
168-229
>229
Core 5
Depth (cm)
0-61
>61
61-152
152-610
610-914
914-1280
Core 6
Depth (cm)
0-122
122 to 244
244 to 518
518-914
914-975
975-1036
1036-1097
1097-1158
1158-1219
Core 7
Depth (cm)
0-122
122-183
183-381
381-457
457-610
Core 8
Depth (cm)
0-457
457-610
610-792
792-914
914-1067
1067-1219
1219-1280
1280-1372
DESCRIPTION
Baker Range, Former Owens River Channel?
Horizon Description
A
Brown sandy loam
Brown gravely sand containing few small cobbles. Coring rig met
Cu
refusal @ 229 cm below surface due to rock
Horizon
A/C
2Ab
2Cu
3R
Baker Range, former channel area
Description
Silty sand
Silty clay loam
Sand with small gravel
Refusal due to rock and cobbles?
Baker Range, swale on mid-fan setting, hollow stem auger
Horizon Description
A
Tan silty sand
Cu
coarse gravel and subrounded to rounded cobbles
skipped
2Cu
alternating layers of sand, gravel, and loess
alternating layers of sand, gravel, and loess with coarse oxidized
2Cu
gravel at base
2Cu
coarse and fine sand
Horizon
A/C
Cu
Cu
Horizon
A/C
2Ab
2Cu
3Ab
4R
Baker Range, mid-fan setting, hollow stem auger
Description
Sand with few large gravels and small cobbles at 122cmbs
fining upwards sand
coarse angular granitic sand
loose sand and gravel, no recovery.
fining downwards sand
skipped
fine well-sorted sand
skipped
fine well-sorted sand
Baker Range, dune setting
Description
loose sand
buried dune soil
loose fine sand
buried dune soil
Basalt scoria and angular gravel
Charlie Range, playa setting, hollow stem auger
Horizon Description
Alternating playa and dunes deposits. Basalt scoria cobble in sand at
Multiple
4.5 m
Multiple Alternating layers of playa and dune deposits
Single coarse alluvial sand and gravel
Cg
Gleyed fine grained lake or playa deposit.
C
Beach sand and gravel
C/Cg
Beach sand and gravel with lacustrine deposit at base
Beach sand overlying desiccated lake
Sand overlying lacustrine deposit at base of core
APPENDIX B
RADIOCARBON LABORATORY DATING RESULTS AND METHODS
June 24, 2009
Dr. William Hildebrandt/D. Craig Young
Far Western Anthropological Research
Group, Incorporated
PO Box 758
Virginia City, NV 89440
RE: Radiocarbon Dating Results For Samples FW718-13, FW718-14, FW718-15, FW718-16, FW718-17,
FW718-18, FW718-19
Dear Dr. Hildebrandt and Dr. Young:
Enclosed are the radiocarbon dating results for seven samples recently sent to us. They each
provided plenty of carbon for accurate measurements and all the analyses proceeded normally. As usual,
the method of analysis is listed on the report with the results and calibration data is provided where
applicable.
As always, no students or intern researchers who would necessarily be distracted with other
obligations and priorities were used in the analyses. We analyzed them with the combined attention of
our entire professional staff.
If you have specific questions about the analyses, please contact us. We are always available to
answer your questions.
The cost of the analysis was charged to the MASTERCARD card provided. As always, if you
have any questions or would like to discuss the results, don’t hesitate to contact me.
Sincerely,
Digital signature on file
Dr. William Hildebrandt/D. Craig Young
Report Date: 6/24/2009
Far Western Anthropological Research Group,
Incorporated
Sample Data
Measured
Radiocarbon Age
Material Received: 5/29/2009
13C/12C
Ratio
Conventional
Radiocarbon Age(*)
Beta - 260150
7300 +/- 40 BP
-23.7 o/oo
SAMPLE : FW718-13
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic material): acid washes
2 SIGMA CALIBRATION :
Cal BC 6240 to 6070 (Cal BP 8190 to 8020)
____________________________________________________________________________________
7320 +/- 40 BP
Beta - 260151
9140 +/- 50 BP
-22.8 o/oo
SAMPLE : FW718-14
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic material): acid washes
2 SIGMA CALIBRATION :
Cal BC 8550 to 8280 (Cal BP 10500 to 10240)
____________________________________________________________________________________
9180 +/- 50 BP
Beta - 260152
4410 +/- 40 BP
-23.0 o/oo
4440 +/- 40 BP
SAMPLE : FW718-15
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic material): acid washes
2 SIGMA CALIBRATION :
Cal BC 3340 to 3210 (Cal BP 5290 to 5160) AND Cal BC 3190 to 2920 (Cal BP 5140 to 4880)
____________________________________________________________________________________
Beta - 260153
9400 +/- 50 BP
-24.5 o/oo
SAMPLE : FW718-16
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic material): acid washes
2 SIGMA CALIBRATION :
Cal BC 8800 to 8560 (Cal BP 10740 to 10520)
____________________________________________________________________________________
9410 +/- 50 BP
Beta - 260154
8090 +/- 50 BP
-23.1 o/oo
8120 +/- 50 BP
SAMPLE : FW718-17
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic material): acid washes
2 SIGMA CALIBRATION :
Cal BC 7250 to 7230 (Cal BP 9200 to 9180) AND Cal BC 7190 to 7040 (Cal BP 9140 to 8990)
____________________________________________________________________________________
Dr. William Hildebrandt/D. Craig Young
Sample Data
Measured
Radiocarbon Age
Report Date: 6/24/2009
13C/12C
Ratio
Beta - 260155
6720 +/- 50 BP
-22.2 o/oo
SAMPLE : FW718-18
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic material): acid washes
2 SIGMA CALIBRATION :
Cal BC 5730 to 5620 (Cal BP 7680 to 7570)
____________________________________________________________________________________
Conventional
Radiocarbon Age(*)
6770 +/- 50 BP
Beta - 260156
9710 +/- 50 BP
-24.1 o/oo
9720 +/- 50 BP
SAMPLE : FW718-19
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic material): acid washes
2 SIGMA CALIBRATION :
Cal BC 9280 to 9140 (Cal BP 11230 to 11090) AND Cal BC 8970 to 8940 (Cal BP 10920 to
10890)
____________________________________________________________________________________
C ALIBR AT IO N OF R AD IO CAR B ON AGE T O CA LE ND AR Y E ARS
(V ariable s: C 13/C 12= -23.7 :lab. m ult= 1)
L ab ora tor y n u m b er :
C on ven tion al rad iocar b on a ge:
2 S igm a calib rated res u lt:
(95% p r ob ab ility )
Beta-26015 0
7320± 40 BP
C al BC 6240 to 6 070 (C a l B P 8190 to 802 0)
Intercept data
Intercep t of rad iocarbon age
w ith c alibration curve:
1 S igm a ca libra ted re sult:
(68% probability)
7 460
Cal BC 6220 (C al BP 8170)
Cal BC 6230 to 61 00 (C al B P 81 80 to 8050 )
732 0±40 B P
Orga nic m aterial
7 440
7 420
7 400
Radiocarbon age (BP)
7 380
7 360
7 340
7 320
7 300
7 280
7 260
7 240
7 220
7 200
7 180
626 0
6240
6220
6 200
61 80
616 0
C al BC
614 0
6120
6100
6 080
R eference s:
Da tab ase used
INTCA L04
Calib ratio n D ata ba se
IN TCAL 04 R adio ca rbo n Age C alibr ation
IntCa l04 : Calib ratio n Iss ue o f Ra diocar bon (V olum e 4 6, nr 3, 20 04) .
Ma them atics
A Simplif ied App roa ch to Ca libra ting C14 D a tes
Ta lma , A . S ., Vo gel, J . C., 1 99 3, Ra diocar bon 35(2) , p 317 -3 22
B eta A na lytic R a dio ca rb o n D a tin g L a bo ra tor y
49 85 S.W . 7 4th Co urt, M iami, Florid a 3 315 5 • Te l: (305)6 67-5 167 • Fax: ( 305)66 3-0964 • E-M ail: beta@ radiocarbo n.c o m
6060
C ALIBR AT IO N OF R AD IO CAR B ON AGE T O CA LE ND AR Y E ARS
(V ariable s: C 13/C 12= -22.8 :lab. m ult= 1)
L ab ora tor y n u m b er :
C on ven tion al rad iocar b on a ge:
2 S igm a calib rated res u lt:
(95% p r ob ab ility )
Beta-26015 1
9180± 50 BP
C al BC 8550 to 8 280 (C a l B P 10500 to 10 240)
Intercept data
Intercep t of rad iocarbon age
w ith c alibration curve:
1 S igm a ca libra ted re sult:
(68% probability)
9 350
Cal BC 8330 (C al BP 10280)
Cal BC 8460 to 83 00 (C al B P 10 410 to 102 50)
918 0±50 B P
Orga nic m aterial
9 300
Radiocarbon age (BP)
9 250
9 200
9 150
9 100
9 050
9 000
8 950
860 0
8 550
85 00
845 0
8400
C al BC
8 350
83 00
825 0
R eference s:
Da tab ase used
INTCA L04
Calib ratio n D ata ba se
IN TCAL 04 R adio ca rbo n Age C alibr ation
IntCa l04 : Calib ratio n Iss ue o f Ra diocar bon (V olum e 4 6, nr 3, 20 04) .
Ma them atics
A Simplif ied App roa ch to Ca libra ting C14 D a tes
Ta lma , A . S ., Vo gel, J . C., 1 99 3, Ra diocar bon 35(2) , p 317 -3 22
B eta A na lytic R a dio ca rb o n D a tin g L a bo ra tor y
49 85 S.W . 7 4th Co urt, M iami, Florid a 3 315 5 • Te l: (305)6 67-5 167 • Fax: ( 305)66 3-0964 • E-M ail: beta@ radiocarbo n.c o m
8200
C ALIBR AT IO N OF R AD IO CAR B ON AGE T O CA LE ND AR Y E ARS
(V ariable s: C 13/C 12= -23:lab. m u lt= 1)
L ab ora tor y n u m b er :
C on ven tion al rad iocar b on a ge:
2 S igm a calib rated res u lts:
(95% p r ob ab ility )
Beta-26015 2
4440± 40 BP
C al BC 3340 to 3 210 (C a l B P 5290 to 516 0) an d
C al BC 3190 to 2 920 (C a l B P 5140 to 488 0)
Intercept data
Intercep t of rad iocarbon age
w ith c alibration curve:
1 S igm a ca libra ted re sults :
(68% probability)
4 580
Cal BC 3090 (C al BP 5040)
Cal BC 3270 to 32 40 (C al B P 52 20 to 5190 ) and
Cal BC 3110 to 30 20 (C al B P 50 60 to 4970 )
444 0±40 B P
Orga nic m aterial
4 560
4 540
4 520
Radiocarbon age (BP)
4 500
4 480
4 460
4 440
4 420
4 400
4 380
4 360
4 340
4 320
4 300
340 0
335 0
330 0
325 0
320 0
3150
C al BC
3100
3050
3000
2950
R eference s:
Da tab ase used
INTCA L04
Calib ratio n D ata ba se
IN TCAL 04 R adio ca rbo n Age C alibr ation
IntCa l04 : Calib ratio n Iss ue o f Ra diocar bon (V olum e 4 6, nr 3, 20 04) .
Ma them atics
A Simplif ied App roa ch to Ca libra ting C14 D a tes
Ta lma , A . S ., Vo gel, J . C., 1 99 3, Ra diocar bon 35(2) , p 317 -3 22
B eta A na lytic R a dio ca rb o n D a tin g L a bo ra tor y
49 85 S.W . 7 4th Co urt, M iami, Florid a 3 315 5 • Te l: (305)6 67-5 167 • Fax: ( 305)66 3-0964 • E-M ail: beta@ radiocarbo n.c o m
2900
C ALIBR AT IO N OF R AD IO CAR B ON AGE T O CA LE ND AR Y E ARS
(V ariable s: C 13/C 12= -24.5 :lab. m ult= 1)
L ab ora tor y n u m b er :
Beta-26015 3
C on ven tion al rad iocar b on a ge:
9410± 50 BP
2 S igm a calib rated res u lt:
(95% p r ob ab ility )
C al BC 8800 to 8 560 (C a l B P 10740 to 10 520)
Intercept data
Intercep ts of radioc arbon a ge
w ith c alibration curve:
1 S igm a ca libra ted re sult:
(68% probability)
9 600
Cal BC 8710 (C al BP 10660) a nd
Cal BC 8660 (C al BP 10610) a nd
Cal BC 8660 (C al BP 10610)
Cal BC 8750 to 86 30 (C al B P 10 700 to 105 80)
941 0±50 B P
Orga nic m aterial
9 550
Radiocarbon age (BP)
9 500
9 450
9 400
9 350
9 300
9 250
9 200
882 0
88 00
8 780
876 0
8 740
8720
870 0
8 680
C al BC
866 0
86 40
8 620
860 0
85 80
8 560
R eference s:
Da tab ase used
INTCA L04
Calib ratio n D ata ba se
IN TCAL 04 R adio ca rbo n Age C alibr ation
IntCa l04 : Calib ratio n Iss ue o f Ra diocar bon (V olum e 4 6, nr 3, 20 04) .
Ma them atics
A Simplif ied App roa ch to Ca libra ting C14 D a tes
Ta lma , A . S ., Vo gel, J . C., 1 99 3, Ra diocar bon 35(2) , p 317 -3 22
B eta A na lytic R a dio ca rb o n D a tin g L a bo ra tor y
49 85 S.W . 7 4th Co urt, M iami, Florid a 3 315 5 • Te l: (305)6 67-5 167 • Fax: ( 305)66 3-0964 • E-M ail: beta@ radiocarbo n.c o m
8540
C ALIBR AT IO N OF R AD IO CAR B ON AGE T O CA LE ND AR Y E ARS
(V ariable s: C 13/C 12= -23.1 :lab. m ult= 1)
L ab ora tor y n u m b er :
C on ven tion al rad iocar b on a ge:
2 S igm a calib rated res u lts:
(95% p r ob ab ility )
Beta-26015 4
8120± 50 BP
C al BC 7250 to 7 230 (C a l B P 9200 to 918 0) an d
C al BC 7190 to 7 040 (C a l B P 9140 to 899 0)
Intercept data
Intercep t of rad iocarbon age
w ith c alibration curve:
1 S igm a ca libra ted re sult:
(68% probability)
8 300
Cal BC 7070 (C al BP 9020)
Cal BC 7140 to 70 60 (C al B P 90 90 to 9010 )
812 0±50 B P
Orga nic m aterial
8 250
Radiocarbon age (BP)
8 200
8 150
8 100
8 050
8 000
7 950
7 900
726 0
7 240
7220
72 00
7 180
716 0
7 140
C al BC
7120
71 00
7 080
706 0
70 40
R eference s:
Da tab ase used
INTCA L04
Calib ratio n D ata ba se
IN TCAL 04 R adio ca rbo n Age C alibr ation
IntCa l04 : Calib ratio n Iss ue o f Ra diocar bon (V olum e 4 6, nr 3, 20 04) .
Ma them atics
A Simplif ied App roa ch to Ca libra ting C14 D a tes
Ta lma , A . S ., Vo gel, J . C., 1 99 3, Ra diocar bon 35(2) , p 317 -3 22
B eta A na lytic R a dio ca rb o n D a tin g L a bo ra tor y
49 85 S.W . 7 4th Co urt, M iami, Florid a 3 315 5 • Te l: (305)6 67-5 167 • Fax: ( 305)66 3-0964 • E-M ail: beta@ radiocarbo n.c o m
7020
C ALIBR AT IO N OF R AD IO CAR B ON AGE T O CA LE ND AR Y E ARS
(V ariable s: C 13/C 12= -22.2 :lab. m ult= 1)
L ab ora tor y n u m b er :
C on ven tion al rad iocar b on a ge:
2 S igm a calib rated res u lt:
(95% p r ob ab ility )
Beta-26015 5
6770± 50 BP
C al BC 5730 to 5 620 (C a l B P 7680 to 757 0)
Intercept data
Intercep t of rad iocarbon age
w ith c alibration curve:
1 S igm a ca libra ted re sult:
(68% probability)
6 950
Cal BC 5660 (C al BP 7610)
Cal BC 5720 to 56 30 (C al B P 76 70 to 7580 )
677 0±50 B P
Orga nic m aterial
6 900
Radiocarbon age (BP)
6 850
6 800
6 750
6 700
6 650
6 600
6 550
574 0
573 0
572 0
571 0
570 0
569 0
568 0
567 0
C al BC
566 0
565 0
564 0
563 0
562 0
R eference s:
Da tab ase used
INTCA L04
Calib ratio n D ata ba se
IN TCAL 04 R adio ca rbo n Age C alibr ation
IntCa l04 : Calib ratio n Iss ue o f Ra diocar bon (V olum e 4 6, nr 3, 20 04) .
Ma them atics
A Simplif ied App roa ch to Ca libra ting C14 D a tes
Ta lma , A . S ., Vo gel, J . C., 1 99 3, Ra diocar bon 35(2) , p 317 -3 22
B eta A na lytic R a dio ca rb o n D a tin g L a bo ra tor y
49 85 S.W . 7 4th Co urt, M iami, Florid a 3 315 5 • Te l: (305)6 67-5 167 • Fax: ( 305)66 3-0964 • E-M ail: beta@ radiocarbo n.c o m
5610
C ALIBR AT IO N OF R AD IO CAR B ON AGE T O CA LE ND AR Y E ARS
(V ariable s: C 13/C 12= -24.1 :lab. m ult= 1)
L ab ora tor y n u m b er :
C on ven tion al rad iocar b on a ge:
2 S igm a calib rated res u lts:
(95% p r ob ab ility )
Beta-26015 6
9720± 50 BP
C al BC 9280 to 9 140 (C a l B P 11230 to 11 090) an d
C al BC 8970 to 8 940 (C a l B P 10920 to 10 890)
Intercept data
Intercep t of rad iocarbon age
w ith c alibration curve:
1 S igm a ca libra ted re sult:
(68% probability)
9 900
Cal BC 9230 (C al BP 11180)
Cal BC 9260 to 92 00 (C al B P 11 210 to 111 50)
972 0±50 B P
Orga nic m aterial
9 850
Radiocarbon age (BP)
9 800
9 750
9 700
9 650
9 600
9 550
9 500
930 0
9250
92 00
915 0
9 100
90 50
9000
8 950
890 0
C al BC
R eference s:
Da tab ase used
INTCA L04
Calib ratio n D ata ba se
IN TCAL 04 R adio ca rbo n Age C alibr ation
IntCa l04 : Calib ratio n Iss ue o f Ra diocar bon (V olum e 4 6, nr 3, 20 04) .
Ma them atics
A Simplif ied App roa ch to Ca libra ting C14 D a tes
Ta lma , A . S ., Vo gel, J . C., 1 99 3, Ra diocar bon 35(2) , p 317 -3 22
B eta A na lytic R a dio ca rb o n D a tin g L a bo ra tor y
49 85 S.W . 7 4th Co urt, M iami, Florid a 3 315 5 • Te l: (305)6 67-5 167 • Fax: ( 305)66 3-0964 • E-M ail: beta@ radiocarbo n.c o m
8850
February 9, 2010
Dr. William Hildebrandt/Liz Honeysett
Far Western Anthropological Group
2727 Del Rio Place
Suite A
Davis, CA 95618
USA
RE: Radiocarbon Dating Results For Samples IW1-300, LDW1-175, LDW1-190-205, LDW1-260-280
Dear Dr. Hildebrandt and Ms. Honeysett:
Enclosed are the radiocarbon dating results for four samples recently sent to us. They each
provided plenty of carbon for accurate measurements and all the analyses proceeded normally. As usual,
the method of analysis is listed on the report with the results and calibration data is provided where
applicable.
As always, no students or intern researchers who would necessarily be distracted with other
obligations and priorities were used in the analyses. We analyzed them with the combined attention of
our entire professional staff.
If you have specific questions about the analyses, please contact us. We are always available to
answer your questions.
Thank you for prepaying the analyses. As always, if you have any questions or would like to
discuss the results, don’t hesitate to contact me.
Sincerely,
Digital signature on file
Page 1 of 6
Dr. William Hildebrandt/Liz Honeysett
Report Date: 2/9/2010
Far Western Anthropological Group
Sample Data
Material Received: 1/11/2010
Measured
Radiocarbon Age
13C/12C
Ratio
Conventional
Radiocarbon Age(*)
Beta - 272225
9740 +/- 50 BP
-24.5 o/oo
SAMPLE : IW1-300
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 9290 to 9170 (Cal BP 11240 to 11120)
____________________________________________________________________________________
9750 +/- 50 BP
Beta - 272226
9780 +/- 60 BP
-11.6 o/oo
SAMPLE : LDW1-175
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (shell): acid etch
2 SIGMA CALIBRATION :
Cal BC 9810 to 9300 (Cal BP 11760 to 11250)
____________________________________________________________________________________
10000 +/- 60 BP
Beta - 272227
9610 +/- 50 BP
-25.3 o/oo
SAMPLE : LDW1-190-205
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 9230 to 8800 (Cal BP 11180 to 10740)
____________________________________________________________________________________
9610 +/- 50 BP
Beta - 272228
10130 +/- 60 BP
-25.6 o/oo
SAMPLE : LDW1-260-280
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 10050 to 9450 (Cal BP 12000 to 11400)
____________________________________________________________________________________
10120 +/- 60 BP
Page 2 of 6
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-24.5 :la b. mult=1)
L aboratory num ber:
B eta-272225
Conventional radiocarbo n age:
9750±50 B P
2 Sigm a calibrated result:
(95% probab ility)
Cal B C 9290 t o 9170 (C al B P 11240 to 11120)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
C al B C 9250 (C al B P 11200)
1 Sigm a calibrated result:
(68% p robability)
9950
C al B C 9270 to 9220 (Cal BP 11 220 to 11170)
9750±50 BP
Organic s edim ent
9900
Radiocarbon age (BP)
9850
9800
9750
9700
9650
9600
9550
9300
9290
9280
9270
9260
9250
9240
9230
C al BC
9220
9210
9200
9190
9180
9170
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 3 of 6
9160
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-11.6 :la b. mult=1)
L aboratory num ber:
B eta-272226
Conventional radiocarbo n age:
10000±60 B P
2 Sigm a calibrated result:
(95% probab ility)
Cal B C 9810 t o 9300 (C al B P 11760 to 11250)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
C al B C 9450 (C al B P 11400)
1 Sigm a calibrated result:
(68% p robability)
10200
C al B C 9670 to 9360 (Cal BP 11 620 to 11320)
10000±60 BP
Shell
10150
10100
Radiocarbon age (BP)
10050
10000
9950
9900
9850
9800
9750
9850
9800
9750
9700
9650
9600
9550
C al B C
9500
9450
9400
9350
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 4 of 6
9300
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-25.3 :la b. mult=1)
L aboratory num ber:
B eta-272227
Conventional radiocarbo n age:
9610±50 B P
2 Sigm a calibrated result:
(95% probab ility)
Cal B C 9230 t o 8800 (C al B P 11180 to 10740)
Inte rcept da ta
Intercepts of radiocarbon age
with ca lib ration curve:
C al B C 9130 (C al B P 11080) and
C al B C 8980 (C al B P 10930) and
C al B C 8930 (C al B P 10880)
1 Sigm a calibrated results :
(68% p robability)
9800
C al B C 9180 to 9110 (Cal BP 11 130 to 11060) and
C al B C 9080 to 9050 (Cal BP 11 030 to 11000) and
C al B C 9020 to 8840 (Cal BP 10 970 to 10790)
9610±50 BP
Organic s edim ent
9750
Radiocarbon age (BP)
9700
9650
9600
9550
9500
9450
9400
9250
9200
9150
9100
9050
9000
8950
C al BC
8900
8850
8800
8750
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 5 of 6
8700
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-25.6 :la b. mult=1)
L aboratory num ber:
B eta-272228
Conventional radiocarbo n age:
10120±60 B P
2 Sigm a calibrated result:
(95% probab ility)
Cal B C 10050 to 9450 (C al B P 12000 to 11400)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
C al B C 9810 (C al B P 11760)
1 Sigm a calibrated results :
(68% p robability)
10350
C al B C 10010 to 9920 ( Cal BP 1 1960 to 11870) and
C al B C 9880 to 9670 (Cal BP 11 830 to 11620)
10120±60 BP
Organic s edim ent
10300
10250
Radiocarbon age (BP)
10200
10150
10100
10050
10000
9950
9900
9850
10100
10050
10000
9950
9900
9850
9800
9750
C al B C
9700
9650
9600
9550
9500
9450
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 6 of 6
9400
June 28, 2010
Dr. William Hildebrandt/ Jack Meyer
Far Western Anthropological Group
2727 Del Rio Place
Suite A
Davis, CA 95618
USA
RE: Radiocarbon Dating Results For Samples CLDW-T3-5Ab, CLIW-60b
Dear Dr. Hildebrandt/ Mr. Meyer:
Enclosed are the radiocarbon dating results for two samples recently sent to us. They each
provided plenty of carbon for accurate measurements and all the analyses proceeded normally. As usual,
the method of analysis is listed on the report with the results and calibration data is provided where
applicable.
As always, no students or intern researchers who would necessarily be distracted with other
obligations and priorities were used in the analyses. We analyzed them with the combined attention of
our entire professional staff.
If you have specific questions about the analyses, please contact us. We are always available to
answer your questions.
Our invoice was previously emailed. Please, forward it to the appropriate officer or send VISA
charge authorization. Thank you. As always, if you have any questions or would like to discuss the
results, don’t hesitate to contact me.
Sincerely,
Digital signature on file
Page 1 of 4
Dr. William Hildebrandt/Jack Meyer
Report Date: 6/28/2010
Far Western Anthropological Group
Material Received: 6/16/2010
Sample Data
Measured
Radiocarbon Age
13C/12C
Ratio
Conventional
Radiocarbon Age(*)
Beta - 280734
10520 +/- 50 BP
-25.6 o/oo
10510 +/- 50 BP
SAMPLE : CLDW-T3-5Ab
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 10740 to 10420 (Cal BP 12690 to 12370) AND Cal BC 10310 to 10300 (Cal BP 12260 to
12250)
____________________________________________________________________________________
Beta - 280735
10240 +/- 50 BP
-24.8 o/oo
SAMPLE : CLIW-60b
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 10180 to 9820 (Cal BP 12120 to 11770)
____________________________________________________________________________________
Page 2 of 4
10240 +/- 50 BP
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-25.6 :la b. mult=1)
L aboratory num ber:
Conventional radiocarbo n age:
2 Sigm a calibrated results:
(95% probab ility)
B eta-280734
10510±50 B P
Cal B C 10740 to 10420 (C al B P 12690 to 12370) a nd
Cal B C 10310 to 10300 (C al B P 12260 to 12250)
Inte rcept da ta
Intercepts of radiocarbon age
with ca lib ration curve:
1 Sigm a calibrated result:
(68% p robability)
C al B C 10650 (C al B P 12600) and
C al B C 10510 (C al B P 12460) and
C al B C 10460 (C al B P 12410)
C al B C 10700 to 10440 ( Cal B P 12650 to 12390)
10510±50 BP
Organic s edim ent
10700
10650
Radiocarbon age (BP)
10600
10550
10500
10450
10400
10350
10300
10800
10750
10700
10650
10600
10550
10500
C al B C
10450
10400
10350
10300
10250
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 3 of 4
10200
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-24.8 :la b. mult=1)
L aboratory num ber:
Conventional radiocarbo n age:
2 Sigm a calibrated result:
(95% probab ility)
B eta-280735
10240±50 B P
Cal B C 10180 to 9820 (C al B P 12120 to 11770)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
1 Sigm a calibrated results :
(68% p robability)
10400
C al B C 10050 (C al B P 12000)
C al B C 10120 to 10020 ( Cal B P 12070 to 11970) and
C al B C 9920 to 9890 (Cal BP 11 870 to 11840)
10240±50 BP
Organic s edim ent
10350
Radiocarbon age (BP)
10300
10250
10200
10150
10100
10050
10000
10200
10150
10100
10050
10000
9950
9900
9850
9800
C al B C
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 4 of 4
9750
July 8, 2010
Dr. William Hildebrandt/Jack Meyer
Far Western Anthropological Group
2727 Del Rio Place
Suite A
Davis, CA 95618
USA
RE: Radiocarbon Dating Result For Sample CLDSL-57715Ab
Dear Dr. Hildebrandt and Mr. Meyer:
Enclosed is the radiocarbon dating result for one sample recently sent to us. It provided plenty of
carbon for an accurate measurement and the analysis proceeded normally. As usual, the method of
analysis is listed on the report sheet and calibration data is provided where applicable.
As always, no students or intern researchers who would necessarily be distracted with other
obligations and priorities were used in the analysis. It was analyzed with the combined attention of our
entire professional staff.
If you have specific questions about the analyses, please contact us. We are always available to
answer your questions.
The cost of the analysis was charged to the MASTERCARD card provided. As always, if you
have any questions or would like to discuss the results, don’t hesitate to contact me.
Sincerely,
Digital signature on file
Page 1 of 3
Dr. William Hildebrandt/Jack Meyer
Report Date: 7/8/2010
Far Western Anthropological Group
Material Received: 6/23/2010
Sample Data
Measured
Radiocarbon Age
13C/12C
Ratio
Conventional
Radiocarbon Age(*)
Beta - 280993
4200 +/- 40 BP
-23.4 o/oo
4230 +/- 40 BP
SAMPLE : CLDSL-57715Ab
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 2910 to 2850 (Cal BP 4860 to 4800) AND Cal BC 2810 to 2750 (Cal BP 4760 to 4700)
Cal BC 2720 to 2700 (Cal BP 4670 to 4650)
____________________________________________________________________________________
Page 2 of 3
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-23.4 :la b. mult=1)
L aboratory num ber:
B eta-280993
Conventional radiocarbo n age:
4230±40 B P
2 Sigm a calibrated results:
(95% probab ility)
Cal B C 2910 t o 2850 (C al B P 4860 to 4800) and
Cal B C 2810 t o 2750 (C al B P 4760 to 4700) and
Cal B C 2720 t o 2700 (C al B P 4670 to 4650)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
1 Sigm a calibrated result:
(68% p robability)
4360
C al B C 2880 (C al B P 4830)
C al B C 2890 to 2870 (Cal BP 48 40 to 4820)
4230±40 BP
Organic s edim ent
4340
4320
4300
Radiocarbon age (BP)
4280
4260
4240
4220
4200
4180
4160
4140
4120
4100
4080
2920
2900
2880
2860
2840
2820
2800
C al BC
2780
2760
2740
2720
2700
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 3 of 3
2680
July 13, 2010
Dr. William Hildebrandt/Jack Meyer
Far Western Anthropological Group
2727 Del Rio Place
Suite A
Davis, CA 95618
USA
RE: Radiocarbon Dating Results For Samples CLC9-6Cg, CLC9-11Cg, CLDW-T3-3Ab, CLDW-T37Ab, CLOK-tufa, CLRV-NCTP-3Cu, CLRV-SCTP-40b, CLSB-snail
Dear Dr. Hildebrandt and Mr. Meyer:
Enclosed are the radiocarbon dating results for eight samples recently sent to us. They each
provided plenty of carbon for accurate measurements and all the analyses proceeded normally. As usual,
the method of analysis is listed on the report with the results and calibration data is provided where
applicable.
As always, no students or intern researchers who would necessarily be distracted with other
obligations and priorities were used in the analyses. We analyzed them with the combined attention of
our entire professional staff.
If you have specific questions about the analyses, please contact us. We are always available to
answer your questions.
The cost of the analysis was charged to the MASTERCARD card provided. A receipt is enclosed
with the paper report copy. Thank you. As always, if you have any questions or would like to discuss the
results, don’t hesitate to contact me.
Sincerely,
Digital signature on file
Page 1 of 11
Dr. William Hildebrandt/Jack Meyer
Report Date: 7/13/2010
Far Western Anthropological Group
Material Received: 6/14/2010
Sample Data
Measured
Radiocarbon Age
13C/12C
Ratio
Conventional
Radiocarbon Age(*)
Beta - 280679
9710 +/- 50 BP
-26.3 o/oo
9690 +/- 50 BP
SAMPLE : CLC9-6Cg
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 9260 to 9120 (Cal BP 11220 to 11070) AND Cal BC 9000 to 8920 (Cal BP 10950 to
10870)
____________________________________________________________________________________
Beta - 280680
14600 +/- 50 BP
-24.6 o/oo
SAMPLE : CLC9-11Cg
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 15960 to 15550 (Cal BP 17910 to 17500)
____________________________________________________________________________________
14610 +/- 50 BP
Beta - 280681
9930 +/- 40 BP
-25.2 o/oo
SAMPLE : CLDW-T3-3Ab
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 9450 to 9290 (Cal BP 11400 to 11240)
____________________________________________________________________________________
9930 +/- 40 BP
Beta - 280682
10460 +/- 40 BP
-25.5 o/oo
10450 +/- 40 BP
SAMPLE : CLDW-T3-7Ab
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 10670 to 10490 (Cal BP 12620 to 12440) AND Cal BC 10470 to 10270 (Cal BP 12420 to
12220) Cal BC 10270 to 10210 (Cal BP 12220 to 12160)
____________________________________________________________________________________
Page 2 of 11
Dr. William Hildebrandt/Jack Meyer
Sample Data
Report Date: 7/13/2010
Measured
Radiocarbon Age
13C/12C
Ratio
Beta - 280683
10950 +/- 50 BP
+4.6 o/oo
SAMPLE : CLOK-tufa
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (carbonate rock): acid etch
2 SIGMA CALIBRATION :
Cal BC 11420 to 11270 (Cal BP 13370 to 13220)
____________________________________________________________________________________
Conventional
Radiocarbon Age(*)
11440 +/- 50 BP
Beta - 280684
8790 +/- 40 BP
-25.0 o/oo
8790 +/- 40 BP
SAMPLE : CLRV-NCTP-3Cu
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 8170 to 8120 (Cal BP 10120 to 10070) AND Cal BC 7970 to 7720 (Cal BP 9920 to 9670)
____________________________________________________________________________________
Beta - 280685
11570 +/- 50 BP
-25.9 o/oo
SAMPLE : CLRV-SCTP-40b
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 11520 to 11350 (Cal BP 13470 to 13300)
____________________________________________________________________________________
11560 +/- 50 BP
Beta - 280686
11270 +/- 50 BP
-8.0 o/oo
SAMPLE : CLSB-snail
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (shell): acid etch
2 SIGMA CALIBRATION :
Cal BC 11510 to 11340 (Cal BP 13460 to 13290)
11550 +/- 50 BP
____________________________________________________________________________________
Page 3 of 11
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-26.3 :la b. mult=1)
L aboratory num ber:
B eta-280679
Conventional radiocarbo n age:
9690±50 B P
2 Sigm a calibrated results:
(95% probab ility)
Cal B C 9260 t o 9120 (C al B P 11220 to 11070) and
Cal B C 9000 t o 8920 (C al B P 10950 to 10870)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
1 Sigm a calibrated result:
(68% p robability)
9850
C al B C 9220 (C al B P 11170)
C al B C 9240 to 9150 (Cal BP 11 190 to 11100)
9690±50 BP
Organic s edim ent
9800
Radiocarbon age (BP)
9750
9700
9650
9600
9550
9500
9450
9300
9250
9200
9150
9100
9050
9000
8950
8900
C al BC
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 4 of 11
8850
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-24.6 :la b. mult=1)
L aboratory num ber:
Conventional radiocarbo n age:
2 Sigm a calibrated result:
(95% probab ility)
B eta-280680
14610±50 B P
Cal B C 15960 to 15550 (C al B P 17910 to 17500)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
1 Sigm a calibrated result:
(68% p robability)
14800
C al B C 15760 (C al B P 17710)
C al B C 15860 to 15650 ( Cal B P 17810 to 17600)
14610±50 BP
Organic s edim ent
14750
Radiocarbon age (BP)
14700
14650
14600
14550
14500
14450
14400
16000
15950
15900
15850
15800
15750
C al B C
15700
15650
15600
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 5 of 11
15550
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-25.2 :la b. mult=1)
L aboratory num ber:
B eta-280681
Conventional radiocarbo n age:
9930±40 B P
2 Sigm a calibrated result:
(95% probab ility)
Cal B C 9450 t o 9290 (C al B P 11400 to 11240)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
1 Sigm a calibrated result:
(68% p robability)
10060
C al B C 9350 (C al B P 11300)
C al B C 9400 to 9310 (Cal BP 11 350 to 11260)
9930±40 BP
Organic s edim ent
10040
10020
10000
Radiocarbon age (BP)
9980
9960
9940
9920
9900
9880
9860
9840
9820
9800
9780
9460
9440
9420
9400
9380
9360
9340
9320
9300
C al B C
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 6 of 11
9280
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-25.5 :la b. mult=1)
L aboratory num ber:
Conventional radiocarbo n age:
2 Sigm a calibrated results:
(95% probab ility)
B eta-280682
10450±40 B P
Cal B C 10670 to 10490 (C al B P 12620 to 12440) a nd
Cal B C 10470 to 10270 (C al B P 12420 to 12220) a nd
Cal B C 10270 to 10210 (C al B P 12220 to 12160)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
1 Sigm a calibrated results :
(68% p robability)
C al B C 10440 (C al B P 12390)
C al B C 10630 to 10520 ( Cal B P 12580 to 12480) and
C al B C 10450 to 10420 ( Cal B P 12400 to 12370) and
C al B C 10310 to 10300 ( Cal B P 12260 to 12250)
10450±40 BP
Organic s edim ent
10580
10560
10540
10520
Radiocarbon age (BP)
10500
10480
10460
10440
10420
10400
10380
10360
10340
10320
10300
10700
10650
10600
10550
10500
10450
10400
C al B C
10350
10300
10250
10200
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 7 of 11
10150
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=4.6:lab. m ult=1)
L aboratory num ber:
Conventional radiocarbo n age:
2 Sigm a calibrated result:
(95% probab ility)
B eta-280683
11440±50 B P
Cal B C 11420 to 11270 (C al B P 13370 to 13220)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
1 Sigm a calibrated result:
(68% p robability)
11600
C al B C 11340 (C al B P 13290)
C al B C 11370 to 11300 ( Cal B P 13320 to 13260)
11440±50 BP
C arbonate roc k
11550
Radiocarbon age (BP)
11500
11450
11400
11350
11300
11250
11200
11440
11420
11400
11380
11360
11340
C al B C
11320
11300
11280
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 8 of 11
11260
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-25:la b. mult=1)
L aboratory num ber:
B eta-280684
Conventional radiocarbo n age:
8790±40 B P
2 Sigm a calibrated results:
(95% probab ility)
Cal B C 8170 t o 8120 (C al B P 10120 to 10070) and
Cal B C 7970 t o 7720 (C al B P 9920 to 9670)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
C al B C 7820 (C al B P 9780)
1 Sigm a calibrated result:
(68% p robability)
8920
C al B C 7950 to 7750 (Cal BP 99 00 to 9700)
8790±40 BP
Organic s edim ent
8900
8880
8860
Radiocarbon age (BP)
8840
8820
8800
8780
8760
8740
8720
8700
8680
8660
8640
8200
8150
8100
8050
8000
7950
7900
C al BC
7850
7800
7750
7700
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 9 of 11
7650
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-25.9 :la b. mult=1)
L aboratory num ber:
Conventional radiocarbo n age:
2 Sigm a calibrated result:
(95% probab ility)
B eta-280685
11560±50 B P
Cal B C 11520 to 11350 (C al B P 13470 to 13300)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
1 Sigm a calibrated result:
(68% p robability)
11750
C al B C 11440 (C al B P 13390)
C al B C 11480 to 11390 ( Cal B P 13430 to 13340)
11560±50 BP
Organic s edim ent
11700
Radiocarbon age (BP)
11650
11600
11550
11500
11450
11400
11350
11540
11520
11500
11480
11460
11440
C al B C
11420
11400
11380
11360
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 10 of 11
11340
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-8:lab . mult=1)
L aboratory num ber:
Conventional radiocarbo n age:
2 Sigm a calibrated result:
(95% probab ility)
B eta-280686
11550±50 B P
Cal B C 11510 to 11340 (C al B P 13460 to 13290)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
1 Sigm a calibrated result:
(68% p robability)
11750
C al B C 11430 (C al B P 13380)
C al B C 11470 to 11380 ( Cal B P 13420 to 13330)
11550±50 BP
Shell
11700
Radiocarbon age (BP)
11650
11600
11550
11500
11450
11400
11350
11520
11500
11480
11460
11440
11420
C al B C
11400
11380
11360
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 11 of 11
11340
July 15, 2010
Dr. William Hildebrandt/Jack Meyer
Far Western Anthropological Group
2727 Del Rio Place
Suite A
Davis, CA 95618
USA
RE: Radiocarbon Dating Results For Samples CLDW-L5-3Ab, CLDW-L5-4Ab
Dear Dr. Hildebrandt and Mr. Meyer:
Enclosed are the radiocarbon dating results for two samples recently sent to us. They each
provided plenty of carbon for accurate measurements and all the analyses proceeded normally. As usual,
the method of analysis is listed on the report with the results and calibration data is provided where
applicable.
As always, no students or intern researchers who would necessarily be distracted with other
obligations and priorities were used in the analyses. We analyzed them with the combined attention of
our entire professional staff.
If you have specific questions about the analyses, please contact us. We are always available to
answer your questions.
The cost of the analysis was charged to the MASTERCARD card provided. As always, if you
have any questions or would like to discuss the results, don’t hesitate to contact me.
Sincerely,
Digital signature on file
Page 1 of 4
Dr. William Hildebrandt/Jack Meyer
Report Date: 7/15/2010
Far Western Anthropological Group
Material Received: 6/28/2010
Sample Data
Measured
Radiocarbon Age
13C/12C
Ratio
Beta - 281207
6960 +/- 40 BP
-23.2 o/oo
SAMPLE : CLDW-L5-3Ab
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 5980 to 5760 (Cal BP 7930 to 7710)
____________________________________________________________________________________
Conventional
Radiocarbon Age(*)
6990 +/- 40 BP
Beta - 281208
6310 +/- 40 BP
-23.2 o/oo
6340 +/- 40 BP
SAMPLE : CLDW-L5-4Ab
ANALYSIS : AMS-Standard delivery
MATERIAL/PRETREATMENT : (organic sediment): acid washes
2 SIGMA CALIBRATION :
Cal BC 5450 to 5450 (Cal BP 7400 to 7400) AND Cal BC 5380 to 5220 (Cal BP 7330 to 7170)
____________________________________________________________________________________
Page 2 of 4
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-23.2 :la b. mult=1)
L aboratory num ber:
B eta-281207
Conventional radiocarbo n age:
6990±40 B P
2 Sigm a calibrated result:
(95% probab ility)
Cal B C 5980 t o 5760 (C al B P 7930 to 7710)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
1 Sigm a calibrated results :
(68% p robability)
7120
C al B C 5880 (C al B P 7830)
C al B C 5970 to 5950 (Cal BP 79 20 to 7900) a nd
C al B C 5910 to 5840 (Cal BP 78 60 to 7790)
6990±40 BP
Organic s edim ent
7100
7080
7060
Radiocarbon age (BP)
7040
7020
7000
6980
6960
6940
6920
6900
6880
6860
6840
6000
5980
5960
5940
5920
5900
5880
5860
C al BC
5840
5820
5800
5780
5760
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 3 of 4
5740
C A L IB R A T IO N O F R A D IO C A R B O N AG E T O C A L E N D A R Y E AR S
(V ariables : C 13/C 12=-23.2 :la b. mult=1)
L aboratory num ber:
B eta-281208
Conventional radiocarbo n age:
6340±40 B P
2 Sigm a calibrated results:
(95% probab ility)
Cal B C 5450 t o 5450 (C al B P 7400 to 7400) and
Cal B C 5380 t o 5220 (C al B P 7330 to 7170)
Inte rcept da ta
Intercept of radiocarbon age
with ca lib ration curve:
1 Sigm a calibrated result:
(68% p robability)
6480
C al B C 5320 (C al B P 7260)
C al B C 5350 to 5300 (Cal BP 73 00 to 7250)
6340±40 BP
Organic s edim ent
6460
6440
6420
Radiocarbon age (BP)
6400
6380
6360
6340
6320
6300
6280
6260
6240
6220
6200
5460
5440
5420
5400
5380
5360
5340
5320
C al BC
5300
5280
5260
5240
5220
Re ferences :
Da tabase u sed
IN T C AL 04
C ali bra tion D ataba se
IN T C A L04 R adi ocarbon A ge C al ibrati on
IntC a l04: C al ibrati on Issue of Ra dioca rbon (V olum e 46 , nr 3 , 2004).
M ath em ati cs
A S im plifi ed A pp roac h t o C ali bratin g C 14 Dat es
T alm a, A. S ., Voge l, J. C . , 1993, Ra dioca rbon 35(2), p317-322
B e ta A n a lytic R a d io c a rb o n D atin g L a b o r ato r y
49 85 S.W . 7 4th Co ur t, M ia mi, Flo rid a 33 15 5 • Tel: (30 5)66 7-516 7 • F a x: (3 05)66 3-09 64 • E-M ail : beta @ rad iocar bon .co m
Page 4 of 4
5200
6/20/08
General Statement of 14C Procedures
at the National Ocean Sciences AMS Facility
All laboratory preparations for AMS radiocarbon analyses of submitted samples occur in the
NOSAMS Sample Preparation Lab unless otherwise noted on the attached report of Final Results.
Procedures appropriate to the raw material being analyzed include: acid hydrolysis (HY), oxidation
(OC or DOC), or stripping of CO2 gas from water (WS) samples. Carbon dioxide, whether
submitted directly (GS) or generated at the NOSAMS Facility, is reacted with Fe catalyst to form
graphite. Graphite is pressed into targets, which are analyzed by accelerator mass spectrometry
along with primary and secondary standards and process blanks. The primary standard NBS Oxalic
Acid I (NIST-SRM-4990) is used for all
14C
measurements. Every group of samples processed
includes an appropriate blank, which is analyzed concurrently with the group.
Process blank
materials include IAEA C-1 Carrara marble and TIRI F Icelandic Doublespar for inorganic carbon
and gas samples; FIRI A and B wood as well as FISONS acetanilide for organic carbon samples; a
14
C- free groundwater for DIC (dissolved inorganic carbon) samples; and Alfa Aeasar graphite
powder for AMS machine background.
Fraction Modern (Fm) is a measurement of the deviation of the 14C/C ratio of a sample from
"modern." Modern is defined as 95% of the radiocarbon concentration (in AD 1950) of NBS Oxalic
Acid I normalized to δ13CVPDB = -19 per mil (Olsson, 1970). AMS results are calculated using the
internationally accepted modern value of 1.176 ±0.010 x 10-12(Karlen, et. al.,1964) and a final 13Ccorrection is made to normalize the sample Fm to a δ13CVPDB value of -25 per mil. NOSAMS has
two accelerators for radiocarbon measurement, either a 3 Megavolt Tandetron system or a 500
kilovolt compact AMS system.
Stable isotope measurements of sample δ13C are used to correct Fm values measured on the
Tandetron system. These are typically made at the NOSAMS Facility with either a VG PRISM or
VG OPTIMA mass spectrometer by analyzing a split of the CO2 gas generated prior to graphite
production.
Some carbonate samples are reacted and measured directly with the VG PRISM
ISOCARB. These δ13C values and source used to calculate the Fm of a sample are specified in the
report of Final Results.
AMS analyses made on the 500 kilovolt AMS system are corrected using measured
ratios. Measured 12C/.13C ratios are not reported.
1
12
C/.13C
6/20/08
Reporting of ages and/or activities follows the convention outlined by Stuiver and Polach
(1977) and Stuiver (1980). Radiocarbon ages are calculated using 5568 (yrs) as the half-life of
radiocarbon and are reported without reservoir corrections or calibration to calendar years. A Δ14C
activity normalized to 1950 is also reported according to these conventions. The activity, or Δ14C, of
the sample is further corrected to account for the decay between collection (or death) and the time of
measurement if a collection date is specified on the submittal form, otherwise Δ14C is reported
assuming that collection and measurement date are the same.
Atoms of
14C
contained in a sample are directly counted using the AMS method of
radiocarbon analysis, therefore, internal statistical errors are calculated using the number of counts
measured from each target in combination with the errors of the standard. An external error is
calculated from the reproducibility of individual analyses for a given target. The error reported is the
larger of the internal or external errors.
When reporting AMS results of samples run at the NOSAMS facility, accession numbers
(e.g. OS-####'s) are required to be listed together with the results. To avoid confusion, we suggest
tabulating OS-numbers and associated radiocarbon ages as they appear on the attached Final Report
in addition to any subsequent corrections that may need to be made to the ages. We ask that
published results acknowledge support from NSF by including the NSF Cooperative Agreement
number, OCE-0753487. The NOSAMS facility would appreciate receiving reprints or preprints of
papers referencing AMS analyses made at the NOSAMS facility.
Any sample material not consumed during sample preparation or AMS radiocarbon analysis
is archived for two years at the NOSAMS Facility unless other arrangements are made by the
submitter.
REFERENCES
Karlen, I., Olsson, I.U.,Kallburg, P. and Kilici, S., 1964. Absolute determination of the activity of two
dating standards.ArkivGeofysik, 4:465-471.
14C
Olsson, I.U., 1970. The use of Oxalic acid as a Standard.In I.U. Olsson, ed., Radiocarbon Variations and
Absolute Chronology, Nobel Symposium, 12th Proc., John Wiley & Sons, New York, p. 17.
Stuiver, M. and Polach, H.A., 1977. Discussion: Reporting of 14C data. Radiocarbon, 19:355-363.
Stuiver, M., 1980.Workshop on 14C data reporting. Radiocarbon, 22:964-966.
2
National Ocean Sciences AMS Facility (NOSAMS) Radiocarbon Results (May, 3, 2010)
NOSAMS
Type (Material)
Accession #
Submitter Identification
Description
OS- 79559
OS- 79586
OS- 79560
OS- 79561
OS- 79562
OS- 79584
OS- 79563
OS- 79585
OS- 79564
OS- 79565
OS- 79583
OS- 79566
OS- 79587
OS- 79567
DSW-L#5771-5Ab Strat. IX (X)
DSW-L#5771-8Ab Strat. V (VI)
DSW-L#5771-13Ab Strat. -I (I)
LDW-L#2-2Ab
Strat. II
LDW-L#2-3ABkb Strat. I
LDW-L#3-3Ab
Strat. V
LDW-L#3-4Ab
Strat. IV
LDW-L#3-5Ab
Strat. III
LDW-L#3-6Ab
Strat. II
LDW-L#3-7Ab
Strat. I
RV-NCTP-2Ab
Strat. III
RV-NCTP-3Cu
Strat. II
RV-SCTP-3Ab
Strat. III
RV-SCTP-4Ob
Strat. II
Near top of section
Buried soil with snails
Basal buried soil
Plant/Wood
Plant/Wood
Sediment Organic carbon
Plant/Wood
Plant/Wood
Sediment Organic carbon
Sediment Organic carbon
Sediment Organic carbon
Sediment Organic carbon
Sediment Organic carbon
Sediment Organic carbon
Plant/Wood
Sediment Organic carbon
Plant/Wood
Buried soil
Buried soil with snails
Buried soil with snails
Buried soil - weak
Buried soil
Basal buried soil
Buried soil of floodplain facies
Channel facies
Upper buried playa
Lower buried playa
Age (14C
BP)
>Mod
>Mod
10300
>Mod
>Mod
9440
10000
10100
10100
10500
985
>Mod
9980
>Mod
Age Error
F
Fm
d13C
D14C
(+/-)
Modern Error
60
95
55
110
55
60
45
55
-21.30
-24.46
-25.41
-20.38
-26.19
-25.16
-24.91
-25.09
-25.45
-25.73
-21.99
-13.14
-24.12
-12.72
1.0542
1.2152
0.2782
1.1791
1.1961
0.3086
0.2873
0.2842
0.2837
0.2710
0.8847
1.5640
0.2888
1.0625
0.0039
0.0050
0.0021
0.0040
0.0037
0.0037
0.0020
0.0038
0.0019
0.0020
0.0049
0.0059
0.0020
0.0035
46.6
206.4
-723.8
170.5
187.4
-693.6
-714.8
-717.9
-718.3
-731.0
-121.7
552.7
-713.3
54.9
APPENDIX C
REGIONAL RADIOCARBON DATING COMPENDIUM
A-0442
Material Dated
housefloor
housefloor
housefloor
Locus B, Feature 01
charred material
charred material
charred material
Stratigraphic unit QLM4
Northern Owens Lake
Feature 03, disturbed rock ring
Feature 09, circular rock ring
Feature 08, circular rock ring
Northern Owens Lake
Northern Owens Lake
Northern Owens Lake
Northern Owens Lake
Northern Owens Lake
Northern Owens Lake
Eastern Owens Lake
Upper Salt, basin
Upper Salt, basin
Southeast shoreline, Trench 2
Southeast shoreline, Trench 3
Southeast shoreline, Trench 1
Southeast shoreline, Trench 2
Southeast shoreline, Trench 3
Southeast shoreline, Trench 1
Southeast shoreline, Trench 3
Southeast shoreline, Trench 1
Southeast shoreline, Trench 1
Southeast shoreline, Trench 2
Southeast shoreline, Trench 3
TU5-A, southeast shoreline
TU2-A
TU2-B
TU2-C
T-5 arroyo cutbank
T-5 arroyo cutbank
T-5 arroyo cutbank
T-5 arroyo cutbank
T-5 arroyo cutbank
T-5 arroyo cutbank
From bulldozer trench (50 m L x 4 m D) on playa surface of sag pond in fault zone
Locus A, N63/W54, Feature B, basalt cobble concentration
Feature 02, circular rock ring
Feature 01, circular rock ring
Owens Playa
Owens Playa
Dates Qe3 unit - early Holocene eolian deposit (dune sand)
Dates Ql2 unit - lates Holocene lacustrine deposit
Hearth
Cultural
Cultural
Cultural
Cultural
Cultural
Cultural
Cultural
Natural
Natural
Cultural
Cultural
Cultural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Cultural
Cultural
Cultural
Natural
Natural
Natural
Natural
Cultural
NV, Las Vegas Vly, Gilcrease Ranch
Spring Mound
Buried spring
Unit E2, 64, dates early spring activity
Natural Organic (tufa)
Drill hole 10 ft N of Smith and Pratt 1957 Core MD-1, with cattail, sedge, and other aquatic
plant pollen
Unit E2, 67a, minimum age of spring
Unit E1, 53, concretionary masses of algal (?) tufa, maxmum age of spring
Unit E2, 49, Cauliflower-like masses of algal (?) tufa, maxmum age of spring
Wood (Juniperus sp. twigs/seeds)
Wood (Juniperus sp. twigs/seeds)
Wood (Juniperus sp. twigs/seeds)
Yucca brevifolia leaves
Nolina bigelovii leaves
Wood (Juniperus sp. twigs/seeds)
Wood (Juniperus sp. twigs/seeds)
Wood (Juniperus sp. twigs/seeds)
Nolina bigelovii leaves
Wood (Juniperus sp. twigs/seeds)
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
A-0451
KER, China Lake, Core MD-1
Lake/Playa
Buried lacustrine
A-0464
A-0470
A-0471
A-1470
A-1538
A-1548
A-1550
A-1551
A-1580
A-1582
A-1615
A-1616
A-1620
NV, Las Vegas Vly, Ellington Scarp
NV, Las Vegas Vly, Ellington Scarp
NV, Las Vegas Vly, Ellington Scarp
SBR, Tunnel Ridge
SBR, Whipple Mountains
SBR, Falling Arches
SBR, Tunnel Ridge
SBR, Whipple Mountains
SBR, Redtail Peak
SBR, Tunnel Ridge
SBR, Whipple Mountains
SBR, Redtail Peak
SBR, Redtail Peak
Spring Mound
Spring Mound
Spring Mound
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Buried spring
Buried spring
Buried spring
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Page 1 of 10
Charcoal (or wood?)
Charcoal (or wood?)
Charcoal (or wood?)
Shell-f (Anodonta)
Charcoal
Charcoal
Charcoal
Carbonate (tufa)
Shell-f (freshwater)
Charcoal
Charcoal
Charcoal
Shell-f (freshwater)
Shell-f (freshwater)
Shell-f (freshwater)
Shell-f (freshwater)
Shell-f (freshwater)
Shell-f (freshwater)
Shell-f (freshwater)
Organic sediment(?)
Organic sediment(?)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Charcoal
Charcoal
Charcoal
Charcoal
Carbonate (oolites)
Organic sediment (marl)
Shell-f (Anodonta)
Shell-f (Anodonta)
Charcoal
Natural Shell-f (Anodonta)
Organic (black mat)
Organic (tufa)
Organic (tufa)
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
20
20
20
40
40
40
1
5
10
10
1
1
1
1
1
1
760
2150
30
39
25
70
107
95
77
90
80
130
62
20
30
40
85
23
35
95
60
142
128
10
10
10
1
-
960
1810
1900
1320
1110
1110
1130
13120
11070
460
510
930
9270
9670
10610
11120
11870
12670
19670
5300
8700
6333
9056
10041
13001
20643
22611
22824
24734
24942
28366
29438
18508
9870
10830
21645
9040
9200
10864
11489
11546
11720
2545
830
660
710
4770
12000
10003
10990
150
- 10810
160
70
90
70
40
50
60
80
60
50
40
40
60
60
60
60
60
60
60
200
200
48
72
62
69
213
191
469
255
204
228
186
155
50
50
408
55
56
59
65
63
64
160
50
40
40
60
60
120
120
15
Upper 2-Sigma cal BP
Type
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface lacustrine
Surface lacustrine
Surface deposit
Surface deposit
Surface deposit
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Buried lacustrine
Buried lacustrine
Surface lacustrine
Lacustrine
Lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Lacustrine
Lacustrine
Lacustrine
Buried lacustrine
Lacustrine
Lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried alluvium
Surface deposit
Surface deposit
Surface deposit
Buried lacustrine
Buried lacustrine
Buried lacustrine
Surface lacustrine
Surface deposit
Cal BP (med. prob.)
Location, Provenience, and/or Description
Fan/Floodplain
Fan/Floodplain
Fan/Floodplain
Floodplain
Hill/Ridge/Floodplain
Hill/Ridge/Floodplain
Hill/Ridge/Floodplain
Fan
Lake/Playa
Basin/Floodplain
Basin/Floodplain
Basin/Floodplain
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Floodplain/Playa
Basin/Floodplain
Basin/Floodplain
Basin/Floodplain
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Cave/Shelter
1-Sigma Error (±)
Dated Deposit
INY-2284, Portuguese Bench
INY-2284, Portuguese Bench
INY-2284, Portuguese Bench
INY-2750
KER-6106, Freeman Spring
KER-6106, Freeman Spring
KER-6106, Freeman Spring
INY, Death Valley/Titus Canyon
INY, Owens Valley, north
INY-5840, Airport Lake
INY-5840, Airport Lake
INY-5840, Airport Lake
INY, Owens Valley, north
INY, Owens Valley, north
INY, Owens Valley, north
INY, Owens Valley, north
INY, Owens Valley, north
INY, Owens Valley, north
INY, Owens Valley (east)
SBR, Searles, Core X-52
SBR, Searles, Core X-52
SBR, Searles Lake, SE Shore
SBR, Searles Lake, SE Shore
SBR, Searles Lake, SE Shore
SBR, Searles Lake, SE Shore
SBR, Searles Lake, SE Shore
SBR, Searles Lake, SE Shore
SBR, Searles Lake, SE Shore
SBR, Searles Lake, SE Shore
SBR, Searles Lake, SE Shore
SBR, Searles Lake, SE Shore
SBR, Searles Lake, SE Shore
SBR, Searles, Christmas Ridge
SBR, Searles, Lagunita Site
SBR, Searles, Lagunita Site
SBR, Searles, Lagunita Site
SBR, Searles, Poison Canyon
SBR, Searles, Poison Canyon
SBR, Searles, Poison Canyon
SBR, Searles, Poison Canyon
SBR, Searles, Poison Canyon
SBR, Searles, Poison Canyon
INY, Coso Range, Little Lake Flt
INY-5830, Airport Lake
INY-5840, Airport Lake
INY-5840, Airport Lake
INY, Owens Valley, playa
INY, Owens Valley, playa
SBR, Silver Lake
SBR, Silver Lake
INY-3415, Rochester Cave
14C BP (CRCY)
Deposit or
Landform
Lower 2-Sigma cal BP
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
State/County, Site/Locality
AVE Depth cm
Lab or Sample No.
Appendix C: China Lake Radiocarbon Database Listed by (1) Lab/Sample No., (2) Source Reference, and (3) State/County
652
1562
1609
1071
932
931
930
15225
12733
428
500
763
10255
11060
12418
12765
13486
14581
23206
4790
8449
7165
10118
11273
15134
24008
26701
26212
28914
29423
31846
33486
21549
11198
12593
24795
10124
10242
12605
13190
13260
13400
2300
672
553
637
5444
12954
11222
12635
170
887
1741
1840
1237
1016
1021
1045
15916
12962
508
533
849
10448
11071
12562
13004
13724
15001
23535
5278
8940
7266
10221
11555
15638
24643
27315
27457
29604
29843
32665
34133
22068
11270
12703
25929
10212
10364
12737
13345
13386
13569
2603
747
615
667
5506
13169
11542
12876
187
1185
1884
2057
1345
1090
1141
1178
16503
13117
557
560
927
10587
11215
12664
13163
13869
15252
23845
5749
9423
7333
10414
11823
16334
25129
27942
28519
30281
30280
33331
34637
22416
11396
12873
27055
10295
10507
12906
13482
13581
13751
2999
802
611
726
5602
13312
11847
13121
281
Source Reference
Faull 2006 - SCA via A. Gold
Faull 2006 - SCA via A. Gold
Faull 2006 - SCA via A. Gold
Faull 2006 - SCA via A. Gold
Faull 2006 - SCA via A. Gold
Faull 2006 - SCA via A. Gold
Faull 2006 - SCA via A. Gold
Klinger 2001
Koehler, 1995; Bacon et al. 2006
McGuire and Gilreath 1998
McGuire and Gilreath 1998
McGuire and Gilreath 1998
Orme and Orme 1993; Bacon et al. 2006
Orme and Orme 1993; Bacon et al. 2006
Orme and Orme 1993; Bacon et al. 2006
Orme and Orme 1993; Bacon et al. 2006
Orme and Orme 1993; Bacon et al. 2006
Orme and Orme 1993; Bacon et al. 2006
Orme and Orme 2000; Bacon et al. 2006
Peng et al. 1978 reported by Ramirez 2004
Peng et al. 1978 reported by Ramirez 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Ramirez de Bryson 2004
Roquemore 1981
Rosenthal and Eerkens 2003
Rosenthal and Eerkens 2003
Rosenthal and Eerkens 2003
Smith et al. 1997; Bacon et al. 2006
Smith et al. 1997; Bacon et al. 2006
Wells et al. 1987, 1989, 1990; McDonald et al. 2003
Wells et al. 1987, 1989, 1990; McDonald et al. 2003
Yohe and Parr 1987; Yohe 1992
400 11399 12640 13436 Haynes 1967
747 28170 2150 31052 32666 34672 Damon, Haynes, and Long 1964 -RCJ
1
1
1
1
1
1
1
1
1
1
9870
13400
10160
10330
9980
11650
12670
9920
8910
12330
10430
10840
10030
400
230
160
300
180
190
260
130
380
350
170
170
160
10290
15223
11242
11195
11069
13146
14015
11103
9118
13414
11701
12418
11170
11414
15903
11814
12039
11547
13518
14965
11437
10023
14475
12256
12757
11604
12645
16597
12394
12757
12150
13875
16270
11842
11105
15667
12662
13121
12148
Haynes 1967
Haynes 1967
Haynes 1967
King and Van Devender, 1977
King and Van Devender, 1977
Rowlands, 1978
King and Van Devender, 1977
Van Devender, 1977a
King and Van Devender, 1977
Wells, 1983a
Mead et al. 1978
Rowlands, 1978
Mead et al. 1978
A-1621
A-1655
A-1661, A-1662, and A1664
A-1663
A-1666
A-1668
A-1761
A-1762
A-1763
A-2465
A-2570
A-2571
A-2585
A-3650
A-3731
A-3732
A-3734
A-3943
A-3944
A-4537
A-4538
A-4539
A-4540
A-4590
A-4591
A-4592
A-4593
A-4594
A-4595
A-4606
A-4607
A-4607
A-4608
A-4609
A-4861
A-4862
A-4899
A-4901
A-4981
A-4986
A-4987
A-4988
A-4990
A-4993
A-4994
A-4995
A-4996
A-5035
A-5222
A-5223
A-5224
A-5305
A-5306
A-5438
A-5439
A-5440
A-5625
A-5626
A-5627
A-5881
Material Dated
Upper 2-Sigma cal BP
Type
Cal BP (med. prob.)
Location, Provenience, and/or Description
Lower 2-Sigma cal BP
Dated Deposit
1-Sigma Error (±)
Deposit or
Landform
14C BP (CRCY)
State/County, Site/Locality
AVE Depth cm
Lab or Sample No.
Appendix C: China Lake Radiocarbon Database Listed by (1) Lab/Sample No., (2) Source Reference, and (3) State/County
Source Reference
SBR, Redtail Peak
SBR, Redtail Peak
Cave/Shelter
Cave/Shelter
Surface deposit
Surface deposit
Wood (Juniperus sp. twigs/seeds)
Wood (Juniperus sp. twigs/seeds)
Natural Packrat Midden
Natural Packrat Midden
1 11520
1 9600
160 13106 13387 13741 King and Van Devender, 1977
170 10413 10924 11345 Van Devender, 1977a
SBR, Redtail Peak
Cave/Shelter
Surface deposit
Midden debris
Natural Packrat Midden
1 10600
105 12362 12511 12703 King and Van Devender, 1977
SBR, Redtail Peak
SBR, Redtail Peak
SBR, Redtail Peak
KER, Indian Wells, Robber's Roost
KER, Indian Wells, Robber's Roost
KER, Indian Wells, Robber's Roost
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Corn Creek Flat
SBR, Redtail Peak
SBR, Redtail Peak
SBR, Whipple Mountains
SBR, Redtail Peak
SBR, Whipple Mountains
SBR, Redtail Peak
NV, Corn Creek Flat
NV, Pahrump/Hidden Valley
NV, Pahrump/Stump Spring
NV, Pahrump/Browns Spring
NV, Pahrump/Stump Spring
NV, Pahrump/Hidden Valley
NV, Pahrump/Hidden Valley
NV, Pahrump/Hidden Valley
NV, Pahrump/Stump Spring
NV, Pahrump/Hidden Valley
NV, Pahrump/Hidden Valley
NV, Pahrump/Stump Spring
NV, Pahrump/Hidden Valley
NV, Pahrump/Hidden Valley
NV, Pahrump/Hidden Valley
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Corn Creek Flat
MNO, White Mountains
NV, Sandy Valley
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Sandy Valley
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Indian Springs Valley
NV, S. Coyote Springs
NV, N. Coyote Springs
NV, N. Coyote Springs
NV, Cactus Springs
NV, Pahrump/Hidden Valley
NV, Pahrump/Browns Spring
NV, Pahrump/Hidden Valley
NV, Pahrump/Stump Spring
NV, N. Coyote Springs
NV, N. Coyote Springs
NV, Pahrump/Hidden Valley
NV, Cactus Springs
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Spring Mound
Spring Mound
Spring Mound
Spring Mound
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Spring Mound
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Spring Mound
Spring Mound
Spring Mound
Spring Mound
Hill/Ridge
Floodplain/Arroyo
Spring Mound
Spring Mound
Floodplain/Arroyo
Spring Mound
Spring Mound
Spring Mound
Spring Mound
Spring Mound
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Buried channel
Buried spring
Buried spring
Buried spring
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Buried spring
Buried alluvium
Buried alluvium
Buried alluvium
Surface deposit
Buried alluvium
Buried soil
Buried alluvium
Buried alluvium
Buried alluvium
Buried spring
Buried spring
Buried spring
Buried spring
Buried alluvium
Buried spring
Buried channel
Buried spring
Buried channel
Surface deposit
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried alluvium
Buried alluvium
Buried spring
Buried spring
Buried soil
Buried spring
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
AA-0?
KER, China Lake, Core SB01
Lake/Playa
Buried lacustrine
Natural Organic sediment
6718 11215
150 12726 13088 13361 Couch Appendix B in Tetra Tech EM Inc. 2003
AA-0?
KER, China Lake, Core SB04
Lake/Playa
Buried lacustrine
Nolina bigelovii leaves
Wood (Pinus monophylla)
Wood (Juniperus sp. twigs/seeds)
Wood (Juniperus sp. twigs/seeds)
Wood (Juniperus sp. twigs/seeds)
Wood (Juniperus sp. twigs/seeds)
Unit E2
CSCarb.-11a
CS81Carb.-11b
CS81Carb. 3a
Neotoma sp. fecal pellets
Neotoma sp. fecal pellets
Neotoma sp. fecal pellets
Neotoma sp. fecal pellets
Neotoma sp. fecal pellets
Wood (Juniperus sp. twigs/seeds)
CS81Carb. 13b
PVCarb.-29b
PVCarb.-7b
PVCarb.-21b
PVCarb.-15a (DE-1)
PVCarb.-37b, base of brown silt cap unit
PVCarb.-31b, basal channel paleosol, overlies mammoth molar
PVCarb.-33b
PVCarb.-11b
PVCarb.-34b
PVCarb-35b
PVCarb.-26b
PVCarb.-26b
PVCarb.-10b
PVCarb.-39b
CS81Carb. 6b
CSC87-2b
Unit D of Haynes
CSC87-8b
Falls Canyon 1 site
SAV.Carb.-1b
CSC87-5b
CSC87-3b
SVC87-1b
CS81Carb.3b
CSC87-6b
CSC87-7b
CSC87-1b
Unit E of Haynes
SCySCarb.-1b
NCySC-5b
NCySC-6b
Cac. Spr.Carb.-6b
PVCarb.-38b
PVCarb.-22b
PVCarb.-41b
PVCarb.-8a
NCySC-8b
NCySC-9b
PVCarb.-36b
Cac. Spr.Carb.-7b
Bore Hole TTIWV-SB01, far northwestern IWV; alluvial deposits date last Owens River
overflow?
Bore Hole TTIWV-SB04, west Ridgecrest near Brady and Sydor streets
Natural Organic sediment
1859 19590
300 22505 23380 24144 Couch Appendix B in Tetra Tech EM Inc. 2003
AA-0?
KER, China Lake, Core SB11
Lake/Playa
Buried lacustrine
Bore Hole TTIWV-SB11, near intersection of N China Lake Blvd and E French Ave.
Natural Organic sediment
9310
AA-0?
KER, China Lake, Core SB11
Lake/Playa
Buried lacustrine
Bore Hole TTIWV-SB11, near intersection of N China Lake Blvd and E French Ave.
Natural Organic sediment
Page 2 of 10
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Wood (?)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Organic (black mat)
Wood (carbonized)
Wood (carbonized)
Wood (carbonized)
Charcoal
Wood (carbonized)
Wood (carbonized)
Wood (carbonized)
Wood (carbonized)
Wood (carbonized)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Wood (carbonized)
Organic (black mat)
Wood (carbonized)
Shell-f (fresh)
Wood (carbonized)
Packrat Midden
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Wood (carbonized)
Wood (carbonized)
Organic (black mat)
Organic (black mat)
Wood (carbonized)
Organic (black mat)
1
1
1
1
1
1
1
1
1
1
1
1
425
505
15
335
625
405
555
415
405
505
405
300
435
1
435
435
575
455
-
9600 160 10490 10926 11314 King and Van Devender, 1977
12960 210 14801 15654 16652 King and Van Devender, 1977
9160 170 9741 10351 10780 King and Van Devender, 1977
12960 270 14524 15644 16736 McCarten and Van Devender, 1988
12820 400 14015 15342 16705 McCarten and Van Devender, 1988
13800 400 15424 16840 17858 McCarten and Van Devender, 1988
10980 270 12233 12930 13410 Quade et al. 1998
6220 250 6535 7085 7573 Quade 1986
8640 150 9404 9686 10172 Quade 1986
10090 160 11214 11694 12239 Quade 1986
8040 120 8594 8909 9276 Van Devender et al. 1990b
9310 150 10200 10528 10878 Van Devender et al. 1990b
8180 130 8752 9143 9470 Van Devender and Hawksworth, 1986
9330 110 10239 10536 10791 Van Devender et al. 1990b
8540 100 9290 9528 9777 Van Devender and Hawksworth, 1986
10490 110 12055 12383 12621 Van Devender et al. 1990b
10220 210 11259 11935 12641 Quade et al. 1998
8610 150 9371 9648 9967 Quade et al. 1998
10090 200 11172 11716 12400 Quade et al. 1998
8120 210 8543 9036 9501 Quade et al. 1998
8570 170 9239 9598 9972 Quade et al. 1995
8480 160 9031 9465 9892 Quade et al. 1998
11190 210 12804 13101 13464 Quade et al. 1998
10940 390 11710 12828 13676 Quade et al. 1995
10380 380 11095 12119 13065 Quade et al. 1995
8600 170 9260 9642 10176 Quade et al. 1998
9120 110 10118 10310 10578 Quade et al. 1998
10090 100 11303 11668 12038 Quade et al. 1998
10090 100 11303 11668 12038 Quade et al. 1998
8510 190 9025 9510 9951 Quade et al. 1998
10920 160 12630 12902 13198 Quade et al. 1998
9220 180 9905 10426 10878 Quade et al. 1995
11580 240 12994 13456 13914 Quade et al. 1998
28090 1080 31277 32407 33696 Quade et al. 1995
11870 200 13290 13725 14150 Quade et al. 1998
8790 110 9555 9846 10160 Jennings and Elliot-Fisk 1990(?)
11020 140 12808 12976 13200 Quade et al. 1995
6340 260 6634 7208 7691 Quade et al. 1998
11800 180 13290 13649 14011 Quade et al. 1998
9620 110 10667 10951 11229 Quade et al. 1998
10140 130 11260 11768 12189 Quade et al. 1995
10390 150 11749 12270 12784 Quade et al. 1998
10200 130 11318 11884 12391 Quade et al. 1998
11760 130 13323 13608 13862 Quade et al. 1995
10410 110 11965 12316 12723 Quade et al. 1995
9970
90 11217 11469 11775 Quade et al. 1995
9500 280 10146 10813 11751 Quade et al. 1995
7790
90 8403 8584 8791 Quade et al. 1998
10410 110 11965 12316 12723 Quade et al. 1995
9760 130 10716 11149 11503 Quade et al. 1998
7230 100 7914 8059 8217 Quade et al. 1998
8600 130 9371 9624 9948 Quade et al. 1998
10450 150 11953 12364 12807 Quade et al. 1998
8145
80 8950 9104 9321 Quade et al. 1998
8400
70 9254 9418 9535 Quade et al. 1998
10170
80 11590 11840 12113 Quade et al. 1998
10060 200 11104 11671 12396 Quade et al. 1998
3250
14447 10195
95
3262
3486
3698 Couch Appendix B in Tetra Tech EM Inc. 2003
150 11308 11870 12411 Couch Appendix B in Tetra Tech EM Inc. 2003
KER, China Lake, hummock
Lake/Playa
Surface lacustrine
AA-0?
AA-00380
AA-012405
AA-01576
SBR, China Lake, SL-01
SBR, Redtail Peak
SBR-5250, Rogers Ridge
SBR, Whipple Mountains
Lake/Playa
Cave/Shelter
Fan
Cave/Shelter
Buried lacustrine
Surface deposit
Surface deposit
AA-02519
MNO, Mono Lake
Lake Basin
Lacustrine
Core in 2.8 m of water placed in Post Office Creek delta; Tsoyowata ash at 363 cm
AA-02520
AA-04450
AA-04692
AA-04898
AA-05879
MNO, Mono Lake
MNO, Tioga Pass Pond
MNO, Mono Lake
SBR, Valley Wells
SBR, Valley Wells
Lake Basin
Glacial Lake
Lake Basin
Spring mound
Spring mound
Lacustrine
Buried lacustrine
Lacustrine
Fossil spring
Fossil spring
Core in 2.8 m of water placed in Post Office Creek delta in 1986
TP (2)
Core in 2.8 m of water placed in Post Office Creek delta in 1986
Black organic mat from fossil spring
Black organic mat from fossil spring
AA-05902
MNO, Mono Lake
Lake Basin
Lacustrine
Core in 2.8 m of water placed in Post Office Creek delta in 1986; large thinolite tufa crystals
Natural Carbonate (tufa)
658
9450
INY-0182, Stahl Site
INY-0182, Stahl Site
INY-0182, Stahl Site
INY-0182, Stahl Site
INY-0182, Stahl Site
NV, Corn Creek Flat
NV, Pahrump/Hidden Valley
NV, Pahrump/Hidden Valley
NV, Pahrump/Hidden Valley
NV, Corn Creek Flat
KER-3939, Clark Wash
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
Fan/Floodplain
Fan/Floodplain
Fan/Floodplain
Fan/Floodplain
Fan/Floodplain
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Fan/Floodplain
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Buried deposit
Buried deposit
Buried deposit
Buried soil
Buried deposit
Buried spring
Buried spring
Buried soil
Buried spring
Buried spring
Buried deposit
Lacustrine
Lacustrine
Lacustrine
Lacustrine
Lacustrine
Trench 20, Unit 04
Trench 20, Unit 09
Trench 20, Unit 06
Trench 21, Unit 01, carbonized matter on large mammal bone
Trench 20, Unit 01 and 02, carbonized matter on large mammal bone
CCS 4, aquatic snail, Physa virgata
SSW 1, aquatic snail, Gyraulus circumstratus
HV 12, semi-aquatic, Succineidae
SSW 1, aquatic snail, Gyraulus parvus
CCS 6, semi-aquatic snail, Succineidae, within black mat (Beta-86431)
Trench 9, Qf1
Pedogenic hardground with dense lower carbonate-cemented layer
Buff travertine with shell fragments
Carbonate-cemented angular alluvial gravels
Carbonated rind between rounded lacustrine cobbles
Brown, nodular travertine
Cultural
Cultural
Cultural
Cultural
Cultural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
75
115
165
85
55
625
455
435
138
1
1
1
1
1
8670
8625
8400
8625
8900
13330
13240
10180
10120
10050
11470
11522
10909
12905
11905
13826
AA-0?
AA-08620
AA-08621
AA-08622
AA-10535
AA-10536
AA-14093
AA-14101
AA-14102
AA-14164
AA-14166
AA-15825/6
AA-61607
AA-61608
AA-62076
AA-62077
AA-62078
Beta- (written comm.)
Natural Organic sediment
Natural
Natural
Cultural
Natural
Shell-f (gastropod)
Packrat Midden
Shell-m (Olivella)
Packrat Midden
45 10070
12825
11360
10495
11015
170
500
85
110
14542
11988
10875
12653
15351
13245
11224
12898
Natural Organic sediment (gyttja)
455
7485
120
8028
8287
Natural
Natural
Natural
Natural
Natural
605 8990
298 8760
715 10765
90 10250
- 11600
Shell-m (Olivella A1)
Shell-m (Olivella A1)
Shell-m (Olivella A1)
Organic Matter (sinew or flesh?)
Organic Matter (sinew or flesh?)
Shell-f (gastropod)
Shell-f (gastropod)
Shell-f (gastropod)
Shell-f (gastropod)
Organic (black mat)
Charcoal
Carbonate (mixed)
Carbonate (mixed)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
16418
14641
11707
13125
Couch Appendix B in Tetra Tech EM Inc. 2003
King and Van Devender, 1977
Basgall and Hall 1994
Van Devender, 1990b
8481 Davis 1999
105 9736 10084 10303
240 9278 9840 10430
105 12528 12670 12921
160 11392 11977 12448
120 13241 13459 13745
Davis 1999
Anderson 1990
Davis 1999
Quade et al. 1995
Quade et al. 1998
95 10484 10721 11105 Davis 1999
85
110
85
60
65
90
180
130
140
70
105
71
68
77
74
84
8592
8521
8356
9494
9765
15404
11631
11318
11243
11286
13124
13228
12606
15013
13568
16736
8969
8901
8621
9597
10018
15820
14325
11845
11734
11578
13331
13369
12782
15436
13759
16921
9302
9295
8966
9737
10205
16258
17010
12250
12187
11827
13569
13577
12969
16141
13946
17147
Schroth 1994
Schroth 1994
Schroth 1994
Schroth 1994
Schroth 1994
Quade et al. 2003
Quade et al. 2003
Quade et al. 2003
Quade et al. 2003
Quade et al. 2003
McGill et al. 2009
Numelin et al. 2007
Numelin et al. 2007
Numelin et al. 2007
Numelin et al. 2007
Numelin et al. 2007
SBR, Silver Lake
Lake/Playa
Surface deposit
Northwest Silver Lake, El Capitan BR II
Natural Shell-f (Anodonta)
SBR, Marble Canyon
Fan
Buried soil
Natural Soil (SOM)
243
9710
Beta-002155
SBR, Ivanpah Mountains
Cave/Shelter
Buried deposit
Natural Charcoal
640
9830
150 10746 11280 11811 Goodwin and Reynolds 1989; Bell and Jass 2004
Beta-010790
Beta-012840
Beta-012843
Beta-012844
SBR-5250, Rogers Ridge
SBR-5250, Rogers Ridge
SBR-5250, Rogers Ridge
SBR-5250, Rogers Ridge
Fan
Fan
Fan
Fan
Fossil spring?
Fossil spring?
Buried deposit
18
60
25
25
7910
8410
8300
8420
420
140
110
210
Beta-018449
KER, Dove Springs Wash
Floodplain/Arroyo
Buried soil
Natural Charcoal (confier branch)
245 10730
110 12511 12642 12894 Whistler 1990, 1994; Miller and Amoroso 2007
Beta-021199
Beta-021200
Beta-024342
Beta-026456
Beta-029552
Beta-029553
Beta-030156
Beta-033103
Beta-038745
Beta-038750
Beta-039767
Beta-040162
Beta-045472
Beta-045473
SBR, Soda Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
INY, Two Goblin
INY, Two Goblin
KER-2584, Red Rock Burial
INY-3812
INY-3433, Coso Trans. Line
INY-3812
NV, Las Vegas Vly, Ellington Scarp
NV, Las Vegas Vly, Ellington Scarp
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Cave/Shelter
Cave/Shelter
Terrace
Fan (inset)
Hill/Ridge
Fan (inset)
Spring Mound
Spring Mound
Surface deposit
Surface deposit
Buried lacustrine
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Buried spring
Buried spring
From 3Bkb horizon in west wall of trench across fault
Near center of Late Pleist.-Early Holo. faunal deposit in Kokoweef Cave (SBCM site no.
SBC1.11.13)
Trench 5
N1043/E940, Feature 3
N1047/E933, Feature 4, spring pit or well
N918/E965
From "lignitic sand" at base of oldest inset terrace in canyon; chalcedony flake in same stratum
40 m away; Qyw4 LP-EH unit of Miller and Amorosa 2006
Beach Ridge-Soda Lake, Elephant Ridge complex
Beach Ridge III, El Capitan complex
Silver Lake Sil-M Core (south end of lake)
Beach Ridge I, El Capitan complex
Beach Ridge V, El Capitan complex
Tidewater Basin Beach, Ridge II-Silver Lake
Neotoma sp. fecal pellets
Neotoma sp. fecal pellets
Whistler Site, south of powerlines, east of Dove Spring Wash, 6-7 m above channel
House structure, post 2
S8/E9, Feature 04, circular rock hearth w/millingstones
Locus 1, housefloor, post 10
-
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Cultural
Cultural
Cultural
Cultural
Natural
Natural
Shell-f (Anodonta)
Shell-f (Anodonta)
Organic sediment
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Packrat Midden
Packrat Midden
Bone (human)
Charcoal
Charcoal
Charcoal
Organic (black mat)
Organic (black mat)
40
1
305
143
138
262
1
1
5
92
15
128
-
11690
10000
9330
13310
9060
15940
9540
7840
3740
1600
90
1340
11630
9820
130
120
95
120
120
310
100
70
65
60
60
50
90
100
13293
11219
10247
15500
9885
18570
10641
8452
3898
1354
8
1172
13295
11067
13549
11538
10533
16300
10215
19114
10885
8646
4099
1485
121
1268
13486
11246
Dune (inland)
Surface deposit
Locus A, E3/S43, Feature 2C ash pit w/Anodonta shells
Cultural Charcoal (w/shells)
80
6640
65
7429
7522
Dune (inland)
Lake/Playa
Lake/Playa
Cave/Shelter
Hill/Ridge
Hill/Ridge
Floodplain/Terrace
Lake/Playa
Cave/Shelter
Cave/Shelter
Surface deposit
Surface lacustrine
Surface lacustrine
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface lacustrine
Surface deposit
Surface deposit
Locus H, from rock cluster/hearth feature
Swansea Bay (S), high barrier beach, sample 5
Swansea Bay (N), low barrier beach, sample 8
Packrat Midden
Unit 01, basalt tablelands
Unit 01, Locus of INY-3017, basalt tablelands
From Bqk-horizon in Q2 (i.e., T2) terrace, soil pit 203
Swansea Bay (S), intermediate beach, sample 7
Neotoma sp. fecal pellets
Neotoma sp. fecal pellets
Cultural
Natural
Natural
Natural
Cultural
Cultural
Natural
Natural
Natural
Natural
1
1
1
15
40
75
1
1
1
820
11880
10610
11470
400
101
6840
11120
7990
9460
70
130
70
70
50
50
100
70
50
50
665
13423
12400
13167
421
9
7559
12750
8696
10567
750
13722
12555
13330
449
120
7689
13002
8860
10703
Beta-?
Beta-045611, ETH-7129 SBR-5251, Tiefort Basin
Beta-045612
Beta-051957
Beta-052398
Beta-052489
Beta-052552
Beta-052553
Beta-053846
Beta-054341
Beta-054713
Beta-054714
SBR-5251, Tiefort Basin
INY, Owens Valley, Swansea Bay
INY, Owens Valley, Swansea Bay
SBR, Granite Mountains
INY-3033, Coso Trans. Line
INY-3455, Coso Trans. Line
INY, Owens River Terrace
INY, Owens Valley, Swansea Bay
INY, Lubkin Canyon
INY, Lubkin Canyon
Page 3 of 10
Natural
Natural
Natural
Natural
?
Soil (SOM)
Soil (SOM)
?
Charcoal
Shell-f (Anodonta)
Shell-f (Anodonta)
Packrat Midden
Charcoal
Charcoal
Carbonate (clast coating)
Shell-f (Anodonta)
Packrat Midden
Packrat Midden
5 11640
Source Reference
155 11203 11658 12153 Couch Appendix B in Tetra Tech EM Inc. 2003
159
1
1
Organic sediment (gyttja)
Organic sediment
Organic sediment (gyttja)
Organic (black mat)
Organic (black mat)
Upper 2-Sigma cal BP
Material Dated
Cal BP (med. prob.)
Type
Lower 2-Sigma cal BP
Location, Provenience, and/or Description
TT13-SL01, N of golf course & Knox Rd; gypsum-rich silty clay hummock dates lake
dessication
TT43-SL01 in lower lake basin;from near-shore death assemblage
Wood (Pinus monophylla needles)
Olivella bead
Larrea tridentata twigs
1-Sigma Error (±)
Dated Deposit
14C BP (CRCY)
Deposit or
Landform
State/County, Site/Locality
AVE Depth cm
Lab or Sample No.
Appendix C: China Lake Radiocarbon Database Listed by (1) Lab/Sample No., (2) Source Reference, and (3) State/County
160 13201 13507 13819 Weldon 1982; Wells et al. 2003
50 11070 11149 11236 Spotila and Anderson 2003
7921
9022
9023
8855
8817
9379
9285
9386
9774
9632
9493
9934
13804
11846
10765
16827
10522
19592
11172
8796
4294
1618
151
1346
13693
11621
Jenkins 1985; Gilreath 1987; CRD 1996
Jenkins 1985
Jenkins 1985
Jenkins 1985; Gilreath 1987; CRD 1996
Wells et al. 2003
Wells et al. 2003
Wells et al. 2003
Brown 1990; Wells et al. 2003
Wells et al. 2003
Brown 1990; Wells et al. 1989; Wells et al. 2003
Koehler and Anderson 1995
Koehler and Anderson 1995
Sutton 1992
Delacorte et al.1993
Hildebrandt and Wohlgemuth 1995
Delacorte et al.1993
DuBarton et al. 1991
DuBarton et al. 1991
7610 Hall 1994
835
14001
12684
13468
521
151
7870
13178
9007
10804
Hall 1994
Orme and Orme 2008
Orme and Orme 2008
Koehler et al. 2005
Hildebrandt and Wohlgemuth 1995
Hildebrandt and Wohlgemuth 1995
Pinter, Keller, and West 1994
Orme and Orme 2008
Koehler and Anderson 1995
Koehler and Anderson 1995
Buried lacustrine
Surface deposit
Surface deposit
Buried lacustrine
Surface deposit
Surface deposit
Buried lacustrine
Buried channel
Buried channel
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried channel
Buried channel
Buried channel
Buried alluvium
Buried alluvium
Buried alluvium
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Buried spring
Surface lacustrine
Surface lacustrine
Buried lacustrine
Buried channel
Buried channel
Buried channel
Buried lacustrine
Buried spring
Buried spring
Buried spring
Beta-094111
SBR, Lake Dumont/Salt Creek, site?
Lake/Playa
Beta-097593
INY, Death Valley (west)
Lake/Playa
Beta-097595
INY, Death Valley, Devil's Speedway
Beta-158755
Beta-163551
Beta-163552
Beta-163553
Beta-163554
Beta-163555
Beta-163556
Beta-163557
Beta-163558
Beta-165600
Beta-166887
Beta-166888
Beta-166889
Beta-166890
Beta-168600
Beta-168601
Beta-168602
Beta-170208
Beta-170209
Beta-170210
Beta-190570
Beta-190572
Location, Provenience, and/or Description
Type
Material Dated
Locus D, BHT 1, organic soil, Stratum Iva
N121/W62.5
Neotoma sp. fecal pellets
Swansea Bay (N), gravel pit, death bed, sample 10
Neotoma sp. fecal pellets
Unit 02
From silty sand below 50 cm of sandy overburden
CSCarb.27b
CSWood1
NCySC-2b
NCySC-3b
NCySC-4b
NCySC-7b
CSC87-9b
CSCarb.28a
CSCarb.28b
CSCarb.30b
PVCarb.-12b
PVCarb.-13b
PVCarb.-14b
PVCarb.-47b
PVCarb.-27b
PVCarb.-27b
CCS 5, aquatic snail, Pyrgulopsis
HV 11, semi-aquatic snail, Succineidae
HV 11, terrestrial snail, Stagnicola caperata
Owens River, fan delta, sample 6 (from gully cutbank?)
Centennial shore, beach ridge, sample 4
Swansea Bay (N), gravel pit, low barrier beach, sample 9
Section OCI-11, CSC-29b
Section OC-11, CSC-27b
Section OC-11, terrestrial snail, Vallonia cyclophorella
Si-1-II, Core at southern end of playa
Cac. Spr.Carb.8
Cac. Spr.QUADE90-100, semi-aquatic snail, Succineidae
CCS 6,
Natural
Cultural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Surface deposit
DU-3-Qal, Alluvium, from dark gray ashy layer over oxidized burn layer (possible hearth?)
Natural Charcoal
Buried lacustrine
Core 9
Natural Organic sediment
Lake/Playa
Buried lacustrine
Core 10
INY, Owens Valley, Keeler
INY, Owens River Bluff
INY, Owens River Bluff
INY, Owens River Bluff
INY, Owens Valley, Alabama Gates
INY, Owens Valley, Alabama Gates
INY, Owens Valley, Quaker
INY, Owens Valley, Quaker
INY, Owens Valley, Quaker
INY, Owens Valley, Quaker
INY, Owens Valley, Keeler
INY, Owens Valley, Keeler
INY, Owens Valley, Keeler
INY, Owens Valley, Keeler
INY, Owens Valley, Quaker
INY, Owens Valley, Quaker
INY, Owens Valley, Quaker
INY-5825, Basalt Ridge, spring
INY-5825, Basalt Ridge, soil
INY-5825, Basalt Ridge, spring
SBR, Searles, Salt Wells Valley
SBR, Searles, Salt Wells Valley
Fan/Floodplain
Basin/Floodplain
Basin/Floodplain
Basin/Floodplain
Basin/Floodplain
Basin/Floodplain
Basin/Floodplain
Basin/Floodplain
Basin/Floodplain
Basin/Floodplain
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Basin/Floodplain
Basin/Floodplain
Basin/Floodplain
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Buried deposit
Buried marsh
Buried marsh
Buried marsh
Buried marsh
Buried marsh
Buried marsh
Buried marsh
Buried marsh
Buried marsh
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Buried marsh
Buried marsh
Buried marsh
Surface deposit
Buried soil
Buried spring
Lacustrine
Lacustrine
Beta-211384
SBR, Searles, Salt Wells Valley
Lake/Playa
Lacustrine
Beta-211385
SBR, Searles, Salt Wells Valley
Lake/Playa
Lacustrine
Swansea (east Owens Lake)
lithofacies 4b, west bank Owens River ~600 m ESE of Quaker
lithofacies 4b
lithofacies 4b
lithofacies 4b, Trench 2
lithofacies 4b, Trench 2
lithofacies 4b, Trench 4
lithofacies 4b, Trench 4
lithofacies 4b, Trench 4
lithofacies 13b, Trench 4
Near Keeler (east Owens Lake)
Near Keeler (east Owens Lake)
Near Keeler (east Owens Lake)
Near Keeler (east Owens Lake)
lithofacies 4a, Pit 4
lithofacies 4a, Pit 4
lithofacies 4a, Pit 4
S48/W30.5, Stain 1, Spring Peat, at Basalt Ridge
S50/W17, Buried Soil Unit, at Basalt Ridge
S48/W30.5, Stain 1, Spring Peat, at Basalt Ridge
From spillway between China and Searles lakes, coll by R. Kaldenberg
From spillway between China and Searles lakes, coll by R. Kaldenberg
RLK # AMP-01, "in Salt Wells Valley west of road between CLP and ammunition storage
areas, near high-water overflow between lakes"
RLK # AMP-02, "in Salt Wells Valley west of road between CLP and ammunition storage
areas, near high-water overflow between lakes"
Page 4 of 10
Organic sediment (marl)
Shell-f (Anodonta)
Packrat Midden
Shell-f (gastropod)
Packrat Midden
Shell-f (freshwater)
Shell-f (Anodonta)
Wood (carbonized)
Wood (carbonized)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Wood (carbonized)
Wood (carbonized)
Wood (carbonized)
Wood (carbonized)
Wood (carbonized)
Wood (carbonized)
Organic (black mat)
Organic (black mat)
Organic (black mat)
Shell-f (gastropod)
Shell-f (gastropod)
Shell-f (gastropod)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Wood (carbonized)
Wood (carbonized)
Shell-f (gastropod)
Organic sediment
Wood (carbonized)
Shell-f (gastropod)
Organic (black mat)
9493
522
8445
10656
9528
13586
12733
14125
13259
12050
8981
7457
9698
9550
14137
14234
13773
11124
10767
10147
8407
10547
10547
12688
10171
11616
13059
14112
12133
14900
13806
14836
10239
11270
13999
11248
9862
598
8672
10927
9689
13828
12962
14416
13373
12275
9119
7539
9986
9765
14434
14598
14053
11227
10989
10225
8785
10675
10675
12801
10249
11886
13244
14518
12441
15126
13951
15115
10380
11536
14193
11412
10218
663
8983
11198
9929
14051
13117
14824
13502
12406
9321
7616
10202
9938
14839
14937
14509
11354
11202
10407
9140
10790
10790
12864
10420
12100
13463
15016
12606
15413
14095
15453
10524
11772
14611
11622
Source Reference
66
5
1
70
1
85
50
455
270
170
300
210
435
405
405
1
1
110
75
25
55
1800
95
-
9440
590
7840
9580
8700
11970
11070
12400
11540
10390
8160
6670
8880
8760
12410
12490
12180
9810
9650
9060
7920
9440
9440
10750
9090
10190
11370
12430
10510
12810
12100
12800
9210
10030
12300
9970
60
9200
800
9780
60 11088 11207 11316 Anderson and Wells 2003a
Natural Organic sediment
300 12420
60 14122 14492 14981 Anderson and Wells 2003a
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
300
300
270
270
200
200
200
100
1
1
1
1
315
315
315
4
40
42
1
1
Shell-f (freshwater)
Charcoal
Organic sediment
Organic sediment
Charcoal
Organic sediment
Organic sediment
Organic sediment
Charcoal
Charcoal
Carbonate (tufa)
Carbonate (tufa)
Shell-f (freshwater)
Carbonate (tufa)
Charcoal
Charcoal
Charcoal
Organic (black mat)
Organic sediment
Organic (black mat)
Shell-f (Anodonta)
Shell-f (Anodonta)
9540
9990
10480
9560
9060
9030
9160
9680
9920
9300
15990
10990
20350
10640
12580
12590
12730
10010
8390
9870
12080
12110
150
60
100
100
80
90
60
60
50
60
70
50
80
60
60
50
110
60
70
60
160
50
50
60
60
60
110
80
80
60
60
80
70
60
60
50
Upper 2-Sigma cal BP
Fan/Floodplain
Floodplain
Cave/Shelter
Lake/Playa
Cave/Shelter
Fan/Terrace (alluvial)
Lake/Playa
Spring Mound
Spring Mound
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Spring Mound
Spring Mound
Spring Mound
Spring Mound
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Lake/Playa
Lake/Playa
Lake/Playa
Spring Mound
Spring Mound
Spring Mound
Lake/Playa
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Cal BP (med. prob.)
INY-0328/H, Owens Valley
INY-2750
INY, Lubkin Canyon
INY, Owens Valley, Swansea Bay
INY, Corsair
INY-3806/H
INY, Owens Valley, Dolomite Site
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, N. Coyote Springs
NV, N. Coyote Springs
NV, N. Coyote Springs
NV, N. Coyote Springs
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Pahrump/Stump Spring
NV, Pahrump/Stump Spring
NV, Pahrump/Stump Spring
NV, Pahrump/Hidden Valley
NV, Pahrump/Stump Spring
NV, Pahrump/Hidden Valley
NV, Corn Creek Flat
NV, Pahrump/Hidden Valley
NV, Pahrump/Hidden Valley
INY, Owens Valley, Swansea Bay
INY, Owens Valley, Centennial
INY, Owens Valley, Swansea Bay
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Corn Creek Flat
SBR, Silurian Lake
NV, Cactus Springs
NV, Cactus Springs
NV, Corn Creek Flat
Lower 2-Sigma cal BP
Dated Deposit
Beta-055681
Beta-055684
Beta-055880
Beta-058386
Beta-059783
Beta-066967
Beta-067673
Beta-073466
Beta-073629
Beta-073958
Beta-073959
Beta-073960
Beta-073961
Beta-073963
Beta-073967
Beta-073968
Beta-073969
Beta-073971
Beta-073972
Beta-073973
Beta-073974
Beta-073975
Beta-073975
Beta-074392
Beta-074873
Beta-074883
Beta-082061
Beta-082062
Beta-082063
Beta-084315
Beta-084316
Beta-084781
Beta-085542
Beta-086427
Beta-086429
Beta-086431
1-Sigma Error (±)
Deposit or
Landform
14C BP (CRCY)
State/County, Site/Locality
AVE Depth cm
Lab or Sample No.
Appendix C: China Lake Radiocarbon Database Listed by (1) Lab/Sample No., (2) Source Reference, and (3) State/County
Delacorte 1999
Delacorte 1999
Koehler and Anderson 1995
Orme and Orme 2008
Koehler and Anderson 1995
Gilreath 1995
Koehler 1995
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 1998
Quade et al. 2003
Quade et al. 2003
Quade et al. 2003
Orme and Orme 2008
Orme and Orme 2008
Orme and Orme 2008
Quade et al. 1998; Quade et al. 2003
Quade et al. 1998; Quade et al. 2003
Quade et al. 2003
Anderson and Wells 2003b
Quade et al. 2003
Quade et al. 2003
Quade et al. 2003
60 10237 10366 10514 Anderson and Wells 2003b
90
40
40
40
40
60
50
50
50
60
90
70
120
70
60
60
60
110
130
50
260
170
10648
11268
12373
10729
10179
10116
10230
11065
11225
10282
18893
12677
23870
12420
14445
14462
14710
11233
9022
11198
13412
13583
10887
11454
12456
10932
10224
10203
10328
11109
11325
10494
19148
12862
24274
12582
14819
14842
15096
11543
9361
11270
14036
14011
11168
11624
12586
11092
10260
10292
10435
11218
11414
10608
19408
13084
24553
12696
15177
15189
15544
11839
9557
11396
14977
14676
Bacon et al. 2006
Bacon, Pezzopane, and Burke 2003
Bacon, Pezzopane, and Burke 2003
Bacon, Pezzopane, and Burke 2003
Bacon, Pezzopane, and Burke 2003
Bacon, Pezzopane, and Burke 2003
Bacon, Pezzopane, and Burke 2003
Bacon, Pezzopane, and Burke 2003
Bacon, Pezzopane, and Burke 2003
Bacon, Pezzopane, and Burke 2003
Bacon et al. 2006
Bacon et al. 2006
Bacon et al. 2006
Bacon et al. 2006
Bacon, Pezzopane, and Burke 2003
Bacon, Pezzopane, and Burke 2003
Bacon, Pezzopane, and Burke 2003
Basgall 2004
Basgall 2004
Basgall 2004
Hildebrandt and Darcangelo 2004
Hildebrandt and Darcangelo 2004
Natural Shell-f (Anodonta)
1 12120
90 13740 13972 14225 Kaldenberg 2006; Rogers 2009
Natural Shell-f (Anodonta)
1 12150
60 13818 13996 14175 Kaldenberg 2006; Rogers 2009
Material Dated
Beta-211386
SBR, Searles, Salt Wells Valley
Lake/Playa
Surface deposit
Beta-211387
SBR, Searles, Salt Wells Valley
Lake/Playa
Lacustrine
Beta-211388
SBR, Searles, Salt Wells Valley
Lake/Playa
Lacustrine
Beta-211389
SBR, Searles, Salt Wells Valley
Lake/Playa
Lacustrine
Beta-211390
Beta-220691
Beta-220692
Beta-237061
Beta-237062
Beta-237063
Beta-237064
Beta-237065
Beta-249418
Beta-249419
Beta-254726
Beta-255187
Beta-259414
Beta-260150
Beta-260151
Beta-260152
Beta-260153
Beta-260154
Beta-260155
Beta-260156
Beta-272225
Beta-272226
Beta-272227
Beta-272228
SBR, Searles, Salt Wells Valley
SBR-12390, China Lake
SBR-12391, China Lake
KER, Indian Wells Canyon
KER, Indian Wells Valley, IK-03
KER, Indian Wells Valley, T1
KER, Indian Wells Valley, T2
KER, Indian Wells Valley, T5
KER, China Lake, Core SB01
KER, China Lake, Core SB01
KER, Beacon Solar/Cantil
KER, Beacon Solar/Cantil
KER, China Lake, Core SB05
INY, Rose Valley flat
INY, Rose Valley, Cinder flat
INY, Rose Valley, Lava end
INY, Rose Valley, Lava end
INY, Rose Valley, Lava end
INY, Rose Valley, Lava end
INY, Rose Valley, Dead Chevy
KER, Indian Wells Canyon
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
Lake/Playa
Lake/Playa
Lake/Playa
Fan
Fan
Fan
Fan
Fan
Lake/Playa
Lake/Playa
Fan/Floodplain
Fan/Floodplain
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Fan
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Surface lacustrine
Lacustrine
Lacustrine
Buried soil
Buried soil
Buried soil
Buried soil
Buried soil
Buried Lacustrine
Buried soil
Buried soil
Buried soil
Buried Lacustrine
Surface deposit
Buried deposit
Buried soil
Buried deposit
Buried deposit
Buried soil
Buried soil
Buried soil
Buried spring/soil
Buried soil
Buried soil
Beta-280679
KER, China Lake, Core 9
Floodplain/Playa
Buried alluvium
Core 9, 6Cg, pale olive silty clay, distal fan, slough, or playa above coarse beach deposit
Natural Organic sediment
Beta-280680
Beta-280681
Beta-280682
Beta-280683
Beta-280684
Beta-280685
KER, China Lake, Core 9
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
SBR, China Lake, tufa knoll
INY, Rose Valley, north pit
INY, Rose Valley, south pit
Floodplain/Playa
Floodplain/Arroyo
Floodplain/Arroyo
Lake/Playa
Floodplain
Lake/Playa
Buried alluvium
Buried soil
Buried soil
Surface lacustrine
Buried alluvium
Buried playa
Natural
Natural
Natural
Natural
Natural
Natural
Beta-280686
SBR, Searles, Salt Wells Valley
Lake/Playa
Surface lacustrine
Beta-280734
Beta-280735
Beta-280993
Beta-281207
Beta-281208
C-0599
C-0894
CAMS-?
CAMS-?
CAMS-?
CAMS-?
KER, Indian Wells, Little Dixie
KER, Indian Wells Canyon
KER, Dove Springs Wash
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
NV, Leonard Rockshelter
SBR, Searles Lake, Core 129
INY, Owens Valley, playa
INY, Owens Valley, playa
INY, Owens Valley, playa
INY, Owens Valley, playa
Floodplain/Arroyo
Fan
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Buried soil
Buried soil
Buried soil
Buried soil
Buried soil
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
CAMS-?
INY-0019/20, Panamint, Lake Hill
Lake/Playa
Buried spring
CAMS-?
CAMS-000078
CAMS-000080
CAMS-000081
CAMS-000082
CAMS-000085
CAMS-000092
CAMS-000094
CAMS-000095
CAMS-000096
CAMS-000097
CAMS-004657
INY, Panamint Valley
NV, Fish Lake, Leidy Creek
NV, Fish Lake, Leidy Creek
NV, Fish Lake, Leidy Creek
NV, Fish Lake, Leidy Creek
NV, Fish Lake, Leidy Creek
NV, Fish Lake, Leidy Creek
NV, Fish Lake, Leidy Creek
NV, Fish Lake, Leidy Creek
NV, Fish Lake, Leidy Creek
NV, Fish Lake, Leidy Creek
INY, Owens Valley, Core OL90-2
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Surface lacustrine
Buried marsh
Buried marsh
Buried soil
Buried soil
Buried soil
Buried marsh
Buried marsh
Buried marsh
Buried marsh
Buried marsh
Buried lacustrine
Core 9, 11Cg, olive gray near-shore sand below coarse beach deposit
Local 4, Auger 1, T-3(?) terrace, 3Ab horizon
Local 4, Auger 1, T-3(?) terrace, 7Ab horizon
Algal tufa on granitic bedrock knoll W of lake outlet
RV-NCTP-3Cu Strat. II, within coarse channel facies
RV-SCTP-4Ob Strat. II, lower playa, east side
Beach deposit of sand, marl, and Anodonta shells perched on bedrock outcrop below China
Lake outlet in Searles Lake basin
Local 4, Auger 1, T-3(?) terrace, 5Ab horizon
Profile IK-01, 6Ob, thin peaty layer near terrace base
DSW-L#5771-5Ab Strat. X (IX in field)
Local 5, Freeman Gulch fan, left bank, 3Ab, with flaketool near base of 3Cu
Local 5, Freeman Gulch fan, left bank, 4Ab, below flaketool in 3Cu
Bat guano lying directly on sand/gravel beach at 4,175 ft, underlain by UCLA-298
Core 129, sub by W.A. Gale of American Potash and Chemical Co., Whittier, CA
Owens Playa
Owens Playa
Owens Playa
Owens Playa
Lake Hill Basin auger, base of black mat with many snails and ostracodes, transition from lake
to spring; same site as Davis 1970
Reefal tufa with encased gastropods on Lake Hill bedrock (Site 1)
Core 1.2
Core 2.6
Core 3.6, A horizon
Core 2.7, A horizon
Core 4.12, A horizon
Core 7.4
Core 7.6
Core 7.7
Core 7.7
Core 7.8
Core OL90-2
Page 5 of 10
1
Natural Shell-f (Anodonta)
1 11700
100 13338 13556 13776 Kaldenberg 2006; Rogers 2009
Natural Shell-f (Anodonta)
1 12110
70 13786 13957 14148 Kaldenberg 2006; Rogers 2009
Natural Shell-f (Anodonta)
1 13470
70 16254 16645 16901 Kaldenberg 2006; Rogers 2009
Charcoal (wood)
Shell-f (Anodonta)
Shell-f (gastropod)
Soil (SOM)
Soil (SOM)
Soil (SOM)
Soil (SOM)
Soil (SOM)
Organic sediment
Soil (SOM)
Soil (SOM)
Soil (SOM)
Organic sediment
Organic sediment
Organic sediment
Organic sediment
Organic (black mat)
Organic (black mat)
Organic sediment
Soil (SOM)
Soil (SOM)
Shell-f (gastropod, Fossaria?)
Soil (SOM)
Soil (SOM)
Organic sediment
Soil (SOM)
Soil (SOM)
Carbonate (tufa)
Organic sediment
Organic sediment
Natural Shell-f (gastropod)
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Soil (SOM)
Organic sediment
Soil (SOM)
Soil (SOM)
Soil (SOM)
Organic (coprolite)
Organic sediment (mud)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
1
15
15
270
115
130
55
70
5258
6371
150
220
3079
15
70
60
165
180
50
90
300
175
198
270
350
13130
14390
8790
2790
9100
4510
2510
16250
12160
12730
9490
180
7320
9180
4440
9410
8120
6770
9720
9750
10000
9610
10120
427
9690
1064
155
268
1
255
470
14610
9930
10450
11110
8790
11560
1 11550
210
373
107
233
285
0
2246
-
10510
10240
4230
6990
6340
11199
10494
9700
10450
11280
12850
Natural Shell-f (gastropod)
312 12575
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
1
148
413
469
464
896
236
423
474
526
573
711
Carbonate (tufa/gastropod)
Peat (silt)
Organic sediment (clay)
Soil (SOM)
Soil (SOM)
Soil (SOM)
Organic sediment (silt)
Organic sediment (silt)
Peat
Peat
Organic sediment (silt)
Organic sediment (marl)
11550
3990
8810
8900
9630
9900
5780
9440
10130
11380
12330
11140
60
40
80
70
40
60
40
40
40
80
70
70
50
40
80
100
80
100
100
100
100
50
60
50
60
511
313
15233
17164
9627
2766
10194
5039
2458
19215
13788
14672
10640
131
7994
10184
4867
10372
8703
7458
10742
11088
11262
10766
11590
588
Source Reference
Cultural Shell-m (Haliotis)
Cultural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
560
Upper 2-Sigma cal BP
Type
Cal BP (med. prob.)
Location, Provenience, and/or Description
RLK # AMP-03, "in Salt Wells Valley west of road between CLP and ammunition storage
areas, near high-water overflow between lakes"
RLK # AMP-04, "in Salt Wells Valley west of road between CLP and ammunition storage
areas, near high-water overflow between lakes"
RLK # AMP-05, "in Salt Wells Valley west of road between CLP and ammunition storage
areas, near high-water overflow between lakes"
RLK #AMP-06, "in Salt Wells Valley west of road between CLP and ammunition storage
areas, near high-water overflow between lakes"
RLK # AMP-07, wood ash from under roasting pit
Parcel 18, test unit
Parcel 16, test unit, snail shell
Profile IK-01, 2Ab buried terrace locality
Profile IK-03, median fan locality
Trench 1, medial fan buried surface
Trench 2, medial-distal fan buried surface
Trench 5, distal plain locality
Bore Hole TTIWV-SB01
Bore Hole TTIWV-SB01
Pine Tree Wash, Stratum 2
TL3, Stratum 3
Bore Hole TTIWV-SB05
Auger 2, Rose Valley Flat
Auger 4, Cinder Flat
Column Sample, Lava End; 2Ab horizon below Cartago soil
Column Sample, Lava End; black mat below Cartago soil
Column Sample, Lava End; black mat below Cartago soil
Lava End Rose Valley Flat; 2Ab horizon below Cartago soil
Auger 7, Dead Chevy Flat, 2Ab
Profile IK-01, 3Ab soil near base of cutbank
Locality 1, cutbank along west side of wash, 2Ab
Locality 1, cutbank along west side of wash, 2Ab
Locality 1, cutbank along west side of wash, 3Ab
Lower 2-Sigma cal BP
Dated Deposit
1-Sigma Error (±)
Deposit or
Landform
14C BP (CRCY)
State/County, Site/Locality
AVE Depth cm
Lab or Sample No.
Appendix C: China Lake Radiocarbon Database Listed by (1) Lab/Sample No., (2) Source Reference, and (3) State/County
399
15939
17504
9811
2897
10246
5163
2587
19416
14008
15095
10760
176
8129
10369
5074
10656
9065
7627
11097
11190
11486
10944
11746
655 Kaldenberg 2006; Rogers 2009
495
16518
17849
9939
3039
10300
5310
2743
19583
14224
15562
10871
230
8323
10588
5295
10887
9321
7797
11289
11250
11722
11167
11988
Kaldenberg 2006; Rogers 2009
Byrd 2007
Byrd 2007
China Lake Legacy project 718
Young 2007
Young 2007
Young 2007
Young 2007
China Lake Legacy project 718
China Lake Legacy project 718
Young 2009
Young 2009
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
50 11067 11123 11225 China Lake Legacy project 718
50
40
40
50
40
50
17501
11235
12202
12773
9627
13276
17780
11324
12387
13000
9811
13395
18026
11410
12549
13138
9939
13567
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
50 13267 13387 13537 China Lake Legacy project 718
50
50
40
40
40
570
560
60
60
60
60
12375
11758
4685
7718
7168
11332
9798
10036
10897
12246
13790
12473
11984
4753
7827
7273
13082
11270
10218
11133
12456
13961
12610
12142
4861
7882
7331
14451
12688
10418
11246
12627
14152
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
Fergusson and Libby 1964
Libby 1954; Flint and Gale 1959
Benson et al. 1997; Bacon et al. 2006
Benson et al. 1997; Bacon et al. 2006
Benson et al. 1997; Bacon et al. 2006
Benson et al. 1997; Bacon et al. 2006
40 14489 14833 15174 Jayko et al. 2005, 2008
70
70
80
80
80
80
80
80
140
90
200
70
13256
4239
9602
9736
10740
11187
6405
10491
11248
13096
13815
12001
13392
4466
9866
10006
10962
11345
6580
10693
11752
13248
14378
12267
13602
4646
10168
10222
11200
11628
6749
10883
12238
13407
15008
12557
Jayko et al. 2008
Throckmorton and Reheis 1993
Throckmorton and Reheis 1993
Throckmorton and Reheis 1993
Throckmorton and Reheis 1993
Throckmorton and Reheis 1993
Throckmorton and Reheis 1993
Throckmorton and Reheis 1993
Throckmorton and Reheis 1993
Throckmorton and Reheis 1993
Throckmorton and Reheis 1993
Bischoff, Stafford, and Meyer 1997
Material Dated
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Surface lacustrine
Buried lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Buried lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL90-2
Core OL84B
Core OL84B
Core OL84B
Core OL84B
Core OL84B
Core OL84B
Core OL84B
Core OL84B
Core OL84B
Core OL84B
Core OL84B
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
?
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
CAMS-098308
INY, Owens Valley, Willow Dip
Lake/Playa
Buried lacustrine
Maximum age of sand-tufa berm from lake highstand, Willow Dip Arroyo wall; w/obsidian flake
Natural Carbonate (tufa)
DE-239
DE-240
DIC-2824
ETH-(4 dates)
ETH-0?
ETH-0?
ETH-0?
ETH-0?
ETH-0?
ETH-0?
ETH-0?
ETH-0?
ETH-0?
ETH-3187
ETH-5268
ETH-5270
GaK-01425
GaK-01854
GaK-02486
INY, Franklin Lake
INY, Franklin Lake
SBR, Silver Lake
NV, Yucca Mtn, Crater Flat
SBR, Searles, Navy Road
SBR, Searles, Poison Canyon
SBR, Searles, Poison Canyon
SBR, Searles, Poison Canyon
SBR, Searles, Poison Canyon
SBR, Searles, Poison Canyon
SBR, Searles, Poison Canyon
SBR, Searles, Poison Canyon
SBR, Searles, Poison Canyon
NV, Yucca Mtn, Crater Flat
NV, Yucca Mtn, Crater Flat
NV, Yucca Mtn, Crater Flat
MNO, Adobe Valley, S.R. 120
MNO, Adobe Valley, S.R. 120
MNO, Adobe Valley, S.R. 120
Lake/Playa
Lake/Playa
Lake/Playa
Fan
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Fan
Fan
Fan
Lake/Playa
Lake/Playa
Lake/Playa
Buried lacustrine
Buried lacustrine
Surface deposit
Surface deposit
Lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Surface deposit
Surface deposit
Surface deposit
Buried marsh
Buried marsh
Buried marsh
Well 10
Well GS-8
Northwest Silver Lake, El Capitan BR II
Pooled mean in-age of Little Cones unit, Calib 5.01
Dry wash W of Navy-Randsburg Rd, SL93-12
Strat. C3c
Strat. C3b
Strat. C2
Strat. C2, shell with sand
Strat. C3a
Strat. C1a
Strat. C1c
Surface location, SL93-21
Min-age of Little Cones unit, CFP-26
Min-age of Little Cones unit, JWB-38
Min-age of Little Cones unit, JWB-41
Core 2, southeast Black Lake, peat near base of Core
Black lake Bog, Core 4, peat below diatamceous clay at base of Core
Core 2, southeast Black Lake, peat below Ash 5
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Page 6 of 10
Carbonate (oolites)
Carbonate (oolites)
Carbonate (oolites)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Carbonate (oolites)
Carbonate (oolites)
Carbonate (oolites)
Carbonate (oolites)
Carbonate (oolites)
Carbonate (oolites)
Carbonate (oolites)
Carbonate (oolites)
Carbonate (oolites)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Organic sediment?
Organic sediment?
Shell-f (Anodonta)
Organic (rock varnish)
Carbonate (tufa)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Shell-f (Anodonta?)
Shell-f (Anodonta?)
Organic sediment (marl)
Organic sediment (marl)
Organic sediment (marl)
Organic (rock varnish)
Organic (rock varnish)
Organic (rock varnish)
Peat
Peat
Peat
372
402
512
721
527
599
523
480
480
465
382
382
429
429
502
502
537
594
567
479
558
732
789
853
907
913
558
709
725
829
80
116
54
70
57
40
52
105
50
50
50
50
-
2990
3060
4760
11360
8930
9980
8280
4970
4980
4330
3750
3950
3800
4070
4680
4680
12570
13680
13080
9170
9520
9680
11520
12650
13360
13270
9540
10050
10870
12230
10150
12960
9640
10090
9990
10100
10250
12900
7910
8960
9550
9460
480
520
480
9660
70
70
80
70
70
70
120
70
70
100
70
70
60
60
80
100
80
70
60
60
60
60
60
70
70
70
60
50
50
50
40
50
40
40
40
40
40
50
40
50
40
40
40
50
40
40
Upper 2-Sigma cal BP
Type
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Cal BP (med. prob.)
Location, Provenience, and/or Description
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL90-2
INY, Owens Valley, Core OL84B
INY, Owens Valley, Core OL84B
INY, Owens Valley, Core OL84B
INY, Owens Valley, Core OL84B
INY, Owens Valley, Core OL84B
INY, Owens Valley, Core OL84B
INY, Owens Valley, Core OL84B
INY, Owens Valley, Core OL84B
INY, Owens Valley, Core OL84B
INY, Owens Valley, Core OL84B
INY, Owens Valley, Core OL84B
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
Lower 2-Sigma cal BP
Dated Deposit
CAMS-004662
CAMS-004663
CAMS-004664
CAMS-004671
CAMS-004672
CAMS-004675
CAMS-006310
CAMS-006314
CAMS-006315
CAMS-006316
CAMS-006317
CAMS-006318
CAMS-006319
CAMS-006320
CAMS-006326
CAMS-006327
CAMS-013469
CAMS-013470
CAMS-013527
CAMS-020025
CAMS-020026
CAMS-020027
CAMS-020028
CAMS-020218
CAMS-020219
CAMS-021541
CAMS-022388
CAMS-059870
CAMS-059871
CAMS-059872
CAMS-076411
CAMS-076412
CAMS-076413
CAMS-076414
CAMS-076415
CAMS-076416
CAMS-076417
CAMS-076418
CAMS-076419
CAMS-076420
CAMS-076421
CAMS-076422
CAMS-076423
CAMS-076424
CAMS-076425
CAMS-076426
1-Sigma Error (±)
Deposit or
Landform
14C BP (CRCY)
State/County, Site/Locality
AVE Depth cm
Lab or Sample No.
Appendix C: China Lake Radiocarbon Database Listed by (1) Lab/Sample No., (2) Source Reference, and (3) State/County
2973
3067
5315
12346
9036
10289
8147
5594
5600
4787
3903
4217
4073
4422
5278
5257
13439
15064
14023
9369
9744
9997
12567
13571
14419
14209
9776
10450
11390
13205
11684
15084
10786
11403
11268
11593
11818
15024
8599
9916
10916
10576
475
497
475
11066
3175
3267
5491
12547
9256
10508
8422
5712
5722
4935
4116
4396
4194
4580
5415
5407
13678
15514
14380
9502
9991
10196
12673
13769
14895
14704
10015
10578
11755
13349
11829
15514
10981
11675
11454
11705
12006
15401
8731
10086
10927
10698
520
543
520
11094
3356
3410
5612
12698
9433
10672
8746
5797
5799
5148
4299
4578
4410
4714
5594
5601
13867
16251
14915
9682
10178
10393
12859
13967
15227
15115
10194
10744
12001
13483
11999
16185
10974
11826
11624
11835
12132
15948
8798
10094
11089
10789
556
567
556
11199
65
5580
35
6297
6359
1220
1100
5
1
1
1
1
1
1
1
1
1
1
1
1
1
534
614
324
13100
12350
11530
9164
12070
11200
12200
12300
11770
11970
12900
13200
13800
10180
8425
11135
11350
8550
5230
150
180
95
111
100
100
100
100
100
100
100
100
95
540
140
210
350
210
110
15158
13873
13189
10229
13703
12010
13119
13218
13392
13575
13749
14119
15170
11168
9286
12884
12569
9087
5839
15877
14436
13381
10335
13926
12347
13327
13418
13615
13827
14033
14579
15803
11875
9444
13043
13220
9575
6013
Source Reference
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Bischoff, Stafford, and Meyer 1997
Benson et al. 1997, 2002
Benson et al. 1997, 2002
Benson et al. 1997, 2002
Benson et al. 1997, 2002; Mensing 2001
Benson et al. 1997, 2002; Mensing 2001
Benson et al. 1997, 2002; Mensing 2001
Benson et al. 1997, 2002; Mensing 2001
Benson et al. 1997, 2002; Mensing 2001
Benson et al. 1997, 2002; Mensing 2001
Benson et al. 1997, 2002; Mensing 2001
Benson et al. 1997, 2002; Mensing 2001
Benson et al. 1997, 2002; Mensing 2001
Benson et al. 1997, 2002; Mensing 2001
Benson et al. 1997, 2002; Mensing 2001
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
Owens et al. 2007
6413 Stine in Bryd and Hale 2003
16586
15079
13629
10441
14185
12608
13527
13695
13828
14059
14565
15079
16460
12782
9537
13217
13943
10171
6220
RCJ 1988
RCJ 1988
Wells et al. 2003
Peterson et al. 1995
Lin et al. 1998
Lin et al. 1998
Lin et al. 1998
Lin et al. 1998
Lin et al. 1998
Lin et al. 1998
Lin et al. 1998
Lin et al. 1998
Lin et al. 1998
Peterson et al. 1995
Peterson et al. 1995
Peterson et al. 1995
Batchelder 1970
Batchelder 1970
Batchelder 1970
Material Dated
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried soil
Buried lacustrine
Buried soil
Buried lacustrine
Buried lacustrine
Buried lacustrine
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Lower Salt, 070-80 cm above base of, suspect date
Lower Salt, 168-177 cm above base of
Lower Salt, 021-24 cm below top of
Lower Salt, 240-250 cm below top of
Strong paleosol, single (trench?), datum 2184 ft
Stake 1, Trench 2, "flaggy sandstone" w/artifacts ~15 cm above
Stake 1, Trench 3, stratum A-1 (3ABKb), w/sandblasted flakes, suspect per Davis
Stake 1, Trench 3, stratum A-2, "flaggy sandstone" with artifacts
Stake 1, Trench 3, stratum B, no associated artifacts, younger than overlying date
Stake 1, Trench 3, stratum C, overlies upper artifact layer, marks late lake retreat
Site 1, beside Collection Area A, Mammoth #6, Basalt Ridge
Neotoma sp. fecal pellets
Neotoma sp. fecal pellets
Miscellaneous twigs and midden debris
Neotoma sp. fecal pellets
Miscellaneous twigs
Miscellaneous twigs
Wood (Juniperus sp. twigs/seeds)
Miscellaneous twigs
Wood (Juniperus sp. twigs/seeds)
Miscellaneous twigs
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
GX-10417
SBR, Calico Lakes-site?
Lake/Playa
Buried deposit
Extinct large mammal, mole, and fish bones, SBCM locality 1.76.35 (Calico Lakes Phase I)
Natural Bone (apatite)
GX-10418
SBR, Calico Lakes-site?
Lake/Playa
Buried deposit
Extinct large mammal, mole, and fish bones, SBCM locality 1.76.35 (Calico Lakes Phase I)
Natural Charcoal
GX-10420
GX-10421
GX-12275
GX-12276
I-0?
I-0?
SBR, Solid Waste
SBR, Luz Foundation
MNO, White Mountains
INY, Volcanic Tableland
KER, China Lake, Core SB03
KER, China Lake, Core SB14
Lake/Playa
Lake/Playa
Hill/Ridge
Cave/Shelter
Lake/Playa
Lake/Playa
Buried deposit
Buried deposit
Surface deposit
Surface deposit
Buried lacustrine
Buried lacustrine
Fossil mole bones, SBCM locality 1.76.33 (Solid Waste site)
Fossil horse and small vertebrates recovered in deposits above sample
Falls Canyon 2 site
Neotoma sp. fecal pellets
Bore Hole TT37-SB03
Bore Hole TTIWV-SB14
Natural
Natural
Natural
Natural
Natural
Natural
I-0?
KER, China Lake, Core SB23
Lake/Playa
Buried lacustrine
Bore Hole TTIWV-SB23, several hundred ft SW of G-1 Tower Rd along old B-29 cutoff rd.
Natural Organic sediment
5044 18690
I-0?
I-0?
I-0?
I-0?
KER, China Lake, Core SB27
KER, China/Mirror Lake, SB10
SBR, China Lake, SL-01
SBR, Searles, Salt Wells Valley
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Buried lacustrine
Buried lacustrine
Buried lacustrine
Lacustrine
Bore Hole TTIWV-SB27
Bore Hole TTIWV-SB10, southwest of Mirror lake
TT43-SL01 in lower lake basin; from near-shore death assemblage
SWV, from base of large tufa tower below east slope of Lone Butte
Natural
Natural
Natural
Natural
3199
8992
159
1
I-0?
SBR, Silver Lake
Lake/Playa
Surface lacustrine
Gravel Pit in NE 1/4 of Sec. 29 3.2 km W of SL Junction, unreported date per H.C. Smith
Natural Shell-f (Anodonta)
25 12820
Natural Shell-f (Anodonta)
173 12820
I-00443
SBR, Silver Lake
I-00444
SBR, Silver Lake
Lake/Playa
Surface lacustrine
I-03690
I-07342
SBR, Clark Mountain
KER, Koehn Lake/Garlock Flt.
Cave/Shelter
Lake/Playa
Surface deposit
Surface lacustrine
I-07717
KER, Koehn Lake/Garlock Flt.
Lake/Playa
Buried lacustrine
MNO, Mono Basin, Wilson Creek
Lake Basin
Buried lacustrine
LJ-0200
SBR, Silver Lake
Lake/Playa
Surface lacustrine
LJ-0932
LJ-0933
LJ-0958
LJ-0977
SBR, Silver Lake
SBR, Silver Lake
SBR, Coyote Lake
INY-0019/20, Panamint, Lake Hill
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Surface lacustrine
Buried lacustrine
Surface lacustrine
Surface lacustrine
LJ-935
SBR, Silver Lake
Lake/Playa
Surface lacustrine
SBR, Valley Wells
SBR, Valley Wells
SBR, Valley Wells
SBR, Valley Wells
SBR, Blackhawk Landslide
INY, Owens Lake, south
Spring mound
Spring mound
Spring mound
Spring mound
Pond
Lake/Playa
Fossil spring
Fossil spring
Fossil spring
Fossil spring
Surface deposit
Buried lacustrine
L-?
nr
nr
nr
nr
nr
OS-72583
Lake/Playa
Buried lacustrine
Upper of two shell layers exposed in gravel quarry in NE 1/4 of Sec. 29 3.2 km W of SL
Junction
Upper of two shell layers exposed in gravel quarry in NE 1/4 of Sec. 29 3.2 km W of SL
Junction
Wood (Pinus monophylla)
From offset beach ridge on Garlock Fault
Carbonate-cemented layer in test pit on crest of 1st spur near bifurcation of gravel bar on
Garlock Fault
Type section cutbank along Wilson Creek
Gravel Pit in NE 1/4 of Sec. 29 3.2 km W of SL Junction, collected by Woodward of Union Oil
Co; associated with Lake Mojave points
Gravel Pit in NE 1/4 of Sec. 29 3.2 km W of SL Junction
Gravel Pit in NE 1/4 of Sec. 29 3.2 km W of SL Junction
From shoreline NE of Coyote Lake (playa)
West side of Lake Hill, lowest shoreline, with stone tools
Wave-rounded tufa 30 cm above upper shell bed in gravel Pit in NE 1/4 of Sec. 29 3.2 km W
of SL Junction
From light brown silt unit that caps Unit E2
From light brown silt unit that caps Unit E2
Organic-rich clay in Unit E2
Organic-rich clay in Unit E2
Freshwater pond formed on landslide debris
5Cg, Strat II, upper lacustrine in E wall of gully
Page 7 of 10
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (nodule)
Organic sediment
Organic sediment
Organic sediment
Organic sediment
Organic sediment
Organic sediment
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Charcoal
Charcoal
Packrat Midden
Packrat Midden
Organic sediment
Organic sediment
Organic sediment
Organic sediment
Shell-f (gastropod)
Organic sediment (marl)
Natural Shell-f (Anodonta)
Natural Packrat Midden
Natural Carbonate (tufa)
2575
3437
2523
2745
85
100
100
180
68
5
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
30770
31420
22290
25270
12170
5975
10275
6775
9360
2465
10800
10460
9515
10090
10325
7930
8925
8905
10555
10690
8330
9455
9090
11210
13060
10230
Natural Carbonate (tufa)
Shell-f (gastropod)
Shell-f (gastropod)
Organic sediment
Organic sediment
Shell-f (freshwater)
Soil (SOM)
Source Reference
Flint and Gale 1959; Stuiver 1964
Flint and Gale 1959; Stuiver 1964
Flint and Gale 1959; Stuiver 1964
Flint and Gale 1959; Stuiver 1964
Davis 1978
Davis 1978
Davis 1978
Davis 1978
Davis 1978
Davis 1978
Davis 1978
Spaulding 1980
Spaulding 1980
Spaulding 1983
Spaulding 1983
Spaulding 1980
Spaulding 1980
Spaulding 1980
Spaulding 1980
Spaulding 1980
Spaulding 1980
Woodcock, 1986
Woodcock, 1986
Woodcock, 1986
Woodcock, 1986
Woodcock, 1986
177
9050
350
12210
10910
7810
9830
16480
14690
430
425
450
280
80
70
40
17380
18280
14060
13040
9670
1 12460
1 11030
225 13300
Natural
Natural
Natural
Natural
Natural
Natural
36312
36987
27681
30528
14995
7174
12547
8164
11629
2949
13318
12966
11237
12658
12920
9474
11093
10705
12909
13189
9914
11752
11092
13881
16923
12714
337
308
1
1
1790
3642
213
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Carbonate (tufa)
35362
35864
26861
30044
14138
6826
12023
7645
10633
2531
12669
12189
10830
11706
12013
8822
10037
9992
12380
12531
9275
10757
10246
13079
15703
11900
900 13063 15295 17659 Reynolds & Reynolds 1985; Reheis et al. 2007
Natural Carbonate (tufa)
Natural
Natural
Natural
Natural
34689
34741
26187
29532
13632
6463
11402
7166
9552
2104
11768
11236
10294
10646
11082
8281
9239
9409
11711
11704
8591
9887
9534
12372
14110
11070
289 12800
Natural Crustacean (ostracodes)
Natural Shell-f (Anodonta)
400
600
200
230
200
150
165
260
365
180
310
330
185
380
350
285
360
265
210
280
250
310
300
380
460
320
Upper 2-Sigma cal BP
Type
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cal BP (med. prob.)
Location, Provenience, and/or Description
SBR, Searles Lake, Core X-20
SBR, Searles Lake, Core X-20
SBR, Searles Lake, Core X-20
SBR, Searles Lake, Core X-20
KER, China Lake, Stake 24
KER, China Lake, Stake 1
KER, China Lake, Stake 1
KER, China Lake, Stake 1
KER, China Lake, Stake 1
KER, China Lake, Stake 1
INY-5825, Basalt Ridge, sediment
SBR, Marble Mountains
SBR, Marble Mountains
SBR, Marble Mountains
SBR, Marble Mountains
SBR, Marble Mountains
SBR, Marble Mountains
SBR, Marble Mountains
SBR, Marble Mountains
INY, Horse Thief Hills
INY, Eureka View
INY, Death Valley
INY, Death Valley
INY, Death Valley
INY, Death Valley
INY, Death Valley
Lower 2-Sigma cal BP
Dated Deposit
Gro-1802
Gro-1805
Gro-1808
Gro-1814
GX-03119
GX-03441
GX-03442
GX-03443
GX-03444
GX-03445
GX-03446
GX-06178
GX-06180
GX-06182
GX-06183
GX-06185
GX-06186
GX-06188
GX-06189
GX-06217
GX-06231
GX-07804
GX-07805
GX-07806
GX-07807
GX-07812
1-Sigma Error (±)
Deposit or
Landform
14C BP (CRCY)
State/County, Site/Locality
AVE Depth cm
Lab or Sample No.
Appendix C: China Lake Radiocarbon Database Listed by (1) Lab/Sample No., (2) Source Reference, and (3) State/County
40
9505
9310
40 9930
173 13340
1 13470
1 12670
10
9422 10199 11198 Reynolds & Reynolds 1985; Reheis et al. 2007
13190
11601
7704
10494
19419
17579
14357
12750
8716
11315
19592
17870
15931
13677
9677
12220
19636
18069
Reynolds & Reynolds 1985; Reheis et al. 2007
Reynolds & Reynolds 1985; Reheis et al. 2007
Jennings and Elliot-Fisk 1990(?)
Jennings, 1996
Couch Appendix B in Tetra Tech EM Inc. 2003
Couch Appendix B in Tetra Tech EM Inc. 2003
60 22114 22308 22483 Couch Appendix B in Tetra Tech EM Inc. 2003
50
60
50
120
20345
21490
16866
13893
20723
21824
17098
14346
21141
22154
17447
14965
Couch Appendix B in Tetra Tech EM Inc. 2003
Couch Appendix B in Tetra Tech EM Inc. 2003
Couch Appendix B in Tetra Tech EM Inc. 2003
Couch Appendix B in Tetra Tech EM Inc. 2003
350 14080 15346 16635 Hubbs et al. 1962; Wallace and DeCosta 1964
240 14223 15348 16448 Hubbs, Bien, and Suess 1965 (RCJ); Ore and Warren 1971
300 10238 11048 12025 Hubbs, Bien, and Suess 1965 (RCJ); Ore and Warren 1971
190 13926 14575 15195 Mehringer and Ferguson, 1969
160 12621 12918 13222 LaJoie card file (USGS-EQ 14)
160 10386 10822 11221 LaJoie card file (USGS-EQ 30)
500 14184 15991 17246 LaJoie 1968
Hubbs et al. 1962; Wallace and DeCosta 1964; Meighan 1965; Ore
9902 10554 11219
and Warren 1971
400 10395 11486 12590 Ore and Warren 1971; Wells et al. 1989
550 14174 16022 17512 Ore and Warren 1971; Wells et al. 1989
600 14199 16183 17790 Hubbs, Bien, and Suess 1965 (RCJ)
700 13280 15115 16974 Hubbs, Bien, and Suess 1965 (RCJ)
240
8830
400
8989
- 7930
- 8630
- 9650
- 10780
45 17070
185 9310
50
60
50
40
550
50
8628
9493
10784
12570
19203
10371
9931 11107 Hubbs et al. 1965
8778
9601
11011
12661
20358
10514
8983
9744
11198
12791
21569
10609
Pigati and Miller 2008
Pigati and Miller 2008
Pigati and Miller 2008
Pigati and Miller 2008
Stout 1977
Meyer, Rosenthal, and Young 2010
INY, Owens Lake, south
INY, Owens Lake, south
Lake/Playa
Lake/Playa
Buried lacustrine
Buried lacustrine
OS-72826
INY, Owens River Bluff
Floodplain
Buried soil
INY, Owens Lake, south
KER, Dove Springs Wash
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
INY, Rose Valley, north pit
INY, Rose Valley, north pit
KER, Indian Wells, Little Dixie
KER, Indian Wells, Little Dixie
INY, Rose Valley, south pit
SBR, Solar One
SBR, Searles Lake, Core X-16
SBR, Searles Lake, Core X-16
RIV, Lake Elsinore
RIV, Lake Elsinore
RIV, Lake Elsinore
Lake/Playa
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain/Arroyo
Floodplain
Floodplain
Floodplain/Arroyo
Floodplain/Arroyo
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Buried soil
Buried soil
Buried soil
Buried soil
Buried soil
Buried alluvium
Buried soil
Buried soil
Buried soil
Buried soil
Surface deposit
Buried lacustrine
Buried lacustrine
Submerged lacustrine
Submerged lacustrine
Submerged lacustrine
UCLA-0298
NV, Leonard Rockshelter
Lake/Playa
Buried lacustrine
UCLA-0510
NV, Las Vegas Vly, Tule Springs
Floodplain/Arroyo
Buried alluvium
UCLA-0512
NV, Las Vegas Vly, Tule Springs
Floodplain/Arroyo
Buried channel-mat
UCLA-0521
NV, Las Vegas Vly, Tule Springs
Floodplain/Arroyo
Buried channel
UCLA-0522
NV, Las Vegas Vly, Tule Springs
Floodplain/Arroyo
Buried channel-mat
UCLA-0529
NV, Las Vegas Vly, Gilcrease Ranch
Spring Mound
Buried spring
UCLA-0530
NV, Corn Creek Flat
Spring Mound
Buried spring
UCLA-0537
NV, Las Vegas Vly, Gilcrease Ranch
Spring Mound
UCLA-0541
UCLA-0542
NV, Corn Creek Flat
NV, Corn Creek Flat
Spring Mound
Spring Mound
UCLA-0548
NV, Las Vegas Vly, Ellington Scarp
UCLA-0549
UCLA-0550
UCLA-0551
UCLA-0755
UCLA-0757
NV, Las Vegas Vly, Ellington Scarp
NV, Las Vegas Vly, Ellington Scarp
NV, Las Vegas Vly, Ellington Scarp
INY, Death Valley, Pyramid Peak
SBR, Negro Butte
UCLA-0989
OS-72855
OS-79560
OS-79563
OS-79564
OS-79565
OS-79566
OS-79583
OS-79584
OS-79585
OS-79587
QC-0937
RC/SM-36
RC/SM-50
UCIAMS-10336
UCIAMS-10337
UCIAMS-10338
UCLA-0990
UCLA-1093A
UCLA-1093B
UCLA-1093C
UCLA-1093D
UCLA-1093E
UCLA-1800
UCLA-1911A
UCLA-1911B
UCLA-2601
UCLA-2609
UCLA-2609A
UCLA-2609B
UCR-01143
UCR-0149
UCR-0181
UCR-0185
UCR-0186
UCR-0187
UCR-0249
UCR-0347
UCR-2323
Material Dated
Upper 2-Sigma cal BP
Type
Cal BP (med. prob.)
Location, Provenience, and/or Description
6Cg, Strat I, lower lacustrine in E wall of gully
2Cg, uppermost buried lacustrine shell/death bed, south lakeshore
2Cu, carbon layer, S bank of T3 terrace below sand layer mapped as Mazourka-Eclipse; same
age as lithofacies 4a of Bacon
3Ab, Strat. IV, E wall of gully, stratum underlies buried hearth
DSW-L#5771-13Ab Strat. I (-I in field), basal unit
LDW-L#3-4Ab Strat. IV, with snails, west bank
LDW-L#3-6Ab Strat. II, west bank
LDW-L#3-7Ab Strat. I, basal unit, west bank
RV-NCTP-3Cu Strat. II, channel facies, north
RV-NCTP-2Ab Strat. III, north wall
LDW-L#3-3Ab Strat. V, with snails, west bank
LDW-L#3-5Ab Strat. III, weak soil, west bank
RV-SCTP-3Ab Strat. III, upper playa, east side
Associated with granitic river sands and lenses of silts (channel deposits?)
Upper Salt, mud seam below top of
Upper Salt, mud seam below top of
Core LESS02-8
Core LESS02-8
Core LESS02-8
Small gastropods (Amnicola sp.) in sandy beach deposit forming base of shelter, overlain by C599
Unit E1, Fenley Hunter Trench Locality 4, fine Charcoal/silt from prairie fire?
Unit E1, Fenley Hunter Trench Locality 4, Charcoal from gray silty clay on gravel; w/small bone
tool and camel bone frags
Unit E1, 17, lower channel fill in gray silty sand on gravel, assoc with mammoth, antelope, and
camel, same context as UCLA-543 shell
Unit E1, Locality 37, Trench 9, Site 5, from lower channel fill in gray silty sand on gravel, assoc
with mammoth, antelope, and camel (burned digging stick?)
Lower 2-Sigma cal BP
Dated Deposit
OS-72584
OS-72752
1-Sigma Error (±)
Deposit or
Landform
14C BP (CRCY)
State/County, Site/Locality
AVE Depth cm
Lab or Sample No.
Appendix C: China Lake Radiocarbon Database Listed by (1) Lab/Sample No., (2) Source Reference, and (3) State/County
Source Reference
Natural Soil (SOM)
Natural Bone (fish)
230
385
9230
7440
55 10250 10396 10522 Meyer, Rosenthal, and Young 2010
75 8154 8263 8395 Meyer, Rosenthal, and Young 2010
Natural Soil (SOM)
155 12650
220 14024 14896 15958 Meyer, Rosenthal, and Young 2010
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Soil (SOM)
Soil (SOM)
Soil (SOM)
Soil (SOM)
Soil (SOM)
Plant (modern roots)
Soil (SOM)
Soil (SOM)
Soil (SOM)
Soil (SOM)
Charcoal
Organic sediment (marl)
Organic sediment (marl)
Organic sediment
Organic sediment
Organic sediment
Natural Shell-f (gastropod)
Natural Charcoal (w/black mat)
Natural Charcoal (w/black mat)
125
440
263
320
350
255
75
203
298
210
60
805
1007
142
301
463
5950
10300
10000
10100
10500
>Mod.
985
9440
10100
9980
7350
10270
11400
6845
8390
12570
40
60
55
55
60
6676
11953
11263
11399
12369
45
95
110
55
115
450
600
25
50
60
788
10479
11271
11250
7968
9764
10777
7615
9290
14429
6778
12102
11482
11697
12454
0
883
10703
11688
11447
8169
10942
12357
7674
9422
14796
6882
12393
11717
11844
12598
971
11099
12058
11645
8377
12320
13722
7722
9502
15163
Meyer, Rosenthal, and Young 2010
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
China Lake Legacy project 718
Reynolds & Reynolds 1985; Reheis et al. 2007
Flint and Gale 1959; Bray and Burke 1960 (RCJ); Smith 1979
Flint and Gale 1959; Bray and Burke 1960 (RCJ); Smith 1979
Kirby, Lund, and Poulsen 2005
Kirby, Lund, and Poulsen 2005
Kirby, Lund, and Poulsen 2005
- 13000 1000 13057 15532 18042 Fergusson and Libby 1964
61
9000 1000
366 12400
8015 10274 12823 Fergusson and Libby 1964
350 13583 14491 15487 Fergusson and Libby 1964
Natural Wood (carbonized)
34 12920
220 14430 15261 15987 Fergusson and Libby 1964; Haynes 1967
Natural Charcoal (w/black mat)
54 13000
200 14765 15377 16057 Fergusson and Libby 1964
Unit E2, 62a, top of Gilcrease Spring
Natural Organic (black mat)
74
Unit E1, 76a, buried by E2 at base/center of Corn Creek Spring
Natural Organic (black mat)
Buried spring
Unit E2, 63a, buried by sand, dates start of spring
Natural Organic (black mat)
9920
150 11075 11449 12026 Haynes 1967
Buried spring
Buried spring
Unit E1, 77a, base of spring mat under gray silt
Unit E2, 75a, base of Corn Creek Spring 8 under gray silt
Natural Organic (black mat)
Natural Organic (black mat)
- 11700
- 10200
250 13092 13566 14081 Haynes 1967
350 11066 11894 12841 Haynes 1967
Spring Mound
Buried spring
Unit E2, 46, spring mat at base of upper E2, below pink/gray silt, assoc w/camel and snail
Natural Wood (carbonized)
-
8000
400
8006
8908
Spring Mound
Spring Mound
Spring Mound
Cave/Shelter
Cave/Shelter
Buried spring
Buried spring
Buried spring
Surface deposit
Surface deposit
Natural
Natural
Natural
Natural
Natural
Organic (black mat)
Organic (black mat)
Organic (black mat)
Packrat Midden
Packrat Midden
- 9520
- 11100
- 9350
1 11600
1 9140
300
200
200
160
140
10119
12764
10178
13164
9907
10844
13036
10603
13467
10331
INY-0020, Panamint, Lake Hill
Lake/Playa
Buried spring/marsh
Natural Organic (black mat)
150 10020
INY-0019, Lake Hill, Panamint Vly
INY-0372, Rose Spring, Locus 1
INY-0372, Rose Spring, Locus 1
INY-0372, Rose Spring, Locus 1
INY-0372, Rose Spring, Locus 1
INY-0372, Rose Spring, Locus 1
KER, China Lake, Mammoth 4
INY-5825, Basalt Ridge, tufa
INY-5825, Basalt Ridge, tufa
SBR, Afton Canyon
SBR, Coyote Lake
SBR, Coyote Lake
SBR, Coyote Lake
SBR-0199, Newberry Cave
SBR, Lucerne Valley, Ord Mountain
SBR, Lucerne Valley
SBR, Lucerne Valley
SBR, Lucerne Valley
SBR, Lucerne Valley
SBR, Lucerne Valley
INY, Death Valley/Titus Canyon
INY-0372, Rose Spring, Locus 1
Lake/Playa
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Lake/Playa
Lake/Playa
Lake/Playa
Lake Basin/Shore
Lake/Playa
Lake/Playa
Lake/Playa
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Cave/Shelter
Fan/Terrace (alluvial)
Buried spring/marsh
Buried deposit
Buried deposit
Buried deposit
Buried deposit
Buried deposit
Lacustrine
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Unit E2, 48, minimum date of spring; below pink/gray silt, assoc w/camel and snail
Unit E2, 60a, minimum age of spring, below pink/gray silt, assoc w/ snail fauna
Unit E2, 61a, minimum age of spring, below pink/gray silt, assoc w/snail fauna
Packrat Midden
Uriniferous material
Organic mat below fan surface, follows former lake bed; "probably assoc w/Paleo-Indian
habitation" Davis 1970
Trench 2, North end of Lake Hill, underlies cultural
Backhoe Trench 1, Stratum 2?
Backhoe Trench 1, Stratum 2?
Backhoe Trench 1, Stratum 3 or 4?
Backhoe Trench 1, Stratum 3 or 4?
Backhoe Trench 1, Stratum 3 or 4?
1972 date on in situ bone, Mammoth #4, T25S, R40E, Sec. 28, NE1/4
Summit of ridge, may be 500-1000 yrs too old
Summit of ridge, may be 500-1000 yrs too old
in situ on the highest shoreline of Lake Manix
?
?
?
Extinct ground sloth ribs
Wood (Juniperus sp. twigs/seeds) from midden
Midden #13, Wood (Juniperus sp. twigs/seeds)
Miscellaneous twigs
Wood (Juniperus sp. twigs/seeds)
Wood (Juniperus sp. twigs/seeds)
Wood (Juniperus sp. twigs/seeds)
Wood (Juniperus sp. twigs/seeds)
Locus 1, X-3, Feature 10, rock-lined hearth, Stratum 1
Natural
Cultural
Cultural
Cultural
Cultural
Cultural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Cultural
36
158
198
219
250
290
1
1
1
1
1
1
1
1
1
1
1
1
50
Page 8 of 10
Plant (burnt reeds)
Charcoal
Charcoal
Charcoal
Charcoal
Charcoal
Bone (mammoth ivory)
Carbonate (tufa)
Carbonate (tufa)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Bone (ground sloth)
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Packrat Midden
Charcoal
9200
- 10800
305
250
9697 10402 11131 Haynes 1967
300 11812 12694 13297 Haynes 1967
9799 Fergusson and Libby 1964; Haynes 1967
11822
13382
11197
13786
10691
Fergusson and Libby 1964; Haynes 1967
Haynes 1967
Haynes 1967
Wells and Berger 1967
Wells and Berger 1967
120 11230 11564 11983 Berger and Libby 1966 (RCJ); Davis 1970
10520 140 11986 12393 12682 Berger and Libby 1966 (RCJ); Davis 1970
2240 145 1924 2244 2553 Berger and Libby 1967 - RCJ; Clewlow et al. 1970
2900
80 2848 3051 3266 Berger and Libby 1967 - RCJ; Clewlow et al. 1970
3520
80 3606 3798 3988 Berger and Libby 1967 - RCJ; Clewlow et al. 1970
3580
80 3686 3883 4090 Berger and Libby 1967 - RCJ; Clewlow et al. 1970
3900 180 3871 4328 4830 Berger and Libby 1967 - RCJ; Clewlow et al. 1970
18600 4500 20965 22181 23526 Davis 1978
12970 150 15036 15649 16469 Davis 1978
11870 120 13428 13711 13970 Davis 1978
13900 1325 14845 16854 18585 Meek 1989
12570 120 14160 14735 15189 Meek 1994a; Jefferson 2003
11480 100 13136 13339 13570 Meek 1994a; Jefferson 2003
13230 145 15264 16108 16724 Meek 1994a; Jefferson 2003
11600 500 12526 13538 15099 Davis 1981; Moratto 1984
11850 550 12580 13894 15658 Taylor 1975 (RCJ); King 1976a
12100 400 13131 14165 15294 Taylor 1975 (RCJ); King 1976a
7820 570 7588 8748 9958 King 1976a
8300 780 7568 9335 11283 King 1976a
11100 420 11953 12962 13869 King 1976a
7800 350 7972 8691 9473 King 1976a
9680 300 10242 11064 12033 Wells and Woodcock 1985
110
50
8
123
151 Yohe 1992, 1998; CRD 1996
140
1400
50
1258
1316
1401 Yohe 1992, 1998; CRD 1996
Cultural Charcoal
300
5460
80
6169
6250
6407 Yohe 1992, 1998; CRD 1996
Cultural
Cultural
Cultural
Cultural
Cultural
Cultural
Cultural
Cultural
Cultural
Charcoal
Charcoal
Charcoal
Charcoal
Charcoal
Charcoal
Charcoal
Charcoal
Charcoal
70
230
65
85
275
45
45
205
45
280
3240
590
1360
4030
2240
330
2070
900
50
60
60
70
100
100
50
90
60
272
3358
522
1167
4280
1987
302
1865
722
365
3466
598
1280
4528
2233
393
2049
823
485
3593
663
1402
4826
2491
496
2214
927
Type
Material Dated
1-Sigma Error (±)
Cultural Charcoal
14C BP (CRCY)
Location, Provenience, and/or Description
Upper 2-Sigma cal BP
Buried soil
Cal BP (med. prob.)
Fan/Terrace (alluvial)
Dated Deposit
Source Reference
UCR-2325
INY-0372, Rose Spring, Locus 1
Fan/Terrace (alluvial)
Buried deposit
UCR-2327
UCR-2328
UCR-2333
UCR-2335
UCR-2341
UCR-2373
UCR-2388
UCR-2513
UCR-2533
INY-0372, Rose Spring, Locus 1
INY-0372, Rose Spring, Locus 1
INY-0372, Rose Spring, Locus 1
INY-0372, Rose Spring, Locus 1
INY-0372, Rose Spring, Locus 1
INY-0372, Rose Spring, Locus 3
INY-0372, Rose Spring, Locus 1
INY-0372, Rose Spring, Locus 1
INY-0372, Rose Spring, Locus 2
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Buried soil
Buried deposit
Buried soil
Buried soil
Buried deposit
Surface deposit
Buried deposit
Buried deposit
Surface deposit
Locus 1, X-1, Feature 12, upper rock-lined pit hearth, Strat. 2
Backhoe Trench 1 (north end), Feature 15 or Hearth A, base of Stratum 3 or 4, top of Stratum
4 or 5?
W-1, Feature 13 and 14, reused pit hearth, Stratum 2 top
Backhoe Trench 1, Feature 16 or Hearth B, on top of lower midden, Stratum 3 or 4?
W-1, Feature 13 and 14, reused pit hearth, Stratum 2 top
Locus 1, X-1, Feature 12, upper rock-lined pit hearth, Strat. 2
E-5, Feature 11, roasting feature below Feat. 2, Strat. 3 or 4?
Locus 3, TU-1, hearth
Locus 1, X-1, base of Stratum 1 and top of Stratum 2
Locus 1, X-1, loose Charcoal concentration, Stratum 2
Locus 2, TU-14, midden
UCR-2534
INY-0372, Rose Spring, Spring Locus
Fan/Terrace (alluvial)
Surface deposit
Spring Locus, SL-2, hearth within housepit
Cultural Charcoal
45
150
10
172
191
UCR-2535
INY-0372, Rose Spring, Spring Locus
Fan/Terrace (alluvial)
Surface deposit
Spring Locus, SL-2, hearth within housepit
Cultural Charcoal
35
150
10
172
191
277 Yohe 1992, 1998; CRD 1996
UCR-2536
UCR-2537
INY-0372, Rose Spring, Locus 1
INY-0372, Rose Spring, Locus 1
Fan/Terrace (alluvial)
Fan/Terrace (alluvial)
Buried deposit
Buried soil
E-5, Feature 11, roasting feature below Feat. 2, Strat. 3 or 4?
W-1, Feature 13 and 14, reused pit hearth, Stratum 2 top
Cultural Charcoal
Cultural Charcoal
265
100
4460
330
110
60
4838
289
5106
392
5326 Yohe 1992, 1998; CRD 1996
504 Yohe 1992, 1998; CRD 1996
MNO, Mono Basin
Lake Basin
Surface lacustrine
Tufa on wood from south lakeshore, 3 meters above present lake level, coll by GI Smith
Natural Carbonate (tufa)
1
1730
60
1527
1644
1814 (RCJ - year?)
USGS-0070
INY-0372, Rose Spring, Locus 1
Deposit or
Landform
Lower 2-Sigma cal BP
UCR-2324
State/County, Site/Locality
AVE Depth cm
Lab or Sample No.
Appendix C: China Lake Radiocarbon Database Listed by (1) Lab/Sample No., (2) Source Reference, and (3) State/County
SBR, Searles Lake, basin
Lake/Playa
Surface lacustrine
W-1680
W-5643
W-5646
W-6411
W-6412
W-6413
WSU-1464
WSU-1466
SBR, Searles Lake, outcrop
NV, Corn Creek Flat
NV, Corn Creek Flat
NV, Fish Lake, Leidy Creek
NV, Fish Lake, Leidy Creek
NV, Fish Lake, Leidy Creek
INY, Little Lake
INY, Little Lake
Lake/Playa
Floodplain/Arroyo
Floodplain/Arroyo
Lake/Playa
Lake/Playa
Lake/Playa
Floodplain
Floodplain
Lacustrine
Buried channel
Buried channel
Buried marsh
Buried marsh
Buried marsh
Buried marsh
Buried marsh
Inner rind of lithoid tufa in near-surface gravel of pluvial lake shoreline bar offset along Garlock
fault
Cac. Spr.Carb.-2b
Cac. Spr.Carb.-2b
Unit B
Parting Mud, Unit C, below lake level
lithofacies 4b, Trench 3
East side of dry wash, Unit A 3 over A1
East side of dry wash, Unit A 3 over A1
East side of dry wash, 0.3 m above base of Strat Unit A1, beach sand
East side of dry wash, on Strat Unit A 4
Dry wash W of Navy-Randsburg Rd, Strat. Unit A
Lithoid tufa from beach gravels near top of shoreline deposit N of Lone Pine; approximate
highstand age, max. age of Yermo fan surface
Overburden Mud, base of, deposited after lake
Parting Mud, Unit C, below lake level
Parting Mud, Unit C, below lake level
Parting Mud, Unit C, below lake level
Parting Mud, Unit C, below lake level
Shell from sand layer 8 ft above valley floor, S of highway, 0.5 miles E of mouth of Salt Wells
Canyon, coll by GI Smith
Parting Mud, Unit C, below lake level
Unit E1, C horizon overlying buried soil
Unit E1, with molluscs
Core 1.8
Core 1.5
Core 1.3
Whole sediment Core
Whole sediment Core
WSU-1474
INY, Little Lake
Floodplain
Buried marsh
WW-4044
WW-4045
INY, Owens Valley, Keeler
INY, Owens Valley, Keeler
Lake/Playa
Lake/Playa
Surface lacustrine
Surface lacustrine
USGS-0635
USGS-2212b
USGS-2213b
USGS-2327(?)
USGS-2328B
USGS-2339
USGS-2841
USGS-2842
USGS-2843
USGS-2844
USGS-2845
USGS-609
KER, Koehn Lake/Garlock Flt.
Lake/Playa
Surface lacustrine
NV, Cactus Springs
NV, Cactus Springs
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
INY, Owens Valley, Alabama Gates
SBR, Searles, Pinnacles Wash
SBR, Searles, Pinnacles Wash
SBR, Searles, Pinnacles Wash
SBR, Searles, Pinnacles Wash
SBR, Searles, Navy Road
Floodplain/Arroyo
Floodplain/Arroyo
Lake/Playa
Lake/Playa
Basin/Floodplain
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Buried spring
Buried spring
Lacustrine
Lacustrine
Buried marsh
Buried lacustrine
Buried lacustrine
Buried lacustrine
Lacustrine
Lacustrine
INY, Owens Valley, Alabama Hills
Lake/Playa
Surface lacustrine
W-0892
W-1317
W-1325
W-1327
W-1419
SBR, Searles Lake, Smith Core
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Buried lacustrine
Lacustrine
Lacustrine
Lacustrine
Lacustrine
W-1575
Natural Carbonate (tufa)
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Organic (black mat)
Organic (black mat)
Shell (fresh-mollusc)
Carbonate (tufa)
Organic sediment
Carbonate (tufa)
Carbonate (tufa)
Carbonate (CaC03)
Carbonate (tufa pod)
Carbonate (lithoid tufa)
Natural Carbonate (tufa)
Natural
Natural
Natural
Natural
Natural
Organic carbon (diseminated)
Carbonate (tufa)
Carbonate (tufa)
Carbonate (oolites)
Organic carbon (tufa)
Natural Shell-f (Anodonta)
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
15 13130
- 9680
- 9460
1 18270
12580
115 10190
1 25070
1 28770
1 31970
1 17770
1 10570
1 20670
681
1
1
1
12390
11670
11780
11400
11720
1
160
165
568
337
210
1134
801
11490
12600
12630
11180
8270
6215
5060
3920
Whole sediment Core
Natural Peat (Scirpus/Typha)
596
3020
Near Keeler (east Owens Lake)
Near Keeler (east Owens Lake)
Natural Shell-f (freshwater)
Natural Carbonate (tufa)
1 20970
1 14475
WW-4519
INY, Rose Valley, south pit
Lake/Playa
Buried soil
Black mat on upper playa, contain snails per Jayko; same as Record 6057
Natural Soil (SOM)
210 10000
WW-4562
WW-4563
WW-4564
WW-4782
WW-4799
WW-4800
WW-5144
WW-5145
WW-5146
WW-5147
WW-5327 H
WW-5327 L
WW-5328 L
WW-5329 L
WW-5351
SBR, Coyote Lake
SBR, Coyote Wash
SBR, Coyote Lake
INY, Owens Valley, Keeler
SBR, Chambless
SBR, Chambless
SBR, Coyote Lake
SBR, Coyote Lake
SBR, Coyote Lake
SBR, Coyote Lake
INY, Slate Canyon, Keeler
INY, Slate Canyon, Keeler
INY, Slate Canyon, Keeler
INY, Slate Canyon, Keeler
SBR, Coyote Lake
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Fan/Floodplain
Fan/Floodplain
Fan/Floodplain
Fan/Floodplain
Lake/Playa
Surface deposit
Buried lacustrine
Surface deposit
Surface lacustrine
Buried lacustrine
Buried lacustrine
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
sandy mud
Lake beds overlain by Qya4
sandy mud
Near Keeler (east Owens Lake)
Upper bed below Qya4
Upper bed below Qya4
lacustrine sand
lacustrine sand
lacustrine sand
lacustrine sand
Fault fissure in south wall of natural wash exposure
Fault fissure in south wall of natural wash exposure
South wall of natural wash exposure, Inyo Mtn Fault
South wall of natural wash exposure, Inyo Mtn Fault
lacustrine sand
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
1
185
185
185
100
-
Page 9 of 10
277 Yohe 1992, 1998; CRD 1996
80 15233 15939 16518 Robinson and Trimble 1983 (RCJ)
100
60
130
50
70
140
240
290
170
40
10733
10556
21451
14473
11601
29531
32504
36136
20510
12421
11016
10710
21824
14832
11879
29928
33274
36503
21181
12538
11245
10871
22233
15179
12136
30275
34460
37150
21551
12618
130 24325 24672 25025
400
400
300
350
500
13430
12678
12956
12593
12580
14588
13581
13662
13271
13688
16173
14654
14603
13982
15171
Quade and Pratt 1989
Quade and Pratt 1989
Benson et al. 1990
Benson et al. 1990
Beanland and Clark, 1994; Bacon et al. 2003
Garcia et al. 1993
Garcia et al. 1993
Garcia et al. 1993
Garcia et al. 1993
Garcia et al. 1993
Wagner et al. 1981; Fullerton 1986; Lubetkin and Clark, 1988; Bacon
et al. 2006
Rubin and Berthold 1961 (RCJ), Smith 1979
Benson et al. 1990
Benson et al. 1990
Benson et al. 1990
Benson et al. 1990
1 28870 1000 31992 33406 34604 Ives, Levin, and Meyer 1967 (RCJ)
Carbonate (oolites)
Wood (carbonized)
Wood (carbonized)
Peat (silt)
Peat (silt)
Peat (silt)
Peat (Scirpus/Typha)
Peat (Scirpus/Typha)
Shell-f (Anodonta)
Shell-f (unknown)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (gastropod, Fossaria)
Shell-f (gastropod, Pupillid)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Organic sediment
Organic sediment
Organic sediment
Organic sediment
Shell-f (Anodonta)
Yohe 1992, 1998; CRD 1996
Yohe 1992, 1998; CRD 1996
Yohe 1992, 1998; CRD 1996
Yohe 1992, 1998; CRD 1996
Yohe 1992, 1998; CRD 1996
Yohe 1992, 1998; CRD 1996
Yohe 1992, 1998; CRD 1996
Yohe 1992, 1998; CRD 1996
Yohe 1992, 1998; CRD 1996
19330
12815
12815
13010
11720
12110
14770
15475
15377
15580
12460
9502
11010
11346
15495
400
300
300
250
140
90
140
120
12554
13863
13900
12716
8973
6883
5581
4065
13376
14726
14768
13100
9241
7109
5810
4353
120
2875
3198
14263
15608
15667
13610
9537
7321
6182
4652
Benson et al. 1990
Quade 1986
Quade 1986
Throckmorton and Reheis 1993
Throckmorton and Reheis 1993
Throckmorton and Reheis 1993
Shepard and Chatters 1976 (RCJ)
Shepard and Chatters 1976 (RCJ)
3456 Mehringer and Sheppard 1974; Shepard and Chatters 1976 (RCJ)
100 24562 25003 25439 Bacon et al. 2006
40 17246 17623 17893 Bacon et al. 2006
40 11275 11473 11637 Jayko 2010, unpublished field notes
70
45
45
40
60
140
45
45
45
45
170
75
100
95
45
22614
14919
14919
15145
13404
13614
17673
18566
18514
18622
13996
10579
12662
13068
18577
23036
15239
15239
15638
13569
13988
17959
18689
18627
18752
14573
10820
12892
13226
18703
23428
15660
15660
16301
13746
14588
18084
18841
18769
18890
15160
11100
13111
13427
18850
Dudash 2006?
Miller et al. 2009
Dudash 2006?
Bacon et al. 2006
Miller et al. 2009
Miller et al. 2009
Dudash 2006?
Dudash 2006?
Dudash 2006?
Dudash 2006?
Bacon, Jayko, and McGeehin 2005
Bacon, Jayko, and McGeehin 2005
Bacon, Jayko, and McGeehin 2005
Bacon, Jayko, and McGeehin 2005
Dudash 2006?
Y-1585
Y-1586
Y-1587
Y-1589
Y-1591
Y-1593
Y-2406
Y-2407
Y-2408
Y-2467
Y-2470
Y-unknown
Y-unknown
Y-unknown
Y-unknown
Y-unknown
Y-unknown
Y-unknown
Type
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Material Dated
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Organic sediment (marl)
Organic sediment (marl)
Wood (twig)
Carbonate (CaC03)
Organic sediment (marl)
Carbonate (CaC03)
Carbonate (CaC03)
Organic sediment (marl)
Carbonate (CaC03)
Carbonate (CaC03)
Organic sediment (marl)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaC03)
Organic carbon (diseminated)
Organic carbon (diseminated)
Carbonate (CaCo3)
Organic carbon (diseminated)
Carbonate (CaC03)
Organic carbon (diseminated)
Organic carbon (diseminated)
Carbonate (CaC03)
Organic carbon (diseminated)
Organic carbon (diseminated)
Organic carbon (diseminated)
Carbonate (CaC03)
Carbonate (CaC03)
Carbonate (CaCo3)
Carbonate (CaCo3)
Carbonate (CaC03)
Carbonate (CaC03)
SBR, Silver Lake
Lake/Playa
Surface lacustrine
Outlet channel, error often misreported as ± 100
Natural Shell-f (Anodonta)
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
SBR, Silver Lake
INY, Death Valley, Tule Spring
INY, Death Valley, Badwater fan
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
SBR, Searles Lake, outcrop
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Fan/Floodplain
Fan/Floodplain
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Buried lacustrine
Buried lacustrine
Buried lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Surface lacustrine
Buried deposit
Buried deposit
Lacustrine
Lacustrine
Surface lacustrine
Lacustrine
Lacustrine
Lacustrine
Lacustrine
Beach ridge
Beach ridge
Gravel Pit in NE 1/4 of Sec. 29 3.2 km W of SL Junction
Gravel Pit in NE 1/4 of Sec. 29 3.2 km W of SL Junction
Gravel Pit in NE 1/4 of Sec. 29 3.2 km W of SL Junction
Bench Mark Bay, northwest beaches
Bench Mark Bay, northwest beaches
Bench Mark Bay, northwest beaches
Core 68-7 on valley floor east of Hanapuah fan
Core 68-10 on valley floor west of Badwater fan
Parting Mud, Unit C, below lake level
Parting Mud, Unit C, below lake level
Parting Mud, Unit C, below lake level
Parting Mud, Unit C, below lake level
Parting Mud, Unit C, below lake level
Parting Mud, Unit C, below lake level
Parting Mud, Unit C, below lake level
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Natural
Page 10 of 10
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Shell-f (Anodonta)
Organic sediment (humate)
Organic sediment (humate)
Carbonate (tufa)
Carbonate (oolites)
Shell (fresh-mollusc)
Carbonate (oolites)
Carbonate (oolites)
Carbonate (tufa)
Shell (fresh-mollusc)
2403
2503
240
163
163
460
947
947
1144
1282
1282
1591
1860
1970
2275
2275
2275
2275
2275
2275
2275
2275
2275
2275
2275
2275
2275
2275
3600
3048
3287
15845
14005
13480
15260
19350
85
10700
12730
3520
6560
6630
9370
10770
11010
10270
10130
11510
9390
9520
9510
10680
10900
10300
10230
11140
10060
10410
10680
10590
10440
11800
12770
17380
19050
22290
25470
24070
50 13290
262
262
173
97
79
40
100
30
845
1360
1
1
1
1
1
1
1
14220
15020
12960
10370
10250
9940
9010
12120
12980
11900
10100
10690
11370
12870
13020
13810
13880
1-Sigma Error (±)
Location, Provenience, and/or Description
lacustrine sand
lacustrine sand
lacustrine sand
sand and gravel
lacustrine sand
Upright shell in sand bed
Well X-20 made by American Potash and Chemical Co.
Well X-20 made by American Potash and Chemical Co.
Core, middle of capping sands
Upper Salt section in testhole L-U-1
Upper Salt section in testhole L-U-1
Upper Salt section in testhole L-U-1
Upper Salt section in testhole L-U-1
Upper Salt section in testhole L-U-1
Upper Salt section in testhole L-U-1
Upper Salt section in testhole L-U-1
Upper Salt section in testhole L-U-1
Upper Salt section in testhole L-U-1
Upper Salt section in testhole L-U-1
Upper Salt section in testhole L-U-1
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
Parting Mud, average thickness of Cores is 371 cm; actual depths not reported
From Lower Salt and Bottom Mud
Lower Salt, 546-549 cm below top, suspect date
Lower Salt, 785-788 cm below top, suspect date
14C BP (CRCY)
Dated Deposit
Surface deposit
Surface deposit
Surface deposit
Surface deposit
Surface lacustrine
Surface deposit
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
Buried lacustrine
45
40
35
45
70
35
130
210
190
140
390
180
180
150
100
170
150
200
180
80
90
90
80
80
100
90
120
110
110
90
130
230
280
250
340
500
400
Upper 2-Sigma cal BP
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Lake/Playa
Cal BP (med. prob.)
SBR, Coyote Lake
SBR, Coyote Lake
SBR, Coyote Lake
SBR, Coyote Lake
SBR, Coyote Lake
SBR, East Cronese Lake
SBR, Searles Lake, Core X-20
SBR, Searles Lake, Core X-20
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core X-23
SBR, Searles Lake, Core X-23
SBR, Searles Lake, Core X-23
SBR, Searles Lake, Core X-23
SBR, Searles Lake, Core X-23
SBR, Searles Lake, Core X-20
SBR, Searles Lake, Core X-20
SBR, Searles Lake, Core X-20
SBR, Searles Lake, Core X-23
SBR, Searles Lake, Core X-20
SBR, Searles Lake, Core X-20
SBR, Searles Lake, Core L-U-1
SBR, Searles Lake, Core L-U-1
Deposit or
Landform
Lower 2-Sigma cal BP
WW-5352
WW-5353
WW-5354
WW-5355
WW-5519
WW-5717
Y-0574b
Y-0575b
Y-1048
Y-1200
Y-1200 B
Y-1201
Y-1202
Y-1202 B
Y-1203
Y-1204
Y-1204 B
Y-1205
Y-1206
Y-1207
Y-1208 B-1
Y-1208 B-2
Y-1209
Y-1209 B
Y-1210
Y-1210 B-1
Y-1210 B-2
Y-1211
Y-1211 B
Y-1212
Y-1212 B
Y-1213
Y-1214
Y-1215
Y-1216
Y-1221
Y-1222 B
State/County, Site/Locality
AVE Depth cm
Lab or Sample No.
Appendix C: China Lake Radiocarbon Database Listed by (1) Lab/Sample No., (2) Source Reference, and (3) State/County
18810
16819
16404
18469
22625
18
11142
13351
3375
7238
5921
10231
12372
11383
11616
11242
12343
10219
10370
10580
12407
12600
11801
11618
12741
11272
11954
12379
12131
12055
13369
14179
20028
22195
25951
29408
27982
19055
17046
16669
18564
23055
108
11492
13879
3821
7457
6760
10626
12679
12008
12040
11760
12680
10658
10837
10841
12606
12784
12108
11953
13015
11609
12271
12599
12492
12322
13641
15205
20734
22771
26876
30251
28897
19324
17248
16873
18692
23443
145
11942
14613
4299
7678
7547
11156
13102
12416
12423
12228
13083
11199
11239
11108
12780
12979
12412
12224
13251
11844
12601
12885
12695
12579
13916
16365
21452
23437
27868
31096
29610
160 15404 16205 16811
140
240
350
100
100
160
140
160
700
200
100
400
160
200
200
120
200
16908
17662
14240
11954
11602
11073
9685
13608
13488
13277
11303
11309
12872
14543
15007
16667
16599
17312
18234
15609
12232
11996
11483
10113
14018
15528
13753
11687
12466
13240
15464
15758
16916
16991
17737
18690
16746
12567
12418
12062
10507
14661
17250
14240
12046
13307
13608
16525
16643
17198
17547
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Dudash 2006?
Dudash 2006?
Miller et al. 2009
Deevey et al. 1959 (RCJ), Smith 1979
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Stuiver 1964; Davis 1978; Smith 1979
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Stuiver 1964
Ore and Warren 1971; Berger and Meek 1992; Wells et al. 1989;
Wells et al. 2003
Ore and Warren 1971; Wells et al. 1989
Ore and Warren 1971; Wells et al. 1989
Ore and Warren 1971
Ore and Warren 1971; Wells et al. 1989
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Benson et al. 1990
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Benson et al. 1990
Benson et al. 1990
APPENDIX D
MICRO-INVERTEBRATES FROM THE CHINA LAKE BASIN ENVIRONS
BY DR. MANUEL R. PALACIOS-FEST
APPENDIX D
MICRO-INVERTEBRATES FROM THE
CHINA LAKE LEGACY PROJECT, CALIFORNIA
TNESR REPORT 10-09
Manuel R. Palacios-Fest
Abstract: The combined analysis of ostracodes and mollusks (micro-invertebrates) constitute a
powerful tool for reconstructing ancient environments in the northern Mojave Desert. China Lake, one of the
missing areas in the study of micro-invertebrates offered a unique opportunity to close the gap with other
associated lakes in the region, like Owens Lake, Searles Lake, Panamint Lake, and those of the Mojave
Drainage Basin (Lake Mojave). Two significantly different environmental settings were identified through
ostracode and mollusk analysis identified in this study as the spring-related environments and the lake basin
environments. Lack of age control posed a major obstacle in defining the paleoenvironmental history of
China Lake. The spring-related sites, however, contained a faunal assemblage consistent with the transition
from the latest Pleistocene to earliest Holocene (Bølling/Allerød-Younger Dryas) recorded elsewhere in the
area. The lake basin, by contrast, in spite of its fauna similar to that identified at Owens Lake, Searles Lake,
and Panamint Lake could not be placed in time.
INTRODUCTION
Micro-invertebrate paleoecology is a powerful tool for reconstructing the paleoenvironmental
history of aquatic environments. Diverse and abundant micro-invertebrates (ostracodes and mollusks), are
common in nonmarine environments where they are sensitive to variations in pH, temperature, salinity,
and water chemistry, among other factors. Similarly, the stable isotopes (carbon and oxygen) of
ostracodes shells provide relevant information on the chemical and physical properties of the host waters.
Ostracodes are microscopic crustaceans characterized by a hinged bivalve carapace made of
calcite ranging in size between 0.5 and 2 mm. The carapace is the only body part that is preserved in the
geologic record (Pokorný, 1978; Horne et al., 2002). In continental waters they are mostly benthic,
although some species are nektic and may swim around the vegetation (Forester, 1991). This group
colonized continental aquatic systems as early as the Carboniferous but has thrived in the oceans since the
Cambrian. Today, ostracodes are diverse and abundant in marine and nonmarine environments.
Paleontologists have devoted more time to the study of ostracodes than have biologists—hence the poorly
understood ecology of ostracodes. Recent progress on the application of ostracodes as indicators of
hydrogeologic variations, however, calls for additional studies of the ecology of springs and seeps, as well
as their associated wetlands or cienegas (Forester, 1983, 1986; De Deckker, 1983; Palacios-Fest, 1994,
2008; Palacios-Fest et al., 1994, 2001; Holmes and Chivas, 2002). Mollusks associated with the ostracode
fauna are also an important element in paleolimnological analysis.
Mollusks include the bivalve clams and mussels (Bivalvia) and the univalve snails (Gastropoda).
Mollusks are soft bodied and unsegmented, with a body organized into a muscular foot, a head region, a
visceral mass, and a fleshy mantle that secretes a shell of proteinaceous and crystalline calcium carbonate
(aragonite) materials. Both marine and nonmarine species exist. The nonmarine species, which are the
subject of this study, include several families of snails (the aquatic Planorbidae, Ancylidae, and
Lymnaeidae and the terrestrial Pupillidae) and at least one family of clams (Pisidiidae). The associations
of mollusks in the sediments reflect the water quality, salinity, and streamflow (Rutherford, 2000; Dillon
and Stewart, 2003). For example, the occurrence of juveniles alone in a sample is interpreted as the
introduction of early-stage individuals during warm or warming months (Rutherford, 2000). If the
population reaches stability and adults are encountered, then it is assumed that the feature held water for a
Appendix D
relatively prolonged period. Some species, like Pisidium sp. require well-oxygenated, lotic (flowing)
waters and prefer neutral to alkaline pH but cannot tolerate organic pollution present in the marsh. By
contrast, other species, like Physa virgata, can tolerate poorly oxygenated (but not disoxic), lentic
(standing) waters and can tolerate some organic pollution and eutrophic conditions (Dillon and Stewart,
2003). The latter species prefer lakes, wetlands, ponds, and the calmest areas of coastal rivers. Like the
ostracode signatures, the signatures of mollusks are used in this study to integrate the paleoecological
characteristics of the China Lake Legacy Project area in California.
Stable-isotope (δ18O and δ13C) geochemistry based on ostracode valves is another approach to
paleoclimatic reconstructions. Lister (1988) and Eyles and Schwarcz (1991), followed by numerous other
researchers (e.g., Lewis et al., 1994; von Grafenstein et al., 2000; Wrozyna et al., 2010), have pursued the
utility of carbon and oxygen isotopes in ostracodes for these reconstructions. The isotopic record from
ostracode valves allowed these investigators to establish the rate and timing of climate change across
space. For example, Lister (1988) determined the Alpine deglaciation, Holocene climatic changes, and
changing lacustrine productivity of Lake Zürich, whereas Wrozyna et al. (2010) utilized stable isotopes to
identify lake-level changes in Lake Nam Co, southern Tibet, during the past 600 years. Stable-isotope
studies of ostracodes have proved their significance in paleoenvironmental reconstructions.
The purpose of this investigation is to combine routine paleoecological analysis of microinvertebrates with the stable-isotope geochemistry (δ18O and δ13C) of ostracodes to reconstruct the late
Pleistocene environmental history of China Lake, California.
MATERIALS AND METHODS
A total of 38 sediment samples from China Lake (20), Dove Springs Wash (3), Little Dixie Wash
(12), Rose Valley (3) and the China Lake outlet (CLSB) areas within the China Lake region were
analyzed for micro-invertebrates to reconstruct China Lake’s environmental history. The sediment
samples were prepared using routine procedures (Forester, 1988) modified by Palacios-Fest (1994).
Samples were air-dried, weighed, and soaked in boiling distilled water with 1 g of Alconox to
disaggregate the sediments. Then they were left to sit at room temperature for 5 days and were stirred
once a day during that period. Using a set of three-sieves, the samples were wet-sieved to separate the
coarse (>1 mm), medium (>106 µm), and fine (>63 µm) sand fractions to help identify the system’s
paleohydraulics. The very fine sand and silt and clay fractions were washed out at this stage. Therefore,
the particle-size analysis departs from the formal USDA procedure (USDA 2003) and it is used only as a
rough reference in this study. It is important to highlight that the possible discrepancy between the
approach used in this investigation and that of the USDA is the result of grouping the very fine sands with
the finer fractions, which in fact change the total percentage of sand, but does not affect the actual
behavior of sands in the ecosystem. The value of the approach used here is that it provides a quick and
easy way to process the data and to estimate the patterns of water discharge into the aquatic system
overtime. More detailed particle-size analysis may be conducted using the appropriate research methods.
The data are shown in Table 1. Table 2 shows the mineralogical composition per sample.
All samples were analyzed under a low-power microscope to identify fossil contents and faunal
assemblages (Table 3). Both mollusks and ostracodes occurred in some samples (Tables 4-7). Ostracodes
(Table 4) occurred in 13 samples across the area, ranging in abundance from extremely rare to extremely
abundant (1-1119) (Table 5); whereas mollusks (Table 6) were recorded in six samples ranging in
abundance from extremely rare to common (1-42)* (Table 7). Total and relative abundance was recorded
from the sediment samples. Based on Delorme (1969, 1989), standard taphonomic parameters, like
fragmentation, abrasion, disarticulation (carapace/valve; C/V ratios), and adulthood (adult/juvenile; A/J
ratios) were recorded to establish the synecology (ecology of the communities) as opposed to the
autoecology (ecology of single species) of the ecosystem (Adams et al. 2002). The taphonomic
Appendix D
parameters were used to recognize degrees of transport and/or burial characteristics like desiccation and
sediment compaction. The rates of fragmentation, abrasion and disarticulation are realistic indicators of
transport; commonly these parameters show increasing damage with increasing transport. One must be
cautious in using this criterion, but the nature of the deposits suggests that micro-invertebrates may reflect
the lake’s hydraulic properties. Other features like encrustation and coating were used to determine
authigenic mineralization or stream action, respectively. Corrosion was used as an indicator of diagenetic
effects overtime. The redox index and color of valves reflected burial conditions. The A/J and C/V ratios
were used as indicators of biocenosis (Whatley 1983; Palacios-Fest et al. 2001).
Finally, in an attempt to obtain an isotopic record from China Lake, all samples containing
ostracodes were searched for specimens to conduct stable isotope (δ13C and δ18O) analysis. Twenty-four
valves of Ilyocypris bradyi were used for this analysis conducted at the Environmental Isotope Laboratory
of the University of Arizona. Four valves were available from RV-NCTP-3Cu (Rose Valley), ten from
DSW-L#5771-5Ab (Dove Springs Wash) split into two batches of five to make a replicate, and ten more
from DSW-L#5771-8AB also split into two batches of five (Table 8). Other specimens were corroded and
unfeasible for isotope analysis. Oxygen and carbon stable isotope ratios were measured using an
automated carbonate preparation device (KIEL-III) coupled to a gas-ratio mass spectrometer (Finnigan
MAT 252). Samples were reacted with dehydrated phosphoric acid under vacuum at 70°C. The isotope
ratio measurement is calibrated based on repeated measurements of NBS-19 and NBS-18 and precision is
± 0.046 ‰ for δ18O and ±0.019‰ for δ13C (1sigma). Isotopic data for calcites are reported in delta
notation relative to the VPDB international scale (Coplen 1994).
RESULTS
THE SEDIMENTARY RECORD
Table 1 and Figure 1, respectively show the textural classification and particle-size diagrams of
all sites studied. A single sample from Horizon 3Cu from the Rose Valley, North Caltrans Pit was
composed of dark gray (2.5Y 4/1) medium sand (Figure 1a). The mineral composition was dominated by
quartz, feldspars, tufa, and more rarely biotite, mollusk and ostracode fragments (Table 2). The unit was
fossiliferous (Table 3). The 3Cu Horizon yielded a radiocarbon date of 7861 BC from about 250 cm
below ground surface (cm bgs) (Table 1; Chapter 4, this volume).
Two unfossiliferous samples from Rose Valley, South Caltrans Pit varied from very dark grayish
brown (2.5Y 3/2) silty clay (Horizon 4Ob) to dark grayish brown (2.5Y 4/2) sand (Horizon 3Ab) (Figure
1b). Quartz, tufa, and feldspars were the dominant minerals followed by biotite, root casts, and charcoal.
As shown in Table 1, A sample from the 3Ab Horizon submitted for age control yielded a date of 9497
BC; whereas, another from the 4Ob Horizon produced a date of 11445 BC (see Chapter 4, this volume).
At Dove Springs Wash Locality # 5771 three samples were analyzed for micro-invertebrates
consisting of dark grayish brown (2.5Y 4/2) sandy silt to light yellowish brown (2.5Y 6/4) sandy to silty
clay (Table 1; Figure 1c). Quartz, tufa, and feldspars dominated the mineral assemblage associated with
root casts, pyrite, biotite, charcoal, and more rarely shell fragments (Table 2). Horizons 5Ab and 8Ab
were fossiliferous (Table 3). Of the three horizons analyzed for micro-invertebrates and submitted for age
control, the 13Ab Horizon yielded a date of 10152 BC, while the 5Ab Horizon returned a date of 2803
BC (Table 1; Chapter 4, this volume).
Twelve samples from Little Dixie Wash (LDW) in three locations ranged from grayish brown
(2.5Y 5/2) sandy silty clay to pale yellow (2.5Y 7/3) silty clay or from grayish brown (10YR 5/2) sandy
silty clay to (10YR 8/1) clay at FW-CLDW-T3 (Table 1; Figures 1d-g). The mineral composition was
dominated by quartz and feldspars, sometimes alternating with tufa or gypsum. Other minerals occurring
at LDW were biotite, charcoal, root casts, and more rarely shell fragments and schist (Table 2). Samples
LDW1, 190-205-2Ab and LDW-L#3-4Ab contained micro-invertebrates (Table 3). Radiocarbon dates
Appendix D
were obtained from three of four sites sampled at Little Dixie Wash. Locality #1 produced three dates in
stratigraphic order, including two from the 2Ab Horizon of 8994 BC and 9536 BC, and one from the 3Ab
Horizon of 9796 BC. Locality #3 produced a geochronological sequence in stratigraphic order ranging
from 10504 BC to 8753 BC (Table 1; Chapter 4, this volume). By contrast, Locality #4 generated dates
from three strata (3Ab, 5Ab, and 7Ab horizons) between 9374 and 10523 BC, the lower two of which are
in reversed startigraphic order (Table 1; Chapter 4, this volume).
Eighteen core samples and two surface samples from China Lake basin were also analyzed for
micro-invertebrates. Cores TTIWV-SB01, TTIWV-SB05, TTIWV-SB08, TTIWV-SB10, and TTIWVSB28 consisted of greenish gray (Gley 1 8/1) silty sand to light gray (10YR 7/2) clay (Table 1; Figure 1hn). The mineral composition of the core samples was dominated by quartz, tufa, feldspars, followed by
biotite, gypsum, root casts, and to a lesser extent charcoal, shell and bone fragments (Table 2). Fossils
occurred in cores TTIWV-SB05, TTIWV-SB08, and TTIWV-SB10. The remaining cores (TTIWV-SB01,
and TTIWV-SB28) were unfossiliferous (Table 3). Core TTIWV-SB01 yielded two radiocarbon dates in
reverse order (see Chapter 4, this volume for explanation). No dates are available from other cores.
The two surface samples from the Lava End Locality consisted of light brownish gray (10YR 6/2)
silty sand (Table 1). The samples consist of light greenish gray (Gley 1 8/1) silty sand to greenish gray
(Gley 1 6/1) sandy silty clay composed of abundant tufa, gypsum, and quartz. Other minerals included
feldspars, biotite, and root casts (Table 2). The samples were unfossiliferous (Table 3). The Lava End
Locality yielded two radiocarbon dates in stratigraphic order (Table 1; Chapter 4, this volume).
A separate sample of mollusk shells was submitted for identification. The sample (CLSB-snails)
was collected from a lacustrine beach deposit composed of sand and marl with Anodonta shells that is
perched atop of bedrock outcrop below the outlet of China Lake within the Searles Lake basin in an area
sometimes known as Salt Wells Valley (Meyer, personal communication). The radiocarbon dates
obtained from Helisoma sp. yielded a calibrated age of 13,387±50 years B.P. (11,437 B.C.) (Table 1;
Chapter 4, this volume).
THE BIOLOGICAL RECORD
Table 3 summarized the biological contents of China Lake samples and the overall taphonomic
characteristics recorded. Ostracodes and mollusks were present. Eleven ostracode species were identified
from the China Lake Legacy Project: Limnocythere sappaensis Staplin 1963, Limnocythere ceriotuberosa
Delorme 1967, Cyprideis beaconensis (Leroy), 1943, Cypridopsis vidua (O.F. Muller, 1776), Candona
patzcuaro Tressler 1954, Fabaeformiscandona caudata (Kaufmann 1900), Fabaeformiscandona
acuminata (Fischer, 1851) Danielopol 1980, Ilyocypris bradyi Sars, 1890, Eucypris meadensis Gutentag
& Benson 1962, and Cypridopsis okeechobei Furtos 1933, as well as an unknown Species 1. Table 4
shows the ecological requirements of the ostracode species identified in this study. Table 5 displays the
total and relative abundance by species, the adulthood and disarticulation ratios
Mollusks were equally diverse (seven species) including the snails Physa virgata (Gould, 1855),
Fossaria parva (Lea, 1841), Gyraulus parvus (Say, 1817), Tryonia sp. Stimpson, 1865, Pseudosuccinea
columella (Say, 1825), Helisoma (Carinifex) newberryi (Lea, 1858), and the clam Pisidium casertanum
(Poli, 1795). Table 6 shows the ecological requirements of the mollusk species identified in this study.
Based upon the ostracode composition a paleosalinity index was developed (Table 5). The
qualitative paleosalinity index takes into consideration the salinity tolerance of the species present in the
area based on our current knowledge of their ecological requirements presented in the North American
Nonmarine Ostracodes Database (NANODe) website (Forester et al. 2005) and other references
(Palacios-Fest, 1994; Curry 1999). The equation used for the present study is:
SI = [5(% Limnocythere sappaensis) + 4(% Limnocythere ceriotuberosa) + 3(% Cyprideis
beaconensis) + 2(% Cypridopsis vidua) + (% Candona patzcuaro)] - [(%
Fabaeformiscandona caudata) + 2(% Fabaeformiscandona acuminata) + 3(% Ilyocypris
bradyi) + 4(% Eucypris meadensis) + 5(Cypridopsis okeechobei)]
Appendix D
The index positively weighs species with incrementally higher salinity tolerances and negatively
weighs species with incrementally lower salinity tolerances. In spite of the fragmented record, the
paleosalinity index shows predominance of saline conditions throughout the area’s environmental history
(see Interpretation and Discussion Sections below).
Continental ostracodes and mollusks inhabit waters of different hydrochemical composition, but
at the species level many are very sensitive to water chemistry. Ostracode and mollusk assemblages can
be used to recognize the three major water types defined by Eugster and Hardie (1978):
•
Type I: Ca2+, Mg2+, and HCO3⎯ -dominated water; typically freshwater or very low salinity
conditions.
•
Type II: Ca2+ -enriched/HCO3⎯ - depleted water; additionally containing the combinations of Na+,
Mg2+, SO42⎯, or Na+, Mg2+, Cl⎯; ranges from low salinity to hypersaline conditions.
•
Type III: Ca2+ -depleted/HCO3⎯ + CO32⎯ (alkaline)-enriched water; usually containing
combinations of Na+, Mg2+, Cl⎯, or Na+, Mg2+, SO42⎯; ranges from low salinity hypersaline
conditions.
This spectrum clearly shows that water chemistry plays a major role in the geographic
distribution of micro-invertebrates. In addition to water chemistry, temperature is another factor that
affects the distribution of these organisms, as their latitudinal distribution demonstrates. Many ostracode
species respond to temperature through both reproductive and survival ability (De Deckker and Forester
1988; Delorme and Zoltai 1984; Forester 1987). For example, Cytherissa lacustris is limited to water
temperatures lower than 23°C, and is common in subpolar regions, whereas Limnocythere bradburyi is
restricted to warm temperatures of low to mid-latitudes (Delorme 1978; Forester 1985). Their sensitivity
to temperature makes ostracodes very useful for paleoclimate reconstructions (Cohen et al. 2000;
Palacios-Fest 2002). Once the ecological requirements of ostracodes are determined, it is possible to
reconstruct paleoenvironments from the geologic record (Delorme 1969; Holmes et al. 2002; PalaciosFest 1994). Similarly, Sharpe (2002, 2003) has documented some of the ecological preferences of several
mollusk species in Western North America. The mollusk record was used to integrate the following
paleoenvironmental reconstruction.
THE STABLE ISOTOPE DATA
Stable isotope values for Ilyocypris bradyi are shown in Table 8. In spite of the limited number of
intervals used for this analysis some matters to consider include:
1. Based on the more than 5 specimens measured with each sample the effects of seasonal variability were
eliminated. This makes the δ18O values more representative of the average climate regardless of the
probable seasonal biases in the timing of ostracode growth;
2. The δ18O values are most responsive to temperature change and to the δ18O values of the water (which
change in response to climate). In this sense, RV-NCTP-3Cu shows the most positive values. DSWL#5771-5Ab and DSW-L#5771-8Ab show more negative values with the latter being the most negative.
Lack of significant variability among the data suggests that the δ18O obtained from I. bradyi reflect
changes in water δ18O rather than temperature (which Dettman estimates to be around 12°C, personal
communication). If this is correct, the more positive values imply increasing aridity or heavier seasonal
rains (like the monsoon); whereas the more negative values may indicate less evaporation. During a wet
period, the volume of a closed-basin lake increases, which typically drives the δ18O value in the lake to
decrease, whereas during a dry period the δ18O value in the lake increases as the lake shrinks (Benson et
al. 2002); thus constraining the direction of lake-level oscillations in the absence of surface data.
3. The δ13C values mainly result from micro-habitat variability and cannot be used for a
paleoenvironmental reconstruction.
Appendix D
INTERPRETATION
The combined information of ostracodes and mollusks provides solid evidence for environmental
change over time in the area of study. For example, a sharp contrast is evident between the China Lake core
samples (FW718o) and the spring related samples analyzed to date. The core samples show an assemblage
dominated by saline, standing water systems dominated by Limnocythere sappaensis, Limnocythere
ceriotuberosa, and Cyprideis beaconensis (the three most common species in the cores); whereas the spring
samples contain an assemblage dominated by crenophilous (spring-prone), stream, and dilute water species
like Ilyocypris bradyi, Eucypris meadensis and Cypridopsis okeechobei. This drastic difference may indicate
the hydrochemical evolution of China Lake over time. To answer this question it is important first to establish
the relationship between the China Lake basin and the springs studied. Is it possible that they are parts of the
whole system? Is it possible that as water flows away from the springs the water chemistry changes to the
point of hosting such different assemblages? Next, I will interpret the environmental history of China Lake
starting from the potential water sources, moving down into the lake basin.
Site Rose Valley, North Caltrans Pit (RV-NCTP):
The North Caltrans Pit at Rose Valley is located along the former Owens River channel, north of
China Lake Basin, and was represented by a single sample from Horizon 3Cu (stratum II). The relatively
coarse sediments accumulated in this horizon are consistent with the coarse-channel facies fining-upwards
into overbank floodplain facies. Figure 1a shows that medium sand conformed more than 65% of the
particle-size analysis indicating a moderately high energy environment.
The poor biological composition is consistent with this interpretation. Three species of microinvertebrates, two ostracodes and one mollusk occurred in Horizon 3Cu. The ostracodes Ilyocypris bradyi
(about 72%) and Fabaeformiscandona acuminata (about 28%) suggest a dilute, spring source (Table 5).
As shown in Table 4, F. acuminata’s salinity tolerance is below 1000 mg L-1 total dissolved solids (TDS)
(Forester et al. 2005) implying that the pit is close to the water source (Figure 2a).
Two specimens of Tryonia sp. were identified in the sample (Table 7). The genus Tryonia is
known to prefer low to moderate salinity (1000-2000 mg L-1 TDS; Sharpe 2002, 2003) (Table 6).
Therefore, it is inferred that ostracodes and mollusks reflect the environmental conditions prevailing at
Horizon 3Cu during deposition.
Five valves of I. bradyi were analyzed for carbon and oxygen isotopes at the Department of
Geosciences of the University of Arizona. As discussed in the Results section, the δ18O value obtained
from sample RV-NCTP-3Cu are the most positive obtained from China Lake suggesting arid conditions
or greater seasonal rainfall at the time of deposition of Horizon 3Cu (Table 8). A date 7861 BC suggests
this sample dates to the early Holocene.
Site Rose Valley, South Caltrans Pit (RV-SCTP):
The South Caltrans Pit at Rose Valley located just south of the north pit along the Haiwee Creek
was represented by two horizons in stratigraphic contact (II/4Ob and III/3Ab). The older unit (II/4Ob)
consisted of fine-grained deposits forming a thin stratum (about 75% very fine sand, silt, and clay).
Horizon 3Ab is a thick, gravelly, fining-upward medium sand (about 67%) overlying Horizon 4Ob
(Figure 1b). The samples were unfossiliferous. Based on organic sediments, Horizon 3Ab yielded a
calibrated radiocarbon age of 11,447±55 years B.P (9497 B.C.), the terminal Younger Dryas. By contrast,
organic material from the underlying Horizon 4Ob yielded a date of 11445 BC (Table 1; Chapter 4, this
volume), prior to the Younger Dryas.
Site Rose Valley, Lava End Locality:
Two samples from the black mat at the Lava End Locality were analyzed for micro-invertebrates.
The two strata consisted mostly of medium sand (greater than 41%) implying an alluvial floodplain
Appendix D
deposit where tufa and gypsum were most abundant (Figure 1m; Table 2). The site was unfossiliferous.
Organic sediments from the black mat yielded calibrated radiocarbon dates ranging from 9,065±100 years
B.P. (7115 B.C.) to 10,656±100 years B.P. (8706 B.C.), latest Pleistocene to earliest Holocene. Lack of
micro-invertebrates prevents establishing the paleoenvironmental history of the site. However, black mat
horizons have previously been associated with the transition from the warm dry climate of the terminal
Allerød to the glacially cold Younger Dryas, so climate change is recorded at the Lava End Locality
(Huckell and Haynes 2007).
Site Dove Springs Wash (DSW-L#5771):
At the southwest end of China Lake is the Dove Springs Wash, Locality #5771. The wash drains
into Koehn Lake to the south (see Chapter 4, this Volume for details). Dove Springs Wash consists of
stratified alluvial floodplain/lacustrine deposits that form an inset terrace along the main valley axis.
Three isolated horizons were analyzed for micro-invertebrates. Horizon 5Ab consisted mostly of very fine
sand, silt and clay (about 79%) (Figure 1c). The fine sediments indicate a ponded deposit that held an
abundant ostracode record (dry mass of 2.6 specimens per gram of sediment). Four species were
identified at Horizon 5Ab including Eucypris meadensis (the most abundant), Ilyocypris bradyi,
Fabaeformiscandona acuminata, and Cypridopsis vidua (Figure 2b). Eucypris meadensis, a dilute-water,
spring-related species and Ilyocypris bradyi, a spring- and stream-related species settled a biocenosis in
the area at the time of deposition (see Table 4). Dominance of Eucypris meadensis indicates salinity did
not exceed 1000 mg L-1 TDS (Forester et al. 2005).
Ten valves of I. bradyi, in two batches of five shells each, were analyzed for carbon and oxygen
isotopes at the Department of Geosciences of the University of Arizona. In the previous section it was
highlighted that the Dove Springs Wash data are more negative than those obtained from Rose Valley. It
is inferred in this study that these values (replicates 1 and 2) indicate less evaporation during deposition of
Horizon 5Ab (Table 8). The stable isotope signature is consistent with the dilute water inference from
micro-invertebrates.
During deposition of the earlier Horizon 8Ab, very fine sand, silt, and clay (about 59%)
accumulated in a ponded or floodplain environment (Figure 1c). Two ostracode and three mollusk species
were identified from Horizon 8Ab including I. bradyi and E. meadensis accompanied by the gastropods
Physa virgata and Tryonia sp. and the clam Pisidium casertanum. Dilute waters hosted this faunal
association. Salinity did not exceed 2000 mg L-1 TDS, the maximum tolerance for Tryonia sp. but more
likely was close to 1000 mg L-1 TDS, the maximum tolerance for E. meadensis (Forester et al. 2005;
Sharpe 2002, 2003) (Figure 2b).
The stable isotope analysis of ten valves of I. bradyi, in two batches of five shells each, from
Horizon 8Ab yielded δ13C and δ18O values similar to those at Horizon 5Ab. As for this latter horizon, it
is inferred that the δ18O values (replicates 1 and 2) in Horizon 8Ab reflect less evaporation (Table 8).
The stable isotope signature is consistent with the dilute water inference from micro-invertebrates.
The lowermost Horizon 13Ab consisted of coarse- to medium-sand (about 66%) indicating a
high-energy alluvial deposit (Figure 1c). The unit was unfossiliferous. Based on organic sediments,
Horizon 13Ab yielded a calibrated radiocarbon age of 12,102±60 years B.P (10,152 BC), middle Younger
Dryas. The uppermost 5Ab Horizon returned a date of 2803 BC, falling near the end of the middle
Holocene. Lack of age control for Horizon 8Ab prevents establishing the site’s complete
paleoenvironmental history (Table 1; Chapter 4, this Volume).
Site Little Dixie Wash (LDW):
North of Dove Springs Wash, three localities (1, 2, and 3) were excavated along the Little Dixie
Wash (LDW). Little Dixie Wash consists of stratified alluvial floodplain/lacustrine deposits that form an
inset terrace along the main valley axis. LDW-Locality #1 was represented by two separate samples.
Horizon 2Ab consisted of sandy silty clay (Figure 1d) indicating a moderately low-energy environment.
Appendix D
Horizon 3Ab, not in direct contact with the previous unit, consisted of very fine sand, silt, and clay (about
83%) suggesting a low-energy system. The units were unfossiliferous. Dates of 8994 and 9536 BC were
obtained from organic material and Helisoma (Carinifex) newberryi shell associated with Horizon 2Ab.
Organic material from the 3Ab Horizon returned a date of 9796 BC.
Two samples from LDW-Locality #2 were analyzed for micro-invertebrates. Horizon II/2Ab was
formed by very fine sand, silt, and clay (about 79%) indicative of low-energy conditions in a ponded
system (Figure 1e); whereas, Horizon I/3ABkb consisted of silty sand (about 63%) suggesting moderately
high-energy conditions. The aquatic gastropod Helisoma (Carinifex) newberryi was the only species
identified from Horizon 2Ab (Table 7). The poor micro-invertebrate record and lack of age control limits
the paleoenvironmental reconstruction of Locality #2.
At LDW-Locality #3 five samples in stratigraphic continuity generated a coarsening upwards
sequence ranging from silty clay to silty sand (Figure 1f). Increasing particle-size indicates increasing
energy overtime from a wetland to a spring-flow environment. Gypsum crystals were abundant in the
lower horizons (5Ab to 7Ab), disappearing from the upper two units (3Ab and 4Ab) where microinvertebrates were recovered. Ostracodes and mollusks occurred at LDW-Locality #3 (Table 3). Three
dilute water, spring-related ostracode species were identified at Horizon 4Ab including
Fabaeformiscandona acuminata, Eucypris meadensis, and Cypridopsis okeechobei. This assemblage
suggests water salinity did not exceed 1000 mg L-1 TDS (Forester et al. 2005). In addition four aquatic
gastropods occurred at the same horizon: Pseudosuccinea columella, Helisoma (Carinifex) newberryi,
Gyraulus parvus, and Fossaria parva (Figure 2c). All four species support a wide range of salinity in a
variety of environments from swamps to streams (Table 6; Sharpe 2002, 2003). LDW-Locality #3 offered
the most complete age control in the region with an age range from 12,454±60 years B.P. (10,504 B.C.) to
10,703±95 years B.P. (8753 B.C.), the Younger Dryas. Ecologically, the micro-invertebrates, sediments,
and mineral composition indicate the gradual advancement of cold, wet climate as the Younger Dryas
progressed at the end of the Pleistocene.
By contrast, LDW-Locality #4 consisting of three samples from three separate horizons (3Ab,
5Ab, and 7Ab) show very fine sand, silt, and clay dominated each environment ranging from 74% to 95%
(Table 1; Figure 1g). The fine particle-size recorded at each of these horizons advocates for alluvial
floodplain conditions. All three units were unfossiliferous (Table 3). Radiocarbon dates from organic
material range from 10523 BC to 9374 BC. Lack of stratigraphic continuity prevents establishing the
geochronology of events.
Site China Lake Basin (Cores):
TTIWV-SB01:
Two separate samples from core TTIWV-SB01 were analyzed for micro-invertebrates. The upper
sample (5212-5303 cm bgs) consisted predominantly of fine sediments (about 49%) and medium sand
(about 38%) suggesting an alluvial floodplain environment deprived of micro-invertebrates. The lower
sample (6279-6340 cm bgs) consisted also of a combination of fine sediments (about 50%) and medium
sand (about 39%) part of an unfossiliferous alluvial floodplain (Figure 1h; Table 3). The calibrated
radiocarbon dates generated from each sample yielded ages in reverse stratigraphic order. The upper unit
yielded an age of 19,416±70 years B.P. (17,466 B.C.); whereas the lower unit yielded an age of
14,008±80 years B.P. (12,058 B.C.) (Table 1; Chapter 4, this Volume). Lack of micro-invertebrates and
the age reversal prevent the paleoenvironmental reconstruction of core TTIWV-SB01 location.
TTIWV-SB05:
Core TTIWV-SB05 consisting of four samples in stratigraphic continuity at the base of the record
was composed of medium sand (about 77%) in a clay matrix fining upwards to very fine sand, silt, and
clay (about 64%) implying a gradual decrease in energy (Figure 1i). Micro-invertebrates occurred
Appendix D
throughout the stratigraphic column. Ostracodes were extremely abundant at the base of the record
decreasing sharply upcore to rare and extremely rare. For descriptive purposes three biostratigraphic
zones were recognized at SB-05. Zone 1 contained the most abundant ostracode composition with
Limnocythere sappaensis dominating the environment (about 48%) associated with Limnocythere
ceriotuberosa (32%), Candona patzcuaro (about 19%) and a few specimens of Fabaeformiscandona
caudata? (less than 1%). Occurrence of L. sappaensis, a high-salinity tolerant species, indicates China
Lake was developing hypersaline conditions. However, at the time of deposition of Zone 1, salinity was
probably below 5000 mg L-1 TDS the maximum tolerance for C. patzcuaro (Table 4; Forester et al.
2005). This interpretation is supported by the moderately common presence of gypsum (Table 2). Zone 2,
an interval not studied for micro-invertebrates, is assumed to be ecologically unfeasible for biological
contents (a biological hiatus). Lack of information on this segment of core SB05 does not warrant further
analysis. Ostracodes re-appear in Zone 3 where they are rare to extremely rare. Limnocythere
ceriotuberosa, C. patzcuaro, and F. caudata? were the species recorded. A single shell of a juvenile
gastropod Helisoma (Carinifex) newberryi was identified at 3109-3170 cm bgs. Low to high
fragmentation and abrasion (5-30%) characterized the shells. Most specimens were coated by authigenic
calcite or gypsum and heavily corroded (Table 3). While fragmentation and abrasion may imply transport,
encrustation, coating and corrosion indicate diagenetic alteration. The poor faunal assemblage associated
with the taphonomic parameters supports the hypothesis that ostracodes were reworked to the site. Three
highly controversial radiocarbon dates place the environmental history of SB05 as a modern event.
However, the fact that these materials proceed from more than 30 m bgs argues against this possibility.
TTIWV-SB08:
Two samples from SB08 were analyzed for micro-invertebrates. The upper sample (2256-2316
cm bgs) consisted mostly of very fine sand, silt, and clay (about 85%); whereas the lower (2377-2438 cm
bgs) contained a lower proportion of the same particle-size fraction (about 64%) (Figure 1j). Tufa and
gypsum were the dominant minerals in both units indicating hypersaline conditions, confirmed by the
extremely rare occurrence of the ostracodes L. sappaensis and L. ceriotuberosa. Lack of age control
prevents further interpretation of the site’s environmental history.
TTIWV-SB10:
Core TTIWV-SB10 consisting of five samples obtained from three separate intervals identified as
zones 1, 2, and 3 (Figure 1k). At the base of core SB10, Zone 1 (below 5250 cm bgs) was composed
mainly of silty sand (more than 50% sand). Biotite was the dominant mineral associated with tufa and
gypsum crystals (Table 2). Zone 1 was unfossiliferous. The high concentration of authigenic minerals
forming the sand fraction suggests a hypersaline environment at the time of deposition. A biological
hiatus was identified between 4250 and 5250 cm bgs, no samples were analyzed from this interval. Zone
2 consisted of very fine sand, silt and clay (about 76% to 87%) dominated by tufa, quartz, and gypsum.
Ostracodes were common to very abundant throughout the interval. Three species prevailed in Zone 2
Cyprideis beaconesis, L. ceriotuberosa, and F. caudata? associated with L. sappaensis, and more rarely
C. patzcuaro (Figure 2f; Table 5). The relative abundance of F. caudata? and the adulthood ratios of all
other species indicate that ostracodes established a biocenosis in a dilute water environment regardless the
presence of high-salinity tolerant species like L. sappaensis, C. beaconensis, and L. ceriotuberosa (Figure
2f). Another hiatus is identified above Zone 2. No samples were available for analysis. Zone 3 is a brief
interval atop the record that resulted unfossiliferous. To date, no radiocarbon dates have been obtained
from core SB10 preventing the historical reconstruction of the environments.
TTIWV-SB28:
Two separate samples from SB28 were analyzed for micro-invertebrates. The two units consisted
of very fine sand, silt, and clay (greater than 73%) composed mostly of clastic sediments with some
authigenic minerals (tufa and gypsum) (Figure 1l). Gypsum was more abundant at the lower unit. A
Appendix D
single reworked valve of F. caudata? was identified in the upper sample (732-808 cm bgs). Core SB28
reflects an alluvial floodplain environment deprived of micro-invertebrates (Table 3). Lack of age control
limits further interpretation.
CLC-8, Cg:
A single sample from core CLC-8, Horizon Cg was analyzed for micro-invertebrates. Dominated
by medium sand (about 56%), the unit was unfossiliferous (Figure 1n; Tables 2 and 3). No further
interpretation is warranted.
CLC-9:
Two samples from core CLC-9 horizons 6Cg and 11Cg were analyzed for micro-invertebrates.
Horizon 6Cg reflects distal fan or slough deposits that overlie coarse, sorted beach sand and gravel. The
particle-size analysis conducted in this study indicates the unit is mostly very fine sand, silt, and clay
(about 78%) (Figure 1n). Downcore, Horizon 11Cg reflects lacustrine deposits that underlie beach
deposits. It was composed of medium sand (about 59%) (Figure 1n). Neither stratum contained microinvertebrates; therefore, a paleoecological interpretation is not warranted. The age control, however,
indicates that the upper unit accumulated sometime around 11,123±50 years B.P. (9173 B.C.); while the
lower unit formed around 17,780±50 years B.P. (15,830 B.C.) (Table 1). That is, this interval includes the
transition from the latest Pleistocene to earliest Holocene (Allerød-Younger Dryas).
Site China Lake Shell Beach (CLSB):
Snails from a lacustrine beach deposit consisting of sand and marl with Anodonta shells were
identified as Helisoma (Carinifex) newberryi. The site locates below the outlet of China Lake within
Searles Lake basin in an area sometimes known as Salt Wells Valley. Occurrence of P. trivolvis suggests
a slow flowing (lentic) aquatic system (Table 7). A radiocarbon date obtained from a mollusk shell (H.
(C.) newberryi) yielded an age of 13,387±50 years B.P. (11,437 B.C.), the early Allerød.
DISCUSSION
The ostracode and mollusk records from the latest Pleistocene to the earliest Holocene at China
Lake provide fragmentary evidence for changing limnological and climatic environments in the northern
Mojave Desert. The paleoenvironments of spring-related sites may be placed during the transition from
the late Pleistocene (19,416±70 cal. years B.P.) to the earliest Holocene (9,065±100 cal. years B.P.),
including parts of the Bølling/Allerød (14,008±80 to 12,454±60 cal. years B.P.) to the Younger Dryas
(12,454±55 to 11,482±55 cal. years B.P.). The China Lake basin cores, however, yielded poor or nil
geochronological control, therefore, the environments described in this study cannot be placed in time
with respect to neighboring locations (e.g., Owens Lake, Searles Lake).
To understand the significance of the species present in the area it is important to consider their
modern ecology. The ostracodes Limnocythere ceriotuberosa Delorme, 1967, Limnocythere sappaensis
Staplin, 1963, Candona patzcuaro Tressler 1954, Fabaeformiscandona acuminata (Fischer, 1851), and
Fabaeformiscandona caudata (Kaufmann 1900), the most common species in the China Lake area, today
live in lakes that have varied chemical, thermal, and hydroclimatic characteristics (Bradbury and Forester
2002; Forester 1986, 1987, 1991; Forester et al. 2005a; Delorme 1989; Forester et al. 1994; Smith and
Forester 1994). For example, C. patzcuaro lives in lakes, wetlands, and springs from Canada to central
Mexico thriving in a wide range of salinity (dilute to saline waters). In saline waters the species prefers a
low alk/Ca ratio often associated with Limnocythere staplini (Forester et al. 2005a) or L. ceriotuberosa, as
it is the case in the present investigation. Its ability to live in environments with high physical and
chemical variability makes it suitable to thrive in the China Lake area. Its occurrence in the lake cores is
inferred to indicate sharp environmental gradients in a frequently changing system.
Appendix D
F. caudata lives from Canada to northern Mexico in streams, flowing springs, and lakes
supported by streams in the dilute water solute field capable of supporting Ca-enriched waters (Table 4).
In the China Lake area, as for Owens Lake and other lakes in the Death Valley its occurrence may
indicate a relatively dilute system supported by significant streamflow (Forester et al. 2005b).
Little information is available for F. acuminata, a rare species reported in western North America
from southwestern Alberta to southern Nevada (Delorme 1970; Forester et al. 2005a). For the first time,
the species is identified from the southern Great Basin in southeastern California in Younger Dryas
sediments of the Little Dixie Wash, Locality 3 (11,482±55 cal years BP). This species also occurs in early
Holocene sediments of the North Caltrans Pit in Rose Valley (9811±40 cal years BP) and middle
Holocene deposits (4753±40 cal years B.P.) at Dove Springs Wash, Locality 5771 (Table 5). The cooccurrence of F. acuminata with other fresh-water species like Ilyocypris bradyi, Eucypris meadensis,
Cypridopsis vidua, and Cypridopsis okeechobei in the China Lake area advocates for a dilute water spring
supported by significant streamflow and ground-water recharge. As shown in Table 4, with the exception
of C. vidua, these species prefer low to moderate salinity and low alk/Ca ratios. Cypridopsis vidua’s
euryhaline (wide-salinity tolerance) properties are not in conflict with this interpretation since the species
thrives in springs and streams. In addition, ostracodes are associated with the gastropods Gyraulus
parvus, Fossaria parva, and Helisoma (Carinifex) newberryi all common in fresh-water lakes and
permanent streams (Miller 1989; Sharpe 2002) consistent with Younger Dryas cold-wet conditions.
Limnocythere ceriotuberosa lives in fresh and saline lakes from Canada to northern Mexico (Baja
California, Palacios-Fest unpublished data). Hydrochemically, the species prefers the low alk/Ca ratio but
thrives through the lower portion of the high alk/Ca ratio where it may co-exist with Limnocythere
sappaensis (Forester et al. 2005a, b). The species is known to live in lakes that receive seasonal pulse of
surface water or groundwater alternating with periods of evaporation. Apparently, this annual variability
is important for the species to complete its life-cycle. Its occurrence in the China Lake basin cores implies
seasonally high streamflow into an alkaline system.
Limnocythere sappaensis has a wide geographic range, living in lakes, wetlands, and springs from
Canada to central Mexico where high alk/Ca ratios and high TDS dominate the lake (Forester et al.
2005a, b). Its presence in the China Lake basin cores indicates periods of alkaline-saline conditions
supported by streamflow. According to Forester (1983) the species cannot tolerate low alk or high Ca
waters and so could not survive in China Lake at any time when high-Ca springs dominated the valley
bottom hydrology.
The previous paragraphs show a significant contrast between the spring-related areas and the China
Lake basin. The faunal assemblage recorded from cores TTIWV-SB05, SB08, SB-10 and SB-28 is similar to
that reported elsewhere in the southern Great Basin (e.g., Owens Lake, Carter 1997; Bacon et al. 2006; Death
Valley, Lowenstein et al. 1999; Forester et al. 2005b; Lake Bonneville, Oviatt et al. 1999; Balch et al. 2005;
Panamint Lake, Jayko et al. 2008). By contrast, the Mojave River Drainage Basin lacustrine systems (e.g.,
Silver Lake) contained very restricted faunal associations often times monospecific of Limnocythere
ceriotuberosa and/or Limnocythere bradburyi (Wells et al. 1989). However, lack of age control forbids a
discussion on the possible correlation among the several basins cited here.
CONCLUSIONS
•
•
The China Lake Legacy Project offered a unique opportunity to analyze the micro-invertebrate fauna
from the lake basin and surrounding areas.
For the first time, Fabaeformiscandona acuminata was identified in the Little Dixie Wash springs,
the Rose Valley springs, and Dove Springs Wash indicating a fresh-water source during the Younger
Dryas and through the early and middle Holocene.
Appendix D
•
•
The significant differences between the spring-related sites and the China Lake basin cores could not
be placed in geochronological perspective due to the poor age control obtained from materials as
diverse as organic sediments, plant/wood, or shell.
Further micropaleontological and geochronological control would be necessary to generate a better
paleoclimate history of China Lake.
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Boersma, pp 109-149. Elsevier North Holland, New York.
Rutherford, Jane
2000
Ecology illustrated field guides. Wilfrid Laurier University, Waterloo, ON, website:
http://info.wlu.ca/~wwwbiol/bio305/Database
Sharpe, Saxon E.
2002
Solute composition: a parameter affecting the distribution of freshwater gastropods, in
Conference proceedings: Spring-fed wetlands: important scientific and cultural resources of
the Intermontane Region: Electronic document. http://wetlands.dri.edu, accessed 12 March
2004.
2003
The Solute Ecotone, A Key to Past Hydrology In XVI INQUA Congress Programs with
Abstracts, 23-30 July, 2003. Reno, NV. (Poster
United States Department of Agriculture (USDA).
2003
Soils Survey Manual. University Press of the Pacific, Honolulu, Hawaii, pp. 207-209.
Von Grafenstein, U., U. Eicher, H. Erlenkeuser, P. Ruch, J. Schwander, and B. Ammann
2000
Isotope signature of the Younger Dryas and two minor oscillations at Gerzensee
(Switzerland): palaeoclimatic and palaeolimnologic interpretation based on bulk and biogenic
carbonates. Palaeogeography, Palaeoclimatology, Palaecology 159:215-229.
Wells, Stephen G., Roger Y. Anderson, Leslie D. McFadden, William J. Brown, Yehouda Enzel, and
Jean-Luc Miossec
1989
Late Quaternary Paleohydrology of the eastern Mojave River Drainage, Southern California:
Quantitative assessment of the Late Quaternary Hydrologic Cycle in large arid watersheds.
New Mexico Water Resources Research Institute, Technical Completion Report Project No.
14-08-0001-G1312.
Appendix D
Whatley, R.
1983
Some simple procedures for enhancing the use of Ostracoda in palaeoenvironmental analysis.
NPD Bulletin. (2): 129-146.
Wrozyna, C., P. Frenzel, P. Steeb, L. Zhu, R. van Gelden, A. Mackensen, and A. Schwalb
2010
Stable isotope and ostracode species assemblage evidence for lake level changes of Nam Co,
southern Tibet, during the past 600 years. Quaternary International 200(1-2).
Appendix D
Appendix D: Sample Identification Numbers, Stratigraphic Position, Bulk and Residual Weight and
Lithological Characteristics of Materials Analyzed for the China Lake Legacy Project, California.
Sample ID
Site/Bore Hole No.
Rose Valley, North Caltrans Pit
Rose Valley, South Caltrans Pit
Rose Valley, South Caltrans Pit
Dove Springs Wash, Loc. 5771
Dove Springs Wash, Loc. 5771
Dove Springs Wash, Loc. 5771
Little Dixie Wash, Loc. 1
Little Dixie Wash, Loc. 1
Little Dixie Wash, Loc. 2
Little Dixie Wash, Loc. 2
Little Dixie Wash, Loc. 3
Little Dixie Wash, Loc. 3
Little Dixie Wash, Loc. 3
Little Dixie Wash, Loc. 3
Little Dixie Wash, Loc. 3
Little Dixie Wash, Loc. 4
Little Dixie Wash, Loc. 4
Little Dixie Wash, Loc. 4
TTIWV-SB01
TTIWV-SB01
TTIWV-SB05
TTIWV-SB05
TTIWV-SB05
TTIWV-SB05
TTIWV-SB08
TTIWV-SB08
TTIWV-SB10
TTIWV-SB10
TTIWV-SB10
TTIWV-SB10
TTIWV-SB10
MK29-SB01/ TTIWV-SB28
MK29-SB01/ TTIWV-SB28
Lava End Locality Upper Black Mat
FW718o-17
Lava End Locality Lower Black Mat
China Lake
FW-CLC-8, Cg
China Lake
FW-CLC-9, 06Cg
China Lake
FW-CLC-9, 11Cg
Outlet
FW-CLSB-Snails
* See Chapter 4, this volume
** Dates in reverse order
RV-NCTP-3Cu
RV-SCTP-3Ab
RV-SCTP-4Ob
DSW-L#5771-5Ab
DSW-L#5771-8Ab
DSW-L#5771-13Ab
LDW1, 190-205-2Ab
LDW1, 260-280-4Ab
LDW-L#2-2Ab
LDW-L#2-3ABkb
LDW-L#3-3Ab
LDW-L#3-4Ab
LDW-L#3-5Ab
LDW-L#3-6Ab
LDW-L#3-7Ab
FW-CLDW-T3, 3Ab
FW-CLDW-T3, 5Ab
FW-CLDW-T3, 7Ab
FW718o-11
FW718o-13
FW718o-01
FW718o-02
FW718o-03
FW718o-04
FW718o-05
FW718o-06
FW718o-07
FW718o-08
FW718o-09
FW718o-10
FW718o-12
FW718o-14
FW718o-15
FW718o-16
Stratum
Depth
UTM Easting UTM Northing Bulk Wt. Fraction Wt >1mm >106mm >63mm <63 mm >1mm >106mm >63mm <63 mm
415295
416035
416035
408904
408904
408904
422956
422956
421743
421743
422592
422592
422592
422592
422592
421761
421761
421761
423635
423635
437475
437475
437475
437475
439201
439201
441112
441112
441112
441112
441112
3991136
3990462
3990462
3918620
3918620
3918620
3935635
3935635
3935117
3935117
3935262
3935262
3935262
3935262
3935262
3935245
3935245
3935245
3961800
3961800
3944908
3944908
3944908
3944908
3944941
3944941
3944072
3944072
3944072
3944072
3944072
416269
3985690
Munsell's Color Name
Radiocarbon Dates*
Code
(g)
73.2
71.5
24.8
21.2
40.8
67.7
58.5
16.6
20.9
65.2
65.7
34.2
25.5
12.8
9.7
2.5
13.4
2.6
12.7
15.7
6.6
8.9
5.2
9.9
3.1
6.6
7.0
3.0
7.1
3.9
17.1
8.5
3.5
10.4
(g)
2.6
1.4
0.5
2.8
0.7
38.4
11.5
4.1
2.9
29.8
2.1
2.1
1.6
0.1
0.2
0.7
1.0
0.5
2.4
2.6
0.3
0.1
0.1
0.4
0.2
0.1
1.0
0.2
0.3
0.1
0.7
1.0
0.2
0.2
(g)
68.8
67.4
22.3
16.7
38.9
27.7
45.0
10.9
17.2
33.0
60.6
27.7
19.7
8.5
8.5
1.4
11.4
1.6
9.3
12.1
4.1
7.1
4.3
8.9
2.7
6.0
5.4
1.9
5.1
3.2
15.4
6.8
2.0
8.9
(g)
1.8
2.7
2.0
1.7
1.2
1.6
2.0
1.6
0.8
2.4
3.0
4.4
4.2
4.2
1.0
0.4
1.0
0.5
1.0
1.0
2.2
1.7
0.8
0.6
0.2
0.5
0.6
0.9
1.7
0.6
1.0
0.7
1.3
1.3
(g)
27.3
28.7
75.4
79.5
59.5
32.7
41.9
83.5
78.7
35.2
33.8
66.1
75.1
87.2
89.8
49.0
38.0
50.9
12.1
15.6
11.9
9.6
8.8
1.7
17.6
12.0
23.4
20.2
22.9
19.9
17.1
23.3
26.0
11.1
(%)
2.6
1.4
0.5
2.8
0.7
38.2
11.5
4.1
2.9
29.7
2.1
2.1
1.6
0.1
0.2
1.4
1.9
0.9
9.7
8.3
1.6
0.5
0.7
3.4
1.0
0.5
3.3
0.9
1.0
0.4
2.0
3.1
0.7
0.9
(%)
68.5
67.3
22.3
16.6
38.8
27.6
44.8
10.9
17.3
32.9
60.9
27.6
19.6
8.5
8.5
2.7
22.2
3.0
37.5
38.7
22.2
38.4
30.7
76.7
13.0
32.3
17.8
8.2
17.0
13.4
45.0
21.4
6.8
41.4
(%)
1.8
2.7
2.0
1.7
1.2
1.6
2.0
1.6
0.8
2.4
3.0
4.4
4.2
4.2
1.0
0.8
1.9
0.9
4.0
3.2
11.9
9.2
5.7
5.2
1.0
2.7
2.0
3.9
5.7
2.5
2.9
2.2
4.4
6.0
(%)
27.2
28.6
75.2
78.9
59.3
32.6
41.7
83.4
79.0
35.1
34.0
65.9
74.7
87.2
90.3
95.1
73.9
95.1
48.8
49.8
64.3
51.9
62.9
14.7
85.0
64.5
77.0
87.1
76.3
83.6
50.0
73.3
88.1
51.6
Sand
Sand
Silty clay
Silty clay
Sandy silty clay
Silty sand
Sandy silty clay
Silty clay
Silty clay
Sandy silt
Silty sand
Sandy silty clay
Sandy silty clay
Silty clay
Silty clay
Silty clay
Sandy silty clay
Clay
Silty sand
Silty sand
Sandy silty clay
Silty clayey sand
Sandy silty clay
Clayey sand
Silty clay
Silty clay
Silty clay
Clay
Silty clay
Silty clay
Silty sand
Silty clay
Clay
Silty sand
Dark gray
Dark grayish brown
Very dark grayish brown
Light yellowish brown
Light yellowish brown
Dark grayish brown
Grayish brown
Gray
Light brownish gray
Gray
Pale yellow
Light gray
Pale yellow
Light brownish gray
Grayish brown
Grayish brown
Gray
White
Light gray
Very pale brown
Greenish gray
Greenish gray
Greenish gray
Greenish gray
Greenish gray
Greenish gray
Light gray
Light gray
Greenish gray
Light greenish gray
Light gray
Greenish gray
Grayish brown
Light brownish gray
2.5Y 4/1
2.5Y 4/2
2.5Y 3/2
2.5Y 6/4
2.5Y 6/3
2.5Y 4/2
2.5Y 5/2
2.5Y 5/1
2.5Y 6/2
2.5Y 6/1
2.5Y 7/3
2.5Y 7/2
2.5Y 7/3
2.5Y 6/2
2.5Y 5/2
10YR 5/2
10YR 6/1
10YR 8/1
10YR 7/1
10YR 8/2
Gley 1 6/1
Gley 1 6/1
Gley 1 6/1
Gley 1 6/1
Gley 1 6/1
Gley 1 6/1
10YR 7/2
10YR 7/1
Gley 1 5GY 6/1
Gley 1 10Y 7/1
10YR 7/1
Gley 1 5GY 5/1
10YR 5/2
10YR 6/2
13
C/ C
-13.1
-24.1
-12.7
-21.3
-24.5
-25.4
12,102±60
-20.4
-26.2
-25.2
-24.9
-25.1
-25.5
-25.7
10,703±95
11,482±55
11,689±110
11,698±55
12,454±60
Modern
Modern
-8753
-9532
-9738
-9747
-10504
Organic sediments
Soil (SOM)
Organic sediments
-25.5
-27.4
-22.8
19,416±70
14,008±80
176±40
-17466**
-12058**
1774
Beta-259415
Beta-259416
Plant (parts)
Plant (pine needles)
-22.4
-21.9
Beta-260154
Organic sediments
(black mat)
Organic sediments
(black mat)
-23.1
9,065±100
-7115
-24.5
10,656±100
-8706
-26.3
-24.5
-8.0
11,123±50
17,780±50
13,387±50
-9173
-15830
-11437
Source
Plant/Wood
Organic sediments
Plant/Wood
Plant/Wood
Plant/Wood
Organic sediments
OS-79561
OS-79562
OS-79584
OS-79563
OS-79585
OS-79564
OS-79565
Plant/Wood
Plant/Wood
Organic sediments
Organic sediments
Organic sediments
Organic sediments
Organic sediments
Beta-249418
Beta-249419
Beta-259414
III/3Ob2
180
416269
3985690
31.0
14.8
0.1
13.5
1.2
16.2
0.3
43.5
3.9
52.3
Silty sand
Light brownish gray
10YR 6/2
Beta-260153
Cg
VI/Cg
XI/Cg
Surface
1204
427
1030
0
431896
434038
434038
447540
3959918
3955277
3955277
3949962
57.1
49.1
70.8
0
36.1
10.7
43.8
0
2.7
0.3
1.2
0
31.9
9.9
41.8
0
1.5
0.5
0.8
0
21.0
38.4
27.0
0
4.7
0.6
1.7
0
55.9
20.2
59.0
0
2.6
1.0
1.1
0
36.8
78.2
38.1
0
Silty sand
Sandy silty clay
Silty sand
---
Light greenish gray
Greenish gray
Greenish gray
---
Gley 1 8/1
Gley 1 6/1
Gley 1 6/1
---
Beta-280679
Beta-280680
Beta-280686
Table 1
12
Calendar Years AD/BC
Modern
-9497
Modern
Modern
Modern
-10152
Lab No.
OS-79566
OS-79587
OS-79567
OS-79559
OS-79586
OS-79560
III/3Ob1
II/3Cu
III/3Ab
II/4Ob
IX (X)/5Ab
V (VI)/8Ab
-I (I)/13Ab
II/2Ab
I/3Ab
II/2Ab
I/3ABkb
V/3Ab
IV/4Ab
III/5Ab
II/6Ab
I/7Ab
3Ab
5Ab
7Ab
(g)
100.5
100.2
100.2
100.7
100.3
100.4
100.4
100.1
99.6
100.4
99.5
100.3
100.6
100.0
99.5
51.5
51.4
53.5
24.8
31.3
18.5
18.5
14.0
11.6
20.7
18.6
30.4
23.2
30.0
23.8
34.2
31.8
29.5
21.5
Textural Classification
(cm bgs)
250-260
200-220
470
102-112
220-225
430-450
190-205
260-280
30-40
50-60
195-210
260-265
295-300
310-330
340-360
155
210
267
5212-5303
6279-6340
3048-3109
3109-3170
3170-3231
5730-5791
2256-2316
2377-2438
671-707
4023-4084
4084-4145
4145-4206
6227-6279
732-808
2865-3018
165
Organic sediments
Organic sediments
Shell-f (gastropod)
Calibrated Years B.P.
11,447±55
Modern
Modern
Appendix D: Mineralogical Composition of Samples Analyzed.
Sample ID
Stratum
Depth
Quartz
Feldspars
Pyrite
Schist
Biotite
(cm bgs)
II/3Cu
250-260
VA
A
R
RV-NCTP-3Cu
III/3Ab
200-220
A
C
R
RV-SCTP-3Ab
II/4Ob
470
VA
A
MC
RV-SCTP-4Ob
IX (X)/5Ab
102-112
A
MC
R
DSW-L#5771-5Ab
V (VI)/8Ab
220-225
VA
A
R
R
DSW-L#5771-8Ab
-I (I)/13Ab
430-450
VA
A
R
DSW-L#5771-13Ab
II/2Ab
190-205
VA
A
VR
LDW1, 190-205-2Ab
I/3Ab
260-280
VA
A
R
LDW1, 260-280-4Ab
II/2Ab
30-40
VA
A
R
LDW-L#2-2Ab
I/3ABkb
50-60
MC
MC
LDW-L#2-3ABkb
V/3Ab
195-210
VA
C
R
LDW-L#3-3Ab
IV/4Ab
260-265
C
MC
R
LDW-L#3-4Ab
III/5Ab
295-300
VA
C
R
LDW-L#3-5Ab
II/6Ab
310-330
VA
C
R
LDW-L#3-6Ab
I/7Ab
340-360
VA
C
R
LDW-L#3-7Ab
3Ab
155
VA
A
FW-CLDW-T3, 3Ab
C
VR
5Ab
210
VA
MC
FW-CLDW-T3, 5Ab
C
7Ab
267
VA
FW-CLDW-T3, 7Ab
C
VA
C
MC
FW718o-11
5212-5303
VA
C
MC
FW718o-13
6279-6340
C
MC
C
FW718o-01
3048-3109
MC
FW718o-02
3109-3170
MC
FW718o-03
3170-3231
FW718o-04
5730-5791
C
MC
MC
FW718o-05
2256-2316
FW718o-06
2377-2438
VA
C
FW718o-07
671-707
C
MC
MC
FW718o-08
4023-4084
VA
MC
MC
FW718o-09
4084-4145
A
MC
MC
FW718o-10
4145-4206
A
C
VA
FW718o-12
6227-6279
VA
C
MC
FW718o-14
732-808
VA
C
MC
FW718o-15
2865-3018
C
MC
R
FW718o-16
III/3Ob1
165
C
MC
R
FW718o-17
III/3Ob2
180
Cg
1204
VA
C
R
FW-CLC-8, Cg
VI/Cg
427
VA
C
C
FW-CLC-9, 06Cg
XI/Cg
1030
VA
C
MC
FW-CLC-9, 11Cg
Surface
0
FW-CLSB-Snails
Explanation of acronyms: VA = very abundant; A = abundant; C = common; MC = moderately common; R = rare; VR = very rare
Table 2
Tufa
Root Casts
C
VA
MC
VA
C
MC
R
C
MC
MC
C
MC
VA
A
VA
R
MC
C
MC
C
Gypsum
Charcoal
C
R
VR
VR
Shell
Fragments
Ostracode
Fragments
R
R
R
R
VR
Bone
Fragments
R
R
A
VR
VR
VR
A
A
A
VR
MC
C
C
VA
VA
VA
VA
VA
VA
C
VA
VA
VA
A
MC
A
VA
VA
MC
MC
R
R
C
C
C
C
MC
R
R
MC
MC
R
R
MC
MC
MC
R
MC
R
MC
C
C
MC
A
A
A
C
C
C
MC
R
MC
A
VA
R
R
R
VR
VR
VR
VR
VR
VR
VR
VR
VR
VR
VR
VR
VR
VR
VR
VR
VR
VR
R
VR
Appendix D: Paleontological Composition and Taphonomic Characteristics of Micro-invertebrates of Samples Analyzed.
Molluscs and Ostracodes were Recorded. Ostracodes are the Subject of this Study; the other Groups are only enlisted as Major Group.
Taphonomy
Sample ID
Stratum
Depth
(cm bgs)
II/3Cu
250-260
RV-NCTP-3Cu
III/3Ab
200-220
RV-SCTP-3Ab
II/4Ob
470
RV-SCTP-4Ob
102-112
IX (X)/5Ab
DSW-L#5771-5Ab
V (VI)/8Ab
220-225
DSW-L#5771-8Ab
-I (I)/13Ab
430-450
DSW-L#5771-13Ab
II/2Ab
190-205
LDW1, 190-205-2Ab
I/3Ab
260-280
LDW1, 260-280-4Ab
II/2Ab
30-40
LDW-L#2-2Ab
I/3ABkb
50-60
LDW-L#2-3ABkb
V/3Ab
195-210
LDW-L#3-3Ab
IV/4Ab
260-265
LDW-L#3-4Ab
III/5Ab
295-300
LDW-L#3-5Ab
II/6Ab
310-330
LDW-L#3-6Ab
I/7Ab
340-360
LDW-L#3-7Ab
3Ab
155
FW-CLDW-T3, 3Ab
5Ab
210
FW-CLDW-T3, 5Ab
7Ab
267
FW-CLDW-T3, 7Ab
FW718o-11
5212-5303
FW718o-13
6279-6340
FW718o-01
3048-3109
FW718o-02
3109-3170
FW718o-03
3170-3231
FW718o-04
5730-5791
FW718o-05
2256-2316
FW718o-06
2377-2438
FW718o-07
671-707
FW718o-08
4023-4084
FW718o-09
4084-4145
FW718o-10
4145-4206
FW718o-12
6227-6279
FW718o-14
732-808
FW718o-15
2865-3018
FW718o-16
III/3Ob1
165
FW718o-17
III/3Ob2
180
Cg
1204
FW-CLC-8, Cg
VI/Cg
427
FW-CLC-9, 06Cg
XI/Cg
1030
FW-CLC-9, 11Cg
Surface
0
FW-CLSB-Snails
* Shells encrusted or coated by microcrystalline gypsum
Ostracodes
Mollusks
(#)
28
0
0
258
78
0
0
0
0
0
0
18
0
0
0
0
0
0
0
0
3
6
2
1119
4
0
0
21
780
27
0
1
0
0
0
0
0
0
0
(#)
2
0
0
0
42
0
34
0
0
0
0
12
0
0
0
0
0
0
0
0
0
1
0
0
0
0
0
0
0
0
0
0
0
0
0
0
0
0
3
Plant
debris
(%)
2
Fragmentation
(%)
10
Abrasion
(%)
10
Encrustation*
(%)
0
Corrosion
(%)
20
Coating*
(%)
0
Redox Index
Color
0
Clear
2
2
5
2
5
2
2
2
20
20
2
2
0, -2
0
Black, Clear
Clear
2
10
10
0
10
0
0
White
2
10
5
0
20
0
0
Clear
2
2
2
2
30
20
5
15
5
20
10
2
5
2
5
5
5
15
5
100
100
100
20
100
100
100
100
100
100
0
0
0
0
0
White
White
White
White
White
15
20
10
5
10
10
5
5
15
20
20
15
100
100
100
0
0, -1, -2
0, -1
White
White to gray
White to light gray
0
0
5
100
100
0
White
2
2
0
0
0
0
White
2
2
Table 3
Appendix D: Ecological Requirements of Ostracode Species Recovered from China Lake, California.
Species
Limnocythere sappaensis Staplin, 1963
Lakes, ponds
Permanence
Permanent or ephemeral
Temperature
4-32°C
Eurythermic
-1
Salinity* (mg L )
500-100,000
Chemistry* (meq L-1)
6.0-10,000
Freshwater to Ca-rich
Worldwide
Limnocythere ceriotuberosa Delorme, 1967
Lakes, ponds
Permanent or ephemeral
2-32°C
Eurythermic
500-20,000
2.0-100
Freshwater to Ca-rich
Western North America
Cyprideis beaconensis (Leroy), 1943
Streams, lakes, ponds
Permanent
2-32°C
Eurythermic
5,000-10,000
0.5-1
Freshwater to Ca-rich
Western North America
Cypridopsis vidua (O.F. Müller, 1776)
Candona patzcuaro Tressler 1954
Springs, streams, lakes
Springs, streams, lakes
Permanent or ephemeral
Permanent or ephemeral
2-32°C
2-32°C
Eurythermic
Eurythermic
100-4,000
200-5,000
0.10-50
0.5-30
Freshwater to Ca-rich
Freshwater to Ca-rich
Worldwide
Worldwide
Fabaeformiscandona caudata (Kaufmann 1900)
Streams, flowing springs,lakes, ponds
Permanent
2-32°C
Eurythermic
10-5,000
0.5-10
Freshwater to Ca-rich
Across North America
Fabaeformiscandona acuminata (Fischer, 1851)
Danielopol 1980
Ilyocypris bradyi Sars 1890
Eucypris meadensis Gutentag & Benson 1962
Lakes, ponds, springs
Permanent
7-25°C
Eurythermic
400-1,000
1.0-10
Freshwater to Ca-rich
Western North America but sparse
Streams, lakes, ponds
Springs, streams, lakes
Permanent or ephemeral
Permanent
7-25°C
7-25°C
Eurythermic
Eurythermic
100-4,000
300-1,000
0.10-50
0.7-10
Freshwater to Ca-rich
Freshwater to Ca-rich
Springs, streams, lakes
Permanent
7-25°C
Eurythermic
50-800
1-5
Freshwater to Ca-rich
Across North America
Western North America: from California to
southern Nebraska
Across North America but sparse
Cypridopsis okeechobei Furtos 1933
Sources:
Delorme (1969, 1989)
Forester (1991)
Forester et al. (2005)
Külköylüoĝlu and Vinyard (2000)
Palacios-Fest (1994)
Habitat
Table 4
Paleo/Biogeography**
Appendix D: Total and Relative Abundance of Ostracode Species Recovered, including Adult/Juvenile (A/J) and Carapace/Valve (C/V) Ratios.
Sample ID
RV-NCTP-3Cu
RV-SCTP-3Ab
RV-SCTP-4Ob
DSW-L#5771-5Ab
DSW-L#5771-8Ab
DSW-L#5771-13Ab
LDW1, 190-205-2Ab
LDW1, 260-280-4Ab
LDW-L#2-2Ab
LDW-L#2-3ABkb
LDW-L#3-3Ab
LDW-L#3-4Ab
LDW-L#3-5Ab
LDW-L#3-6Ab
LDW-L#3-7Ab
FW-CLDW-T3, 3Ab
FW-CLDW-T3, 5Ab
FW-CLDW-T3, 7Ab
FW718o-11
FW718o-13
FW718o-01
FW718o-02
FW718o-03
FW718o-04
FW718o-05
FW718o-06
FW718o-07
FW718o-08
FW718o-09
FW718o-10
FW718o-12
FW718o-14
FW718o-15
FW718o-16
FW718o-17
FW-CLC-8, Cg
FW-CLC-9, 06Cg
FW-CLC-9, 11Cg
FW-CLSB-Snails
Stratum
II/3Cu
III/3Ab
II/4Ob
IX (X)/5Ab
V (VI)/8Ab
-I (I)/13Ab
II/2Ab
I/3Ab
II/2Ab
I/3ABkb
V/3Ab
IV/4Ab
III/5Ab
II/6Ab
I/7Ab
3Ab
5Ab
7Ab
III/3Ob1
III/3Ob2
Cg
6Cg
11Cg
Surface
Depth
(cm bgs)
250-260
200-220
470
102-112
220-225
430-450
190-205
260-280
30-40
50-60
195-210
260-265
295-300
310-330
340-360
155
210
267
5212-5303
6279-6340
3048-3109
3109-3170
3170-3231
5730-5791
2256-2316
2377-2438
671-707
4023-4084
4084-4145
4145-4206
6227-6279
732-808
2865-3018
165
180
1204
427
1030
0
Bulk Wt.
(g)
100.5
100.2
100.2
100.7
100.3
100.4
100.4
100.1
99.6
100.4
99.5
100.3
100.6
100.0
99.5
51.5
51.4
53.5
24.8
31.3
18.5
18.5
14.0
11.6
20.7
18.6
30.4
23.2
30.0
23.8
34.2
31.8
29.5
21.5
31.0
57.1
49.1
70.8
0
Ostracodes
#
28
Dry-Mass
Ostracodes/g
0.3
258
78
2.6
0.8
18
0.2
3
6
2
1119
4
0.16
0.32
0.14
96.47
0.19
360 32.17
2
50
0.35
1
0.17
0
2
100
540 48.26
2
50
1
0.35
1
0
0.13
0
21
780
27
0.91
26
1.13
85
2
0.69
1
0.19
1
3 14.29
195
25
16 59.26
1
0.67
0.88
0.67
0.49
0.63
1
0.03
#
L. ceriotuberosa
%
A/J
C/V
#
L. sappaensis
%
A/J
C/V
#
C. beaconensis
%
A/J
C/V
#
C. vidua
% A/J
C/V
13 5.0
0.69
#
50
213 19.03
3 14.29
270 34.62
3 11.11
0.33
0.72
0.33
#
F. caudata?
%
A/J
C/V
0
3
10.90
7.41
C. patzcuaro
%
A/J
C/V
4
6
1
0.35
0
19.05
0.77
3.70
0.33
0
3
3
100
50
0
0.33
0
0
0.40
0
6
0.5
0.33
0
0.25
0.33
1
0
0
0
0.18
0.37
0.33
0
0
1
0
11 52.38
190 24.36
3 11.11
1
Table 5
100
#
8
F. acuminata
%
A/J
C/V
28.6 0.25
0.5
I. bradyi
#
%
A/J
20 71.4
1
C/V
0
13
5.0
0.08
0
53 20.5
49 62.8
0.08
0
8
44.4
0
0
0.70
0.82
#
E. meadensis
%
A/J
C/V
179 69.4
29 37.2
4
22.2
0.33
0.76
0.01
0
1
0
#
C. okeechobei
%
A/J
C/V
#
Species 1
%
A/J
C/V
Paleosalinity
Index
43
-113
-12
6
33.3
1
0.67
-189
-200
-150
200
173
250
40 5.13
2 7.41
0.38
1
0
0
-81
52
104
-200
Appendix D: Ecological Requirements of Mollusk Species Recovered from the China Lake Legacy Project.
Species
Physa virgata (Gould, 1855)
Fossaria parva (Lea, 1841)
Gyraulus parvus (Say, 1817)
Tryonia sp. Stimpson, 1865
Pseudosuccinea columella (Say, 1825)
Helisoma (Carinifex) newberryi (Lea, 1858)
Pisidium casertanum (Poli, 1795)
Habitat
Streams, lakes, ponds
Streams, lakes, ponds, marshes
Streams, lakes, ponds
Soft sediments, still water, springs
Amphibious, weedy, lakes,
streams, swamps
perennial freshwater lakes and
permanent streams
Springs, lakes, streams
Chemistry (in HCO3/Ca)*
Permanence
Salinity*
Permanent or ephemeral
1-5 mg L-1 Freshwater to Ca- or HCO3-rich
10-5,000 mg L-1
Permanent or ephemeral or moist soil 200-5,000 mg L-1 -2 to mg L-1 Freshwater to Ca- or HCO3-rich
Permanent or ephemeral or moist soil 10-5,000 mg L-1
1-5 mg L-1 Freshwater to Ca- or HCO3-rich
-1
Permanent
1-2 mg L-1 Freshwater to Ca- or HCO3-rich
1,000-2,000 mg L
Permanent
Permanent (eutrophic environments)
Permanent
NA= information not available
Sources:
Vokes and Miksicek, 1987
Miksicek, 1989
Bequaert and Miller, 1973
Webb, 1942
*Sharpe 2002, 2003
Table 6
NA
NA
~2,000 mg L-1
NA
NA
NA
NA
~2 mg L-1 Freshwater to Ca- or HCO3-rich
Appendix D: Total and Relative Abundance of Mollusk Species Recovered, including the Adult/Juvenile (A/J) Ratios.
Sample ID
RV-NCTP-3Cu
RV-SCTP-3Ab
RV-SCTP-4Ob
DSW-L#5771-5Ab
DSW-L#5771-8Ab
DSW-L#5771-13Ab
LDW1, 190-205-2Ab
LDW1, 260-280-4Ab
LDW-L#2-2Ab
LDW-L#2-3ABkb
LDW-L#3-3Ab
LDW-L#3-4Ab
LDW-L#3-5Ab
LDW-L#3-6Ab
LDW-L#3-7Ab
FW-CLDW-T3, 3Ab
FW-CLDW-T3, 5Ab
FW-CLDW-T3, 7Ab
FW718o-11
FW718o-13
FW718o-01
FW718o-02
FW718o-03
FW718o-04
FW718o-05
FW718o-06
FW718o-07
FW718o-08
FW718o-09
FW718o-10
FW718o-12
FW718o-14
FW718o-15
FW718o-16
FW718o-17
FW-CLC-8, Cg
FW-CLC-9, 06Cg
FW-CLC-9, 11Cg
FW-CLSB-Snails
Stratum/Horizon
II/3Cu
III/3Ab
II/4Ob
IX (X)/5Ab
V (VI)/8Ab
-I (I)/13Ab
II/2Ab
I/3Ab
II/2Ab
I/3ABkb
V/3Ab
IV/4Ab
III/5Ab
II/6Ab
I/7Ab
3Ab
5Ab
7Ab
III/3Ob1
III/3Ob2
Cg
VI/Cg
XI/Cg
Surface
P. virgata
Tryonia sp.
P. columella
Depth
Bulk Wt.
Mollusks
Dry-Mass
(cm bgs)
250-260
200-220
470
102-112
220-225
430-450
190-205
260-280
30-40
50-60
195-210
260-265
295-300
310-330
340-360
155
210
267
5212-5303
6279-6340
3048-3109
3109-3170
3170-3231
5730-5791
2256-2316
2377-2438
671-707
4023-4084
4084-4145
4145-4206
6227-6279
732-808
2865-3018
165
180
1204
427
1030
0
(g)
100.5
100.2
100.2
100.7
100.3
100.4
100.4
100.1
99.6
100.4
99.5
100.3
100.6
100.0
99.5
51.5
51.4
53.5
24.8
31.3
18.5
18.5
14.0
11.6
20.7
18.6
30.4
23.2
30.0
23.8
34.2
31.8
29.5
21.5
31.0
57.1
49.1
70.8
0
(#)
2
Mollusks/g
0.02
#
%
A/J
#
2
%
100
A/J
0
1
2.38
0
4
9.52
0
42
0.42
34
0.34
12
0.12
1
0.05
#
1
3
Table 7
%
8.33
A/J
0
Helisoma (Carinifex)
newberryi
#
%
A/J
34
100
0.09
3
25
0
1
100
0
3
100
1
Gyraulus parvus
#
4
%
33.33
A/J
0
Fossaria parva
#
4
%
33.33
Pisidium casertanum
A/J
0
#
%
A/J
37
88.10
0.19
Appendix D: Stable Isotope Data Obtained from Valves of Ilyocypris bradyi Present in Rose Valley, North Caltrans Pit and Dove Springs Wash.
Two batches of five specimens were clustered from the Dove Springs Wash to generate replicates to improve the paleoclimate signature.
Sample ID
Stratum/Horizon
13
18
Replica 1
C std dev
Replica 2
Average
Replica 1
-5.69
0.021
---
0.021
-7.54
---
-11.54
-11.67
0.020
0.028
0.024
-9.52
-10.85
-10.75
0.013
0.009
0.011
-9.93
Depth
(cm bgs)
Replica 1
II/3Cu
250-260
-3.85
---
DSW-L#5771-5Ab
IX (X)/5Ab
102-112
-11.79
DSW-L#5771-8Ab
V (VI)/8Ab
220-225
-10.66
d C VPDB
Replica 2 Average
Replica 1
O std dev
Replica 2
Average
-7.54
0.052
---
0.052
-9.11
-9.31
0.053
0.041
0.047
-10.02
-9.98
0.040
0.037
0.039
d O VPDB
Replica 2 Average
Remarks
18
RV-NCTP-3Cu
Table 8
18
d O values in shells reflect changes in water d O rather than
temperature. Increasing aridity at this time.
Increasing winter precipitation or less evaporation. Less
evaporation is inferred for the site at this time.
Increasing winter precipitation or less evaporation. Less
evaporation is inferred for the site at this time.
China L
Lake, Califfornia
Particcle-Size Anaalysis
Weig
ght Percent (%
%)
Roose Valley,
Northh Caltrans Pit
II/3Cu
R
Rose
Valley,
Soutth Caltrans Pitt
Dove Sprin
ngs
Wash Loc. 5
5771
IX (X)/5Ab
III/3Ab
V(VI)/8Ab
II/4Ob
-I (I)/13Ab
b
a
Coarse Saand
Medium
m Sand
Finee Sand
Very F
Fine Sand,
Silty and Clay
c
Unconformitty
FIGURE 1.
Particle-size analysis of: (a) Rose Valley, North Caltrans Pit; (b) Rose Valley, South Caltrans Pit;
(c) Dove Springs Wash Locality #5771.
China L
Lake, Califfornia
Particcle-Size Anaalysis
Weig
ght Percent (%
%)
Little Dixie Wash
Loc. 1
Litttle Dixie Wash
Loc. 3
100
50
II/2Ab
0
Ab
2A
Little Dixie W
Wash
Loc. 2
Little Dixie Wash
Loc.. 4
3Abb
200
3A
Ab
I/3ABkb
Depth (cm bgs)
260
5Ab
300
320
7A
Ab
350
d
f
e
g
FIGURE 1 continued.
(d) Little Dixie Wash, Locality #1; (e) Little Dixie Wash, Locality #2; (f) Little Dixie Wash, Locality
#3; (g) Little Dixie Wash, Locality #4
-
China L
Lake, Califfornia
Particcle-Size Anaalysis
Weig
ght Percent (%
%)
TTIWV
V-SB01
TTIWV
V-SB05
TT
TIWV-SB10
750
75
3500
1250
405
4000
2250
315
415
2750
4500
FW718o-06
Depth (cm bgs)
FW718o-13
Depth (cm bgs)
1750
3250
425
3750
5000
4250
325
525
4750
5500
5250
620
5750
630
6250
575
h
i
j
FIGURE 1 continued.
(h) bore hole TTIWV-SB01; (i) bore hole TTIWV-SB05; (j) bore hole TTIWV SB08;
(k) bore hole TTIWV-SB10
k
100
FW718o-05
3000
305
50
0
100
50
0
FW718o-11
TTIWV-SB08
T
China L
Lake, Califfornia
Particcle-Size Anaalysis
Weig
ght Percent (%
%)
TTIWV-SB28
China Lake-CLC
L
Lava
End LoccUpper Black M
U
Mat
8, Cg
FW718o-16
FW718o-14
9, 06Cg
FW718o-15
L
Lava
End LoccLower Black M
L
Mat
FW718o-17
9, 11Cg
l
m
n
FIGURE 1 continued.
(l) bore hole TTIWV-SB28; (m) Lava End Locality- Upper Black Mat and Lower Black Mat; and
(n) bore holes CLC-8 and 9. Particle-size analysis is described in the text.
China Lake
Lake, California
RV-NCTP-3Cu
(Rose Valley
Valley, North Caltrans Pit)
Ostracodes
Ilyocypris bradyi
Fabaeformiscandona acuminata
FIGURE 2a.
Micro-invertebrate relative abundance of: Rose Valley, North Caltrans Pit
China Lake, California
DSW-L# 5771 (Dove Springs Wash)
Ostracodes
Mollusks
IX (X)/5Ab
I bradyi
V (VI)/8Ab
V (VI)/8Ab
yyi
Tryonia sp.
sp
casertanum
FIGURE 2b.
Micro-invertebrate relative abundance of: Dove Springs Wash Locality #5771
China Lake, California
LDW-L# 3 (Little Dixie Wash)
Horizon 4Ab
Ostracodes
Mollusks
newberryi
FIGURE 2c.
Micro-invertebrate relative abundance of: Little Dixie Wash, Locality #3
China Lake, California
TTIWV-SB05
Mollusks
r ry
be
a ta
ew
)n
in i
f ex
s
as
x
ar
-M
(C
ry
sk
om
a
sD
li n
it y
sa
He
Mo
lis
l lu
le o
Pa
Fa
Ca
ba
nd
ef
on
or
m
ap
isc
In
an
cu
a tz
re
th e
cy
no
L im
de
ar
do
o
ae
pp
sa
r io
ce
re
th e
cy
no
L im
na
ns
ca
is
ud
a
os
er
tu b
s
as
M
ry sD
de
co
t ra
Os
i
?
Ostracodes
300
3000
Zone 3
350
3500
Zone 2
450
4500
500
5000
550
5500
Zone 1
1
10
100 0
20
Organisms/g
40 0
20
40
60
80
100 0
20
40 0.0001 0.001 0.01 0.1
1
10
100-200
0
2000.00
0.02
0.04
0.06 0
20
40
60
80
100
High
0.1
Low
Depth (cm bgs)
400
4000
Frequency (%)
FIGURE 2d.
Micro-invertebrate relative abundance of: Bore hole TTIWV-SB05
Organisms/g
Frequency (%)
China Lake, California
TTIWV-SB08
FW718o-05
Ostracodes
FIGURE 2e.
Micro-invertebrate relative abundance of: Bore hole TTIWV-SB08
China Lake, California
da
ec
i
Sp
Pa
es
1
le
os
al
in
ity
In
de
x
nd
on
ca
or
m
si
ba
ef
Fa
C
C
an
d
yp
rid
on
a
ei
s
pa
be
a
tz
cu
ar
o
co
ne
n
a
si
s
ca
u
is
ne
s
pa
sa
p
re
cy
th
e
no
Li
m
O
st
Li
m
no
ra
co
d
cy
th
e
es
re
D
ce
r
ry
-M
as
s
io
tu
b
er
os
a
ta
?
TTIWV-SB10
75075
Zone 3
125
1250
175
1750
Hiatus
2750
275
3250
325
375
3750
Zone 2
425
4250
Hiatus
475
4750
525
5250
Zone 1
575
5750
625
6250
10
20
Organisms/g
30 0
20 0
20
40
60 0
20
40 0
20 0
20
40
60 0
Frequency (%)
FIGURE 2f.
Micro-invertebrate relative abundance of: Bore hole TTIWV-SB10.
-120
-40
40
120
Hig
gh
0
Lo
ow
Depth (cm bgs)
225
2250
Jack Meyer