U.S. DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY

THE LAST INTERGLACIATION AT OWENS

LAKE, CALIFORNIA: CORE OL-92

Edited by 

James L. Bischoff1

Open-File Report 98-132

This report is preliminary and has not been reviewed for conformity with U.S. Geological 

Survey editorial standards (or with the North American Stratigraphic Code). Any use of 

trade, product, or firm names is for descriptive purposes only and does not imply 

endorsement by the U.S. Government

! U.S. Geological Survey, Menlo Park, CA 94025

1998
THE LAST INTERGLACIATION AT OWENS LAKE, CALIFORNIA

U.S. Geological Survey Open File Report 98-132

Table of Contents

Pages

1. Introduction and rationale of study (J.L. Bischoff) 1-5

2. Sedimentary features in core OL-92,0.9-82.5 m depth, Owens Lake, California 6-34 

(J. P. Smoot)

3. A high-resolution study of sediments from the last interglaciation at Owens Lake, 35-65 

California: Geochemistry of sediments in core OL-92, 83-32 m depth (J.L. Bischoff, 

D. Chazan, and R.W. Canavan, IV)

4. Climatic and hydrologic conditions in Owens Basin California between 45 and 145 ka 66-81 

as reconstructed from the high-resolution stable isotope records. (H.-C. Li, T.-L. Ku, 

J.L. Bischoff, and L.D. Stott)

5. Carbonate mineralogy in Owens Lake, California from 45-145 ka: a proxy for lake 82-98 

hydrology and productivity (H.-C. Li, T.-L. Ku, and J.L. Bischoff)

6. Sediment magnetic data (83-18 m depth) and XRF geochemical data (83-32 m depth) 99-119 

from lacustrine sediment in core OL-92 from Owens Lake, California (R.L. Reynolds, 

J.G. Rosenbaum, N. Mazza, W. Rivers, and F. Luiszer)

7. Diatom count data and Owens Lake paleolimnology during the last interglacial (J.P. 120-14 

Bradbury and M. Paquette)

8. Ostracodes from Owens Lake core OL-92 and the paleoenvironment of the last 142-15 

interglacial (R.M. Forester and C. Carter)

9. Testing climate stability during the last interglacial interval: pollen evidence from 156-17 

Core OL-92 (R.J. Litwin)

10. Thermoluminescence and optical dating of fine-silt-size feldspars from mud from 171-17 

Owens Lake, California Core OL-92 (G.W. Berger)

11. A test of uranium-series dating of ostracode shells from the last interglaciation at 180-18 

Owens Lake, California, core OL-92 (J.L. Bischoff, T.D. Bullen, R.W. Canavan IV, 

and R.M. Forester)
INTRODUCTION AND RATIONALE OF STUDY

James L. Bischoff

Owens Lake, located at the eastern base of the central Sierra Nevada (Fig. 1), was the 

terminus of the Owens River prior to the lake's complete desiccation shortly after 1913 

due to river diversion by the City of Los Angeles. During earlier wetter cycles, the lake 

overflowed to fill a series of downstream basins including China Lake Basin, Searles 

Valley, Panamint Valley, and ultimately, Death Valley (Smith and Street-Perrott, 1983). 

In 1992 the U.S. Geological Survey drilled a 323-m-deep core (OL-92) into Owens Lake 

sediments near the depocenter of the basin to obtain a continuous record of silty-clay 

sediment spanning the last 800,000 yrs. A multi-parameter reconnaissance study of the 

entire core (ca 7000-yr resolution), was reported in a 13-chapter summary volume (Smith 

and Bischoff, 1997). A document containing the numerical and other detailed forms of 

raw data collected by that volume's authors was prepared earlier (Smith and Bischoff, 

1993). The reconnaissance study provided an approximate time-depth model for the 

entire core, based on radiocarbon dates from the top 31m, the Bishop Ash (759,000 yrs) 

at 304 m, ten within-Brunhes paleomagnetic excursions, and a compaction-corrected 

mass-accumulation rate of 51.4 g/cm/lOOOyr (Bischoff et al., 1997a). Application of this 

model to observed sediment parameters indicates that Owens Lake was saline, alkaline, 

and biologically productive at times of decreased water-flow, and was generally 

hydrologically flushed and relatively unproductive during times of increased water-flow. 

Grain size, abundance of CaCOs, organic carbon, clay mineralogy, cation-exchange 

capacity of the clay fraction, fossil pollen, fish, ostracodes, and diatoms (see summary by 

Smith et al., 1997) all show cyclic variation down the core. CaCOs abundance, in 

particular, strongly reflects an approximately 100 ka dominant cycle, characteristic of

global ice-volume indicated by the MIS 818O record. Four of the last five marine isotope 

terminations are clearly shown in the OL-92 record.

An intermediate resolution (1500 yr) study was later undertaken and the results are 

reported by Menking et al (1997) and Bischoff et al (1997b). The results show that, to a

first order, the records match well the marine 818O record (MIS), but that the last 

interglaciation appears to span the entire period from 120 to 53 ka (corresponding to 36- 

75 m depth in the core, see Fig. 2). The interglaciation appears to have been punctuated 

by three short periods of wetter, spilling-lake conditions during an otherwise dry climate. 

This study also revealed that the timing of Termination II, the end of the penultimate 

glaciation, is proxy-dependent. The onset of the last interglaciation is shown by abrupt 

increases in a number of parameters including authigenic CaCOs and an abrupt decrease 

in rock flour, at about 118 ka (at 75.0 m). according to our time scale. In contrast, the

boundary appears to be gradual in the 8 18O record in which the change from light to 

heavy values begins at about 140 ka (85.5 m depth). Conditions of high carbonate and 

low rock-flour prevailed during the entire period from 118 ka until the glacial advance at 

53 ka (36 m depth) signaled the end of this long interglaciation.

The present study was focused on the Last Interglaciation, referred to as MIS 5 in the 

marine record, or as Sangamon and Eemian in the North American and European 

continental records respectively. The objective was to obtain a high resolution record of 

this interval as a comparison to the Holocene, in order to observe fine-scale climatic 

departures not observable at the resolution of the earlier studies. The earlier studies 

identified the interval 36-75 m depth in the core as representing this interglaciation. 

Accordingly, in order to include the transitions of the beginning (MIS 5/6 boundary) and 

end (MIS 4/5 boundary) sampling spanned the interval from 32-83 m depth, representing
the time span of ca 35-145 ka. Channel samples each of 10 cm length were taken 

continuously through this interval, with each sample representing about 250 years. These 

samples were dried and homogenized by light grinding, and aliquots were split for 1.)

TIC, TOC and acid-leachable chemistry (Bischoff and others, part 3), 2.) 818O and 813C 

and mineralogy of the carbonate fraction, (Li and others, parts 4 and 5) 3.) pollen studies 

(Litwin, part 9), and 4.) magnetic studies including bulk chemical analyses (Reynolds and 

others, part 6). In a second suite, point samples were taken approximately every 10 to 20 

cm for diatoms (Bradbury and Paquette, part 7) and every 20 cm for ostracodes (Forester 

and Carter, part 8). In addition, the sedimentary features of the interval were described 

and photographed in fine detail (Smoot, part 2). Also presented are the preliminary 

results of continuing efforts to improve the geochronology U-series results on 6 ostracode 

samples (Bischoff and others part 10) and the results of optical dating of 8 samples 

(Berger, part 11).

The purpose of the present volume is to present the data collected by the collaborating 

investigators in a single document. Data are reported in terms of depth rather than time 

because the chronology of the core is subject to refinement and further improvement. 

Because the data are correlative from study to study, the volume provides a basis for indepth analysis and interpretation by each principle investigator of his own data in light of 

the data obtained by others, and a citable data base for the preparation of formal 

publication in the outside literature.

ACKNOWLEDGMENTS

The chapters in this collection benefited from careful reviews by G.I. Smith, John Barron, 

Brian Edwards, and Robert Rosenbauer. I thank them warmly for their considerable 

efforts and for the many useful suggestions.

REFERENCES

Bischoff, J.L., Stafford, T.W., Jr., and Rubin, M. (1997a). A time-depth scale for Owens 

Lake sediments of core OL-92: Radiocarbon dates and constant mass-accumulation 

rate. In "An 800,000-year geologic and climatic record from Owens Lake, California: 

Core OL-92" (G.I. Smith and J. Bischoff, Eds.), pp. 91-98. Geological Society of 

America Special Paper 317.

Bischoff, J.L., Menking, K.M., Fitts, J.P., and Fitzpatrick, J.A. (1997b). Climatic 

oscillations 10,000-155,000 yr B.P. at Owens Lake, California reflected in glacial 

rock flour abundance and lake salinity in core OL-92. Quaternary Research. 48, 

313-325.

Menking, K.M., Bischoff, J.L., Fitzpatrick, J.A., Burdette,v J.W., and Rye, R.O. (1997). 

Climatic/hydrologic oscillations since 155,000 yr B.P. at Owens Lake, CA, reflected 

in abundance and stable isotope composition of sediment carbonate. Quaternary 

Research. 48, 58-68.

Smith, G.L, and Bischoff, J.L., eds (1993). Core OL-92 from Owens Lake, southeast 

California. U.S. Geological Survey Open File Report 93-683.

Smith, G.L, and Bischoff, J.L., eds. (1997). An 800,000-year geologic and climatic 

record from Owens Lake, California: Core OL-92 Geological Society of America 

Special Paper 317.

"2.
Smith, G.I., Bischoff, J.L., and Bradbury, J.P. (1997). Synthesis of the paleoclimate 

record from Owens Lake core OL-92. In "An 800,000-year geologic and climatic 

record from Owens Lake, California: Core OL-92" (G.I. Smith and J. Bischoff, Eds.), 

pp. 143-160, Geological Society of America Special Paper 317.

Smith, G.I., and Street-Perrott, F.A. (1983). Pluvial Lakes In the Western United States. 

In "Late Quaternary Environments of the United States" (H.E. Wright, Jr., Ed.), pp. 

190-211. University of Minnesota Press, Minneapolis.
36.5°

38°

Map area

T, ^^^F river Present-day _ _ _ _

playaorlake Pleistocene

5*srf^ river

Pleistocene 

lake

CA-NV 

border

Drainage 

divide

X \ \ '

\v< \<«J \ \ \\ +- I ^*

j V; \ \ O \ > / ^ % w. \_ V

w \Manly

0 20 40 60 Km

s0\^> -^(^>V^

i ^^

116° 115°

118°

Fig. 1. Location of Owens Lake and core OL-92. 

Extent of modem lakes and playas indicated by 

black pattern, maximum pluvial lakes by grey 

pattern, and basin outline by dashed lines.
OL-92

36m 

75m 

100 m

I oolite

| silty-clay 

| sand 

I tephra

53 kyr

-118 kyr

Last Interglaciation

200 m

300 m 759 kyr Bishop Ash

Fig. 2. Schematic drawing of Owens Lake core OL-92 

showing position of last Interglaciation and Bishop 

Ash.
U.S. DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY

SEDIMENTARY FEATURES IN CORE OL-92,

0.9-82.5 M DEPTH, OWENS LAKE, CALIFORNIA

by 

Joseph P. Smoot1

Open-File Report 98-132 (part 2)

This report is preliminary and has not been reviewed for conformity with U.S. Geological 

Survey editorial standards (or with the North American Stratigraphic Code). Any use of 

trade, product, or firm names is for descriptive purposes only and does not imply 

endorsement by the U.S. Government

!U.S. Geological Survey, Reston, VA 20192

1998
Introduction

The U.S. Geological Survey drilled a series of cores into Owens Lake sediments in 

1992 (OL92-1, 2, 3) that collectively penetrated to a depth of 323 m. Core was recovered 

using a rotary drill rig with three-inch (7.6 cm), split-spoon core liner. Individual drive 

depths varied considerably with a maximum of fifteen feet (4.6 m). The core drives were 

cut lengthwise into an archive and working half. Long core drives were cut into 1.5 m 

lengths (slugs). Preliminary core logs by Smith (1993, 1997) emphasized grain size and 

color variations. Sedimentary structures in those descriptions noted the presence of 

layering, sand pods, clastic dikes, or color veins. This report provides a more detailed 

description of the sedimentary structures and features of the archive half of OL92 cores for 

the depths 0.9 m to 82.5 m to provide environmental and paleoclimatic information.

Methods

The surface of each core slug was scraped smooth using a razor then photographed 

continuously in overlapping 15-cm intervals using 35-mm color slide film. Initial logs 

were made at the hand-lens scale on the prepared surfaces. Color and grain size reported in 

the sections were visually estimated in the initial descriptions. Each photographic slide 

was scanned at 1000 dpi resolution and 30-bit color on an Epson 1200-C scanner and 

imported into Adobe Photoshop 3.0 for Macintosh. The scanned images were 

reconfigured into a continuous image of each core segment and stored on 650 MB 

rewritable optical disks. Using the initial notes and the scanned images to check for 

uniformity of criteria, continuous sections were produced in Adobe Illustrator 5.5.

Descriptive Criteria

The nature of the sedimentary deposits were emphasized by their relative variations that 

produce visible changes in the character of the core (Fig. 1). Grain sizes were estimated 

using shadow charts for silt and coarser sediment. Clay and silty clay have a slick waxy 

feel, whereas silty mud and muddy silt have a grainy feel and commonly have a knap when 

scraped. Grain types are only noted where they affect the sedimentary character, such as 

the occurrences of mica or ostracode shells. Grain size distributions are noted where they 

define the nature of layering.

Graded beds have a gradual decrease of grain size from the base and reverse graded 

beds have a gradual increase of grain size from the base. Fine laminae that are comprised 

of diatoms, carbonate crystals, or tephra are differentiated where possible, but most 

commonly are queried to emphasize the lack of confirming data. Colors are used only to 

differentiate between sediment types and are not intended for differentiating the abundance 

of carbonate minerals, organic content, or other mineralogical features.

The thickness of layering in OL92 is based on the classification of McKee and Weir 

(1953). Laminae are less than 1 cm thick and thin beds are greater than 1 cm thick. I have 

used the additional division of thin laminae which are less than 1.0 mm thick and 

microlaminae which are less than 0.1 mm thick. Clay or mud partings are thin laminae or 

microlaminae within silt or sand layers. Layers are continuous across the width of the core 

unless otherwise noted. Discontinuous layers have the same thickness over their extent of 

occurrence and patchy layers are discontinuous layers with irregular lateral distributions 

within unbedded material. Thickness variations of the layers are indicated by the terms 

lenticular or pinch-and-swell. Streaky laminae are thin laminae to microlaminae with 

irregular discontinuous distributions and wispy bedding refers to discontinuous layers with 

indefinite boundaries. Bedding is mostly flat and significant variations from horizontal are 

shown to scale on the diagram. Wavy bedding and deformed layering are depicted on the 

diagram to provide the sense of the feature rather than the precise angles or spacing. 

Bedding contacts are depicted by black lines if they are sharp and by dashed lines ofpattern 

changes if they are indistinct or diffuse. Erosive or scour contacts appear to truncate
underlying deposits. Fault offsets and shear planes are shown to scale on the vertical 

sections with the actual changes in bedding orientation.

Other sedimentary features within the cores are identified in the description and shown 

to scale on the figures. Discontinuous areas of different sediment types or colors are only 

roughly depicted and referred to as blobs if they are relatively large and blebs if they are 

relatively small. Pods are blebs that have circular cross-sections. Burrows in the core are 

recognized as circular or ovate cross-sections of cylinders and are mostly shown as one of 

four symbols with no attempt to depict the location or shape of each burrow. The vertical 

distribution and relative abundance of burrows are indicated by the density of symbols. 

Burrow symbols with vertical parallel lines depict burrowing styles with a significant 

vertical component and diameters greater than 2 mm. If these symbols include black dots, 

the burrows are recognized by the concentration of coarser material in the tubes. Burrow 

symbols with long, wavy, horizontal parallel lines represent burrows oriented parallel to 

bedding that are greater than 2 mm in diameter. Burrow symbols with horizontal straight 

lines represent burrows oriented parallel to bedding that are less than 2 mm in diameter. 

Burrow mottling refers to situations where changes in color, grain size, or grain orientation 

produces curved planes that resemble partial sections of cylinders.

Arrows along the margins of the vertical core sections are used to denote successions of 

sedimentary features that are gradual from an abrupt basal contact. Large arrow heads are 

used for successions that involve decreasing grain size. Small arrow heads are used for 

successions that are defined by changes in layering style, an increase of grain size, or other 

criteria. Where successions are too small to be marked in this manner, their thickness and 

number are noted in the caption.

Missing intervals in the core are shown as blank with a black "X". Blank areas with 

breaks in the vertical section outline indicate where significant portions of the archive half 

of the core were removed during splitting or by sampling before descriptions. Areas that 

were too broken up to be smoothed, mostly by problems during splitting of the core, are 

shown schematically by irregular-shaped patterns of the sediment type. In several slugs, 

the actual observed thickness of sediment was significantly greater than that reported by 

Smith (1993) and recorded on the archive half of the core. The excess thickness is shown 

with a dashed border and the core depth is kept constant for that thickness for those 

intervals.

Discussion

The upper part of almost every drive in OL92-1 consists of clay with irregular blobs, 

blebs, and streaks of sediment. These intervals are characteristically soft and wet and 

exhibit a strong orientation of features parallel to the core wall. These intervals are 

identified as fluidized on the caption and are believed to represent coring artifacts. The soft 

gray clay is probably a mixture of drilling mud and fluidized sediment, whereas the blobs 

and blebs represent more coherent blocks of sediment that fell into the hole from the bottom 

of the previous drive as it was being removed. Most of the faulting observed in OL92 is 

also probably a coring artifact. High-angle normal faults formed as each drive was 

removed from the hole and a part of the core slipped through the core catcher. Low-angle 

shear planes, which are particularly abundant in the part of OL92-2 that was examined, 

formed from portions of the core spinning within the barrel during drilling. These shear 

planes have a diagnostic feature of flaring at the edges where they join material that lines the 

core barrel.

There is a strong correlation between changes in sedimentary style (Fig. 2) and changes 

in climatic proxies from these cores (Bischoff and others, 1997a, b; Bradbury, 1997; 

Litwin and others, 1997; Menking, 1997; Smith and others, 1997). Cold, glacial 

conditions are characterized by gray to green clay and silty clay with burrows and/or 

scattered sand and granules. Micaceous silty mud have mineralogy and diatom 

assemblages similar to the glacial conditions, but pollen assemblages indicative of warmer
conditions. Burrowed silty mud that exhibit vague banding are coincident with moderate 

carbonate values, mixed diatom assemblages, and warmer pollen. The warmest driest 

conditions by all indicators are coincident with sandy laminites. The fine-scale variability 

of sedimentary features within any sedimentary package also coincide with fluctuations of 

climatic indicators in this volume suggesting a higher resolution of climate change.

References

Bischoff, J.L., Fitts, J.P., and Fitzpatrick, J.A., 1997a, Responses of sediment 

geochemistry to climate change in Owens Lake sediment: An 800-k.y. record of 

saline/fresh cycles. In "An 800,000-year geologic and climatic record from Owens 

Lake, California: Core OL-92", G.I. Smith and J. Bischoff, eds., Geological Society 

of America Special Paper 317, p. 37-47.

Bischoff, J.L., Menking, K.M., Fitts, J.P., and Fitzpatrick, J.A., 1997b, Climatic 

oscillations 10,000-160,000 years BP at Owens Lake, California, reflected in 

geochemical proxies for glacial rock flour and for lake salinity in core OL-92: 

Quaternary Research, v. 48, p. 1-13.

Bradbury, J.P., 1997, A diatom-based paleohydrologic record of climate change for the 

past 800 k.y. from Owens Lake, California. In "An 800,000-year geologic and 

climatic record from Owens Lake, California: Core OL-92", G.I. Smith and J.L. 

Bischoff, eds., Geological Society of America Special Paper 317, p. 99-112.

Litwin, R.J., Adam, D.P., Fredericksen, N.O., and Woolfenden, W.B., 1997, An 

800,000-year pollen record from Owens Lake, California. In "An 800,000-year 

geologic and climatic record from Owens Lake, California: Core OL-92", G.I. Smith 

and J.L. Bischoff, eds., Geological Society of America Special Paper 317, p. 127- 

142.

Menking, K.M., 1997, Climatic signals in clay mineralogy and grain-size variations in 

Owens Lake core OL-92, southeast California. In "An 800,000-year geologic and 

climatic record from Owens Lake, California: Core OL-92", G.I. Smith and J.L. 

Bischoff, eds., Geological Society of America Special Paper 317, p. 25-36.

McKee, E.D., and Weir, G.W., 1953, Terminology of stratification and crossstratification: Bulletin Geological Society of America, v. 64, p. 381-390.

Smith, G.I., 1993, Field log of Core OL-92. In G.I. Smith and J.L. Bischoff, eds. "Core 

OL-92 from Owens Lake, southeast California", U.S. Geological Survey Open-File 

Report 93-683, p.4-57.

Smith, G.I., 1997, Stratigraphy, lithologies, and sedimentary structures of Owens Lake 

core OL-92. In "An 800,000-year geologic and climatic record from Owens Lake, 

California: Core OL-92", G.I. Smith and J.L. Bischoff, eds., Geological Society of 

America Special Paper 317, p. 9-23.

Smith, G.I., Bischoff, J.L., and Bradbury, J.P., 1997, Synthesis of the paleoclimatic 

record from Owens Lake core OL-92. In "An 800,(XX)-year geologic and climatic 

record from Owens Lake, California: Core OL-92", G.I. Smith and J.L. Bischoff, 

eds., Geological Society of America Special Paper 317, p. 143-160.
Figure 1

Detailed stratigraphic sections with brief caption for cores OL92-1, 2, and 3. Scale to left 

in each column is in meters and represents drilling depths as reported by Smith (1993). 

Small numbers on left side of each column denote the base of each slug with the core 

number/drive/slug shown for each. Correlative beds between cores are marked with pale 

gray dashed lines.

o
OL92-1 OL92-3

0.91

1.00

92-1/3/A

1.50

2.00

5.49

o o

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oo o°o o e o

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oo eo o e o o e

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O° Q O° Q O

V. fine sand with clay partings capped by efflorescent crust

Clay with tiny white crystals and capped by white crust

Crystal crust with vertical tubes (pan)

Clear crystal mush overlying layered clear and green crystals

Tan clay

White crystals with open crystal molds

Gray crystal mush with clear crystal blobs

Green sandy crystals alternating with white crystals

White crystal crust with vertical fabnc.

3 layers with clay partings 

Gray crystal mush with clear crystal blobs 

Clear crystal crust with vertical fabric 

Crystal sand (blades) with pore spaces. 

V. fine sand with holes near top

Poorly sorted oolitic sand up to granule size 4.00

92-3/1A

Poorly sorted oolitic sand up to granule size 

with randomly distributed large crystals

Fine sand with no crystals

4.50

Poorly sorted oolitic sand up to granule size 

with randomly distributed large crystals

5.00

5.50

92-3/l/E

>° o o° o 

> e o o e o

[>« O o o e o o'

o o e o o°o o e o ' O O O O O O

o o e o o e o o e o V O O O O O O

( o 0*0 0*0 0*0 

> o 0*0 0*0 0*0 

o 0*0 o^o 0*0 

o 0*0 0*0 0*0

9* O O*O O*O 0*O

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o o flo 9 o v 9 o o 

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4

Poorly sorted oolitic sand appears to have slight grading 

from base. Black grains observed at 3.77 and 4.02 m.

Coarse oolitic sand with large randomly distributed crystals 

and mud clumps near the bottom.

Fine oolitic sand with a hint of layering and scattered crystals. 

Overlies a thin red and green mud.

Fine oolitic sand with mud clumps bounded on top and bottom 

by coarse oolitic sand.

Fine oolitic sand with layering defined by grain size. Green mud 

has large crystals. Suggestion of large vertical burrows.

Green clay with crystals around outer edges, smaller ones 

near the upper contact Chalky patch occurs at contact

Green clay with crystals around outer edges. Fine sand as 

stringers and filling small burrows.

Green clay with lenses and pinch-and-swell layers of fine sand.

Green clay with sand-filled and clay-filled burrows.

Silty mud with a sharp basal contact grading upward to green 

^ clay. Lower pan is more silty going to more clay with 

silt-filled burrows.

LSilty mud with silt-filled burrows. Becomes more clayey 

upwards.
OL92-1 OL92-3

5.49

6.00

92-1/6/A

6.50

7.00

7.50

T

 * V ** *»«* -r *. * '**' ' » « « « ' A

B B

n B B 0

B B fl

B B 6 t

Green soft clay with irregular streaks and blobs of fine 

sand and silt indicating fluidizalion. i

Silly mud becoming more clay rich upward from a sharp 

basal contact Clay-filled burrow mottles.

5.90

6.00

Silty mud becoming more clay rich upward from a sharp 

basal contact Silt-filled burrows in clay-rich material 

at top and horizontal streaks of green clay in silt-rich base.

Silty mud becoming more clay rich upward from a sharp 

basal contact Silt-filled burrows in clay-rich materiaL. 

at top and horizontal streaks of green clay in silt-rich base.

7

Muddy silt filling broad, curved scour grading upward to 

silly mud with burrows.

6.50

Silty mud becoming more clay rich upward from a sharp 

basal contact Silt-filled burrow mottles.

Silty mud becoming more clay rich upward from a sharp 

basal contact Silt-filled burrow mottles.

7.00

92-.VI/C

Green soft clay with irregular streaks and blobs of fine 

sand and silt indicating fluidizalion.

Silty mud becoming more clay rich upward from a sharp 

basal contact Burrow structures were not noted.

Green clay with sharp upper and lower boundaries. Silt-filled 

burrows are common.

Coarse sand overlying a sharp contact grading upward into 

silly mud thai is progressively more clay rich. Silt-filled 

burrow mottles in the upper part

 Loss of section?

Green clay with randomly oriented orange burrows, fewer near 

the top.

"

fi V»

m

- *<? »" P *xfe&vv

^%wr"CfrN

Silty mud fining up from a sharp base. Silt-filled burrows.

Silly mud becoming more clay rich upward from a sharp 

basal contact Burrows are more horizontal near top where 

green clay defines laminae about 2 mm thick.

Silty mud becoming more clay rich upward from a sharp 

basal contact Burrows are more horizontal near top where 

green clay defines laminae about 2 mm thick.

Muddy silt filling steep-sided scour grading upward to 

silly mud with burrows.

A Silty mud becoming more clay rich upward from a sharp 

I basal contact Burrows are more horizontal near top in 

green clay.

Muddy sill forming thick laminae with sharp upper and 

lower contacts within a gradationally upward fining 

sequence to silly mud with silt-filled burrows. Burrow 

mottling throughout

Silty mud becoming more clay rich upward from a sharp 

basal contact Burrows arc more horizontal near top in 

green clay.

Silty mud becoming more clay rich upward.
OL92-1 OL92-1

7.90

8.00

8.50

92-1/7/A

9.00

92-1/8/A

9.50

10.00

000

000

00 0

Q \< G ; ' 0

0

A °

G

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LABEL

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000

000

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Green clay with small orange horizontal burrows. ' U.OO

10.50

Green clay with randomly oriented orange burrows.

Green clay with small orange horizontal burrows.

Green clay with randomly oriented orange burrows.

92-1/8/B

11.00

Core label that degraded in contact with the wet sediment and 

could not be removed.

Gray soft clay with irregular streaks and blobs of fine 

sand and silt indicating fluidization.

92-1/9//

11.50

Green muddy silt with thin stringers of greenish gray clay. 

This may be loose material from up hole that was recored, 

possibly including drilling mud or recirculaied clay.

Green clay with randomly oriented orange burrows.

Green clay with small orange horizontal burrows.

Green clay with randomly oriented orange burrows.

Green clay with small orange horizontal burrows.

Green clay with randomly oriented orange burrows.

Green clay with small orange horizontal burrows.

Green clay with randomly oriented orange burrows.

0 0, 0

0 . 0 0

0

Green day with randomly oriented orange burrows.

Green clay with small orange horizontal burrows.

Green clay with randomly oriented orange burrows.

Green clay with small orange horizontal burrows.

Gray soft clay with irregular streaks and blobs of fine 

sand and silt indicating fluidization.

o

000

Gray soft clay with irregular streaks and blobs of fine 

sand and silt indicating fluidization.

Green clay with randomly oriented orange burrows.
OL92-1 OL92-1

12.75

13.00

13.50

14.00

92-1/9/C

14.02

14.50

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Green clay with small orange horizontal burrows. 

Green clay with randomly oriented orange burrows.

Green clay with small orange horizontal burrows.

Silly mud layer with diffuse boundaries

Green clay with randomly oriented orange burrows.

Green clay with small orange horizontal burrows.

Green clay with randomly oriented orange burrows.

Green clay with small orange horizontal burrows.

Green clay with randomly oriented orange burrows. 

Green clay with small orange horizontal burrows.

Green clay with randomly oriented orange burrows. 

Green clay with small orange horizontal burrows.

Green clay with randomly oriented orange burrows.

14.8!

15.00

15.50

Green clay with small orange horizontal burrows.

Green clay with randomly oriented orange burrows and a

lense of muddy silt 

Green clay with small orange horizontal burrows.

Green clay with randomly oriented orange burrows that have 

smaller diameters than those above.

Green clay with small orange horizontal burrows.

Green clay with small randomly oriented orange burrows.

92-l/IO/R

16.00

Green clay with small orange horizontal burrows.

Green clay with randomly oriented orange burrows that

have smaller diameters than those above. 

Green clay with orange horizontal burrows that are little more

dots and streaks of orange. 

Green clay with small randomly oriented orange burrows.

Orange silt layer with sharp contacts

Green clay with no obvious burrows.

Green clay with small orange burrows that are not quite horizontal. 

Green clay with no obvious burrows. 

Green clay with orange horizontal burrows that are little more 

dots and streaks of orange.

16.50

Gray soft clay with irregular streaks and blobs of fine 

sand and silt indicating fluidization.

Muddy silt and fine sand with swirls of gray clay and patches 

of medium sand. Looks fluidized.

Gray soft clay with irregular streaks and blobs of fine 

sand and silt indicating fluidization. 17.00

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Gray soft clay with irregular streaks and blobs of fine 

sand and silt indicating fluidizalion.

Spots and blebs of orange silly mud within gray clay.

Gray soft clay with small clumps of green clay and 

irregular streaks and blobs of fine sand and sill 

indicating fluidization.

Spots and blebs of orange silty mud within gray clay.

Green silty mud with soft gray clay around outer edge. 

Looks fluidized.

Brown sand as lenses projecting in from sides. Probably 

injected into mud from movement along the core 

margin.

Muddy silt with blebs and streaks of green clay, 

very irregular contact Contact suggests a coring 

artifact

Green clay with dark band near top. The band may be a 

spin-out feature.

Green clay with orange silty blobs that may he burrows.

Green clay with two silly laminae that may be the 

edges of a bed.

Green clay sillier than above. Horizontal burrows define 

O.S cm bands separated by green clay.

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OL92-1 OL92-1

CD>

17.50

18.00

18.50

19.00

92-l/ll/H

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Green slightly silty clay with horizontal burrows that 

define 0.5 cm bands separated by green clay.

19.30

19.50

Gray-green clay with orange silty blobs that could be 

burrows, but edge-parallel streaks and irregular open 

cracks indicate fluidization.

Gray-green clay with orange silty blobs and gray clay streaks 

and blobs. May be burrow fabric, but looks more like 

fluidization.

20.00

Silty mud becoming more clay rich upwards from a sharp base 

possible burrow structures.

Green clay with sharp upper and lower boundaries.

Orange muddy silt filling scour and becoming slightly 

finer grained upward. Silty mud right at contact in 

lowest part

Silty mud becoming more clay rich upwards to a gray clay 

with silt-filled burrows. Silty mud is also burrow 

mottled and grades to an orange muddy silt at the base. _-. ~

Core broken into blocks of orange muddy silt

Orangish-gray silty mud becoming more clay rich upwards 

from a sharp base. Brown clay-filled horizontal burrows 

in distinct horizons.

21.00

Orangish-gray silty mud becoming more clay rich upwards. 

Brown clay-filled horizontal burrows in distinct horizon. 

Broken up zone near the base.

92-1/12/A

21.50

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Green slightly silty mud with small brown burrows 

Orange silty layer that is penetrated by brown tubes

Green slightly silty mud with graded dark-to-light silty 

laminae at base becoming more diffuse and widely 

spaced upwards as brown burrows become more 

abundant and less horizontal.

Green slightly silty mud with graded dark-to-light silty 

laminae at base becoming more diffuse and widely 

spaced upwards as brown burrows become more 

abundant and less horizontal. A 3 mm-lhick light 

laminae near the top.

Green slightly silty mud with graded dark-to-light silty 

 laminae at base becoming more diffuse and widely 

spaced upwards as brown burrows become more 

abundant and less horizontal, then becoming more 

distinct and less bioturbated in gradation to the 

overlying unit

Green slightly silty mud with graded dark-to-light silty 

laminae at base becoming more diffuse and widely 

spaced upwards as brown burrows become more 

abundant and less horizontal.

Silty mud with a 1 cm thick orange, silty thick lamina 

and a 3 cm thick orange silty thin bed disrupted by 

small horizontal burrows. Between the silt layers 

burrows arc filled with white material (tephra?).

Silty mud becoming more clay rich upwards to a gray, 

slightly silty clay with brown, clay-filled burrows.
OL92-1 OL92-1

21.60

92-1/12//

22.00

92-1/I3M

22.50

23.00'

23.50

92-1/13/B

23.57

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23.85

24.00

Silty mud with streaks and blobs of clay. Looks 

fluidized.

Muddy silt with 1 mm diameter burrow mottles filled 

with light clay and dark material. A thin dark band 

occurs near the top.

Muddy silt alternating with thin bands of lighter silty 

mud that have small horizontal burrow mottles.

Silty mud with graded dark-to-light laminae at the base 

becoming less distinct upwards to a more mud-rich top. ,

Silty mud with graded dark-to-light laminae at the base 

becoming less distinct upwards with more brown clayfilled burrows. A light clay(?) layer separates two 04 50 

graded laminae at the base.

r Silly mud with graded dark-to-light laminae at the base 

becoming less distinct upwards with more brown clayfilled burrows, then more distinctive grading to the 

overlying unit. A small pebble occurs in the bioturbated 

mud.

Silly mud with graded dark-to-light laminae at the base 

becoming less distinct upwards with more hrown clayfilled burrows, then more distinctive grading to the 

overlying unit.

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92-1/13/Cr- -^ -, ^- -Z' *

Silly mud with graded dark-to-light laminae becoming 

less distinct upwards with more brown clay-filled 

burrows, then more distinctive grading to the overlying 

unit. A medium sand forms a graded bed at the base of 

the unit. It has mud mottles like large burrows.

25.00

Silty mud with graded dark-to-light laminae becoming 

less distinct upwards with more brown clay-filled 

burrows. A large granule occurs in the bioiurbaicd 

mud.

Silty mud with vague dark-to-light laminae disappearing 

upwards with more brown clay-filled burrows. A large 

granule occurs in the bioturbated mud.

Silty mud with brown clay-filled burrows. At the base, 

is an orange, streaky. silt(?) layer overlain by a light 

clay with a sharp top and base.

, Silty mud becoming more clay-rich upwards from a 

sharp basal contact. Burrow mottles near top.

26.00

ft

0 .

8* ~ 0

8

Silty mud with dark and light laminae at the base 

becoming less distinct upwards with more brown clayfilled burrows.

Silty mud with graded dark-to-light laminae at the base 

becoming less distinct upwards with more brown clayfilled burrows.

Silty mud with graded dark-io-light laminae at the base 

becoming less distinct upwards.

Silty mud with graded dark-io-lijht laminae near the top 

becoming less distinct downward. A light clay(?) layer 

occurs near the top.

Gray clay with scattered silt. sand, and granules.

Slightly silly mud with random burrows.

Muddy silt with sharp top and basal contacts. 

Slightly silty mud with random burrows.

Silty mud with streaks of clay, and irregular pods of 

muddy silt and sand indicating fluidi/ation.

Slightly silly mud with random burrows. 

Slightly silly mud with small horizontal burrows.

Slightly silly mud with random burrows. 

Slightly silly mud with small horizontal burrows.

Slightly silly mud with random burrows that become 

smaller and more horizontal downward as mud gets 

sillier.

Silly mud that is sandier towards an abrupt basal contact 

and more clay rich upward with progressively larger 

burrows.

Gray, slightly silly mud with random sill-filled burrows 

gradationally overlying muddy sand and silt defining 

two graded layers.

Silty mud that is more clay rich upward with 

progressively larger burrows. Overlies a sharp basal 

contact.

Gray, slightly silty mud with random sill-filled burrows.

I Co
OL92-1 OL92-1

26.00

t

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92-1/14/A

^0\ %

26.50

27.0O

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27.50'

92-I/I4/B

28.00-

(

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:

Slightly silly mud with sill-filled burrows 

gradationally overlying poorly sorted muddy 

sand with an abrupt basal contact

Slightly silly mud with silt-filled burrows

gradationally overlying poorly sorted muddy

sand with an abrupt basal contact 

Silty mud becoming more clay rich upward from a

sharp base. Burrow moules are smaller and more

horizontal toward base. 

Silty mud becoming more clay rich upward from a

sharp base. Burrow moules are smaller and more

horizontal toward base.

Silly mud becoming more clay rich upward from a 

sharp base. Burrow moules are smaller and more 

horizontal toward base.

Silty mud becoming more clay rich upward from a 

muddy silt with a sharp base. Burrow moules are 

smaller and more horizontal toward base.

Silly mud becoming more clay rich upward from a 

sharp base. Burrow moules are smaller and more 

horizontal toward base.

Silly mud becoming more clay rich upward from a 

sharp base. Burrow mottles are smaller and more 

horizontal toward base.

Silty mud becoming more clay rich upward with mostly 

horizontal clay-filled burrows. Faint layering near the 

base and burrows are smaller and more horizontal.

28.301

28.50

29.00

29.50

Silty mud becoming more clay rich upward from a 

sharp base. Burrow moules are smaller and more 

horizontal toward base. Upper contact is gradational 

to the next unit.

Gray clay with brown random burrows gradationally 

overlying sandy mud with pods of sand (burrows?).

Gray clay with brown random burrows.

30.00

30.50

.« 

Loose clumps of gray silty mud.

Brown silty mud with gray clay injected from the 

edges and small blebs of gray clay that look 

a little like burrows, but are probably fluidization 

features.

Soft gray clay with clumps and folded blebs of brown 

silty mud indicating fluidized sediment
OL92-1 OL92-1

30.60

31.00

92-1/16/A

31.50

32.00'

32.50

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Brownish silt with blobs of coarser silt

Soft gray clay with folded blebs and stringers of 

brownish silt Probably fluidized.

Brownish muddy silt with stringers of gray clay. 

Probably fluidized.

Gray clay with small clumps of muddy silt around the 

edges and scattered sand grains. Fluidized?

Brown silly mud with scattered sand grains.

Brown silly mud in loose blocks with some small 

blocks of gray clay.

Brown silly mud is coarser downward and has mostly 

horizontal burrow mottles near top.

32.90

92-1/17/A

33.00

33.50

Brown silly mud with mostly horizontal burrows.

Green clay with sequences of small brown horizontal 

burrows overlain by small brown random burrows 

that become larger upwards.

Dark silly layer with sharp upper and lower contacts and 

green clay-filled horizontal burrows.

92-1/17/B

34.00

Green clay with sequences of small brown horizontal 

burrows overlain by small brown random burrows 

that become larger upwards.

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Alternating dark silly layer with sharp upper and 

lower contacts and green clay-filled horizontal burrows 

and green clay with brown horizontal burrows.

35.00

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Green clay with horizontal burrows overlying dark 

silly layer with green horizontal burrows.

Light mud with faint layers defined by 

concentrations of dark silu

Sandy mud with scattered granules becoming 

more silly and clay-rich upwards with 

mottles that are probably burrows. George 

Smith says the basal contact is sharp, hut I 

didn't see that.

Silty mud becoming coarser upwards and more 

micaceous.

Soft. gray, sticky clay with separation cracks and 

blebs of silL Fluidized.

Brown silt irregularly injected into clay. Silt 

parallels the core margin in plan view indicating 

fluidizau'on during coring.

Brown silt irregularly with irregular streaks and 

hlobs of gray clay indicating fluidization.

Sandy mud becoming less sand rich upwards from 

a sharp base.

Sandy mud becoming less sand rich upwards from 

a sharp base.

Sandy mud becoming less sand rich upwards. 

Sand pods (burrows?) in mud at top. Basal 

contact is diffuse.
OL92-1 OL92-1

35.15

35.50

92-l/lX/B

36.00

36.50

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37.07

Silty mud with more sand upward and downward. 

Diffuse contacts with adjoining units.

Sandy mud with scattered pods of sand (burrows?) 

Contacts are gradational.

Silty mud becoming sandier upward to the overlying 

unit Basal contact is diffuse, but more abrupt.

Sandy mud with scattered pods of sand (burrows?). 

Becomes less sandy downwards.

Silty mud with silt-filled burrows and ostracods 

near the base.

Tan silty clay with horizontal burrows.

Silty mud with sill-filled burrows. A single grain 

layer of sand rests on an abrupt contact Lower 

pan is a gray clay with scattered sand and silt 

grains.

Buff, muddy silt with osiracodes(?).

Gray clay with bands of sandier material that 

includes black grains.

Greenish silty mud with thin streaks of gray 

clay. Silt may be diatoms.

37.50

38.00

Gray mud with green mottles.

Gray mud with blobs and streaks of yellowish 

silty mud indicating fluidization.

38.50

Coarse sill filling burrows and forming layers may

be small ostracodes. 

Green silty clay with orange silt forming thick

laminae.

Green silty clay with orange-to-yellow silt forming 

thick laminae near the base and silt-filled tubes near 

the top.

Light laminae (1 mm thick) of dialoms{?) with dark green 

clay partings.

Silty clay with ostracodes filling burrows and forming 

lenticular layers. 39.00

Gray mud with green mottles.

s

Greenish silt with small blebs and streaks of 

brown silt and gray clay. Looks fluidized.

Crumbly green clay with ostracodes.

Graded laminae (0.5-1.0 cm) of dark silt and 

light clay. Ostracodes in light layers and filling 

tubes near top.

Green clay with vague color bands and scattered 

ostracodes.

Green clay with white lense of coarse ostracode 

fragments and concave-up lenses of ostracoderich sand overlying sharp contacts.

Laminated sill and clay comprising four upwardfining units. The basal lamina of each unit is an 

ostracode-rich sand overlying a sharp, possibly 

erosive contact and grading upward imo a green sill 

with a thin, brown clay cap. Subsequent laminae are 

comprised of graded silt with a brown clay cap. These 

laminae are less distinct upward in each unit with an 

increase in abundance of small horizontal burrows.

Silty mud with ostracodM?). 

A Brown and green clay laminae overlying graded 

T laminae of very fine sand to clay.

Two sequences of sand overlying a sharp contact with 

, a green clay drape then clay with green bands and 

tubes filled with sand and silt

 

Two sequences of sandy material overlying a sharp 

contact followed by graded laminae of dark sandy 

clay-to-lighi silty clay that become broader and 

, more diffuse upwards.

Ostracode-rich sand laminae with clay drapes 

overlying sharp contacts followed by graded 

laminae of dark sandy clay-to-lighi silly clay 

that become broader and more diffuse upwards 

with increased disruption by ostracode-filled 

tubes.

Laminated clay in 2-5 cm thick sequences consisting of 

very fine sand-grading-to-clay laminae(about 0.5-2.0 mm 

thick) near the base overlain by laminae (0.5-0.25 mm 

thick) consisting of clay alternating with white material 

(diatoms?). Ostracodes in the clay near the top.
OL92-1 OL92-1

39.25

j » i ' » ' ' '

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39.50

92-I/I9/B §

40.00

fs>^s>^j^!^Sgv:

40.50

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41.00

41.50

92-1/20/A

Continuation of overlying pattern with more sand 

that may include oscillatory ripples.

Muddy sand alternating with clay that has sand-filled 

burrows.

Well-sorted fine sand lenses and pinch-and-swell layers 

alternating with clay that has sand-filled burrows.

Fine sand lenses and pinch-and-swell layers alternating 

with sandy clay that has sand-filled burrows.

Fine sand with mud clumps. Looks disturbed (coring

artifact?). 

Hard, chalky layer with alternations of fine sand or silt

and mud.

Green clay with scattered sand at top. vague banding and 

silt-filled burrows toward base.

41.54

42.00

Sticky gray clay with blobs of brownish muddy sill 

indicating fluidizaiion.

Brownish muddy sill with streaks of gray clay suggesting 

fluidizaiion.

Gray silty mud with layers of greenish clay disrupted by random

burrows. Thicker layers have sharp upper and lower contacts.

Thinner clays are streaky. All are disrupted by random burrows.

Basal contact is sillier grading up to silly clay. White blebs

along top of thickest clay layer. 

Gray silly mud grading upward to greenish clay.

Gap.

Green clay with scattered ostracodes and dark silly vague laminae.

Gray silly mud with scattered ostracodes comprising graded layers 

intcrbedded with green clay and very fine, ostracode-rich sand 

layers that pinch-and-swell or are flat Layers are disturbed by 

burrows.

Green silly mud grading up from coarse ostracode-rich sand 

overlying sharp base. Internal beds defined by concentrations of 

ostracode-rich sand, all disturbed by sand-filled burrows. Upper 

contact is brown.

42.50

i i Graded beds of sandy mud with ostracodes upward to 

silly mud with sand-filled burrows. Upper contact of 

each bed is orangish. Lowest bed is only slightly sandy 

at base and does not have orange at top.

92-1/20/B

43.00

Gray sandy clay with ostracodes grading up lo greenish clay with a 

band of greenish clay near the middle. Sand-filled burrows are 

common. Core is broken up in the middle of this unit.

Gray clay has sandy base and patchy orange stains near contacts.

Graded beds of sandy mud with ostracodes upward to silty mud 

with sand-filled burrows. Upper contact of each bed is orangish. 

Light-colored layer is broken up near base of uppermost bed.

Pale green clay with sandy layers comprising a graded sequence.

Graded thick laminae of fine sand going to silly mud. Upper two 

layers appear reverse graded from clay to silly mud. Next two 

layers are thicker sand. Lower half consits of alternations of mmthick graded laminae and cm-thick layers more clay rich.

Orange, med. sand with ostracodes and internal flat beds. 

Probably a wave-formed turbidile.

Dark-green silty mud in graded laminae that are sandy near top.

Dark silly graded laminae grade up to pale green laminae

then burrow-mottled silty mud. Pale green laminae at

top. 

Coarse, orange sand appears graded. Tephra? Blocks of chalky

clay at base appear graded. 

Pale green clay with graded sandy laminae at base (0.5 mm thick)

becoming fainter and more disrupted by tubes upward. Top of

layer is light chalky, and fractured. 

Orange silt with sharp base and slightly diffuse top. Tephra? 

Pale green clay with sand laminae at base grading upward to silt

laminae. Thicker laminae are not graded, but finer laminae are.

All layers are disrupted by horizontal burrows. 

Thick laminae of pale green clay alternating with silt layers of

similar thickness. A thin dark sandy layer near the base

may be a tephra. Some mottling by horizontal burrows.

43.50

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Graded laminae (5 mm) of dark silty mud to green 

clay. Minor disruption by horizontal burrows.

j L Graded laminae of fine sand to clay grading upward 

to silt-clay laminae, then to very thin beds of 

silly mud and clay, and finally clay with silty 

partings. Burrow mottling increases upward. 

Graded laminae (5 mm) of dark silty mud to green 

clay grading up to clay with silty partings and 

biolurbation.

I , Two sequences with thin sand laminae at the base 

overlain by green clay with silly partings and 

burrows. Light laminae occur around the sandy 

laminae at the base.

Silly mud with vague banding becoming more clay 

rich upwards.

Light colored and brown clay beds alternating with 

silly mud.

Two sequences with graded sandy layers at the base 

and a thicker sand bed. overlain by clay with silly 

parting and biolurbation. Thin white lamina at base 

of lowest unit

Thin sand bed and light colored laminae overlain by 

clay with silly partings and burrows.

Disrupted clay with hints of white laminae in large 

chunks. 

Disrupted clumps of orange muddy sand.

Disrupted clumps of silly mud.

Green silly clay with ostracodes and clay layers. 

Burrows mottling disrupts layering. Basal contact 

is sharp.

Dark green silty to sandy mud with burrow mottling. 

Lower pan is coarser with layers of medium sand 

and sand-filled burrows.

Pale green clay is also present in loose clumps 

including a sharp contact with underlying layer.

Loose clumps of green silly clay with ostracodes.

t L Gray clay with hlebs of muddy silt. Fluidized.

Sandy mud overlying scour contact grading up into 

silly mud with burrows. Discontinuous green clay 

near the base.

Sandy mud overlying sharp contact grading up into 

silly mud with burrows.

Light green clay with sharp upper and lower 

boundaries is cut by faults.

Light green sandy clay is sandier at the base. Internal 

dark layers are sharply capped by light.

Two graded layers of sandy mud grading upward to 

silly mud with intcrbcds of lighter clay. Clay layers 

have both sharp boundaries and gradations! 

boundaries to underlying silly mud. Distortions of 

layers include faults and fluidizaiion features.

Yellowish green mottled muddy sill with blobs of 

overlying sandy mud at top (burrows or load casis). 

A thin, ragged clay layer is near base.

A Yellowish green muddy sill grading up into silty mud. 

I vague burrow(?) mottles.
OL92-1 OL92-1

43.80

44.00

44.50

45.00

45.50

92-1/2I/B

46.00

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46.10

46.50

A Yellowish muddy sill overlying abrupt contact

A Yellowish muddy sill overlying abrupt contact and grading 

I into green silty mud with abundant burrow mottles.

Yellowish muddy sill overlying abrupt contact and grading 

into green silty mud with abundant brown burrow mottles.

Yellowish muddy sill overlying abrupt contact and grading 

into green silly mud with abundant brown burrow mottles 

that are smaller and more horizontal toward top.

A Yellowish muddy silt overlying abrupt contact and grading 

T into green silly mud with abundant brown burrow mottles 

1 that are smaller and more horizontal toward top.

Alternations of sillier layers (diatoms?) with horizontal burrows 

and more clayey layers with larger horizontal burrows at a scale 

of 1-4 cm.

Sequences of yellowish muddy sill with large, random 

burrows (orangish brown) grading to gray silty mud with 47.00 

small, horizontal burrows. Basal sequence is sandier and has 

a sharp, burrow-mottled, basal contact, whereas the 

upper sequences have abrupt diffuse contacts.

| Two sequences of muddy sill with larger random burrows 

grading to silty mud with small horizontal burrows. Contacts 

are all diffuse.

47.50

92-1/22/A

Three sequences of yellowish muddy sill with random burrows 

grading to silly mud with more horizontal burrows. Lowest 

sequence is sandy. Contacts are all diffuse.

Muddy silt overlying an abrupt contact grading to silty mud with 

small, horizontal burrows. Sill has random large burrows (up to 

0.5 cm) which also project into the underlying layer.

Gray silly mud with hint of cm-scale banding from sillier layers^ 

Burrowing looks mostly horizontal. Basal contact is very sharp.

92-1/22/B

Yellowish muddy sill with random silt-filled burrows.

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Soft greenish gray silty mud with swirls and Mobs or 

gray clay. Lots or open cracks. Fluidized.

Three upward-fining sequences of yellowish muddy sill 

with large random burrows grading to grayish silry mud 

with small horizontal burrows. Lowest sequence is 

sandy at the base and sand-filled burrows project into 

the underlying layer.

Two upward-fining sequences of yellowish muddy sill 

with large random burrows grading to grayish silty mud 

penetrated by sill-filled burrows from above. Lowest 

sequence has sand near the base.

Broken up interval appears to define a single upwardfining sequence of yellowish muddy silt grading to gray 

silly mud. Lower contact is sharp and irregular due to 

bioturbalion.

Gray silly mud with lighter colored bands of clay. Coarse 

sand to granules are scattered throughout

Muddy dark, medium sand that is poorly sorted with 

sand-filled burrows.

Badly jumbled clumps of silty mud with patches of 

ostracode sand and scattered ostracodes.

Badly jumbled clumps of green silty mud with silt-filled 

burrows. There is a suggestion of layering of silly 

horizons.

Badly jumbled clumps of silly mud with patches of 

ostracode sand and scattered ostracodes.

Large clump shows lenses and pinch-and-swell layers 

of ostracode sand.

Clumps of medium ostracode sand.

George Smith reports base of this slug at 48.02 m.

^\
OL92-1 OL92-1

48.40

48.50

49.00

50.00

50.50

92-1/2.VA1

e» _ e»

v»,\v:iftiv^vV5i^iv%>

50.70i

51.00

Soft gray clay with irregular blobs and streaks of muddy 

silt Fluidized. 51.50

Thick laminae defined by dark clay (0.5 cm) with streaky mm-thick 

white layers (diatoms) alternating with silty mud (0.5 cm). Three 

sequences are defined by more diffuse layering upwards with more 

burrows. Middle sequence has more white layers comprising 

finer laminae at the base.

Yellowish muddy silt overlies sharp base and grades upward to silty 

mud. Two light layers (diatoms?) are highly disrupted by burrows.

Silty laminae become more bioturbated upward grading to silty clay.

White ash layer is about 0.5 cm thick. 

Clay laminae have thin white diatom caps at base and become more

diffuse and bioturbated upwards. 

Two upward-fining sequences of ostracode-rich muddy silt grading to

bioturbated silty mud.

Light muddy silt with silty mud parting that has sharp, bioturbated 

contacts. Includes a lot of horizontal burrows. co (VY

Two sequences of ostracode-rich sandy mud grading to silty mud that 

I are broken up clay-filled fractures and separated by a silty mud layer

with sharp contacts. The lower sandy unit is coarser with a lens 

A of medium sand. The fractures are coring artifacts.

Light muddy silt with silty mud parting that has sharp, bioturbated 

contacts. Silty mud layers are very ostracode rich.

A Gradational sequence from layers of light muddy silt alternating with 

T dark silty mud at base to dark-green silty clay with vague light bands 

I of muddy silt Ostracodes are common and so are burrows. Layer 

near base has a sandy top.

Dark green clay with vague very thin beds to thick laminae of silty clay 

and wispy lenses of very fine sand near base. Burrows are more 

abundant and larger toward top.

, Laminated green clay and light diatoms (suh-mm scale) grade into clay 

with abundant small. horizonlal(?) burrows. 92-1/24//

52.50

Upward-fining sequence of silty mud with wispy very fine sand laminae 

and bands of muddy silt becoming less silty upward with disrupted 

diatom laminae.

Green silty mud with scattered ostracodes and silt-filled burrows.

Thick laminae of very fine sand with clay partings. Tephra at 

base.

Green silty mud with scattered ostracodes and silt-filled burrows.

53.00

 "© " «-

Orange med sand (tcphra?) with soft-sediment

deformation and clumps of gray clay 

Lamina of ostracode sand with gray clay cap overlain

by silty mud with ostracodes

Ostracode-rich silty mud grading upward to silty mud 

with fewer ostracodes

Thin ostracode sand overlain by silty mud with streaks 

of ostracode sand with less sand upward

Alternations of white ostracode-rich fine sand or 

brownish muddy very fine sand and gray silty mud 

with burrows and scattered ostracodes

Laminated (0.5 mm) muddy silt and silty mud grading 

to burrow mottled silty mud. Lower laminae are 

sillier.

Pale clay with mm-scalc layers of light and dark

(coarser). 

Upward-coarsening succession comprised of two

fining sequences of silty beds with sharp bases going

to silty mud with burrows.

Upward-coarsening succession of grayish silty mud with 

burrows going to progressively coarser flat layers of silt 

to fine sand. Top layer is pinch-and-swell.

97-
OL92-1 OL92-1

53.00

53.50

55.25

92-1/25/A

54.00

54.50

55.00'

n

-r

e

Alternation of brownish-gray, thick-laminated, sill and mud 

with layers and lenses of v. fine sand and grayish silly mud 

and muddy sill with scattered ostracodes and burrows. 

Laminated layers are thicker to top as burrowed layers are 

thinner and finer grained.

Thick laminae of silty mud with brownish clay partings 

alternating mottled layers. Toward base layers are thicker 55.50 

and coarser.

Light-dark silly mud laminae grading upward into burrow 

mottled silly mud. Lower pan is pale green comprised of 

thicker sill layers with mud parting.

Thick silt lamina grading to progressively finer silty mud 

and brown clay laminae

Fine sand layers brownish mud partings grading to silt 

laminae with clay partings. Laminae become thinner 

upwards as silt thins. Four laminae of white fine sand 

near top may be tephra. Top of sequence is bioturbated.

Fine sand grading to gray silt layers with brownish mud 

1 partings. Laminae are thinner upwards. 

Fine sand grading to gray silt layers with brownish mud

partings. Laminae are thinner upwards except for burrow

mottled sand and mud at top.

Silly mud with burrows including one about 2 cm in diameter.

Silt and fine sand with brownish mud partings. Coarser layers 

thicken and thin.

Silty mud with burrows alternating with laminae of silt with

brownish mud partings. Layering is better toward base with

fine sand layers. 

Pale green silty mud with thick laminae of sillier and muddier

layers 

Ostracode sand at base overlain by silt layers alternating with

silty mud and brownish clay laminae at top. 

Pale green silly mud thick laminae separated by brownish mud. 

Brown clay with wisps of silt

Silt to very fine sand forming layers and lenses with silly mud 

interbeds. Some coarse layers are inclined.

Silty mud with vague internal layering and burrows.

56.00

56.50

Thin beds to thick laminae of very fine sand to coarse silt grading 

upward into silly mud. Defines iwo sequences with overlying 

unit with sharp bedding grading to more bioturbated.

Thin beds to thick laminae of very fine sand to coarse silt grading 

upward into silly mud. Sequence from sharp bedding to mostly 

burrowing consists of three smaller less well defined sequences.

92-1/26/A

Burrowed silty mud with beds of silt to very fine sand that 

have sharp basal contacts and gradational upper contacts. 

Layers are sharp toward the base and more bioturbated to

"* 57.00

Upward fining sequence with more bioturbation toward the 

top. Fine sand at base has thin mud partings internally. 

Subsequent silt and very fine sand beds have sharp bases 

and gradational tops.

Green-gray siliy mud with abundant burrows and disrupted 

layers toward base

Silly mud with 0.5 cm thick layers of light (coarser) and 

dark. Fine sand with mud drape at base.

57.50

»-%,*t ».* »»«* 

u;K;t«:ss2

*&:

Q f J

Brown silty mud with blobs and stringers of muddy silt 

Fluidized.

Thin beds of silt to very fine sand overlying sharp basal

' contacts grading up in burrowed silty mud. Fine sand

layers at base have sharp tops and bottoms. Overall

sequence fines upward with more burrowing toward

top.

Brown silty mud with diffuse beds of sill and ostracodc 

sand all heavily burrowed.

Coarse sill to very fine sand with internal layers of fine 

silt Grades up into overlying mud. Light 2 mm thick 

layer at base may be carbonate.

Two upward-fining sequences of muddy coarse silt 

grading to brown silty mud all heavily burrowed. 

Lenses of very fine sand at top.

Brown silty mud with light laminae (O.S mm) at base 

and more burrows toward the top with silt fillings 

forming three sequences.

Thin ostracode sand at base overlain by sill layers grading

into burrowed silly mud. Contacts less distinct toward

top. 

Brown and green clay defining flat <O.S mm laminae.

5 mm green lamina has horizontal burrow mottles. 

Brown silly mud with light layers about 1 cm apart.

Thin fine ostracode-rich sand at base. 

Brown silty mud with burrows and sharp base. 

Clay with <.S mm laminae of brown, green, and white.

Grainy layers at top and base made of orangish clumps. 

Brown clay with white partings at .5 mm intervals

grading to thicker layers of silly mud with white partings 

Graded laminae of silt to clay <-5 mm thick grading to

very fine sand to clay laminae about 3 mm thick. 

Fine sand with wavy clay parting or trains of clay

clumps defining layers 1-2 cm thick 

Green clay with pinch-and-swell to lenticular brown

silly mud defining wavy lamination.

Fine sand with wavy clay parting or interbeds of 

laminated clay defining pinch-and-swell layers 

ranging from 0.5-2 cm thick.

Graded laminae of silt to silly mud to lenses of fine sand 

in silty mud.

Green clay with white layer at base overlain by graded 

laminae of silt and mud S mm thick going to 3 cm 

thick thin beds and lenses of fine sand.

Graded laminae of silt to silty mud 3 mm thick to S mm 

thick at top. Green clay at base has white blebs.

. Brown silty mud with thin layers of green clay. Silly 

mud is sandier near top with a very fine sand bed.

Upward coarsening sequence of brown silly mud with 

green clay at base overlain by graded muddy sand to 

brown silt In middle sand has silty partings.

Brown silty mud with thick graded silt laminae at top 

and thin beds defined by green clay layers at bottom. 

Base is a chalky indurated white layer.

, Brown silty mud with lenses and beds of fine sand all 

disrupted by burrows. At base green clay laminae 

(0.5 mm) alternate with brown laminae.

Thick laminae of pale green silty mud grading to brown 

. silty mud or sand. Layering less distinct toward top.

Three sequences of thick laminae of green silly mud 

grading to imbedded brown silly mud.

Green silty clay that appears to be amalgamated laminae.
OL92-1 OL92-1

57.55

58.00

58.29

;.' 0 r 0

58.50

59.00

59.50

92-1/27/A

 6- V. Jit . Q«v :'

7^1; -;-0>r

>""'.S 0

>V:.VI>.i-AT..

59.79,

t

Thick laminae of silty mud and sandy mud grading up from 

a pale green silty clay.

Thick laminae of brown silty mud and green silty clay 

becoming more diffuse upward and sandier with burrows. 

Thin white fine sand layer near top pinch and swells.

Graded beds of coarse sand to fine sand and sandy mud. 

Lower beds are mostly finer grained defining an upward 

coarsening sequence. Pebbles occur along some sand 

basal contacts.

Reverse graded bed of silty mud to fine sand.

Upward coarsening sequence with overlying bed. Base is 

silty mud with light layers overlain graded beds of coarse 

silt to silty mud. Top has fine sand layers with burrowed 

contacts into silty mud.

Silty mud with silt-filled burrows. Lower mud is less silty 

and disrupted.

Silly mud with discontinuous layers of silt and ostracode 

sand disturbed by burrows. Basal contact is sharp.

Dark green silty mud with silt-filled burrows.

Silty mud with vague ligbt bands. Pale green clay layer at 

top and tan clay at base.

Dark green micaceous silty mud with thin bands of green 

clay disrupted by silt-filled burrows.

Silty mud with layers of silL Top and bottom beds are tan 

coarse silt

Thick laminae (3-5 mm) of light muddy silt with diffuse 

edges inlet-bedded with gray silty mud. White layer in 

middle is very fine sand (tephra?) and basal layer has 

sharp upper and lower boundaries.

Yellowish silty mud with burrows from above.

60.00

60.50

61.00

Yellowish silty mud grading up into a finer-grained

gray silty mud with silt-filled burrows. 

Two pale green clays interbedded with silly mud. Upper

clay is overlain by gray and lower clay is overlain by

coarser yellow grading to gray silty mud.

Gray silty mud with diffuse concentrations of silt and very fine 

sand defining layers that are disrupted by brown burrows. 

Sharp contact at base is overlain by sandy mud with pebbles.

61.34

92-1/27/C

 Gray silty mud with silt-filled burrows and a more silt-rich 

layer overlying an abrupt contact

Gray silty mud with muddy silt layers overlying sharp bases.

Two thin white lenses occur within the second layer from the

base (possible tephra?). 

Yellowish muddy silt overlying a sharp contact and grading up

into gray silty mud.

Yellowish muddy silt overlying an abrupt contact and grading 

up into gray silty mud with silt-filled burrows.

Yellowish muddy silt alternating with gray silty mud forming 

1-2 mm thick laminae that are finer-grained upward.

Three sequences of yellowish muddy silt grading up to gray 

silly mud. Contacts arc abrupt and disturbed by burrows.

Gray silty mud with diffuse bands of sillier mud with 

burrows.

Gray silly mud grading up from dark sandy mud. Hard 

while blebs arc scattered throughout

Dark sandy mud grading up into light gray silty mud.

000

0 0

* ° 0° 

a u n

£>

O

kUJi 

 " 0""" 0

Pale green muddy sand and sandy mud in fault block.

Gray green clay with alternations of small horizontal 

burrows and larger random burrows. Basal contact 

is sharp and burrows filled with clay extend into 

lower unit

Dark green silty mud with wispy layers of higher silt 

content Top is finer grained and base has silt-filled 

random burrows.

Gray muddy silt grading to brownish silly mud capped 

by a thin deformed brown clay.

Gray-green muddy silt with wisps of brown silty mud

grading up to gray silty mud. 

Gray silty mud with scattered granules grading up to

thin green clay with blobs of fine sand. 

Green silty mud with wispy brown silty laminae and

horizontal burrows sharpy overlying thin gray clay.

Green silty mud imerbedded with wispy gray clay 

all disrupted by mostly horizontal burrows.

Gray clay with numerous wisps of green silty mud 

that resemble burrows.

Green silty mud with wisps of gray clay that resemble 

burrows.

Green and gray clay make mm-scale laminae in two 

sequences with brown very fine sand grading to clay.

Brown fine sand with wispy gray clay partings fines 

upward.

Gray clay with patchy layers of silt and green clay and 

with random burrows.

Yellowish silty mud with pale green clay partings. Basal 

layer is a muddy silt

Pale green clay with burrows which extend into the

underlying unit. 

Green silty mud with sharp laminae of very fine sand.

A pale green clay lamina fills burrows into mud.

Green silty mud with thin clay laminae that are abrum. 

at the top and base, lowest laminae is bioturbaicd:'" '"'

Green muddy silt with two doublets of pale green clay 

laminae. Bottom silt looks deformed.

Yellowish silly mud with ostracode-fillcd burrows and a 

layer rich in ostracodes near the base.
OL92-2 OL92-2

61.26

61.50

62.00

62.50

92-2/l/A

62.76

63.00-

63.50

^'.n- '% & ft ! &

f

0.

' :/r. :»

Green muddy sill with iwo doublets of pale green clay.

Green silty mud with a diffuse sillier layer. Base is an 

orange silt overlying burrow mottled gray clay underlain by a thin brown clay.

Silty mud with burrow mottles. Orange silt layer at base.

Yellowish silty mud with abundant ostracodes. Wispy 

layering near base of more silt

DO. OD

Silty mud with burrows filled by oslracodes.

Silty mud with 2-5 mm thick layers of light and dark silty 

mud. A thin very fine sand layer is at top.

64.00

92-2/l/B(

U4

Gray silty mud with some zones of higher silt content Green 

muddy silt at base is very micaceous overlying an irregular 

sharp contact Abundant white silt grains may be diatoms.

64.50

Green micaceous muddy silt grading to silty mud.

White layer at top has horizontal mottles of dark clay and 

base is a chalky hard white layer. Between these is mix of 

white and gray mud with dark horizontal burrows.

Gray silty mud with burrows filled with white. Basal contact 

is abrupt.

Green muddy silt grading to silty mud with burrow mottles *^ 

Micaceous sandy mud grading up to silty mud with burrow 

mottles.

A Pale green clay with dark burrow mottles.

Silty mud with brown burrows. Zones of higher silt 

and lower sill content

Silty mud grading to pale green clay with burrow mottles. fi _ __. 

Top clay has sharp base. DO. 50

Light coarse silly mud grading up to dark finer-grained 

silty mud.

Light coarse silty mud grading up to dark finer-grained 

silty mud. Some sillier horizons within sequence.

Light coarse silty mud grading up to dark finer-grained 

silty mud.

92-2/2/A

==&==

.

 . * .-Q. «b* -ol

Light coarse silty mud grading up into dark silty mud. 

' Dark muddy sill layer with sharp upper and lower contacts.

: Graded bed with muddy sand overlying a scoured base 

grading up into silly mud.

Pale green clay with burrows sharply overlying coarse 

sill layer also filling burrows.

Silly gray mud with floating sill and sand grains near 

base and finer ai top.

1 Yellowish silly mud with thin white laminae (<0.5 mm) 

comprising 3-4 sequences of continuous laminae to 

highly fragmented laminae.

Yellowish silly mud with thin white laminae (<O.S mm). 

A wedge of fluidized silty mud is at the lop.

Coarse yellowish silty mud with large burrows grading to 

fine gray silty mud with small burrows.

Coarse yellowish silty mud grading to fine gray silty 

mud with silt-filled burrows.

Dark gray silty mud with suggestion of silty bands.

Green micaceous sandy mud with granules grading to 

yellowish silty mud alternating with gray silty mud. 

Lens of fine sand near top.

Yellowish coarse silty mud grading up into gray silty mud 

with sand-filled burrows.

Very fine muddy sand overlying a scour surface abruptly 

grading upward into yellowish silty mud.

Silty mud becoming sandy at the sharp basal contact with 

scattered granules.

Coarse sand grading to fine sand overlying a scour surface 

grading up into a yellowish silty mud with large, brown, 

horizontal burrows.

i Two coarse sand layers overlying sharp contacts grading 

to silty mud with horizontal burrows. Each sand is 

underlain by an orange silty mud (stain?). Top of upper 

layer is pale green clay with sand-filled burrows. 

Coarse sand overlying a sharp contact sharpy overlain by 

silly mud with scattered sand grains. This is followed by 

laminated green and brown clay producing sequences 

2-4 cm thick with finer-grained (more brown) and thinner 

laminae upwards which also fine upward.

Multiple sequences of fine laminae (about 0.5 mm) of 

, brown and green clay grading up to thicker laminae

(as much as 5 mm thick) of green slightly silty clay or 

' fine silt Lamina sequences are disrupted by growth 

' faults.

Dark green clay with a mm-thick silt layer and streaks of

silty mud. 

Multiple sequences of fine laminae (about 0.5 mm) of

green and brown clay grading up to thicker laminae 

t which have white speckles in lower cycles and green

slightly silly clay in the upper sequences. On lefl side

I

of upper fault sequences start with thick laminae of 

silly clay and become progressively finer and thinner 

T laminae unconformanly overlying more steeply dipping 

lower sequences. Black nodule at top of lowest sequence.
OL92-2 OL92-2

65.84

66.00

66.50

92-2/2/1^

67.00

67.50

68.00- -is

68.10

Multiple sequences of fine laminae (about 0.5 mm) 

of brown and green clay grading up to thicker laminae 

(up to 3 mm) with while specks.

Silty mud comprising graded laminae about 2-10 mm thick 

with some white or pale green layers. Two places have 

inclined bedding that truncates underlying layers.

92-2/3/A

68.50

Brown and green clay comprising laminae (0.5-2 mm) 

that become thicker and slightly sillier upward in 

two sequences. Some white laminae intermixed.

Yellowish silty mud comprising thick laminae 

(3-4 mm) that become thinner and finer 

toward base.

Two upward coarsening sequences of thin laminae of 

brown clay and tan silty mud grading to thicker 

laminae (3-5 mm) of pate green silty mud that looks 

disrupted and some white laminae.

Two sequences of fine laminae of brown clay alternating 

with green silty mud with white specks where laminae 

become thinner upward with more brown clay then thicker 

with more green silty mud.

Two fine sand laminae with irregular bulbous bases are

separated by an upward fining sequence of silty green

mud and brown clay laminae that are about 2-5 mm thick

near the base and < I mm thick near the top. 

Thick laminae of silty green mud with white specks and p

thin brown clay partings. O 

Fine sand with pebble-size steinkems (?) of gastropods

near the top. Changes in grain size suggest flat beds. 

Coarse to medium sand with gastropods at base and white

clumps near top which may be steinkerns or ooids. 

Fine sand with wavy bedding defined by thin layers of

medium sand that pinch and swell.

Medium sand with wavy bedding defined by fine sand

layers that pinch and swell. 

Loose clumps of muddy fine sand. 

Gray silty mud with brown parangs forming <0.1 mm laminae.

Upper part is disrupted and has a gray pebble. 

Brown silty mud with graded silt laminae 0.5 mm thick.

Silt to fine sand laminae 2-4mm thidt alternating with dark 

brown mud. Laminae at top are graded and include layers of 

ostracode (?) shells. Base is more muddy with graded laminae.

Mjfti**** i? * ' * 

v~ **? *

., *Jf *- -

' ^"C«

S .SIS

Upward-coarsening sequence of silty clay with interbcdded 

of silt and sand pinch-and-swell laminae to lenses. Coarse 

to medium sand at top has sharp upper and lower 

boundaries, but fine sand and silt toward base grades 

into silty mud above a sharp transition.

Silty mud with silt-filled burrows and blebs. Faint layering 

near top defined by less-silty mud and granules occur 

near the base.

Light and dark clay laminae from < 0.1 mm to laminae 

2-5 mm thick which are slightly silty or milky white. 69.50

Fine white sand with brown and orange clay interbeds.

I Two upward thinning sequences of graded laminae. Sand 

. layers with clay partings in the lower pan and graded silt 

I to clay in the upper pan.

Gray silly mud with pebble-size cemented (?) clumps.

Brown silty clay with graded white sand laminae at top

T and an upward thickening sequence graded silt to clay.

Upward coarsening sequence of 0.5 mm silty clay and diatom 

t laminae grading to I -2 mm silt and silty clay laminae. Sand

beds at top and base.

I Clay with < 0.1 mm laminae of silty or diatom mud. 

Muddy silt laminae (3-5 mm) overlying silty mud and clay 

laminae (0.5-1 mm) and an irregular sand layer. 

Silty clay with brown clay partings forming < 0.1 mm 

laminae sharply caps a cm-thick sand layer. 

4 Two upward fining and thinning sequence of gray silt laminae

t grading from about 2mm thick to < 0.1 mm thick. Base is 

silty clay laminae overlying a thin basal sand. 

{Ripple cross-laminated fine sand upward coarsening sequence 

overlying flat laminated upward fining sequence.

92-2/3/B

Alternation of ripple cross-laminated fine sand and clay or -,,*. p^-, 

silty mud with flat lamination. Base of unit is a medium ' U.UU 

brown sand.

1 Upward-coarsening sequence of laminated clay (<0.1 mm) 

grading to wavy bedded silty and fine sand with clay partings 

overlying a coarse brown sand with gastropods (?).

Mostly graded flat laminae of silt or fine sand with clay. Two 

medium hrown sands overlie sharp contacts and are sharply 

overlain by fine laminae. Middle area has more inclinded 

lamination with medium sand lenses.

I Upward-coarsening sequence of laminated clay (<0.1 mm) 

grading to graded laminae (5 mm) of silt and clay. 

A Silty clay with lenses of medium to fine sand.

Silty to sandy mud with silt-filled burrows and vague 

layering defined by more clay-rich areas. Pebble-sized 

clast(?) at top.

Fine sand to silt comprising two ripple cross-laminated

layers capped by flat sand laminae and clay. Medium sand

layer near base is sharply capped by clay. 

Upward-fining sequence of flat graded laminae (2-5mm) of

fine sand or silt to clay. 

Graded sequence of silty mud with very fine sand layers at

base and burrow-mottled silty clay at top. 

Ripple cross-laminated fine sand overlying laminated silty 

1 clay and overlain by upward-fining laminae of silt and mud

\t i Two graded silty mud layers separated by a green clay 

lamina. Upper layer is muddier than lower.

Upward-coarsening sequence of silty mud to very fine sand 

all with thin clay interbeds. Coarse layers are wavy to 

lenticular and appear to define ripple-scale cross-laminaiion. 

Silty mud beds near the base are graded. Basal clay bed 

is tan.

Very fine sand forming graded laminae with silty mud and 

fine sand forming lenses or thin beds with wavy layering. 

Silty mud with graded laminae and lenticular fine sand.

Very fine sand to fine sand forming wavy beds that may be

cross-lamination perpendicular to flow. 

Silty clay with lenses of fine sand and laminae of silt to very

fine sand that are inclined around the lenses. A laminated

green clay is at the base. 

Cross laminated fine sand with an interval of flat laminated

very fine sand with silty clay partings.

Fine sand comprising a sequence with progressively smaller 

scale cross-lamination and thicker more common clay 

drapes.

Green clay with light and dark fine laminae (<0.5 mm).

Fine sand with wavy thin beds and ripple-scale crosslamination. Thin clay drapes occur between layers 

near the middle.

Flat laminae of fine to medium sand with clay partings

separated into thicker units of mostly clay or mostly sand. 

Gray silty clay with 2 mm graded laminae overlain by brown

clay with < I mm laminae. Orange carbonate layer at top. 

Medium sand with flat laminae. 

Graded sand-io-clay laminae overlying and underlying sand

alternating with clay. Coarser interval is more lenticular

and deformed. 

Thick graded silt to silty mud laminae are wavy to lenticular.

Graded sand-lo-clay laminae.

Thick graded silt to silty mud laminae. Fine sand lense in 

middle has muddy partings. Laminae toward base are finer.

Graded silt to silty mud overlying scour surface.

Finely laminated silt mud grading to clay.

Clay laminae (<0.1 mm) becoming coarser and thicker to

graded silly-clay laminae capped by unbedded silty mud

with scattered sand and granules. 

Silty mud laminae (0.5 mm) with thin green clay partings. 

Paper thin clay-white (carbonate?) laminae becoming thicker

and sillier upward. 

Two sequences of thin gray laminae grading upward to thick

graded silt to silty mud laminae.

Silty clay with sand lenses and burrows(?)

Sandy mud with deformed clump of laminated clay.

20?
OL92-2 OL92-2

70.35

92-2/3/C

70.5

71.00

Graded fine sand to sandy mud overlying a sharp 

scour contact

Silty mud with deformed layers of muddy silt and loose 

clay clumps. Upper two cm has silt laminae that are 

slightly deformed.

Fine sand in wavy to lenticular layers with thin clay 

partings. Thick silly mud and clay layers near middle. 

. Finely laminated clay with white and brown laminae 

J grading to sillier, thicker laminae. 

' ' Finely laminated clay with diatoms becoming thicker 

and sillier upwards. There are several smaller -scale 

sequences internally within the larger one. 

Thin laminae (0.5 mm) with clay or diatom partings 

grading up into thicker silty mud laminae.

Upward coarsening succesion of three sequences each 

grading from fine laminae to thicker laminae. Base is 

clay with diatom laminae and top is muddy silt with 

faint internal lamination and a laminated gray clay 

layer.

Brown microlaminae grading up to graded silly mud 

laminae about 3-5 mm thick.

Upward fining sequence of laminated fine sand grading 

to laminated silty mud. There are 3 internal fining 

sequences each becoming more muddy silt

72.50

71.5

72.00

73.00

92-2/4/B

Three sequences of clay with fine lamination grading to 

silty mud with thick graded laminae. There is 

progressively less clay and thicker layers upwards.

, Fine sand with wavy thin beds becoming thinner with 

clay lenses then clay laminae.

Sandy mud with vague more clay-rich bands and scattered 

burrows. Laminated sequence at top is mostly silly clay 

with clay and fine sand laminae. __ _

73.50

Two upward-coarsening sequences with thin laminae of graded 

silty mud to clay becoming thick laminae of very fine sand 

alternating with clay.

Two sequences of clay with fine lamination including diatoms 

grading up to thicker laminae of graded muddy silt to clay.

Two upward-coarsening sequences with thin laminae of graded 

silly mud to clay becoming thick laminae of very fine sand 

alternating with clay.

Two sequences of clay with fine lamination including diatoms 

grading up to thicker laminae of graded muddy silt to clay.

Silty clay with flat to wavy laminae of very fine sand and -JA r\r\ 

lenses of fine sand. /*KUU

Green clay with fine laminae grading upward to alternations 

of graded silty mud laminae and thin, finely laminated 

green clay partings.

Two sequences of silty mud with very fine lamination grading 

. i to thicker lamination. Top sequence has a fine sand lense.

Two sequences of brown microlaminated clay grading to 

1 ' silty clay with thicker lamina

, ; Silty mud with very fine lamination grading to thicker laminae 

including an organish brown layer at top. 

Thick laminae of silt or fine sand grading to clay. Some layers 

are wavy or lenticular with internal cross lamination.

Thin laminae of green clay grading upward to thick graded 

laminae of silt and clay.

Silt with fine sand lenses grading upward into silty mud with '

Three sequences of green clay with fine laminae grading 74.50i 

upward to silty mud with thick graded laminae. Interval 

disrupted by splitting.

72.50

Green clay with thick laminae grading to silty mud with 

I thick graded laminae.

T Two sequences of laminated clay grading upward to thick 

* laminae of silt or very fine sand grading to clay.

Two sequences of laminated clay grading upward to thick 

, | laminae of silt and clay or fine sand lenses with clay drapes. 

, \ Clay with fine laminae grading upward to silty mud with 

graded thick laminae.

Graded thick laminae of very fine sand and silt to silty mud. 

'| Brown clay finely laminated clay grading to green clay with 

'' slightly thicker laminae. Upper sequence is two successions 

of dark brown mkrolaminae grading to green clay.

Graded thick laminae of very fine sand and silt with clay layers.

Green clay with fine laminae thickens on one side of fault

A Sandy mud overlying sharp base grading upward to siliy mud.

o

0

Three upward coarsening sequences of graded silty mud to clay 

in thin laminae grading to thick laminae of silt or fine sand. 

The sequences are disrupted by a fault and intruded by muddy 

silt

Silty mud with burrows that may overlie a scour. 

Upward coarsening sequences of graded silty mud to clay

in thin laminae grading to thick laminae of silt or fine sand. 

Silty mud truncates underlying laminae and may be intruded. 

Two upward coarsening sequences of graded silty mud to clay

in thin laminae grading to thick laminae of silt or fine sand.

', Two sequences of laminated clay grading up to graded silt 

and clay thick laminae then sand layers.

Green clay with fine laminae grading upward to silty mud 

laminae in two upward thickening successions.

Fine sand lenses with clay partings grading up to graded silt 

thick laminae with clay partings.

o

Clay with graded thin laminae grading upward to silty mud with 

thick graded laminae

Silty mud with clay laminae grading to muddy silt with burrows. 

4 Numerous faults are probably coring artifacts.

Clay with graded thin laminae grading upward to silty mud with 

thick graded laminae

Two upward fining sequences. Basal sequence is fine sand with 

clay intraclasts grading to silly mud. Upper sequences is 

muddy silt grading to silty mud with thin carbonate streaks.

Four upward-fining sequences of burrowed silty mud grading 

to less silty mud with vague laminae. Uppermost sequence 

has better defined laminae at top grading to next unit Lowest 

sequence is yellowish.

Interval broken up during splitting. Mud clumps include 

silty mud and clay with laminae near the base.

Clay with brown partings defining fine laminae to very fine 

in 2-3 cm thick packets. Layering is disrupted by faults and 

green clay filled injection features. Euhedral crystals 1-2 mm 

long are scattered throughout

Blebbly green clay filling injection(?) around clumps of 

laminated brown clay.

Gap in core.

Fine silty laminae grading to very fine clay laminae.

Silly mud sharply capped by pale tan clay layers of equivalent 

thickness.

Two sequences of silty mud with scattered sand grading upward 

to finely laminated clay.

Loose clumps of yellowish silty mud.

Yellowish silty mud with burrows overlying streaky carbonate 

laminae and grading up from a silty basal contact to streaky 

laminae.

Two sequences of clay with irregular carbonate and silt laminae 

grading up to silty mud with streaky diatom hairline laminae 

that are more discontinuous upwards.

7.1
OL92-2 OL92-2

74.75

75.00

75.50

92-2/6/A

76.00

92-2/3/C

76.50

92-2/6/B

77.00

-iff;

.

 v.-v vry -ifffT. vv

* -fj » 

s. :. .. V? ..*...»...'

a ; 0

0

0

8e

 *S>»4

~ «>. . . .g>.

0

0 

.ft. '._fl_

i

Silty mud with streaky carbonate laminae near base and ' ' 'JU

and diatom(?) laminae near the top. 

Purplish micaceous silty mud grading up to greenish silty

mud with carbonate streaks. Coarse sand-sized clumps

(snail steinkems?) near sharp basal contact overlying

greenish silty mud with coarse grains.

Purplish micaceous silty mud with burrows and diffuse 

bands of sandy mud. Middle zone of greenish silty mud 

with granules and pebbles. Base is a muddy fine sand.

Medium sand overlying erosive base grading up to sandy 

micaceous mud with burrows.

Green silty mud with orange silt-filled burrows and silty 

layers. Gray layers near base.

Two graded layers of sandy mud grading to silty mud 

with large horizontal burrows.

77.50 Graded sequence with muddy silt at base with random 

burrows grading upward to silty mud with horizontal 

burrows at top.

Medium sand overlying sharp contact grading upward 

to sandy mud with random burrows and silty mud with 

horizontal burrows.

Gray silty mud with random burrows and a silt-rich 

layer near the top.

Gray clay with small horizontal burrows grading upward 

to large random burrows.

' ' Gray clay with small horizontal burrows grading upward 

to silty mud with large random burrows.

7ft OO Gray clay with small horizontal burrows interbedded with ' o-*Ju 

silty mud and muddy silt with horizontal burrows then 

grading upward to silty mud with large random burrow

Gray clay with small horizontal burrows grading upward 

to silty mud with large random burrows.

i Gray silty mud with random burrows.

Two sequences of gray clay with horizontal burrows and 

light wisps grading upward to silty mud with large random 

burrows.

Gray clay with no visible burrows overlain by horizontal 

burrows (some filled with light material of wisps) and then 

silty mud with large random burrows.

Gray silty mud with large horizontal burrows and some light 

burrow fillings.

78.50 Gray clay with no visible structure with increasing abundance 

of light streaks upward. Orange stained inclined feature 

demarks a break in the character of streaks (fault?).

Gray silty mud with sharp contacts.

Gray clay with light streaks that decrease in abundance 

upward. '

Orange muddy silt with mud streaks intruded around the outer 

edge of the core.

Two graded sequences of silty mud with random burrows 

and light wisps near tops overlain by gray clay. Basal 

contacts are sharp with more silt

79.00

Graded sequences of silty mud with random burrows to gray clay. 

Basal contacts are sharp with more silt

\

a

8

80

**'&

Interbedded silly gray mud and gray clay all disrupted by 

random burrows. Silly layers are thicker and coarser near 

base.

k Gray clay with vague burrow mottles and orange stained 

streaks and blobs. Disrupted by dark cross-cutting shear 

planes.

Gray silly mud with scattered sand and burrowsgrading up to 

gray clay. Disrupted by dark cross-cutting shear planes.

Gray clay with vague burrow monks and dark silly layers 

near base. Disrupted by dark cross-cutting shear planes.

Gray silly mud with hints of dark layers and burrows. 

Disrupted by dark cross-cutting shear planes.

Gray clay with vague burrow mottles and dark silly layers 

near base. Disrupted by dark cross-cutting shear planes.

Four upward-fining sequences of gray silty mud grading to 

gray clay. Basal contacts are sharp and slightly coarser and 

burrows occur throughout Dark cross-cutting shear planes 

disrupt bedding.

Gray silly mud with streaks of silt grading upward into gray 

clay with silty patches and silt-filled burrows. Dark crosscutting shear planes disrupt bedding.

Thick, dark shear plane indicating spin-out of core. 

Gray clay with burrows has concentration of silt at base.

Silty mud with sharp basal contact grades upward to gray 

clay with burrows.

Thick, dark shear plane indicating spin-out of core. Orange 

streak is truncated.

Gray clay with burrow monies, orange stains and zones of 

more silt Dark cross-cutting shear planes throughout

Thick, dark shear plane indicating spin-out of core.
OL92-2 OL92-2

79.25

80.00

80.50

81.00

92-2/8/A

0

0 0

0

e

0

Silty gray mud grading upward to gray clay with 

burrows. Dark cross-cutting shear planes occur 

throughout

81.50 ----.

Silty gray mud at base is streaky toward transition to 

gray clay with burrows. Dark cross-cutting shear planes 

occur throughout

No core.

Dense gray clay with vague burrow mottles near top. 

Dark cross-cutting shear planes occur throughout

82.00

92-2/7/A,

82.50

Dense gray clay with disrupted white tephra layers.

Dense gray clay with possible burrow mottles.

Dark shear planes.

Dense gray clay with orange burrow mottles.

Dark shear plane.

Dense gray clay with vague burrow mottles.

Dense gray clay.

Dark shear plane.

Dense gray clay with vague burrow mottles and dark 

shear planes. 79.00

83.00

Dark shear plane.

Gray clay with vague layers of darker material and an orange 

silty layer (tephra?). Dark shear planes offset layers.

1 Gray silty mud overlies sharp contact and grades to gray clay. 

Dark shear planes offset layers.

Gray clay with white tephra layers and vague darker laminae. 

Horizontal burrows cross layers. Dark shear planes offset 

layers.

Gray silty mud overlies a discontinuous light silt layer and 

grades upward into gray clay with vague burrow mottles. 

Dark shear planes offset layers.

Gray silty mud overlies a discontinuous light silty layer and 

grades upward into gray clay with vague burrow mottles. 

Dark shear planes offset layers.

Gray silty mud overlies a sharp contact and grades upward 

into gray clay with vague burrow mottles. Dark shear planes 

offset layers.

, Gray silty mud overlies a sharp contact and grades upward 

into gray clay with vague burrow mottles. Dark shear planes 

offset layers. Core distrubed by splitting.

Dark sandy mud abruptly grades into gray clay. Dark shear 

planes offset layers. Burrow mottles of silty mud near top.
Figure 2

Generalized log of sediment types in OL92-1, 2, and 3. Scale on left of each column is in 

meters and represents drilling depths as reported by Smith (1993).
OL92-3 OL92-1 OL92-1 OL92-1 OL92-1

3.00

4.50

»T. *e»^

Oolitic sand 2.00

150

Calcaraous sllty mud 

with burrows

6.00

Oolitic aand

nTTT

Evaporltes

6.50

Oolitic aand

9.50

Fluldlzed

Calcaraous sllty mud 

with burrows

Muddy micaceous 

silt grading to 

sllty mud "-00

Muddy micaceous 

silt grading to 

sllty mud

Muddy micaceous 

ailt grading to 

sllty mud

m

Bloturbated 

Qrtcn cuy

13.50

FluWIzed

14.00

17j50

Bloturbatod 

green clay

Bioturbatad 

Qi^vwi cwy

15.50

Fluldlzed

Calcaraous allty mud 

with burrows

Fluldlzed

Bioturbated muddy 

mlcacsous silt hi 

graded bads

Calcaraous sllty mud 

and muddy ailt

18.50

Fluldized

2050

Calcareous sllty mud 

with aandy laminae

Calcareous sllty mud 

with burrows

Bloturbatsd 

green clay

'l^^Lii^A Calcaraous sllty mud 

$*:p*&&£ with burrows

£ii!» s.ii.-ifil'i'i
OL92-1 OL92-1 OL92-1 OL92-1 OL92-1

22£0

Muddy micaceous 

allt with vague 

banding

2630

Calcareous allty mud 

with aandy laminae 

and scattered 

pebbles

Gray clay with 

scattered granules

Calcareous allty mud 

with aandy laminae 

and scattered 

pebbles

Gray clay wtth »-00 

scattered granules

25.00

2530

mm

Clay wtth burrows 

and silt bands

Flutdlzed

Bloturbated 

gray clay

30.00

Calcareous sltty mud 

with burrows

3030

Calcareous allty mud 

with burrows P5555

Calcareous allty mud 

with allty layers

Calcareous ailty mud 

wtth burrows

Muddy micaceous 

allt grading to 

allty mud 32-00

Gray day with burrows 

and scattered sand

33.00

34.00

FIU.d«»d ,,. ,

W

HuUbad

Calcareous sltty mud 

with burrows

Calcareous sltty mud 

wHh burrows 36.00

Btoturbated 

green day

Gray day wtth 

scattered sand 

and aandy pods

40.00

Calcareous altty mud 

with burrow* 40.50

41.00

Calcareous sltty mud 

wtth aand tonaas and

>S,<1 -*,- <

: |

* -*"1

Clay wtth muddy 

silt bands

Gray clay with 

scattered granules

\m 42.00

Clay wtth allt and 

fine sand laminae

Ruldlzed

3830

Muddy micaceous 

allt In graded beds

39.00

Gray clay wtth 

scattered aand 

and aandy pods

43.00

Clay wtth burrows and 

Una aand to allt

Clay wtth fine tommaa 

of allt

: * * . :* ** :

-.SMXl-Mii:

::;,.: :::; .;.

:^t:"^isj..

X

)>)>)

,»?»»-»,*.«-:»; v5

'^tV£vit~«?«

:;:S*v:;;:d:

S^ife^-i

;:;;;:*j ::>;;*;:

fi^Jj^e 

.-.-*,, >:,*i»..i.i>

r-r-ii^'Sxsi:

 ^S^S-^'iK^v^ 

y^-.'it>f-2P&

><

11:11

j*:.«¥«-i« « » »-> 

.i*;;,,.^*-^, (i^

'*<!<* »-»» -? ».' 

:-j^v>v*ivK

daywrU

day wit

andlnt

Oaywhl

laminai

No core

HuMUM

Calcareo 

with si

daywrUj 

ofsUt*

Calcareo 

wtthbu

No core

Calcareoi 

wtthaa
OL92-1 OL92-1 OL92-1 OL92-1

45.50

Calcaraou* allty mud 

with burrow*

No core

t(t(l

46.50

47.00

48.00

Calcaraoua allty mud 

with burrow*

Muddy mlcaceou* 

allt grading to 

allty mud

Clay and muddy allt 

band* with scattered 

granules

Calearaous allty mud 

with burrow*

Calcareous allty mud 

with aand lenses

No core

4850

53.00

50X10

5030

)\)\)

No core

Fluldlzad

Claywtthlainlnai 

of diatoms and 

silt

Calcaraoua allty mud 

with sandy bads

Claywtthailtlamlnaa 

and aand lenses

Calcaraoua ailty mud 

with sandy bads

Calcaraoua silly mud 

with burrows

Clay with laminae 

of allt and Una sand

54.00

54.50

55.00

56.00

V\ » \ \ \

Clay with laminae 

of allt and Una 

aand

Calcareous silly mud 

with aandy beds

Calcaraoua ailty mud 

with burrow*

Clay with laminae 

of allt

Calcareou* allty mud 

with aandy beds

Calcaraoua silly mud 

wllli burrows

Calearaous silly mud 

with aandy bads

Bloturbatadday 

with allty laminae

Clay with laminae 

of allt and Una 

aand

Sand with mud

Clay with laminae 

of allt and Una 

aand

Calearaous ailty mud 

wtth aandy laminae

58.00

-IXI^nK

V^i.;*^,

IWlli|$gllij

itit;tiiiti«i«

i;--'--.--,',^ * -" *- ' *:

; >.»-+-*» -« ». *: * * ?. 

;- *^.£«^^*i>

^*£^it*3& .x&^:>u.x. :-*-.x,:".--.v.-c-.

^v**«rrs

Cateareoii

Graded bi 

aand

Calcareoii 

wtthgm

5830

5830

60.00

60.50

51.00

Calcareou* allty mud 

wtth burrows

Calcaraoua allty mud 

wtth aandy laminae

Graded bed* of 

muddy micacaous 

allt to ailty mud

Bloturbatad 

gray clay

Muddy micacaous silt 

and allty mud Intarbada

Bloturbatad 

gray clay

Inlarbaddad aand 

and clay

Calcareou* ailty mud 

with clay laminae

Muddy mlcaceou* 

 lit grading to 

allty mud

 5CW"*!*fe Calcaraoua allty mud 

wtth aandy laminae
OL92-2 OL92-2 OL92-2 OL92-2 OL92-2

62.00

63.00

6350

64.00

6450

65.00

6550

|

'. ' '- "V* V ***

**" ^i '* V1 V xr

; -*; 'j^'r'ifi

f«R8 __Bl__ri

i^HHaaam! a^LaHf

Bi

8HHK

JK'P&SfSx */ ;

slPift^i"*

a|pv;^

WSZ'£& ' -^f'f*:-i'--^-^'

ft- m

Li B_a_aaaji

* * , ' *

,,;,..,M,,,,,,,,,,,M,,^.

J^^/rV^

0-:-^&-N

r^;M

vv'HSK

-.":;» -v;'-i;v ''-

iitlilllli

.;,.« -.. _ ... ;

ii^ri!

U^M-tfl.t

SSSiJI-ir;

iil^ii

:::;::;':i:';':: ?:rr*:

6600

Calcareous sllty mud

with burrows

6650

Muddy micaceous

silt grading to

67.00

Clay with chalky 

JIWIB bands

Calcareoua sllty mud

Muddy micaceous Moo

sand grading to 

slltymud

Gray day with

and green clay

Calcareoua sllty mud

Calcareous sHty mud 

wtth burrows

69.00

Muddy micaceous

aand grading to 

sllty mud

wtth burrows

_____

Muddy micaceous

day with granules

Calcareous sllty mud 

wtth sand layers

Clay with laminae 

of silt and fine

aand 70.00

lamination ,

;;: v^iiiM.s::-:

,;«-...>.;. »:.. ; *.;

i§^§Mfi!l

I:=l&i I.'l£^ i'v!^

ZiKMtXzi

*K:^? ^I^

Kiii^i^si.:?-*

:W:«:l:lil:i

:i:l:Sit:t:«:t

:«:W:J4:W:t .*AA^Ti.7nnT.j

s^^-n-f -:

;i'

jl:-::-^^^

fe^%M^

-- --

^~.;~*«;

r^P ^

W^K^

.:< -*.-***%

^ t^SS;

 ^.^^iiW.

,ji,;?r-S: .... T - r

::;:::::::;::

 '-(:. *-«.:.*-.*::* -*:*-

ijn^r^EW-

|ig;«i|$j:t

«i«!lliitiilt

5;\:\:\:\:\:\r\:j

*^H IH£

*j^?"^ '-"-^

««HW:

Clay wtth fine 

temlnation

7050

Clay wtth laminae 

of silt and fine 

sand

71.00

Coarse to fine 

aand

 7150

day wtth lamina*

aand '

72.00

wtth aand laminae and 

cross laminae

 7250 

Calcareous sllty mud 

wtth sand tens**

Calcareous sllty mud 

wtth burrows and

scattered granules 

73.00

Calcarsous sllty mud

cross lamina* 7350

Fine sand with mud 74-°° 

interbeds and ripple

Calcareous sllty mud 

wtth aand laminae and ,

scattered granules 

7450

day with fin* 

lamination

day wtth silt laminae 1 

and sand lenses

,"-,-~-

i,...;*;-^^*^*.

:::;;ii|i5;v;^

i'::;;:*:::':^ 

.\.\.\.\.\.\.\.\.

:»K::.::,::>

il^l-iSi:

iSIT^^'5^

:i^;^:;;::

iim:ife£

vw>:,ii>,s, .-;»!,

;;";ij-in^JiJJt

 JKfir:iIIi

SiSi!

v/\

I^&B

:!«""!»:??:;

^Jf»^f,» ,;.;:.;,

:- " '

i*. . , . »...»,;

i>s,.,^, ... i^

pm* ^;

tep?,i

^^

v '-''-m^

Calcareous sllty mud 

with sand beds

Clay wtth fine 

lamination

day wtth laminae

Fine sand

elav

CtoywHh laminae 

of silt and aand

day wtth fine 76.00

lamination

Clay wtth laminae

of am and fine 

aand 

day wtth fine

lamination

Clay wtth laminae T7-00 

aand

7750

No core

76.00

Clay with laminae

aand

Calcareoua sllty mud

with aand beds 

7850

day wtth fine

79.00

with clay Laminae

lilsSffiiliss? mm

. jm^>

^^^^

?

;'

Calcareous sllty mud

Graded beds of

muddy micaoaoua

sand and allt to 

slHymud T9JO

Gray day wtth

and burrows

No core

81.00

8150

Gray clay wtth

 no burrowa

82.50

"

^^.^

F. -

i

"

-

s-

- t

;>

Gray day wtth

 and burrows

No core

Gray day with 

aUty IntaWvala
U.S. DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY

A HIGH-RESOLUTION STUDY OF SEDIMENTS FROM THE LAST

INTERGLACIATION AT OWENS LAKE, CALIFORNIA: GEOCHEMISTRY

OF SEDIMENTS IN CORE OL-92,83-32 M DEPTH

by

James L. Bischoff1 , Dahlia Chazan1 , and Richard W. Canavan IV2

Open-File Report 98-132 (part 3)

This report is preliminary and has not been reviewed for conformity with U.S. Geological 

Survey editorial standards (or with the North American Stratigraphic Code). Any use of 

trade, product, or firm names is for descriptive purposes only and does not imply 

endorsement by the U.S. Government.

*U.S. Geological Survey, Menlo Park, CA 94025

Department of Botany, Connecticut College, New London CT 06320

1998
Introduction

In 1992 the U.S. Geological Survey drilled a 323-m-deep core (OL-92) into Owens 

Lake sediments near the depocenter of the basin to obtain a continuous record of siltyclay sediment spanning the last 800,000 yrs. A multi-parameter reconnaissance study of 

the entire core (ca 7000-yr resolution), reported in a 13-chapter summary volume (Smith 

and Bischoff, 1997), revealed cycles characterized by closed and overflowing lake 

conditions.

We report here the geochemical results of a high-resolution study of sediments from 

the last interglaciation (presumably Marine Isotope Stage 5), and extending slightly into 

the glaciations of stages 4 and 6 to observe the 6/5 boundary and 5/4 transitions. We 

present analyses for total inorganic carbon (TIC), organic carbon (TOC), and for acid 

soluble elements (in order of abundance): Ca, Mg, Fe, Na, Al, K, Si, Ti, P, Mn , Sr, Li, 

B, Ba, V, Cu, Co, and Mo

Sampling

A total of 444 channel samples, each 10-cm in length, were taken from core OL-92 

continuously from 83 to 32 m depth. This depth span represents deposition from 

approximately 134 up to 46 kyrs before present according to the time-depth scale 

estimated by Bischoff et al (1997b). Thus, each sample represents an integration of 

approximately 170 yrs. The samples were dried, lightly ground and homogenized, and 

separated into aliquots for distribution to cooperating laboratories.

Analytical Techniques

TIC was determined by standard coulometry, which measures carbonate as CO2 

released by acid dissolution. Total carbon was measured as CO2 released by inductionfurnace combustion. TOC is taken as the difference between total carbon and TIC. 

Sample splits of 0.5 grams were leached in 10 mis of 3N HC1 overnight, and the 

supernate was analyzed by inductively coupled plasma spectrometry (ICP) for Ca, Mg, 

Fe, Na, Al, K, Si, Ti, P, Mn , Sr, Li, B, Ba, V, Cu, Co, and Mo.

Results

Results are shown in Tables 1 and 2, and averages in Table 3. Time plots and interelement correlations indicate the analyzed components reflect four different sedimentfractions, each of which has climatic implications. These fractions are, 1) authigenic 

carbonate (TIC, Ca, Mg, Sr), 2) organic matter (TOC, Mo, and Ba), 3) authigenic silicates 

and exchangeable ions (Mg, Si, Li, Na, B), and, 4) a detrital biotite component (Fe, K, Al, 

Ti, Mn, V, Cu, and Co).

TIC and leachable Ca (Fig. 1) represent the authigenic CaCOs fraction. XRD 

analyses of high-carbonate samples in the reconnaissance study (Bischoff et al., 1997a) 

indicated that calcite is the dominant carbonate mineral, with minor dolomite and 

aragonite found in a few samples.

Low carbonate contents reflect overflowing, fresh-lake conditions, whereas high 

carbonate contents reflect saline-lake, closed-basin conditions, in which Owens Lake was 

below its sill level much of the time (Bischoff et al, 1997a). Low CaCOs values from 

30-35 m and 75-82 m suggest overflowing conditions whereas fluctuating high values 

between 35 and 76 m indicate generally closed lake conditions. A unique occurrence at 

62.4 to 62.5 m (seen as a spike in Fig. 1) is a 10-cm bed of almost pure dolomite, 

unconsolidated, finely-crystalline, and ordered

TOC (Fig. 1) reflects biological productivity, and generally follows TIC, indicating 

that nutrient abundance generally increases with water residence-time. Some of the 

maxima in TOC, however, occur in regions where TIC is only intermediate. These 

regions may reflect periods of extreme salinity during which nutrients and productivity 

are maximized, but in which riverborne Ca is precipitated near where it enters the lake,

iln
60 km north of the coring site, because of high carbonate alkalinity. Thus, maxima in 

TIC may reflect intermediate or moderate salinities, in which the water chemistry 

accommodates roughly equal amounts of Ca and carbonate

Fig. 2 shows the carbonate and authigenic silicate components derived from TIC, 

leachable Ca, and Mg. All Ca is attributed to CaCOs. COs in excess of Ca is attributed 

to a MgCOs component. Mg, however, exceeds this excess COs, and this "excess" Mg is 

attributed to an authigenic Mg-silicate phase (Fig. 2). Such acid-soluble authigenic 

phases form in saline lakes by reaction of dissolved Mg and silica in alkaline solution 

(Bischoff et al, 1997a and 1997c). For semiquantitative estimates, we use the 

stoichiometry of dehydrated sepiolite for this phase (i.e. Mg4Si6Ois(OH)2).

Chemical mass balance calculations based on the lake area at the spill elevation and 

the pre-diversion Ca flux from the Owens River suggested that sediments should contain 

an average of about 11 dry wt % CaCOs at the limit of a steady-state full, but not spilling, 

lake (Bischoff et al., 1997a). This conclusion assumes that CaCOs is homogeneously 

distributed throughout the sediment surface. CaCOs falls below this limit for at least five 

short-lived events from 35-76 m (Fig. 2), indicating brief spilling events during the 

generally dry intergalciation.

Li seems to correlate closely to the Mg-silicate component, particularly for the 

pronounced minimum from 43 to 48 m (Figs. 2 and 3). Na and B correlate closely to 

each other, and less strongly to Li and Mg-silicate. Na is likely the dominant 

exchangeable ion on the Mg-silicate phase, and B is well know to have an adsorption 

affinity for smectitic clays (You et al., 1995), but how the negative borate ion is actually 

incorporated is not clear. Al, Fe, K, and Ti correlate strongly with each other (Fig. 4). 

Mn, V, Cu, and Co (not shown) also correlate strongly with this group. The triangular 

diagram of Al, K, and Fe (Fig. 5) indicates that this entire group of elements plots within 

the field of biotite compositions. Fig. 5 suggests that a portion of the biotite dissolves 

congruently during the acid leach.

REFERENCES

Bateman, P.C. (1961). Granitic formations in the east-central Sierra Nevada near Bishop, 

California. Geological Society of America Bulletin 72, 1521-1538.

Bischoff, J.L., Fitts, J.P., and Fitzpatrick, J.A. (1997a). Responses of sediment 

geochemistry to climate change in Owens Lake sediment: An 800 ky record of 

saline/fresh cycles. In "An 800,000-year geologic and climatic record from Owens 

Lake, California: Core OL-92" (G.I. Smith and J. Bischoff, Eds.), pp. 37-47. 

Geological Society of America Special Paper 317.

Bischoff, J.L., Stafford, T.W., Jr., and Rubin, M. (1997b). A time-depth scale for Owens 

Lake sediments of core OL-92: Radiocarbon dates and constant mass-accumulation 

rate. In "An 800,000-year geologic and climatic record from Owens Lake, California: 

Core OL-92" (G.I. Smith and J. Bischoff, Eds.), pp. 91-98. Geological Society of 

America Special Paper 317.

Bischoff, J.L., Menking, K.M., and Fitts, J.P. (1997c). Climatic oscillations 10,000- 

160,000 yrs B.P. at Owens Lake, California reflected in geochemical proxies for 

glacial rock-flour and for lake salinity in core OL-92. Quaternary Research (Nov).

Deer, W.A., Howie, R.A., and Zussman, J. (1962). "Rock Forming Minerals." Longmans, 

London.

Smith, G.I., and Bischoff, J.L. (1997). Core OL-92 from Owens Lake: Project rationale, 

geologic setting, drilling procedures, and summary. In "An 800,000-year geologic
and climatic record from Owens Lake, California: Core OL-92" (G.I. Smith and J. 

Bischoff Eds.), pp. 1-8, Geological Society of America Special Paper 317.

You, C.-F., Spivack, A.J., Gieskes, J.M., Rosenbauer, R. and Bischoff, J.L. (1995) 

Experimental study of boron geochemistry: Implications for fluid processes in 

subduction zones. Geochimica et Cosmochimica Acta, v. 59, p. 2435-2442.
age (kyrs)

53 68 81 97 118 134

6.0

4.0

2.0

0

cr*

+- 

£

10-

TOC

30 40 50 60 

depth (m)

Fig. 1

Depth plots of organic carbon (TOC), inorganic carbon (TIC) and acid-leachable Ca in core 

OL-92; 83-32 m depth interval. Ages shown at top of diagram from Bischoff et al (1997b).
53

20

80

age (kyrs)

68 81 97 118 134

Authigenic Mg-silicate

spill 

level

50 60 

depth (m)

Rg. 2

Depth plots of CaCOs, Sr, MgCX>3 and authigenic Mg-silicate in core OL-92; 82-32 m depth. 

Ages shown at top of diagram from Bischoff et al (1997b).
53

age (kyrs)

68 81 97 118 134

400

1200

Q.

0

600

Q.300

Q.

0

Li

Q

Na

20 30 40 50 60 70 80 90

depth (m)

fig. 3

Depth plots of acid-leachable B, Li and Na in core OL-92; 83-32 m depthinterval. Ages 

shown at top of diagram from Bischoff etal (1997b).
53

age (kyrs)

68 81 97 118 134

2.0

1.0

Al

0^

4.0 

2.0

0 

1.5

1.0 

0.5

Fe

K

4.0

2.0

20x wt % Ti

depth (m)

20 30 40 50 60 70 80 905

Rg. 4

Depth plot of add-leachable Al, Fe, K and Ti In core OL-92; 83-32 m depth Interval. Ages 

shown at top of diagram from Blschoff et al (1997b).
lerran 

Plutonic 

Rocks

\/ \/ \/ \/ \/ \/ \/

K Fe

Rg. 5

Diagram showing AI-K-Fe relations for acid-leachable components from core OL-92; 83-32 m 

depth interval. Field for Sierra plutonic rocks from Bateman (1961), for biotites from Deer, 

Howie and Zussman (1962).
Table 1

Analyses of high-resolution (10 cm) samples from core OL-92 (83 to 32 m depth) 

for TIC, TOC and acid-leachable major elements. Depth refers to midpoint of 

sample from the surface in meters. Concentrations in weight %.

sample depth TIC TOC Ca Mg Fe Na Al K Si

1

2

3

4

5

6

7

8

9

10

1 1

12

13

14

15

16

17

18

19

20

21

22

23

24

25

26

27

28

29

30

31

32

33

34

35

36

37

38

32.1

32.2

32.3

32.4

32.5

32.6

32.7

32.8

32.9

33.0

33.1

33.2

33.3

33.4

33.5

33.6

33.7

33.8

33.9

34.8

34.9

35.0

35.1

35.2

35.3

35.4

35.5

35.6

35.7

35.8

35.9

36.0

36.1

36.2

36.3

36.4

36.5

36.6

<0

<0

0.

0.

0.

0.

0.

1.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

1.

1.

1.

1.

1.

.01

.01

15

33

24

21

66

19

88

53

31

09

01

04

03

04

11

21

06

06

06

19

19

16

23

27

18

24

23

21

41

83

72

40

45

18

45

43

1.29

1.27

1.55

1.54

1.60

1.47

1.40

1.45

1.58

1.68

1.41

1.18

1.05

0.94

0.89

0.89

0.75

0.67

0.74

0.77

0.69

0.63

0.66

0.60

0.59

0.57

0.58

0.57

0.56

0.52

0.57

0.67

1.16

0.80

0.92

1.02

0.67

0.69

0.56

0.56

1.17

2.05

1.62

1.45

3.13

4.95

4.00

2.70

2.21

1.12

0.59

0.67

0.52

0.54

0.83

1.24

0.62

0.69

0.57

1.07

1.09

0.92

1.24

1.40

1.05

1.30

1.29

1.21

1.95

3.64

5.33

6.90

6.53

6.48

6.45

6.04

0.93

0.80

0.74

0.67

0.66

0.67

0.66

0.67

0.72

0.67

0.75

0.78

0.76

0.81

0.83

0.79

0.92

0.81

0.82

0.84

0.80

0.84

0.87

0.93

0.93

0.89

0.88

0.93

0.86

0.88

0.90

0.81

0.77

0.80

0.93

0.95

0.97

1.12

2.52

2.17

1.96

1.80

1.81

1.82

1.73

1.74

1.95

1.85

2.07

2.05

1.93

2.07

2.07

1.99

2.45

2.13

2.22

2.24

2.31

2.43

2.51

2.68

2.65

2.52

2.44

2.57

2.32

2.33

2.48

2.19

2.15

2.17

2.37

2.44

2.44

2.79

0.83

0.73

0.78

0.76

0.75

0.77

0.75

0.69

0.72

0.79

0.80

0.74

0.71

0.71

0.69

0.72

0.68

0.70

0.72

0.74

0.65

0.58

0.60

0.62

0.64

0.63

0.62

0.66

0.62

0.64

0.63

0.68

0.73

0.71

0.67

0.63

0.61

0.69

1.23

1.07

0.93

0.87

0.88

0.90

0.84

0.80

0.92

0.88

1.01

1.02

0.96

1.04

1.06

0.98

1.33

1.03

1.08

1.08

1.05

1.10

1.15

1.31

1.30

1.18

1.12

1.22

1.11

1.13

1.20

1.04

0.98

1.01

1.13

1.13

1.21

1.30

0.63

0.61

0.55

0.53

0.48

0.49

0.51

0.48

0.57

0.54

0.55

0.58

0.59

0.64

0.59

0.63

0.62

0.62

0.65

0.65

0.73

0.73

0.77

0.83

0.75

0.77

0.76

0.84

0.76

0.77

0.75

0.68

0.68

0.62

0.68

0.79

0.74

0.90

0.17

0.19

0.23

0.25

0.23

0.21

0.21

0.27

0.27

0.27

0.32

0.31

0.21

0.29

0.29

0.26

0.28

0.34

0.31

0.27

0.31

0.36

0.38

0.37

0.35

0.40

0.40

0.38

0.37

0.36

0.36

0.34

0.38

0.37

0.42

0.45

0.44

0.50
Table 1 cont. 

sample depth TIC TOG Ca Mg Fe Na Al K Si

39

40

41

42

43

44

45

46

47

48

49

50

51

52

53

54

55

56

57

58

59

60

61

62

63

64

65

66

67

68

69

70

71

72

73

74

75

76

77

78

79

80

81

36

36

36

37

38

38

38

38

38

38

38

38

38

38

39

39

39

39

39

39

39

39

39

39

40

40

40

40

40

40

40

41

41

41

41

41

41

41

41

41

41

41

42

.7

.8

.9

.0

.0

.1

.2

.3

.4

.5

.6

.7

.8

.9

.0

.1

.2

.3

.4

.5

.6

.7

.8

.9

.3

.4

.5

.6

.7

.8

.9

.0

.0

.1

.2

.3

.4

.5

.6

.7

.8

.9

.0

1.49

1.91

1.86

1.87

1.93

2.12

2.18

1.76

1.99

1.89

2.00

1.29

1.82

1.55

1.57

1.62

1.57

1.06

0.75

1.70

3.44

2.39

3.82

1.87

1.76

1.94

2.70

2.77

3.16

3.62

3.66

3.58

3.17

1.98

4.68

2.24

1.25

1.68

3.67

3.13

3.33

3.72

2.60

0.79

0.85

0.94

0.91

1.10

1.06

1.61

2.29

2.44

2.61

2.74

3.31

1.23

1.40

1.71

1.84

2.03

2.55

2.78

2.85

2.18

3.52

1.76

0.81

0.71

1.23

2.00

2.36

1.96

2.01

1.80

2.07

2.67

0.74

1.42

1.08

0.92

2.87

2.15

1.93

1.76

1.83

2.19

5.64

7.06

7.17

6.84

7.72

7.98

8.06

7.01

7.56

7.40

7.97

7.59

6.80

6.07

5.89

6.11

5.88

4.19

3.18

7.23

13.54

16.16

16.49

6.26

6.36

6.90

9.94

9.99

11.89

12.33

11.42

11.94

10.21

6.99

10.31

6.11

4.17

9.05

11.87

10.46

11.99

11.21

12.54

1.00

1.45

1.47

1.53

2.50

2.64

2.73

2.83

2.64

2.91

2.68

2.49

2.56

2.42

2.46

2.74

2.62

2.77

2.75

2.61

2.66

2.90

2.70

2.77

2.30

2.39

3.15

3.06

2.98

3.48

3.31

3.37

3.79

3.12

5.14

3.15

2.22

3.49

2.85

2.65

2.82

2.96

2.90

2.33

2.67

2.71

2.63

2.48

2.38

2.25

2.46

2.20

2.37

2.22

2.15

2.53

2.57

2.40

2.60

2.44

2.59

2.50

2.09

1.22

1.14

1.26

2.61

2.42

2.07

1.76

1.40

1.07

1.20

1.09

1.31

1.43

1.18

1.27

1.27

1.59

1.73

1.53

1.75

1.80

1.98

1.66

0.61

0.68

0.71

0.77

1.08

1.15

1.25

1.34

1.30

1.32

1.27

1.19

1.17

1.17

1.20

1.29

1.21

1.24

1.25

1.12

0.81

0.83

0.68

1.03

1.01

1.03

1.00

1.30

1.24

1.08

1.02

1.04

1.04

0.59

0.69

0.53

0.79

0.93

1.02

0.97

1.02

0.98

0.93

1.08

1.27

1.28

1.28

1.38

1.35

1.36

1.46

1.26

1.40

1.29

1.26

1.50

1.47

1.37

1.58

1.43

1.50

1.37

1.16

0.71

0.69

0.77

1.47

1.39

1.23

1.07

0.79

0.64

0.71

0.63

0.82

1.03

0.79

0.78

0.71

0.92

1.12

0.91

0.97

0.98

1.26

0.95

0.80

0.91

0.81

0.84

0.94

0.89

0.82

0.89

0.85

0.90

0.84

0.82

0.94

0.99

0.95

1.01

0.96

0.98

1.01

0.76

0.42

0.37

0.39

0.89

0.91

0.83

0.45

0.45

0.37

0.41

0.38

0.40

0.46

0.32

0.42

0.34

0.52

0.47

0.52

0.55

0.56

0.52

0.48

0.42

0.45

0.47

0.47

0.31

0.18

0.19

0.10

0.16

0.18

0.15

0.14

0.20

0.22

0.22

0.17

0.19

0.11

0.11

0.10

0.10

0.09

0.09

0.33

0.33

0.27

0.10

0.08

0.08

0.08

0.12

0.08

0.09

0.08

0.09

0.10

0.12

0.10

0.10

0.12

0.13

0.11

0.10
Table 1 cont. 

sample depth TIC TOG Ca Mg Fe Na Al K Si

82

83

84

85

86

87

88

89

90

91

92

93

94

95

96

97

98

99

100

101

102

103

104

105

106

107

108

109

110

111

112

113

114

115

116

117

118

119

120

121

122

123

124

42.1

42.2

42.3

42.4

42.5

42.6

42.7

42.8

42.9

43.2

43.3

43.4

43.5

43.6

43.7

43.8

43.9

44.0

44.1

44.2

44.3

44.4

44.5

44.6

44.7

44.8

44.9

45.0

45.1

45.2

45.3

45.4

45.5

45.6

45.7

45.8

45.9

46.0

46.4

46.6

46.7

46.8

46.9

3.56

3.79

3.58

3.07

2.69

3.42

2.93

2.76

3.08

2.65

2.88

3.08

2.99

3.19

3.21

2.59

2.28

1.80

1.91

2.27

2.36

2.17

2.08

1.89

1.74

1.65

1.80

1.83

2.00

1.98

1.69

1.66

1.56

1.49

1.68

1.95

2.07

2.09

1.93

1.92

1.79

1.79

1.82

1

2

1

1

2

2

2

2

2

2

1

1

1

1

1

1

1

1

1

1

1

1

1

2

1

1

1

1

1

1

1

1

1

1

1

2

1

2

1

1

1

1

1

.64

.08

.97

.70

.05

.02

.15

.20

.22

.04

.59

.48

.56

.69

.36

.67

.56

.83

.77

.74

.98

.90

.92

.04

.96

.86

.78

.93

.90

.90

.88

.73

.77

.69

.91

.07

.94

.06

.94

.87

.66

.63

.79

11.91

12.47

13.54

13.25

10.49

10.72

11.47

9.53

8.62

9.03

9.61

10.68

9.00

10.04

9.54

8.69

7.85

7.31

7.62

8.80

9.40

8.78

8.88

7.55

7.33

7.00

7.43

7.59

8.00

8.15

7.27

6.85

6.85

6.28

6.90

8.40

8.79

9.09

8.08

8.08

7.71

7.59

7.62

2.76

2.96

2.83

3.21

3.24

4.09

3.07

3.32

2.76

2.59

2.68

2.42

2.35

2.93

2.76

1.15

0.95

0.80

0.83

1.20

0.91

0.68

0.77

0.59

0.66

0.68

0.72

0.76

0.78

0.73

0.70

0.68

0.69

0.71

0.73

0.79

0.81

0.75

0.80

0.79

0.77

0.74

0.77

1.74

1.61

1.55

1.86

1.28

1.55

1.60

1.73

1.62

1.77

1.70

1.75

1.51

1.70

1.71

1.55

1.57

1.58

1.59

1.65

1.45

1.33

1.63

1.35

1.47

1.60

1.54

1.60

1.59

1.60

1.56

1.61

1.69

1.74

1.69

1.72

1.76

1.73

1.81

1.88

1.85

1.77

1.82

0.97

0.97

0.93

0.96

0.98

1.05

0.85

1.00

0.95

1.00

1.07

0.97

0.88

0.81

0.62

0.79

0.80

0.76

0.79

0.76

0.71

0.74

0.86

0.82

0.96

0.84

0.78

0.78

0.75

0.80

0.91

0.82

0.84

0.86

0.84

0.86

0.89

0.91

1.05

0.98

0.89

0.84

0.81

0.90

0.82

0.76

1.16

0.74

0.81

0.70

0.83

0.71

0.83

0.80

0.86

0.73

0.80

0.75

0.63

0.67

0.72

0.72

0.70

0.63

0.57

0.73

0.54

0.68

0.69

0.77

0.75

0.72

0.73

0.72

0.72

0.72

0.78

0.77

0.76

0.76

0.70

0.78

0.82

0.80

0.74

0.78

0.49

0.46

0.44

0.40

0.39

0.50

0.47

0.57

0.52

0.50

0.57

0.57

0.51

0.52

0.53

0.44

0.46

0.51

0.48

0.45

0.43

0.37

0.42

0.39

0.45

0.46

0.45

0.47

0.48

0.47

0.47

0.49

0.54

0.57

0.56

0.55

0.51

0.46

0.44

0.48

0.54

0.52

0.56

0.12

0.09

0.10

0.09

0.09

0.09

0.13

0.11

0.13

0.09

0.13

0.10

0.11

0.15

0.21

0.19

0.22

0.19

0.19

0.22

0.18

0.17

0.18

0.15

0.17

0.19

0.17

0.20

0.19

0.23

0.20

0.20

0.24

0.22

0.22

0.22

0.19

0.21

0.22

0.20

0.25

0.25

0.29
Table 1 cont. 

sample depth TIC TOG Ca Mg Fe Na Al K Si

125

126

127

128

129

130

131

132

133

134

135

136

137

138

139

140

141

142

143

144

145

146

147

148

149

150

151

152

153

154

155

156

157

158

159

160

161

162

163

164

165

166

167

47

47

47

47

47

47

47

47

47

47

48

49

49

49

49

49

49

50

50

50

50

50

50

52

52

52

52

52

52

52

53

53

53

53

53

53

53

53

53

53

54

54

54

.0

.1

.2

.3

.4

.5

.6

.7

.8

.9

.0

.3

.5

.6

.7

.8

.9

.0

.1

.2

.3

.4

.5

.3

.4

.5

.6

.7

.8

.9

.0

.1

.2

.3

.4

.5

.6

.7

.8

.9

.0

.1

.2

1.76

1.65

1.60

1.65

1.65

1.90

2.04

1.21

1.99

1.67

3.25

2.25

2.60

2.42

1.53

1.94

2.50

3.64

1.38

1.58

1.22

1.27

1.45

1.29

0.77

0.80

2.70

0.82

1.86

2.30

1.77

1.16

2.06

1.22

2.12

3.25

2.14

1.72

1.78

3.43

3.53

3.92

2.28

1.77

1.64

1.73

1.94

1.98

1.52

1.67

2.77

2.70

2.90

2.00

2.76

3.45

3.54

2.67

2.59

2.42

2.41

2.69

2.44

3.33

3.16

2.99

3.03

3.52

1.77

3.04

4.25

5.69

2.63

2.61

3.04

3.23

3.47

3.12

2.69

3.35

3.42

4.22

3.13

2.97

2.63

3.80

7.32

6.88

6.80

7.29

7.59

8.05

8.47

5.12

7.96

6.30

11.03

7.23

7.35

7.39

5.50

6.15

8.21

11.89

7.05

6.82

5.34

5.62

6.41

5.22

5.18

3.79

8.77

8.90

14.82

8.61

8.00

5.23

9.02

5.34

7.83

10.85

8.82

9.97

11.49

9.53

10.88

13.69

9.72

0.72

0.67

0.71

0.71

0.71

0.77

0.79

2.34

2.65

2.94

2.77

3.46

3.91

4.07

2.98

3.64

3.53

3.65

3.11

2.86

3.35

3.12

2.91

3.12

2.92

1.56

3.72

3.46

7.78

4.10

2.92

3.14

3.92

3.61

5.37

4.70

3.86

3.33

3.92

4.84

5.31

5.79

4.21

1.73

1.76

1.81

1.80

1.88

1.71

1.73

1.84

1.80

1.91

1.44

1.70

1.54

1.62

2.04

2.02

1.98

1.70

2.05

1.96

2.02

1.90

1.84

2.41

2.29

1.49

1.83

2.20

1.75

1.99

2.11

2.33

2.52

2.33

2.64

1.83

2.14

2.11

1.82

1.90

1.86

1.74

1.87

0.79

0.77

0.80

0.81

0.97

0.88

0.85

1.09

1.06

1.23

0.95

1.11

1.15

1.04

1.17

1.16

1.07

0.98

1.48

1.41

1.67

1.55

1.53

1.69

1.63

0.85

1.38

1.50

1.09

1.47

1.42

1.67

1.57

1.58

1.68

1.25

1.58

1.53

1.71

1.96

1.29

1.37

1.74

0.75

0.70

0.75

0.72

0.71

0.74

0.69

0.85

0.82

0.91

0.66

0.85

0.65

0.70

0.92

0.88

0.87

0.73

1.05

0.95

1.07

0.95

0.93

1.10

1.07

0.61

0.85

0.99

0.79

0.90

0.93

1.03

1.33

1.05

1.22

0.80

1.02

1.04

0.89

0.96

0.82

0.77

0.90

0.52

0.47

0.54

0.53

0.44

0.52

0.50

0.61

0.61

0.64

0.47

0.47

0.50

0.54

0.62

0.70

0.64

0.56

0.69

0.67

0.60

0.65

0.60

0.87

0.82

0.42

0.61

0.70

0.51

0.64

0.67

0.78

0.62

0.79

0.80

0.58

0.65

0.66

0.59

0.63

0.61

0.56

0.61

0.25

0.27

0.28

0.29

0.32

0.25

0.26

0.10

0.11

0.11

0.10

0.11

0.14

0.16

0.13

0.19

0.24

0.20

0.10

0.10

0.09

0.09

0.09

0.10

0.10

0.10

0.14

0.14

0.13

0.15

0.11

0.10

0.11

0.11

0.14

0.12

0.12

0.11

0.12

0.12

0.12

0.13

0.11
Table 1 cont. 

sample depth TIC TOG Qa Mg Fe Na Al K Si

168

169

170

171

172

173

174

175

176

177

178

179

180

181

182

183

184

185

186

187

188

189

190

191

192

193

194

195

196

197

198

199

200

201

202

203

204

205

206

207

208

209

210

54.3

54.4

54.5

54.6

54.7

54.8

54.9

55.0

55.1

55.2

55.3

55.4

55.6

55.7

55.8

55.9

56.0

56.1

56.2

56.3

56.4

56.5

56.6

56.7

56.8

56.9

57.0

57.1

57.2

57.3

57.4

57.5

57.6

57.7

57.8

57.9

58.0

58.1

58.2

58.3

58.4

58.5

58.6

2.51

3.31

3.17

2.37

2.70

2.66

3.03

3.20

2.99

3.22

3.24

3.07

3.18

2.99

3.18

3.13

3.02

3.29

2.92

2.70

3.20

4.00

4.29

3.15

2.04

2.61

3.36

2.51

2.13

2.61

1.71

2.51

2.90

2.69

2.74

4.62

4.56

2.91

2.61

2.88

5.00

3.75

3.49

3.42

2.92

2.87

2.85

2.97

2.93

3.30

2.36

2.26

3.00

3.02

3.00

3.07

2.52

1.96

2.31

2.44

2.37

2.32

2.44

0.97

0.78

0.82

1.84

2.44

2.24

1.68

2.38

2.12

2.98

2.09

2.03

2.18

2.43

2.23

1.51

1.48

1.95

1.67

2.00

1.19

0.94

0.54

9.46

11.32

10.23

8.64

9.63

9.66

11.86

12.62

12.69

13.30

12.68

12.91

13.05

11.43

12.60

11.47

11.53

12.36

10.24

7.83

7.96

12.73

14.48

10.16

7.47

9.20

7.69

7.58

6.27

7.97

6.08

8.09

9.20

9.35

8.65

12.42

10.97

8.54

7.84

8.38

10.15

8.63

7.09

4.06

4.55

4.21

4.18

4.61

4.43

5.14

4.51

4.23

5.39

5.79

4.42

4.76

3.60

3.17

3.70

3.64

3.59

3.54

3.31

2.98

2.21

2.05

2.85

2.67

3.76

2.78

3.35

3.13

3.11

2.04

2.77

2.71

2.27

2.57

4.24

4.23

2.75

2.23

2.62

4.43

2.73

2.33

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

2

1

1

1

1

1

1

1

1

1

0

0

1

1

1

1

1

1

.78

.61

.57

.77

.67

.74

.41

.34

.26

.37

.23

.47

.46

.54

.47

.56

.59

.46

.68

.59

.58

.18

.06

.47

.68

.09

.13

.61

.80

.63

.80

.84

.30

.23

.34

.99

.94

.33

.31

.47

.19

.36

.42

1.49

1.25

1.42

1.44

1.48

1.44

1.57

1.33

1.31

1.58

1.90

1.55

1.68

1.16

0.93

1.19

1.23

1.24

1.31

1.40

1.28

0.76

0.60

1.04

1.16

1.34

0.77

1.00

1.04

0.96

1.13

1.17

1.09

1.17

1.19

0.66

0.70

0.95

0.97

1.07

0.92

0.85

0.94

0.83

0.75

0.74

0.82

0.78

0.79

0.70

0.71

0.66

0.74

0.74

0.74

0.76

0.71

0.66

0.68

0.75

0.68

0.82

0.77

0.78

0.54

0.51

0.68

0.78

1.00

0.46

0.68

0.83

0.68

0.79

0.86

0.49

0.51

0.51

0.40

0.33

0.51

0.45

0.58

0.44

0.45

0.50

0.57

0.52

0.54

0.58

0.61

0.59

0.48

0.44

0.38

0.40

0.44

0.56

0.53

0.50

0.50

0.54

0.48

0.49

0.52

0.60

0.57

0.42

0.33

0.55

0.61

0.66

0.41

0.55

0.62

0.55

0.63

0.63

0.51

0.56

0.56

0.37

0.41

0.50

0.50

0.59

0.50

0.54

0.58

0.11

0.11

0.11

0.11

0.11

0.12

0.11

0.11

0.11

0.13

0.12

0.12

0.11

0.13

0.11

0.16

0.12

0.13

0.11

0.14

0.10

0.11

0.09

0.11

0.14

0.19

0.10

0.16

0.14

0.16

0.13

0.18

0.16

0.12

0.19

0.11

0.14

0.14

0.22

0.22

0.19

0.19

0.21
Table 1 cont. 

sample depth TIC TOC Ga Mg Fe Ma Al K Si

211

212

213

214

215

216

217

218

219

220

221

222

223

224

225

226

227

228

229

230

231

232

233

234

235

236

237

238

239

240

241

242

243

244

245

246

247

248

249

250

251

252

253

58.7

58.8

58.9

59.0

59.1

59.2

59.3

59.4

59.5

59.6

59.7

59.8

59.9

60.0

60.1

60.2

60.3

60.4

60.5

60.6

60.7

60.8

60.9

61.0

61.1

61.2

61.3

61.4

61.5

61.6

61.7

61.8

61.9

62.0

62.1

62.2

62.3

62.4

62.5

62.6

62.8

63.0

63.1

3.82

2.37

4.09

2.32

2.83

2.51

2.54

2.33

3.27

3.23

3.46

4.43

2.50

1.94

2.06

2.32

1.85

1.50

1.55

1.61

1.38

2.22

2.27

2.15

2.60

1.95

2.11

2.07

2.05

1.72

1.34

1.45

1.42

1.83

1.80

1.88

2.34

0.49

9.68

2.36

2.60

2.48

2.60

0.41

1.77

1.47

1.90

2.13

1.88

1.70

1.38

1.61

1.29

1.30

1.12

1.50

1.05

1.78

1.68

1.33

1.40

1.39

1.20

1.73

2.37

2.49

1.91

1.45

2.12

2.33

2.24

1.97

2.22

2.79

2.48

2.66

2.37

2.17

2.13

1.87

1.99

0.22

0.16

1.49

2.04

1.84

7.22

6.40

8.51

6.75

7.70

6.23

7.17

6.63

8.84

8.90

9.52

9.41

8.84

7.23

7.80

9.17

6.89

6.00

6.11

6.33

7.41

8.76

7.45

8.09

7.86

7.70

8.07

7.80

7.95

7.44

6.46

5.43

6.32

7.32

7.11

7.53

8.17

2.07

16.63

1.75

8.90

8.53

8.08

2.

2.

3.

2.

2.

2.

2.

2.

3.

2.

3.

3.

1.

0.

0.

0.

0.

0.

0.

0.

0.

1.

1.

1.

1.

1.

1.

2.

1.

1.

1.

1.

1.

1.

1.

1.

1.

1.

10

1.

1.

1.

1.

58

55

75

04

62

39

46

34

22

89

04

14

15

69

86

83

59

62

71

77

98

42

61

75

69

65

96

43

84

71

68

54

63

55

49

43

32

25

.43

66

05

62

84

1.39

1.70

1.49

1.40

1.46

1.44

1.54

1.54

1.43

1.44

1.36

1.56

1.22

1.22

1.44

1.51

1.27

1.41

1.65

1.71

1.81

1.52

1.41

1.60

1.52

1.28

1.44

1.85

1.63

1.43

1.57

1.64

1.33

1.50

1.59

1.46

1.34

1.79

0.92

1.49

1.54

2.04

1.84

0.97

0.99

0.89

0.86

0.87

0.96

0.89

0.82

0.91

0.95

0.97

0.96

0.88

0.82

0.84

0.94

0.85

0.88

0.81

0.84

0.91

1.03

1.18

1.21

1.14

1.09

1.25

1.32

1.38

1.31

1.30

1.27

1.33

1.20

1.25

1.22

1.14

1.19

0.52

1.20

1.07

1.10

1.25

0.50

0.72

0.49

0.48

0.49

0.46

0.50

0.49

0.48

0.52

0.50

0.66

0.45

0.41

0.49

0.49

0.43

0.48

0.51

0.58

0.65

0.60

0.61

0.68

0.62

0.57

0.61

0.89

0.67

0.62

0.60

0.63

0.60

0.62

0.63

0.60

0.54

0.79

0.32

0.64

0.67

1.01

0.82

0.61

0.66

0.56

0.60

0.61

0.56

0.60

0.60

0.59

0.59

0.55

0.58

0.49

0.47

0.56

0.55

0.50

0.60

0.60

0.68

0.68

0.68

0.67

0.69

0.66

0.63

0.66

0.68

0.70

0.67

0.66

0.65

0.61

0.69

0.72

0.67

0.56

0.69

0.22

0.69

0.54

0.65

0.66

0.20

0.19

0.20

0.19

0.21

0.25

0.25

0.30

0.21

0.19

0.18

0.17

0.20

0.22

0.24

0.27

0.22

0.25

0.30

0.30

0.31

0.17

0.16

0.15

0.14

0.11

0.14

0.15

0.18

0.12

0.14

0.19

0.11

0.12

0.14

0.12

0.15

0.15

0.12

0.13

0.19

0.19

0.17
Table 1 cont. 

sample depth TIC TOC Ca Mg Fe Na Al K Si

254

255

256

257

258

259

260

261

262

263

264

265

266

267

268

269

270

271

272

273

274

275

276

277

278

279

280

281

282

283

284

285

286

287

288

289

290

291

292

293

294

295

296

63.2

63.3

63.4

63.5

63.6

63.7

63.8

63.9

64.0

64.1

64.2

64.3

64.4

64.5

64.6

64.7

64.8

64.9

65.0

65.1

65.2

65.3

65.4

65.5

65.6

65.7

65.8

65.9

66.0

66.1

66.2

66.3

66.4

66.5

66.6

66.7

66.8

66.9

67.0

67.1

67.2

67.3

67.4

2.48

2.36

2.87

2.69

3.29

3.13

3.46

3.53

3.50

2.08

2.31

1.01

1.26

1.71

1.34

2.02

1.68

1.63

1.51

1.93

2.47

2.76

1.86

1.69

2.03

1.26

2.12

1.25

1.31

1.14

1.80

1.56

1.68

1.85

2.03

1.55

1.93

6.05

4.36

4.00

3.26

2.98

4.62

2.74

2.68

2.12

2.26

1.72

2.02

1.90

1.52

2.23

3.25

2.35

3.01

2.74

2.64

2.69

2.04

2.17

2.13

1.65

1.61

1.37

2.79

2.95

2.81

2.74

3.36

2.85

2.69

2.66

1.63

2.31

2.61

2.38

2.09

2.11

2.49

2.15

1.38

4.19

3.08

3.60

2.37

1.51

9.88

10.89

10.31

9.86

10.13

10.67

12.96

8.30

10.05

10.16

9.48

7.91

7.42

8.55

8.76

8.43

7.84

7.82

7.32

8.29

10.03

13.50

7.75

6.84

8.08

6.15

8.31

5.44

5.27

6.03

7.90

7.54

7.15

7.26

7.54

7.62

7.75

21.72

23.76

12.14

11.35

8.42

12.98

2.40

2.10

1.99

2.39

2.30

2.05

1.74

1.74

0.95

0.80

0.63

0.63

0.67

0.82

0.84

0.73

0.77

0.83

0.82

0.83

1.22

2.25

2.95

2.77

2.67

3.46

3.00

3.30

3.13

2.79

3.60

3.53

3.68

3.83

3.45

3.36

3.36

6.02

6.29

7.20

7.33

5.09

5.81

1.82

1.62

1.58

1.85

1.64

1.46

1.42

1.93

1.10

1.28

1.20

1.39

1.39

1.57

1.62

1.52

1.56

1.73

1.63

1.69

1.69

1.67

1.85

2.02

1.88

1.93

1.81

2.25

2.36

2.72

2.82

2.46

2.37

2.78

2.33

2.39

2.23

0.85

0.80

1.65

1.90

1.96

1.59

1

1

1

1

1

1

0

1

0

1

1

1

1

1

1

1

1

1

1

1

0

1

1

1

1

2

1

1

1

1

1

1

1

1

1

1

1

0

0

1

1

1

1

.24

.10

.07

.15

.09

.01

.91

.11

.88

.20

.17

.11

.05

.04

.05

.02

.11

.09

.04

.06

.99

.22

.68

.56

.57

.13

.84

.81

.83

.61

.76

.80

.85

.79

.81

.70

.63

.80

.87

.04

.18

.29

.39

0.97

0.83

0.77

0.99

0.82

0.72

0.69

1.00

0.43

0.53

0.44

0.53

0.55

0.66

0.68

0.60

0.64

0.73

0.71

0.66

0.85

0.81

0.92

1.00

0.95

1.02

0.93

1.19

1.15

1.32

1.57

1.30

1.25

1.60

1.19

1.21

1.12

0.56

0.52

0.80

0.98

0.96

0.89

0.57

0.53

0.54

0.54

0.55

0.45

0.47

0.57

0.34

0.38

0.36

0.40

0.42

0.43

0.42

0.43

0.45

0.47

0.47

0.48

0.51

0.53

0.61

0.62

0.63

0.65

0.59

0.76

0.76

0.85

0.83

0.81

0.80

0.82

0.74

0.76

0.74

0.22

0.23

0.47

0.53

0.58

0.47

0.12

0.17

0.15

0.13

0.14

0.14

0.17

0.18

0.12

0.16

0.17

0.16

0.15

0.18

0.19

0.17

0.18

0.20

0.19

0.22

0.22

0.11

0.11

0.12

0.11

0.10

0.10

0.10

0.11

0.12

0.11

0.11

0.10

0.11

0.10

0.10

0.10

0.10

0.10

0.10

0.10

0.10

0.09
Table 1 cont. 

sample depth TIC TOG Qa Mg Fe Na Al K Si

297

298

299

300

301

302

303

304

305

306

307

308

309

310

311

312

313

314

315

316

317

318

319

320

321

322

323

324

325

326

327

328

329

330

331

332

333

334

335

336

337

338

339

67.5

67.6

67.7

67.8

67.9

68.0

68.1

68.2

68.3

68.4

68.5

68.6

68.7

68.8

68.9

69.0

69.1

69.2

69.3

69.4

69.5

69.6

69.7

69.8

69.9

70.0

70.1

70.2

70.3

70.4

70.5

70.6

70.7

70.8

70.9

71.0

71.1

71.2

71.3

71.4

71.5

71.6

71.7

2.41

1.29

2.05

2.01

2.22

2.18

2.03

1.83

1.30

1.50

1.66

1.94

1.79

2.80

1.85

1.75

1.89

1.68

3.08

2.00

2.24

1.74

1.60

1.93

2.04

1.97

1.44

2.12

2.38

2.87

2.89

1.88

2.66

1.42

2.11

2.33

1.86

1.33

1.53

1.92

2.41

1.71

2.18

2.

3.

1.

1.

1.

1.

1.

0.

0.

0.

0.

0.

0.

<0

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

1.

2.

2.

1.

1.

1.

1.

2.

1.

2.

1.

1.

1.

0.

1.

1.

1.

1.

55

01

20

19

73

08

15

96

95

74

85

63

76

.01

89

81

70

87

81

81

63

73

55

90

95

54

13

08

91

75

55

93

13

75

01

76

13

03

91

07

79

51

96

13.08

11.24

10.08

9.95

11.18

9.63

8.87

8.08

6.82

7.51

8.48

8.78

9.07

9.47

9.43

9.03

8.80

7.61

9.05

9.50

8.61

7.74

6.98

6.85

8.19

7.68

7.99

8.76

10.09

10.95

9.88

8.12

10.29

6.96

8.32

9.88

7.40

5.99

6.35

7.75

7.65

7.63

9.09

3.34

3.06

2.79

2.29

2.36

2.39

2.39

2.36

1.85

1.68

1.74

1.66

1.73

1.92

2.01

1.68

1.82

2.31

4.12

1.83

2.53

2.31

1.76

1.76

2.60

2.74

2.51

2.77

2.89

3.07

3.31

3.50

3.41

2.42

2.71

2.45

2.57

2.03

2.24

2.59

2.55

2.56

2.54

1.87

1.92

2.11

1.99

1.74

1.82

1.70

1.89

2.01

1.93

1.93

1.78

1.85

1.82

1.90

1.74

1.90

1.91

1.84

1.52

1.61

1.60

1.39

1.40

1.86

2.11

2.13

2.02

2.17

1.76

1.91

2.02

2.11

2.14

2.39

2.23

2.41

2.00

2.32

1.91

1.91

2.06

2.16

1.40

1.28

0.96

0.79

0.99

0.92

0.97

0.84

0.83

0.77

0.80

0.74

0.82

0.82

0.86

0.75

0.81

0.81

0.75

0.71

0.73

0.83

0.64

0.64

0.88

1.10

1.28

1.27

1.14

1.12

1.16

1.20

1.20

1.09

1.27

1.07

0.98

0.87

0.92

0.90

0.89

0.92

1.15

1.03

0.98

1.09

0.96

0.81

0.86

0.83

0.89

0.88

0.86

0.89

0.79

0.83

0.86

0.90

0.82

0.92

0.92

0.85

0.71

0.86

0.85

0.71

0.72

0.88

0.95

0.95

0.95

1.07

0.89

0.98

0.99

1.03

1.04

1.12

1.03

1.17

0.93

1.12

0.90

0.91

1.00

1.01

0.55

0.60

0.65

0.63

0.58

0.61

0.59

0.57

0.73

0.65

0.68

0.63

0.64

0.61

0.71

0.64

0.73

0.66

0.63

0.56

0.56

0.64

0.53

0.50

0.61

0.67

0.68

0.67

0.66

0.55

0.66

0.59

0.61

0.71

0.73

0.69

0.80

0.71

0.78

0.65

0.64

0.71

0.69

0.10

0.09

0.09

0.09

0.11

0.10

0.10

0.10

0.11

0.12

0.11

0.11

0.12

0.11

0.13

0.12

0.13

0.13

0.18

0.11

0.11

0.12

0.10

0.10

0.10

0.14

0.17

0.16

0.13

0.11

0.11

0.11

0.16

0.12

0.18

0.20

0.19

0.13

0.15

0.17

0.13

0.16

0.19
Table 1 cont. 

sample depth TIC TOC Ca Mg Fe Na Al K Si

340

341

342

343

344

345

346

347

348

349

350

351

352

353

354

355

356

357

358

359

360

361

362

363

364

365

366

367

368

369

370

371

372

373

374

375

376

377

378

379

380

381

382

71.8

71.9

72.0

72.1

72.2

72.3

72.4

72.5

72.6

72.7

72.8

72.9

73.0

73.1

73.2

73.6

73.7

73.8

73.9

74.0

74.1

74.2

74.3

74.4

74.5

74.6

74.7

74.8

74.9

75.0

75.1

75.2

75.3

75.4

75.5

75.6

75.7

75.8

75.9

76.0

76.1

76.2

76.3

2.14

1.59

1.90

1.91

2.47

2.14

1.92

1.81

1.98

1.40

1.80

2.13

1.93

1.71

2.19

2.03

2.22

1.98

2.37

5.33

3.58

2.16

1.72

0.90

5.47

2.33

2.72

2.92

3.09

2.70

0.04

<0.01

<0.01

<0.01

<0.01

0.01

<0.01

0.02

0.01

0.01

0.01

0.02

0.05

1.65

1.90

1.81

1.60

1.68

1.52

1.62

1.92

1.80

2.53

2.06

1.62

1.58

1.49

1.41

1.87

1.60

1.18

1.73

1.47

1.79

3.12

2.25

2.62

2.33

2.45

2.19

1.95

1.30

1.08

0.65

0.60

0.44

0.51

0.49

0.43

0.39

0.37

0.44

0.38

0.41

0.48

0.25

8.43

7.58

7.57

7.80

9.04

8.63

7.81

7.51

8.09

7.79

7.49

8.10

7.73

6.86

7.99

8.77

8.25

7.81

8.19

13.59

10.73

7.27

7.34

4.23

15.79

9.10

8.90

12.80

11.12

11.00

0.93

0.35

0.30

0.34

0.34

o.sa

0.36

0.40

0.41

0.38

0.42

0.47

0.47

2.53

2.62

2.55

2.57

2.59

2.39

2.26

2.12

2.15

1.74

1.68

2.15

2.45

1.97

2.23

2.05

2.16

1.54

2.82

5.61

4.08

0.91

1.06

1.78

5.34

0.75

0.55

1.28

1.03

0.80

0.65

0.64

0.65

0.74

0.65

0.72

0.72

0.89

0.80

0.79

0.84

0.87

1.20

2.18

2.21

2.24

2.24

2.15

2.26

2.18

2.25

2.15

2.19

2.27

2.23

2.22

2.36

2.37

2.24

2.29

2.23

2.25

2.06

2.16

1.48

2.11

2.27

1.48

1.81

1.37

2.18

1.62

1.50

2.40

2.49

2.26

2.57

2.56

2.34

2.36

2.67

2.43

2.49

2.73

2.63

3.05

1.07

1.10

1.10

1.10

1.25

1.10

1.11

1.11

1.11

1.05

1.02

1.07

1.09

1.17

1.24

1.21

1.19

1.02

1.04

0.88

0.99

0.83

1.03

1.00

0.92

1.20

1.04

1.43

1.00

1.02

0.90

0.85

0.91

1.02

0.92

1.07

1.06

0.96

0.99

0.92

1.03

0.97

1.02

1

1

0

1

0

1

0

1

1

0

1

0

0

0

1

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

1

0

0

0

1

1

1

1

1

1

.03

.02

.99

.03

.94

.05

.99

.00

.03

.97

.01

.93

.91

.98

.01

.87

.90

.94

.93

.86

.93

.52

.87

.95

.64

.85

.51

.09

.79

.77

.84

.85

.88

.09

.86

.93

.94

.18

.03

.08

.20

.23

.62

0.70

0.65

0.69

0.69

0.66

0.67

0.68

0.74

0.67

0.69

0.68

0.67

0.61

0.73

0.67

0.63

0.67

0.67

0.64

0.50

0.58

0.52

0.66

0.68

0.39

0.56

0.48

0.59

0.50

0.46

0.55

0.59

0.62

0.65

0.57

0.68

0.73

0.83

0.74

0.81

0.74

0.78

1.05

0.15

0.17

0.21

0.15

0.25

0.22

0.22

0.27

0.15

0.23

0.19

0.26

0.21

0.26

0.26

0.27

0.31

0.24

0.36

0.25

0.26

0.18

0.32

0.19

0.24

0.32

0.27

0.32

0.14

0.28

0.12

0.11

0.13

0.18

0.16

0.39

0.44

0.35

0.42

0.56

0.51

0.38

0.60
Table 1 cont. 

sample depth TIC TOG Ca Mg Fe Na Al K Si

383

384

385

386

387

388

389

390

391

392

393

394

395

396

397

398

399

400

401

402

403

404

405

406

407

408

409

410

411

412

413

414

415

416

417

418

419

420

421

422

423

424

425

76.4

76.5

76.7

76.8

76.9

77.0

77.1

77.2

77.3

77.4

77.5

77.6

77.7

77.8

77.9

78.0

78.1

78.2

78.3

78.4

78.5

78.6

78.7

78.8

78.9

79.0

79.1

79.2

79.3

79.4

79.5

79.6

79.7

79.8

79.9

80.0

80.1

80.2

80.3

80.4

80.5

80.6

80.7

0.05

0.05

0.44

0.17

0.11

0.08

0.11

0.06

0.34

0.08

0.12

0.06

0.07

0.05

0.07

0.20

0.16

0.04

0.04

0.05

0.11

0.09

0.11

0.19

0.12

0.07

0.10

0.13

0.08

0.04

0.06

0.09

0.10

0.03

0.08

0.12

0.10

0.15

0.24

0.11

0.05

0.04

0.05

0.26

0.31

0.44

0.26

0.25

0.27

0.23

0.21

0.22

0.19

0.23

0.15

0.16

0.21

0.25

0.24

0.30

0.19

0.18

0.17

0.18

0.19

0.21

0.19

0.24

0.25

0.22

0.22

0.20

0.86

0.24

0.29

0.22

0.15

0.24

0.14

0.14

0.21

0.15

0.15

0.15

0.15

0.15

0.69

0.56

1.69

0.66

0.56

0.54

0.56

0.50

1.00

0.57

0.69

0.55

0.53

0.52

0.54

0.79

0.73

0.48

0.43

0.47

0.63

0.65

0.66

0.86

0.95

0.54

0.57

0.63

0.55

0.47

0.45

0.47

0.64

0.44

0.66

0.72

0.60

0.66

0.85

0.65

0.50

0.45

0.43

1.72

1.34

1.14

1.10

1.19

1.19

1.20

1.20

1.38

1.37

1.48

1.43

1.40

1.44

1.39

1.46

1.32

1.43

1.22

1.27

1.30

1.31

1.23

1.28

1.25

1.24

1.26

1.33

1.25

1.24

1.06

1.00

1.30

1.17

1.25

1.10

1.18

1.22

1.29

1.32

1.28

1.24

1.21

4.58

3.49

2.92

3.02

3.15

3.22

3.23

3.10

4.25

3.48

3.90

3.53

3.49

3.57

3.47

3.99

3.74

3.49

2.96

3.14

3.25

3.21

2.98

3.35

3.05

2.96

3.16

3.38

3.01

3.00

2.71

2.69

3.13

2.77

3.14

2.73

2.84

2.98

3.26

3.18

2.98

2.88

2.79

1.29

1.04

1.11

1.02

1.04

1.00

1.07

1.01

1.04

1.02

1.09

1.08

1.08

1.07

1.05

1.10

1.12

1.03

1.00

1.00

1.05

1.03

0.97

0.99

1.00

1.08

1.13

1.11

1.13

1.07

1.09

1.12

1.00

0.99

0.91

0.84

1.00

1.00

0.99

0.95

0.99

0.97

1.00

2.47

1.89

1.46

1.57

1.68

1.71

1.73

1.68

1.93

1.95

2.18

1.97

1.95

1.99

1.92

2.05

1.86

2.01

1.64

1.71

1.76

1.76

1.62

1.72

1.70

1.71

1.69

1.79

1.64

1.69

1.49

1.36

1.70

1.63

1.70

1.49

1.61

1.67

1.76

1.77

1.71

1.69

1.60

1.40

1.12

0.93

0.99

1.08

1.07

1.07

1.14

1.11

1.14

1.13

1.27

1.24

1.23

1.19

1.20

1.12

1.25

1.16

1.20

1.14

1.17

1.15

1.19

1.16

1.16

1.18

1.21

1.19

1.21

1.00

0.95

1.19

1.10

1.14

0.99

1.08

1.09

1.14

1.23

1.14

1.13

1.15

0.75

0.59

0.56

0.57

0.55

0.56

0.61

0.48

0.65

0.60

0.52

0.64

0.61

0.55

0.60

0.58

0.70

0.60

0.53

0.66

0.60

0.63

0.48

0.66

0.61

0.67

0.72

0.75

0.57

0.69

0.55

0.44

0.55

0.69

0.65

0.67

0.67

0.61

0.69

0.68

0.66

0.64

0.50
Table 1 cont. 

sample depth TIC TOG Ca Mg Fe Na Al K Si

426

427

428

429

430

431

432

433

434

435

436

437

438

439

440

441

442

443

444

80.8

80.9

81.0

81.1

81.2

81.3

81.4

81.5

81.6

81.7

81.8

81.9

82.0

82.1

82.2

82.3

82.4

82.5

82.6

0.05

0.08

0.05

0.08

0.13

0.29

0.11

0.02

0.30

0.25

0.22

0.31

0.36

0.17

0.14

0.23

0.26

0.15

0.23

0.15

0.21

0.15

0.11

0.18

0.04

0.50

0.40

0.16

0.15

0.14

0.22

0.23

0.20

0.19

0.19

0.22

0.19

0.21

0.46

0.67

0.41

0.43

0.66

0.78

1.35

1.15

1.16

1.08

1.03

1.33

1.42

0.82

0.80

0.95

1.12

0.78

1.02

1.18

1.22

1.19

1.16

1.18

1.27

1.18

1.23

1.20

1.14

0.85

1.32

1.29

1.28

1.33

1.35

1.29

1.41

1.33

2.74

2.97

2.74

2.68

2.81

3.09

2.97

3.01

2.86

2.60

2.01

3.15

3.17

2.97

3.10

3.22

3.02

3.24

3.13

1.00

1.00

0.98

1.08

1.08

1.11

1.06

0.95

0.97

1.01

0.74

1.07

1.07

1.01

1.04

1.06

1.12

1.14

1.15

1.61

1.67

1.61

1.62

1.59

1.75

1.59

1.63

1.55

1.50

1.17

1.75

1.69

1.78

1.79

1.81

1.71

1.88

1.80

1

1

1

1

1

1

1

1

1

1

0

1

1

1

1

1

1

1

1

.11

.11

.10

.06

.05

.13

.07

.10

.07

.00

.70

.14

.13

.10

.17

.14

.13

.22

.17

0.52

0.52

0.49

0.54

0.53

0.54

0.50

0.56

0.51

0.58

0.62

0.57

0.61

0.63

0.60

0.58

0.53

0.57

0.54

54
Table 2

Analyses of high resolution (10-cm) samples from core OL-92 (83 to 32 m depth) 

for acid-leachable minor elements. Depth refers to midpoint of sample from the 

surface in meters. Concentrations in ppm.

sample depth Ti P Mn Sr Li B Ba V Cu Mo Co

1

2

3

4

5

6

7

8

9

10

1 1

12

13

14

15

16

17

18

19

20

21

22

23

24

25

26

27

28

29

30

31

32

33

34

35

36

37

32.05

32.15

32.25

32.35

32.45

32.55

32.65

32.75

32.85

32.95

33.05

33.15

33.25

33.35

33.45

33.55

33.65

33.75

33.85

34.75

34.85

34.95

35.05

35.15

35.25

35.35

35.45

35.55

35.65

35.75

35.85

35.95

36.05

36.15

36.25

36.35

36.45

881

762

688

640

631

635

583

556

663

640

745

769

717

780

786

733

967

763

797

798

762

793

832

944

921

840

828

886

830

842

876

760

701

695

842

892

938

879 488

723 461

720 563

768 524

653 494

629 504

723 670

1144 982

1058 972

1023 733

885 686

769 538

763 448

738 499

659 483

721 476

661 614

766 697

780 580

660 647

706 643

654 794

638 796

647 796

657 804

566 790

593 696

659 689

595 589

559 547

534 591

693 756

2968 1170

5859 1536

2000 1350

3334 1107

2776 1035

37

33

50

66

56

51

84

133

116

82

69

47

33

35

30

31

42

50

36

35

32

45

45

42

51

55

45

53

53

51

69

113

207

312

241

261

244

72

62

58

54

54

52

50

51

54

53

59

63

64

65

65

66

69

67

66

67

66

67

68

71

73

71

71

76

70

73

74

68

65

66

71

72

71

97

91

111

105

103

99

95

100

96

108

102

91

81

88

86

91

90

75

88

83

83

76

74

82

83

78

77

86

78

79

80

89

103

99

98

88

80

70

59

57

57

56

66

71

89

86

78

58

54

58

68

85

85

102

98

95

90

91

106

109

111

107

111

108

109

105

103

109

113

110

169

129

159

132

58

52

50

47

47

50

47

42

47

47

49

48

48

51

50

45

54

45

48

47

45

40

45

49

47

42

41

45

42

43

44

38

40

41

46

45

44

26

27

23

21

19

22

20

20

22

19

24

22

24

24

27

24

26

24

25

24

26

25

24

25

25

24

24

26

26

23

24

20

19

20

23

21

20

9

1 1

8

14

17

21

20

17

19

21

17

12

1 1

9

3

7

5

<0.01

7

2

7

8

3

4

3

1

4

2

2

6

2

1

11

4

<0.01

3

4

9

9

10

7

9

10

9

9

11

6

5

14

7

8

11

13

13

12

10

14

1 1

1 1

14

16

1 1

12

9

16

8

12

12

9

8

9

1 1

1 1

13

38 36.55 1044 1225 825 231 85 93 134 49 25 3 10
Table 2 cont. 

sample depth Ti P Mn Sr Li B Ba V Cu Mo Co

39

40

41

42

43

44

45

46

47

48

49

50

51

52

53

54

55

56

57

58

59

60

61

62

63

64

65

66

67

68

69

70

71

72

73

74

75

76

77

78

79

80

81

36.65

36.75

36.85

36.95

37.95

38.05

38.15

38.25

38.35

38.45

38.55

38.65

38.75

38.85

38.95

39.05

39.15

39.25

39.35

39.45

39.55

39.65

39.75

39.90

40.25

40.35

40.45

40.55

40.65

40.75

40.85

40.95

41.03

41.09

41.16

41.25

41.35

41.45

41.55

41.65

41.75

41.85

41.95

839

1001

1011

1028

1077

993

996

1088

944

1033

973

932

1145

1153

1074

1207

1089

1181

1052

892

523

511

614

1189

1125

876

685

524

433

444

371

492

636

494

502

467

510

656

521

528

526

664

529

989

823

897

715

424

486

410

371

381

385

398

442

421

397

350

425

356

317

320

346

346

310

365

411

467

540

379

274

292

361

450

449

375

550

528

697

564

497

518

523

614

600

568

715

762

774

743

709

722

614

648

582

650

648

607

701

700

661

734

682

679

666

539

362

354

461

752

797

789

490

438

326

422

414

508

546

330

477

415

566

621

584

603

652

642

600

218

443

450

448

581

698

730

589

586

585

494

543

570

501

490

535

478

297

241

516

867

1056

991

437

406

405

553

510

677

659

636

646

580

408

498

-282

169

451

763

642

721

682

709

80

107

110

120

238

247

283

323

330

341

347

295

271

262

276

313

313

338

344

314

350

374

304

227

199

218

410

492

410

330

292

298

337

280

218

170

188

241

258

244

259

251

229

82

96

102

102

139

153

177

201

194

199

200

186

171

178

187

198

186

196

203

186

122

115

108

153

142

161

181

223

189

178

172

187

191

136

117

94

123

150

193

175

178

178

190

141

230

182

173

161

169

175

152

155

162

246

281

297

270

241

242

209

155

116

157

199

218

227

146

124

111

107

87

115

118

113

114

112

101

88

68

57

105

253

217

208

200

179

44

64

67

64

67

61

61

63

60

61

62

62

65

64

62

69

68

71

69

56

40

35

36

63

62

61

60

58

44

49

44

51

58

37

57

37

37

51

54

54

53

60

56

20

26

27

27

29

27

25

28

24

27

23

24

30

32

27

32

28

29

27

19

5

2

5

30

30

27

9

1 1

7

6

4

8

7

<0.01

5

<0.01

9

7

15

16

17

16

11

5

19

26

38

16

20

24

29

24

27

24

20

18

20

16

17

23

20

14

18

15

9

13

16

11

16

23

28

28

31

30

29

29

14

19

23

31

24

39

35

29

30

31

12

12

10

14

15

13

15

9

12

13

12

9

1 1

1 1

13

16

14

11

9

10

9

4

7

9

13

10

8

6

4

6

5

7

7

7

8

6

8

6

7

8

7

10

8
Table 2 cont. 

sample depth Ti P Mn Sr Li B Ba V Cu Mo Co

82

83

84

85

86

87

88

89

90

91

92

93

94

95

96

97

98

99

100

101

102

103

104

105

106

107

108

109

110

111

112

113

114

115

116

117

118

119

120

121

122

123

124

42.05

42.15

42.25

42.35

42.45

42.55

42.65

42.75

42.85

43.15

43.25

43.35

43.45

43.55

43.65

43.75

43.85

43.95

44.05

44.15

44.25

44.35

44.45

44.55

44.65

44.75

44.85

44.95

45.05

45.15

45.25

45.35

45.45

45.55

45.65

45.75

45.85

45.95

46.43

46.55

46.65

46.75

46.85

486

451

414

597

395

444

420

491

434

501

466

485

414

461

485

491

527

561

549

514

469

440

564

401

499

509

576

567

537

544

530

524

513

548

550

557

553

512

572

603

572

528

571

757

665

465

594

447

410

474

483

524

542

459

522

556

654

1034

402

568

461

412

641

678

564

645

516

534

736

420

560

555

474

450

426

514

451

454

509

532

543

524

427

419

476

424

625

615

551

597

516

552

528

504

494

624

545

582

525

569

698

542

498

441

473

818

741

554

608

471

454

461

473

549

639

542

495

461

463

447

490

575

608

605

597

600

555

538

575

659

627

707

712

539

506

539

554

490

399

470

548

557

581

449

287

246

229

250

344

326

278

296

239

221

225

226

253

295

259

220

203

198

181

218

291

314

292

270

250

232

241

243

225

208

216

231

361

461

255

325

244

239

222

212

183

165

111

68

72

74

73

74

60

57

65

56

66

68

69

70

69

72

75

75

74

80

79

77

78

72

70

75

79

76

77

189

192

201

218

186

205

186

175

163

146

151

144

137

131

104

137

130

130

130

135

125

129

141

140

152

147

131

132

134

145

143

140

145

145

147

141

153

149

134

150

151

140

144

154

169

152

162

134

124

125

134

124

109

124

144

159

186

136

78

79

76

77

104

102

92

100

72

83

86

90

95

104

96

88

86

77

83

91

103

106

93

103

97

100

96

100

47

51

49

60

48

58

51

50

42

45

44

41

39

40

48

38

42

40

42

41

38

34

43

31

40

41

47

48

43

40

39

39

38

43

39

41

42

36

42

39

41

36

42

12

14

16

14

8

9

14

8

9

1 1

11

14

11

6

12

10

9

10

12

8

4

4

4

3

9

8

6

10

6

7

6

9

8

9

9

9

9

8

1 1

14

16

10

11

29 9

37 6

33 8

32 7

32 8

42 10

36 9

41 4

36 2

25 4

32 3

30 5

22 3

22 2

25 6

26 <0.01

13 4

9 2

8 5

4 1

3 <0.01

4 <0.01

6 1

6 1

2 4

2 2

6 3

4 4

1 1

2 3

1 3

4 4

6 5

4 5

2 1

<0.01 3

<0.01 7

<0.01 3

12 4

5 <0.01

2 2

2 1

<0.01 3
Table 2 cont. 

sample depth Ti P Mn Sr Li B Ba V Cu Mo Co

125

126

127

128

129

130

131

132

133

134

135

136

137

138

139

140

141

142

143

144

145

146

147

148

149

150

151

152

153

154

155

156

157

158

159

160

161

162

163

164

165

166

167

46.95

47.05

47.15

47.25

47.35

47.45

47.55

47.65

47.75

47.85

47.95

49.33

49.45

49.55

49.65

49.75

49.85

49.95

50.05

50.15

50.25

50.35

50.45

52.25

52.35

52.45

52.55

52.65

52.75

52.85

52.95

53.05

53.15

53.25

53.35

53.45

53.55

53.65

53.75

53.85

53.95

54.05

54.15

559

530

566

559

549

590

555

598

562

619

511

644

495

526

698

694

725

635

843

788

821

751

718

908

902

590

712

811

645

713

753

816

983

820

939

615

760

769

647

639

599

552

622

402

509

496

550

491

495

560

596

766

564

436

559

542

692

605

719

676

659

433

418

306

352

419

447

381

345

412

456

662

498

418

445

497

505

643

617

468

401

349

434

559

609

415

544

519

534

546

520

539

577

543

593

554

465

421

436

461

513

518

570

536

530

495

514

496

485

539

506

327

497

528

516

526

497

507

596

537

668

509

540

499

478

517

532

569

467

230

192

193

228

222

240

288

243

383

276

598

497

480

483

350

406

544

807

323

296

277

251

385

243

250

207

486

320

1020

423

349

246

527

298

460

.631

542

535

575

526

627

739

496

67

67

72

72

70

73

72

292

289

328

258

303

278

269

295

289

233

218

379

359

449

420

391

420

424

225

401

439

279

415

401

451

475

496

498

381

475

460

512

575

404

367

536

136

135

136

132

155

141

146

183

185

225

161

181

206

188

194

191

178

165

249

243

303

277

278

306

270

158

258

279

201

281

262

316

307

314

337

253

324

307

327

389

264

251

351

95

85

86

87

79

97

103

85

105

97

146

116

103

111

83

92

117

150

86

81

71

72

96

64

69

81

105

84

126

88

88

68

134

90

102

122

127

142

151

127

121

115

112

37

38

42

39

42

45

43

56

54

63

44

58

60

60

66

64

61

55

64

62

67

62

56

71

74

35

60

68

76

65

62

68

80

74

86

61

67

64

59

64

67

58

61

13

10

10

8

6

12

8

13

11

12

4

9

8

10

17

14

11

9

13

14

10

9

10

17

17

3

7

14

8

14

12

17

13

15

17

7

12

12

1 1

10

8

6

9

<0.01 5

2 <0.01

<0.01 8

<0.01 6

7 2

<0.01<0.01

2 4

24 3

26 3

34 4

22 <0.01

25 3

22 <0.01

22 <0.01

17 6

21 10

26 5

27 4

30 5

31 5

32 7

24 4

27 1

25 9

21 9

18 <0.01

30 1

32 11

23 4

31 5

32 3

27 4

26 4

24 7

25 7

28 5

30 2

32 7

37 <0.01

44 6

27 3

30 2

42 5
Table 2 cont. 

sample depth Ti P Mn Sr Li B Ba V Cu Mo Co

168

169

170

171

172

173

174

175

176

177

178

179

180

181

182

183

184

185

186

187

188

189

190

191

192

193

194

195

196

197

198

199

200

201

202

203

204

205

206

207

208

209

210

54.25

54.35

54.45

54.55

54.65

54.75

54.85

54.95

55.05

55.15

55.25

55.43

55.55

55.65

55.75

55.85

55.95

56.05

56.15

56.25

56.35

56.45

56.55

56.65

56.75

56.85

56.95

57.05

57.15

57.25

57.35

57.45

57.55

57.65

57.75

57.85

57.95

58.05

58.15

58.25

58.35

58.45

58.55

562

496

495

498

470

487

414

410

399

389

393

420

435

426

425

393

428

397

472

467

473

372

390

457

511

605

311

433

522

442

504

500

287

314

297

297

241

323

276

348

281

316

308

469

448

394

488

438

557

582

501

413

489

489

431

377

610

559

472

531

565

462

446

490

383

319

424

420

489

408

429

446

436

404

469

401

303

402

479

581

642

496

834

653

611

537

485

491

452

498

481

494

493

464

415

452

417

457

445

479

453

449

443

432

467

480

484

456

428

453

464

549

350

431

483

487

439

533

465

384

422

442

386

436

437

499

441

431

409

499

567

518

457

497

560

677

652

624

695

693

632

674

525

523

515

541

598

538

554

613

760

845

538

411

571

512

486

419

520

384

521

547

573

496

802

697

496

455

516

588

511

385

440

410

422

428

448

413

408

421

440

472

566

444

490

340

298

333

359

370

352

385

335

255

219

315

325

375

206

268

286

243

287

313

296

335

303

226

192

236

207

210

174

181

175

294

249

276

290

301

302

321

284

271

339

392

310

338

254

205

264

275

266

288

265

246

139

108

186

217

244

138

197

197

168

204

207

188

195

198

109

117

162

155

176

134

138

149

112

114

110

94

98

110

123

151

169

158

171

137

138

107

120

101

113

126

107

115

120

171

197

130

102

119

112

110

95

116

96

118

119

120

111

181

151

107

104

114

135

131

102

58 8

51 8

48 4

53 8

53 7

52 8

43 4

41 <0.01

31 <0.01

45 4

46 4

44 2

46 1

44 6

35 4

42 7

46 7

40 6

50 9

43 16

45 17

31 7

27 <0.01

40 9

45 16

58 16

32 2

44 9

54 13

49 11

49 15

50 16

33 6

37 7

32 8

34 <0.01

29 <0.01

30 11

29 4

33 10

36 2

34 3

33 7

35

32

35

30

30

29

37

26

23

33

40

30

33

28

28

28

25

27

34

36

37

20

16

30

36

35

21

31

31

29

36

35

37

29

34

15

19

25

29

25

21

21

23

2

3

6

1

4

2

2

<0.01

<0.01

<0.01

3

1

<0.01

<0.01

1

4

2

5

<0.01

3

8

4

4

5

8

10

4

7

7

6

7

6

4

9

7

4

5

7

5

5

3

6

8
Table 2 cont. 

sample depth Ti P Mn Sr Li B Ba V Cu Mo Co

211

212

213

214

215

216

217

218

219

220

221

222

223

224

225

226

227

228

229

230

231

232

233

234

235

236

237

238

239

240

241

242

243

244

245

246

247

248

249

250

251

252

253

58.65

58.75

58.85

58.95

59.05

59.15

59.25

59.35

59.45

59.55

59.65

59.75

59.85

59.95

60.05

60.15

60.25

60.35

60.45

60.55

60.65

60.75

60.85

60.95

61.05

61.15

61.25

61.35

61.45

61.55

61.65

61.75

61.85

61.95

62.05

62.15

62.25

62.35

62.45

62.63

62.83

62.95

63.05

310

437

310

331

337

316

319

302

303

339

308

397

294

283

307

320

284

288

307

338

370

331

296

343

317

317

336

480

357

330

351

379

339

350

373

356

317

455

214

367

450

609

476

557

607

782

719

709

656

762

769

715

809

758

729

618

528

2448

1567

653

513

512

628

1792

1233

453

444

501

552

539

561

713

580

708

765

476

526

557

515

476

757

299

810

528

731

616

422

452

472

448

449

415

488

475

455

473

469

490

560

484

887

742

396

372

395

481

678

691

498

525

495

451

446

480

440

404

411

418

403

431

453

425

402

349

297

358

466

570

511

401

361

483

373

416

333

370

327

469

495

533

526

404

247

385

445

227

207

221

250

407

547

385

420

376

387

414

404

443

401

327

285

356

419

392

434

458

93

947

109

408

490

438

172

176

145

156

137

123

129

115

125

143

146

151

89

68

86

77

65

75

84

91

108

180

242

251

256

235

269

297

255

250

251

223

227

209

215

189

164

161

74

134

92

162

200

146

153

141

134

142

141

143

137

135

143

143

144

123

115

132

148

125

119

124

121

137

163

187

199

193

180

201

210

215

207

202

208

187

185

191

177

172

179

58

177

149

176

196

105

105

132

103

114

100

109

94

131

141

148

147

116

78

114

119

74

76

83

94

123

147

114

124

125

122

125

126

119

116

97

92

103

111

110

117

118

43

147

49

105

132

113

37

44

42

33

34

34

38

34

39

39

38

42

27

24

27

32

24

28

26

29

28

33

33

37

31

30

36

48

38

34

33

34

31

34

36

36

32

38

43

35

35

50

43

9

10

9

8

6

9

14

17

8

7

6

7

9

12

8

13

7

10

7

8

11

12

9

10

8

3

3

9

10

7

9

11

9

8

10

10

10

16

<0.01

20

6

14

12

21

24

23

24

18

15

18

22

18

17

1 1

11

6

8

8

13

6

8

3

5

17

23

30

25

26

16

21

25

26

22

21

19

18

18

23

18

26

25

4

16

11

18

23

5

5

6

7

6

2

6

4

10

6

2

6

2

4

5

9

6

7

6

6

8

8

7

8

6

6

5

7

7

6

8

7

4

7

5

6

5

6

<0.01

8

5

6

8
Table 2 cont. 

sample depth Ti P Mn Sr Li B Ba V Cu Mo Co

254

255

256

257

258

259

260

261

262

263

264

265

266

267

268

269

270

271

272

273

274

275

276

277

278

279

280

281

282

283

284

285

286

287

288

289

290

291

292

293

294

295

296

63.15

63.25

63.35

63.45

63.55

63.65

63.75

63.85

63.95

64.05

64.15

64.25

64.35

64.45

64.55

64.65

64.75

64.85

64.95

65.05

65.15

65.25

65.35

65.45

65.55

65.65

65.75

65.85

65.95

66.05

66.15

66.25

66.35

66.45

66.55

66.65

66.75

66.85

66.95

67.05

67.15

67.25

67.35

517

485

445

542

468

420

444

612

301

385

349

426

456

518

529

488

519

590

574

551

603

561

626

685

663

710

634

880

857

984

1194

1007

960

1209

893

971

900

379

362

541

642

591

509

577

428

469

566

664

625

2580

1867

1328

702

572

597

541

561

548

486

443

415

497

1094

3342

313

412

542

566

334

469

437

476

656

526

444

434

529

478

461

383

380

475

501

426

622

531

554

520

493

522

506

485

589

619

592

659

563

440

406

484

496

460

446

455

472

621

686

458

528

550

565

525

532

570

578

770

757

675

646

776

647

606

608

384

308

475

522

559

533

588

631

584

534

596

620

693

449

530

475

344

253

237

301

308

265

248

252

248

316

637

1147

609

465

620

485

701

394

391

394

560

511

479

511

526

482

471

1211

1300

641

582

361

598

199

163

157

173

159

142

116

168

66

58

50

62

68

71

72

67

74

77

78

81

128

304

396

350

327

461

394

434

400

320

382

397

414

391

392

394

395

353

323

289

368

385

466

196

161

162

173

162

151

146

188

146

190

149

145

141

145

151

137

151

153

139

144

133

183

270

250

265

349

300

287

296

274

312

308

325

319

321

294

284

109

114

168

204

237

237

144

160

152

155

158

148

171

117

121

118

88

75

77

87

88

86

85

89

88

96

145

207

129

125

157

134

176

124

115

133

166

148

144

156

151

153

143

263

294

143

143

124

174

55

38

39

47

40

37

35

56

29

35

32

36

37

41

44

38

43

46

43

43

45

50

58

62

61

66

63

79

66

70

75

69

69

78

65

67

64

43

42

57

65

65

65

9

5

7

7

7

8

4

12

<0.01

<0.01

15

15

16

19

19

17

20

17

17

18

18

19

24

22

24

22

25

25

27

32

27

26

24

26

25

22

20

1

1

14

16

17

12

20

17

14

15

12

16

12

10

17

12

1

5

1

2

2

6

1

<0.01

3

8

6

17

59

55

53

46

42

41

37

37

36

35

36

35

36

26

19

<0.01

1

39

34

19

18

7

6

7

7

5

6

10

8

2

3

8

6

7

9

7

6

8

7

5

5

10

1 1

7

9

8

7

10

10

10

14

19

11

13

12

12

15

12

3

7

10

9

7

7
Table 2 cont. 

sample depth Ti P Mn Sr Li B Ba V Cu Mo Co

297

298

299

300

301

302

303

304

305

306

307

308

309

310

311

312

313

314

315

316

317

318

319

320

321

322

323

324

325

326

327

328

329

330

331

332

333

334

335

336

337

338

339

67.45

67.55

67.65

67.75

67.85

67.95

68.05

68.15

68.25

68.35

68.45

68.55

68.65

68.75

68.85

68.95

69.05

69.15

69.25

69.35

69.45

69.55

69.65

69.75

69.85

69.95

70.05

70.15

70.25

70.35

70.45

70.55

70.65

70.75

70.85

70.95

71.05

71.15

71.25

71.35

71.45

71.55

71.65

617

616

751

680

516

575

534

624

656

629

654

594

627

626

638

572

632

674

593

522

570

544

493

496

551

539

513

461

611

537

550

555

541

597

574

637

744

662

778

607

608

667

590

504

530

663

537

498

502

568

612

566

592

659

610

599

583

618

603

627

714

615

644

688

724

871

795

650

514

523

534

643

549

602

663

598

670

608

654

685

665

759

714

677

660

710

485

558

649

634

571

569

578

592

604

622

643

604

633

626

657

650

698

661

635

538

545

533

457

458

602

679

694

661

711

566

656

636

731

699

789

734

800

651

760

664

669

704

707

632

521

451

444

515

418

398

375

318

348

385

408

420

448

452

411

403

380

571

418

412

371

324

321

383

356

339

391

505

582

513

419

567

332

401

528

381

302

303

367

358

385

484

425

417

388

336

330

345

328

350

300

267

295

283

302

313

328

268

290

280

229

269

258

261

202

203

284

275

248

257

278

280

255

253

218

221

218

228

245

207

219

236

237

200

211

247

224

165

145

174

156

160

144

134

126

131

121

133

135

148

124

129

127

126

107

96

117

83

84

150

187

215

224

210

197

208

207

210

183

225

185

168

139

144

147

145

150

212

203

146

121

114

123

109

91

111

97

92

90

97

99

104

118

102

107

99

132

110

118

99

93

103

106

106

108

130

171

193

167

129

158

125

136

162

139

132

136

135

125

134

142

58

52

51

38

42

44

39

43

39

39

37

34

38

34

41

37

37

39

43

31

36

30

28

27

39

45

46

47

56

46

52

51

54

52

59

53

52

43

52

47

45

44

49

18

18

17

15

19

15

16

14

17

16

15

16

14

13

17

14

17

14

13

10

10

10

8

7

15

18

22

21

20

14

19

18

23

25

31

22

25

16

22

15

14

19

24

22

15

11

14

14

12

12

13

13

14

10

8

8

13

15

1 1

6

10

9

8

13

1 1

8

8

18

23

22

23

11

10

15

23

24

14

27

19

14

10

11

8

13

18

23

9

10

12

12

10

12

9

9

6

10

11

8

12

9

12

12

9

1 1

9

9

1 1

7

7

7

9

9

12

12

13

9

15

1 1

8

12

13

10

13

1 1

11

12

10

12

1 1
Table 2 cont. 

sample depth Ti P Mn Sr Li B Ba V Cu Mo Co

340

341

342

343

344

345

346

347

348

349

350

351

352

353

354

355

356

357

358

359

360

361

362

363

364

365

366

367

368

369

370

371

372

373

374

375

376

377

378

379

380

381

382

71.75

71.85

71.95

72.05

72.15

72.25

72.35

72.45

72.55

72.65

72.75

72.85

72.95

73.05

73.15

73.55

73.65

73.75

73.85

73.95

74.05

74.15

74.25

74.35

74.45

74.55

74.65

74.75

74.85

74.95

75.05

75.15

75.25

75.35

75.45

75.55

75.65

75.75

75.85

75.95

76.05

76.15

76.25

652

595

584

589

541

645

618

629

648

611

623

583

584

531

575

521

523

562

557

498

516

304

490

568

392

546

319

673

482

466

594

614

621

789

695

791

815

1054

900

903

988

966

1382

667

686

669

731

694

738

696

705

712

683

680

610

672

695

634

524

627

709

696

515

595

536

754

717

1032

1055

945

2306

3273

4076

743

687

666

657

704

589

601

621

652

658

658

709

776

722

743

743

742

715

746

713

757

700

721

702

748

711

719

785

606

699

679

830

713

804

455

562

654

798

609

577

1955

2059

2542

404

378

434

567

697

662

657

736

676

743

900

856

839

434

345

342

362

464

443

381

349

373

337

334

367

355

302

363

425

397

372

355

683

490

407

401

134

946

843

849

903

543

480

40

23

20

22

22

22

20

23

24

22

26

29

31

211

204

212

195

197

211

212

223

220

189

175

177

176

161

179

165

147

122

116

103

108

73

86

95

59

68

51

74

60

55

59

55

62

65

56

57

57

62

58

59

61

66

80

172

178

180

182

214

190

183

177

181

164

156

163

160

194

182

179

170

145

148

116

139

126

148

148

123

215

179

243

186

202

116

107

142

154

139

137

143

136

128

137

145

143

134

139

114

115

127

142

150

130

133

149

142

140

138

127

114

129

132

133

139

146

220

150

110

132

58

259

212

265

175

110

160

32

26

48

62

50

60

61

57

65

81

79

88

191

53

57

52

54

53

56

50

54

54

53

51

55

50

52

59

48

55

53

54

58

57

30

45

50

45

42

27

56

43

41

41

43

43

55

41

46

47

55

50

50

52

55

65

23

23

22

22

23

24

22

25

23

28

27

28

22

28

29

26

28

30

30

23

26

22

30

35

18

30

24

30

26

27

30

26

29

31

31

30

34

36

33

36

35

37

42

28

23

32

22

22

16

20

19

16

20

24

21

21

32

29

33

26

30

15

11

19

30

48

32

10

26

22

23

10

5

2

7

<0.01

<0.01

5

6

3

2

<0.01

2

<0.01

<0.01

1

10

1 1

13

12

11

9

13

12

12

13

11

13

12

13

10

1 1

14

14

15

1 1

12

9

15

12

10

9

6

6

8

9

10

12

10

10

10

8

14

12

9

12

1 1

13

12
Table 2 cont. 

sample depth Ti P Mn Sr Li B Ba V Cu Mo Co

383

384

385

386

387

388

389

390

391

392

393

394

395

396

397

398

399

400

401

402

403

404

405

406

407

408

409

410

411

412

413

414

415

416

417

418

419

420

421

422

423

424

425

76.35

76.45

76.65

76.75

76.85

76.95

77.05

77.15

77.25

77.35

77.45

77.55

77.65

77.75

77.85

77.95

78.05

78.15

78.25

78.35

78.45

78.55

78.65

78.75

78.85

78.95

79.05

79.15

79.25

79.35

79.45

79.55

79.65

79.75

79.85

79.95

80.05

80.15

80.25

80.35

80.45

80.55

80.65

2061

1578

1108

1245

1319

1335

1337

1333

1588

1616

1809

1671

1656

1692

1615

1739

1546

1665

1290

1391

1445

1429

1286

1393

1329

1322

1355

1483

1332

1341

1141

1043

1372

1236

1363

1168

1289

1349

1437

1462

1372

1336

1290

1060

715

1435

731

735

794

919

846

1065

741

837

818

738

730

779

861

789

739

733

742

853

840

843

926

835

777

764

832

687

773

731

725

808

817

889

892

856

804

838

827

818

757

742

1236

890

935

854

879

953

945

827

1457

880

1065

847

835

857

858

1341

1320

815

699

812

1004

1008

996

1352

976

754

973

1086

812

731

752

885

954

704

1063

988

914

929

1203

1089

792

701

677

48

38

125

45

39

41

45

41

75

38

48

35

34

34

35

48

44

33

29

30

41

43

43

53

69

35

35

38

35

30

28

27

42

31

43

39

36

39

50

40

35

32

33

107

83

76

72

75

75

76

73

76

78

79

80

78

78

78

79

74

79

74

73

74

75

71

73

75

75

75

77

74

73

66

64

75

70

72

63

68

68

70

71

73

69

69

173

143

157

139

145

137

150

133

153

136

150

150

146

144

141

146

161

143

127

141

152

142

132

131

136

150

157

150

152

143

138

149

137

137

123

106

125

133

139

127

139

132

134

279

222

192

203

225

250

263

241

366

266

293

276

271

269

274

315

293

283

248

268

278

281

241

304

280

252

270

288

249

257

218

185

275

255

290

247

255

268

301

293

273

260

257

97

72

59

63

66

67

67

65

76

75

79

74

73

76

76

76

70

74

63

63

66

64

61

62

63

64

63

64

61

63

54

53

62

58

62

52

55

60

64

63

63

61

63

64

48

41

44

46

46

48

44

47

44

49

49

49

49

51

52

51

54

48

50

48

47

44

48

46

47

51

51

48

48

41

40

47

47

48

43

44

47

47

49

51

47

46

<0.01

<0.01

4

3

<0.01

<0.01

<0.01

2

<0.01

<0.01

<0.01

<0.01

<0.01

<0.01

<0.01

<0.01

1

<0.01

<0.01

3

<0.01

<0.01

1

<0.01

2

<0.01

<0.01

<0.01

2

1

7

4

<0.01

1

<0.01

1

<0.01

<0.01

<0.01

1

<0.01

<0.01

<0.01

23

16

14

15

17

15

13

15

15

14

20

19

17

14

16

13

17

19

15

19

15

16

15

14

15

15

15

13

15

14

14

14

12

15

16

15

13

12

15

13

13

14

15
Table 2 cont.

sample depth Ti Mn Sr Li B Ba V Cu Mo Co

426 80.75 1282 807 723 37

427 80.85 1342 916 945 51

428 80.95 1258 731 655 31

429 81.05 1268 740 664 32

430 81.15 1293 764 869 46

431 81.25 1442 919 1032 56

432 81.35 1267 855 982 70

433 81.45 1360 822 1020 58

434 81.55 1287 727 928 48

435 81.65 1194 747 757 47

436 81.75 879 854 632 37

437 81.85 1507 792 931 55

438 81.95 1424 747 1011 62

439 82.05 1494 754 810 39

440 82.15 1532 743 841 40

441 82.25 1565 750 916 46

442 82.35 1479 728 849 45

443 82.45 1615 660 876 40

444 82.55 1551 769 886 46

67 138 261 55 44 <0.01 13

66 139 286 57 43 <0.01 16

67 142 250 57 45 5 10

66 156 250 55 46 1 11

66 149 268 57 44 <0.01 15

70 158 303 60 46 <0.01 15

65 150 308 58 44 1 13

67 137 295 61 47 <0.01 15

63 135 259 58 43 <0.01 16

64 135 245 53 45 <0.01 13

49 90 179 39 33 2 8

68 153 298 67 46 <0.01 18

68 156 311 62 48 <0.01 14

67 136 269 62 45 <0.01 17

69 147 288 66 49 1 19

69 149 297 69 50 <0.01 18

67 160 282 65 49 1 17

74 157 296 67 51 <0.01 17

68 159 285 67 50 2 17
Table 3

Averaged analyses (n=444) from Tables 1 and 2 

for TIC, TOC and acid-leachable components of 

sediments from OL-92 (83 to 32 m depth).

wt %

Ca

Mg

Fe

Na

Al

K

Si

TIC

TOC

Ti

P

Mn

Sr

Li

B

Ba

V

Cu

Mo

Co

6.8

2.2

2.0

1.0

1.0

0.7

0.2

1.8

1.6

ppm

711

681

633

357

197

169

142

50

20

16

8
U.S. DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY

Climatic and Hydrologic Conditions in Owens Basin, California, 

Between 145 and 45 ka as Reconstructed from the Highresolution Stable Isotope Records

by

Hong-Chun Li 1 , Teh-Lung Ku1 , James L. Bischoff2, and Lowell D. Stott 1

Open-File Report 98-132 (part 4)

This report is preliminary and has not been reviewed for conformity with U.S. Geological 

Survey editorial standards (or with the North American Stratigraphic Code). Any use of 

trade, product, or firm names is for descriptive purposes only and does not imply 

endorsement by the U.S. Government

1 Department of Earth Sciences, University of Southern California, Los Angeles, 

CA 90089-0740

2 U.S. Geological Survey, Menlo Park, CA 94025

1998

Col
Introduction

That glacial/interglacial climatic variations on Earth are paced by Milankovitch cycles 

has been well documented by the oxygen isotopic record of marine sediments which 

reflects changes in seawater temperature and continental ice volume (Emiliani and 

Shackleton, 1974; Imbrie et al., 1993). Whereas terrestrial temperature variations can be 

linked to those in the sea, thus to the orbital forcing, any linkage between precipitation on 

land and the orbital elements would be subtle at best. Being strongly affected by changes 

in atmosphere-ocean circulation patterns, precipitation exhibits substantial spatial and 

temporal variability. For example, studies of lake sediments show that the Great Basin of 

the southwestern U.S. was a region dotted with large pluvial lakes during glacial periods 

(Bischoff et al., 1985, 1997a; Li et al., 1997; Menking et al., 1997; Morrison, 1975; 

Phillips et al., 1992, 1994; Smith and Street-Perrott, 1983; Street-Perrott and Harrison, 

1984, 1985). On the other hand, studies of the loess-paleosol sequence in northern China 

indicate alternations of cold-dry glacial climate (loess) and warm-wet interglacial climate 

similar to the current one (paleosol) (An et al., 1991; Kukla et al., 1990; Ding et al., 1995). 

The following questions may be posed: (1) If the periodicity of the glacial and interglacial 

fluctuations in both regions matches that of the marine 8 18O record, what causes the 

regional climatic differences? 2) To what extent do the high-latitude climatic variations 

shown by the marine isotopic record correlate with the paleoclimate of the mid- to lowlatitudes on continents? While the mechanism that causes regional differences in 

continental climates on glacial-interglacial time scales remains unclear, a reorganization of 

the marine and atmospheric circulation systems could well be involved. In order to address 

these questions, more regional climatic reconstructions from long-term, high-resolution 

records are of value, especially for information on the variability of paleoprecipitation. 

Closed-basin lakes serve as an excellent deposition system for such reconstructions.

Located in eastern central California within the rainshadow of the Sierra Nevada, 

Owens Lake is one in a chain of quasi-closed basin lakes in the Owens River system. A 

323 m long core, OL-92, retrieved from the depocenter of the lake bed in 1992 represents 

continuous lacustrine sedimentation spanning the last 800,000 years. A multi-parameter 

reconnaissance study of the entire core, having a resolution of 7000 years, was carried out 

by Smith and Bischoff (1997). It was followed by a more detailed study of the core with a 

resolution of -1500 years by Menking et al. (1997) for the last 155,000 years. Using data 

on stable isotopes, wt.% CaCOs, and grain size of the lake sediments, they concluded that 

climate during the last interglacial period in Owens Valley was dry, punctuated with several 

short periods of wet conditions. We report here a study of core OL-92 over the period of 

45 and 145 ka with even finer time resolutions. The study attempts to develop a stable 

isotope mass balance model to reconstruct lake volume variations. Using the 818O and 

8 13C records, we will also determine closed and overflowing lake conditions, lake 

productivity, and general climatic variations during the study period.

Sample Analysis and Data

We subsampled core OL-92 at 10 cm intervals from core depths 32 to 83 m, 

corresponding to an average resolution of -170 years. The samples were washed with deionized water to remove interstitial salts and then oven-dried at 60°C. About 100 ^ig of 

sample material were reacted with 100% phosphoric acid at 90°C and the CO2 produced 

was analyzed for 818O and 813C using a VG Prism triple-collecting mass spectrometer 

equipped with an Isocarb II automatic device for sample loading. Analytical precisions 

were about ±0.25%o for 818O and ±0.15%o for 813C based on replicate analyses of a calcite 

standard performed during sample runs. The isotope ratios are reported as the per mil 

deviation from the PDB standard. A total of 443 samples were analyzed and the results are 

presented in Table 1. Many sediment samples from depths between 75.15 and 82.45 m did 

not contain enough carbonate for analysis. Samples from 32 to 75.15 m contained mainly
calcite with moderate amounts of aragonite; only a few samples formed during low lake 

level periods contained mainly dolomite. Two samples, at 62.45 and 62.55 m, were pure 

dolomite (which gave very heavy 818O and 8 13C values). In view of the difficulty in 

dissolving dolomite with phosphoric acid and dolomite-containing samples were relatively 

rare, most of the isotopic values given in Table 1 represent those of calcite and aragonite. 

Their variations are due to changes in lake hydrologic conditions rather than by changes in 

the relative proportion of calcite and aragonite, because isotopic fractionation between 

calcite and aragonite is small (e.g., 0.6%c at 25°C for 818O).

Figure 1 shows the 818O and 813C profiles of core OL-92 from 32 to 83 m depth. 

The 818O values range from -11.47%o to 0.5 l%o (PDB) and the 8 13C values vary from 

-1.38%o to 13.59%c, excluding the questionable data from the 75.15-82.45 m interval 

(Table 1). The profiles generally match the coarser-resolution profiles of Menking et al. 

(1997) except for the interval between 75.15 and 82.45 m. While the 7 818O values of 

Menking et al. profile in this interval range from -8%o to -3%c, the 48 818O values of our 

profile from the same interval vary from -8.4%o to 7.45%o (Table 1). Eight of these 48 

values are greater than \%o which are abnormally heavy for lacustrine sediments. Analyses 

of the calcite standard accompanying the sample runs (one standard for every 5 sample 

runs) indicate signs of contamination of heavy 818O signals from these anomalous samples, 

an experience shared by James C. Zachos (personal communication) of University of 

California, Santa Cruz, when he analyzed several samples from the 75.15 - 82.45 m 

interval of the Menking et al. profile. It appears that the abnormally high 818O values were 

not caused by analytical error, though further investigations are in order. If so, as will be 

discussed below, they should not be taken to reflect the hydrological balance of the lake.

Comments on the Data

513C-518O covariance

Authigenic carbonates formed away from the sediment-water interface are generally in 

isotopic equilibrium with lake water (Fritz and Poplawski, 1974; Gasse et al., 1987; 

Johnson et al., 1991; Lister et al., 1991; Li et al., 1997), hence their downcore variations 

in 818O and 8 13C reflect past changes in the isotopic composition of lake water. Changes 

in 818O and 813C of a closed-basin lake record changes in lake volume (Li and Ku, 1997).

Li et al. (1997) showed that fresh water input reduces the lake 13C and 18O during 

rapid transgression (Precipitation > Evaporation under wet climates). Under such a 

circumstance, both 8 18O and 813C values move toward lighter values as the lake volume 

increases, giving rise to a good 818O-813C covariance. A rapid decline of the lake volume 

due to intense net evaporation (P < E under dry climates) will increase the lake 8 18O. 

Curtailment of freshwater input to the lake will also result in an increase of 813C in the lake 

DIC because of increased productivity and decreased input of light-813C source water. 

Consequently, a rapidly declining lake will lead to an increase of both its 813C and 818O. 

In summary, in a closed-basin lake, 813C and 818O tend to covary.

When the lake level of a closed-basin lake rises high enough to spill over its sill, the 

lake becomes open with a stable level. For an open lake, the lake 818O is close to the input 

water 8 18O which is related to the moisture source and air temperature (Stuiver, 1970). 

Lake productivity for an over-flowing lake is generally lower than that of a closed lake 

because the nutrient concentrations in an open lake are usually diluted by fresh water. As 

both 818O and 813C in open lakes are relatively invariant, with the 818O being close to the 

input 8 18O and the 813C being around l-3%o (equilibrium with the atmospheric CC>2, 

covariance between 813C and 818O tends to be poor (Li and Ku, 1997).

Figure 2 shows the 813C-818O covariance in core OL-92 for the 32 to 83 m interval. 

Excluding the data from 75.15 to 82.45 m, they can be separated into two groups: those 

with 818O values heavier than -5%o when the lake was closed and those with 818O lighter
than -5%o when the lake was open. The overflowing Owens Lake had a weak 813C-S18O 

covariance, with a correlation coefficient R = 0.2. Its S13C values, mostly within the range 

of l-3%o, indicate low lake productivity. In contrast, during the closed period the lake had 

a better S13C-618O covariance (R = 0.56), and its S13C values (excluding those of the two 

pure dolomite samples) were mostly between 3 and 12%o, reflecting very high productivity 

of the lake. The high lake productivity is also indicated by a parallelism between the total 

organic carbon (TOC) and S13C distributions in the sediments (Fig. 3a).

&8O-TIC and &8O-Li Correlations

Lake-level drop is generally conducive to enhanced carbonate precipitation. Thus the 

818O of lake sediments is expected to have a positive correlation with the total inorganic 

carbon concentration (TIC), which is shown in Fig. 3b. Bischoff et al. (this volume) 

suggest that the acid leachable Li concentration in lake sediments is of diagnostic value for 

lake-level information. This is seen from the observed strong correlation between S18O and 

the Li concentration for the depth interval 32-75 m (Fig. 3c).

Heavy &8O values of 75.15-82.45 m

Data on TIC, TOC, trace metal, acid-leachable metal and XRD indicate that intervals 

75.15-82.45 m and 32-36 m in core OL-92 were deposited under a similar climatic 

condition of being cold and wet (see Fig. 3). Under this condition, the lake probably 

overflowed and would have S18O values lighter than -4%o (PDB) (Menking et al., 1997). 

However, Figure 1 shows that the 818O of sediments from 75.15 to 82.45 m (an interval 

with very low carbonate content) is mostly heavier than 4%o. The heavy values may be 

ascribed to the presence of detrital carbonates brought in by wind and/or glacial meltwater 

They may also be due to the presence of carbonate minerals formed in very cold lake water 

or in icy water that feeds the lake. If either of these two hypothetical scenarios is correct, 

then caution should be exercised for interpreting the S18O record in terms of hydrological 

balance of the lake in low-carbonate sediments deposited during glacial periods, particularly 

if the record is derived from measurements of very small samples (e.g., -100 jLLg), as we 

have done.

An alternative chronology for the interval of 32-82.5 m depth in core OL-92

Bischoff et al. (1997c) and Menking et al. (1997) have interpreted the sediments from 

75.15 to 82.45 m depth to have deposited under a major ice advance during the penultimate 

glacial cycle of marine isotope stage 6. Data on TIC, TOC, acid-soluble Li, Ca, Sr, and 

Mg, and glacial rock flour abundance all show a sharp change from 75.15 m upward, 

indicating a transition from glacial to interglacial. If we take this transition as 

corresponding to Termination II of the marine record, then the age at 75.15 m would be 

close to 128 ka, about 11 ka older than the 117 ka age-assignment based on extrapolating 

the radiocarbon dates from upper part of the core (Table 1). In order to relate the 

chronology of OL-92 with that of the marine isotope stages, we have added 11 ka to the 

original age assignments between 32 and 82.5 m (Table 2) as a possible alternative 

chronology for OL-92. This chronology would put the ages of studied interval of the core 

(32.05-82.45 m) at 58-145 ka.

Changing climatic and hydrological conditions in the Owens Basin

The S18O and S13C variations can be grouped into seven periods. Table 2 lists the 

averages and ranges of S18O and S13C for each of the periods. During Periods I, IE, V and 

VII the climate in the Owens Basin was cold and wet, and Owens Lake overflowed with 

fresh and low productivity water. The lake was closed and had high productivity during 

Periods n, IV and VI, under dry and warm climatic conditions. During much of the last 

interglaciation, climate in the Owens Basin was dry and warm. The intervening wet and
cold periods were comparatively short. Glacial periods corresponding to marine stages 4 

and 6 were cold and wet in the Owens Basin. Transitions between the cold/wet and 

warm/dry climates appeared to have occurred rather abruptly to within a few hundred 

years.

Acknowledgments

We thank G. I. Smith and R. Rosenbauer for their helpfully reviews. Financial 

support from the USGS and NSF grant ATM-9615875 is gratefully acknowledged.

References

An, Z. S., Kukla, G., Porter, S. C., and Xiao, J. L., 1991. Magnetic susceptibility 

evidence of monsoon variation on the Loess Plateau of central China during the last 

130,000 years. Quaternary Research, 36: 29-36.

Bischoff, J. L., Rosenbauer, R. J., and Smith, G. I., 1985. Uranium-series dating of 

sediments from Searles Lake: Differences between continental and marine climate 

records. Science, 227: 1222-1224.

Bischoff, J. L., Fitts, J. P., and Fitzpatrick, J. A., 1997a. Responses of sediment 

geochemistry to climate change in Owens Lake sediment: An 800 ky record of 

saline/fresh cycles. In: G. I. Smith and J. Bischoff (eds.), An 800,00-year geologic 

and climatic record from Owens Lake, California: Core OL-92. pp. 37-47. Geological 

Society of America Special Paper, 317.

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sediments from the last interglacial at Owens Lake, California: Geochemistry of 

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Ding, Z. L, Liu, T. S, Rutter, N. W., Yu, Z. W., Guo, Z. T., and Zhu, R. X., 1995. Icevolume forcing of East Asian Winter Monsoon variations in the past 800,000 years. 

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Emiliani, C., and Shackleton, N. J., 1974. The Brunhes epoch: Isotopic paleotemperatures 

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Palaeoclimatology, Palaeoecology, 60: 1-46.

Fritz, P. and Poplawski, S., 1974. 18O and 13C in the shells of freshwater molluscs and 

their environments. Earth and Planetary Science Letters, 24: 91-98.

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Imbrie, J., Berger, A., Boyle, E. A., Clemens, S. C., Duffy, A., Howard, W. R., Kukla, 

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Johnson, T. C., Halfman, J. D. and Showers, W. J., 1991. Paleoclimate of the past 4000 

years as Lake Turkana, Kenya, based on the isotopic composition of authigenic calcite. 

Palaeogeography, Palaeoclimatology, Palaeoecology, 85: 189-198.

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susceptibility record of Chinese loess. Transactions of the Royal Society of Edinburgh: 

Earth Sciences, 81: 263-288.

Lister, G. S., Kelts, K., Chen, K.-Z., Yu, J.-Q. and Niessen, F., 1991. Lake Qinghai, 

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latest Pleistocene. Palaeogeography, Palaeoclimatology, Palaeoecology, 84: 141-162.

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the last 150 years. Limnology and Oceanography, 42 (2): 230-238.

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for closed-basin lakes. Palaeogeography, Palaeoclimatology, Palaeoecology, 133: 69- 

80.

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mineralogy to inflow water sources and climate during the past 100 k.y. in Death 

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Smith, G. I., and Street-Perrott, F. A., 1983. Pluvial lakes in the Western United States. 

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211. University of Minnesota Press, Minneapolis.

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(eds.), An 800,00-year geologic and climatic record from Owens Lake, California: 

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processes and climate sensitivity. Geophysical Monograph, AGU, v. 29.

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precipitation in the Great Lakes. Limnology and Oceanography, 23: 877-887
46.4

8

ooo 

CO

58.4

40

72.6

Age (ka) 

89.0 107.5

Mid-point depth (m)

50 60 70

Mid-point depth (m)

128.1 150.9

80 90

Fig. 1 Oxygen and carbon isotopic compositions of total carbonates in the sediments 

of OL-92 core. The age assignment is based on: Age (ka) = 23.254+0.448x+0.018x2 

where x = depth (m), according to Bischoff et al. (1997b).
15

10--

CQ

fi

uco 

CO

0

-5

closed-basin lake

overflow 

period

I

very low 

carbonate 

content and 

samples older 

than 115ka

X 

X

tx

-12 -10 -8 -6 -4 -2 

8180 (%o, PDB)

0

Fig. 2 813C - 818O covariance in sediments of core OL-92. Triangles 

denote data points with poor 813C - 818O correlation (R = 0.2), showing 

that the lake overflowed and had low productivity. Open circles denote 

data points of a closed-basin lake with better 813C - 818O covariance 

(R = 0.56) than that during lake overflowing periods, showing that lake 

productivity increases with decreasing lake volume. The cross symbols 

represent samples of older than 115 ka. These samples have 818O values 

less than -0.5%o and contain very low carbonate concentrations. The 

source of the carbonate remains unclear.

7S
15

-14

30

Mid-point depth (m)

Fig. 3 (a) Similar patterns between 613C and total organic carbon (TOC) indicate 

that the 613C record mainly reflects changes in lake productivity, (b) Comparison 

of 618O with total inorganic carbon (TIC) in the sediments of core OL-92. (c) 

Comparison of 618O with lithium concentration in the sediments of core O1-92, 

showing a strong correlation between the two properties from 36 to 75 m. Data 

sources for TOC, TIC and Lithium are from Bischoff et al. in this volume.
Table 1 Carbon and oxygen isotopic compositions (PDB) of carbonates in core OL-92 

from Owens Lake, California. Depth in core refers to the mid-point depth of each 10-cm 

sampling interval. Age assignments are based on the chronology of Bischoff et al. 

(1997b).

Sample 

No.

1

2

3

4

5

6

7

8

9

10

11

12

13

14

15

16

17

18

19

20

21

22

23

24

25

26

27

28

29

30

31

32

33

34

35

36

37

38

39

40

41

42

43

44

Depth 

(m)

32.05

32.15

32.25

32.35

32.45

32.55

32.65

32.75

32.85

32.95

33.05

33.15

33.25

33.35

33.45

33.55

33.65

33.75

33.85

34.75

34.85

34.95

35.05

35.15

35.25

35.35

35.45

35.55

35.65

35.75

35.85

35.95

36.05

36.15

36.25

36.35

36.45

36.55

36.65

36.75

36.85

36.95

37.95

38.05

Age 

(kyrs)

46.22

46.40

46.58

46.76

46.94

47.12

47.30

47.48

47.66

47.84

48.02

48.19

48.36

48.53

48.70

48.86

49.03

49.20

49.37

50.89

51.06

51.23

51.40

51.57

51.74

51.91

52.08

52.25

52.41

52.58

52.75

52.92

53.09

53.25

53.41

53.56

53.72

53.88

54.03

54.19

54.35

54.50

56.06

56.22

8l3C

(%c)

3.53

5.85

1.02

1.71

3.48

1.72

1.41

1.57

1.60

1.78

0.83

0.24

3.99

3.30

-0.03

0.38

0.93

1.48

1.48

1.32

1.95

1.89

1.58

1.90

1.62

1.76

1.25

1.21

0.87

1.57

1.39

1.91

2.27

3.41

3.00

2.75

2.73

2.61

2.91

2.87

3.12

3.11

4.15

3.91

51*0

(%c)

-6.99

-4.97

-10.00

-9.97

-6.62

-9.52

-10.73

-10.20

-10.06

-10.74

-11.27

-9.55

-5.28

-5.91

-7.44

-7.92

-9.52

-9.55

-8.24

-8.73

-7.39

-9.15

-9.41

-8.93

-9.32

-9.42

-9.61

-9.87

-10.12

-9.67

-10.19

-9.45

-9.27

-8.50

-8.67

-8.66

-8.26

-8.27

-7.67

-6.19

-4.68

-4.96

-3.90

-3.67

Sample

No.

45

46

47

48

49

50

51

52

53

54

55

56

57

58

59

60

61

62

63

64

65

66

67

68

69

70

71

72

73

74

75

76

77

78

79

80

81

82

83

84

85

86

87

88

Depth 

(m)

38.15

38.25

38.35

38.45

38.55

38.65

38.75

38.85

38.95

39.05

39.15

39.25

39.35

39.45

39.55

39.65

39.75

39.90

40.25

40.35

40.45

40.55

40.65

40.75

40.85

40.95

41.03

41.09

41.16

41.25

41.35

41.45

41.55

41.65

41.75

41.85

41.95

42.05

42.15

42.25

42.35

42.45

42.55

42.65

Age

(kyrs)

56.38

56.53

56.69

56.84

57.00

57.16

57.31

57.47

57.63

57.78

57.93

58.08

58.23

58.37

58.52

58.67

58.81

59.03

59.55

59.69

59.84

59.99

60.13

60.28

60.43

60.57

60.69

60.77

60.88

61.01

61.16

61.31

61.45

61.60

61.75

61.90

62.04

62.19

62.33

62.47

62.61

62.76

62.90

63.04

5l3C

(%c)

4.27

4.46

4.46

4.64

4.91

5.23

4.52

4.57

4.79

4.48

4.97

4.64

5.12

5.46

5.83

5.74

5.54

7.13

3.66

4.85

5.68

3.22

4.05

6.72

7.01

6.29

6.99

6.25

10.56

9.78

4.27

6.26

5.54

5.35

4.93

5.22

4.56

5.34

5.28

5.35

5.02

4.43

5.94

6.16

5180

(%o)

-3.44

-3.83

-2.64

-3.20

-2.74

-2.59

-3.05

-2.84

-2.62

-3.00

-2.98

-2.58

-3.32

-2.91

-2.58

-2.24

-2.04

-2.82

-3.60

-3.90

-2.66

-1.64

-1.20

-1.94

-2.12

-2.26

-2.18

-2.25

-2.43

-2.60

-3.34

-2.70

-2.31

-2.73

-3.06

-2.46

-3.14

-2.69

-2.57

-2.45

-2.97

-4.20

-4.69

-4.89

77
Table 1 continued

Sample

89

90

91

92

93

94

95

96

97

98

99

100

101

102

103

104

105

106

107

108

109

110

111

112

113

114

115

116

117

118

119

120

121

122

123

124

125

126

127

128

129

130

131

132

133

134

135

136

137

138

139

140

141

Depth 

(m)

42.75

42.85

43.15

43.25

43.35

43.45

43.55

43.65

43.75

43.85

43.95

44.05

44.15

44.25

44.35

44.45

44.55

44.65

44.75

44.85

44.95

45.05

45.15

45.25

45.35

45.45

45.55

45.65

45.75

45.85

45.95

46.43

46.55

46.65

46.75

46.85

46.95

47.05

47.15

47.25

47.35

47.45

47.55

47.65

47.75

47.85

47.95

49.33

49.45

49.55

49.65

49.75

49.85

Age 

(kyrs)

63.18

63.32

63.74

63.88

64.02

64.16

64.30

64.45

64.59

64.73

64.87

65.01

65.15

65.29

65.43

65.57

65.71

65.85

65.99

66.13

66.28

66.42

66.56

66.69

66.83

66.97

67.11

67.25

67.39

67.52

67.66

68.33

68.49

68.63

68.77

68.91

69.05

69.18

69.32

69.46

69.60

69.74

69.88

70.01

70.15

70.29

70.43

72.34

72.52

72.66

72.80

72.93

73.07

8^0

<%o)

5.90

6.29

4.53

4.49

4.56

5.63

6.69

7.12

4.63

4.20

3.38

3.32

4.69

3.77

3.07

3.20

3.19

2.88

3.17

3.20

3.26

3.43

3.33

3.10

3.01

2.95

2.75

2.92

3.22

3.15

3.01

3.30

3.23

3.01

3.14

3.05

2.87

2.64

2.52

2.73

2.76

2.85

3.23

4.55

4.64

5.24

5.92

8.20

9.44

10.24

7.80

9.12

9.76

8180

<%o)

-4.96

-4.78

-5.40

-4.83

-4.88

-3.61

-3.19

-3.58

-8.41

-9.12

-10.15

-9.79

-7.01

-8.61

-9.94

-9.48

-9.53

-10.52

-10.18

-10.34

-9.97

-8.71

-9.54

-10.34

-10.30

-10.45

-10.82

-10.63

-9.56

-9.24

-9.58

-9.17

-9.65

-9.81

-9.24

-9.55

-9.67

-10.21

-10.51

-10.23

-10.14

-10.01

-8.82

-4.08

-3.92

-3.92

-3.42

-2.64

-2.37

-1.96

-2.96

-2.42

-1.89

Sample

142

143

144

145

146

147

148

149

150

151

152

153

154

155

156

157

158

159

160

161

162

163

164

165

166

167

168

169

170

171

172

173

174

175

176

177

178

179

180

181

182

183

184

185

186

187

188

189

190

191

192

193

194

Depth 

(m)

49.95

50.05

50.15

50.25

50.35

50.45

52.25

52.35

52.45

52.55

52.65

52.75

52.85

52.95

53.05

53.15

53.25

53.35

53.45

53.55

53.65

53.75

53.85

53.95

54.05

54.15

54.25

54.35

54.45

54.55

54.65

54.75

54.85

54.95

55.05

55.15

55.25

55.43

55.55

55.65

55.75

55.85

55.95

56.05

56.15

56.25

56.35

56.45

56.55

56.65

56.75

56.85

56.95

Age 

(kyrs)

73.21

73.35

73.49

73.63

73.77

73.91

76.47

76.61

76.75

76.90

77.04

77.19

77.33

77.47

77.62

77.76

77.90

78.05

78.19

78.34

78.48

78.62

78.77

78.91

79.05

79.20

79.35

79.50

79.65

79.81

79.96

80.11

80.26

80.41

80.56

80.72

80.87

81.13

81.32

81.47

81.63

81.78

81.93

82.08

82.23

82.38

82.54

82.69

82.84

82.99

83.14

83.29

83.45

8l3C

(%o)

9.37

3.64

3.64

3.23

3.39

3.85

4.98

4.51

4.68

8.20

7.15

12.45

11.25

5.92

5.31

5.75

5.18

10.15

9.56

6.41

5.24

4.89

5.91

9.21

10.16

5.45

7.01

8.25

7.03

7.33

7.66

7.96

8.21

6.81

6.16

6.97

6.53

6.30

6.31

6.40

6.57

6.90

6.54

6.35

6.20

6.80

6.31

5.04

4.75

6.27

4.97

7.37

8.99

8180

(%o)

-1.94

-3.40

-3.53

-3.63

-3.50

-3.33

-3.05

-3.08

-3.03

-2.20

-2.49

-1.16

-1.33

-2.67

-2.80

-2.61

-2.71

-1.57

-1.90

-2.45

-3.20

-3.10

-2.71

-2.02

-1.91

-3.29

-3.01

-2.62

-2.66

-3.15

-3.01

-2.46

-2.61

-3.40

-3.17

-3.12

-3.40

-3.60

-3.42

-3.84

-3.65

-3.68

-3.94

-3.98

-4.04

-3.76

-3.82

-4.51

-3.35

-3.29

-4.41

-3.62

-2.42
Table 1 continued

Sample

195

196

197

198

199

200

201

202

203

204

205

206

207

208

209

210

211

212

213

214

215

216

217

218

219

220

221

222

223

224

225

226

227

228

229

230

231

232

233

234

235

236

237

238

239

240

241

242

243

244

245

246

Depth 

(m)

57.05

57.15

57.25

57.35

57.45

57.55

57.65

57.75

57.85

57.95

58.05

58.15

58.25

58.35

58.45

58.55

58.65

58.75

58.85

58.95

59.05

59.15

59.25

59.35

59.45

59.55

59.65

59.75

59.85

59.95

60.05

60.15

60.25

60.35

60.45

60.55

60.65

60.75

60.85

60.95

61.05

61.15

61.25

61.35

61.45

61.55

61.65

61.75

61.85

61.95

62.05

62.15

Age 

(kyrs)

83.60

83.75

83.91

84.07

84.24

84.40

84.56

84.73

84.89

85.05

85.22

85.38

85.54

85.70

85.87

86.03

86.19

86.36

86.52

86.68

86.85

87.01

87.17

87.34

87.50

87.66

87.82

87.99

88.15

88.31

88.48

88.64

88.81

88.99

89.16

89.34

89.51

89.69

89.87

90.04

90.22

90.39

90.57

90.74

90.92

91.09

91.27

91.45

91.62

91.80

91.97

92.15

§13C

(%o)

9.12

9.59

10.59

4.23

4.11

6.63

4.14

5.90

10.83

11.28

7.43

7.17

7.58

11.29

9.64

8.49

8.74

9.24

11.59

8.00

9.42

9.62

9.09

10.15

10.24

9.27

8.92

9.96

3.68

2.53

3.93

2.51

2.13

2.14

2.05

1.75

2.32

3.11

3.40

3.02

3.30

3.56

3.55

3.66

3.12

3.11

3.14

3.34

3.45

3.38

2.92

2.68

§180

(%o)

-2.41

-2.33

-1.63

-4.43

-4.91

-3.84

-4.88

-4.02

-1.47

-1.33

-3.86

-4.09

-3.37

-1.71

-2.40

-3.20

-2.93

-2.64

-1.47

-3.63

-2.93

-2.88

-3.36

-2.84

-2.58

-2.98

-2.84

-2.43

-6.76

-9.39

-7.54

-8.28

-10.64

-10.48

-10.70

-10.57

-8.92

-6.03

-5.91

-6.35

-6.55

-5.69

-5.97

-5.90

-5.29

-6.00

-6.61

-6.64

-6.11

-5.69

-6.14

-6.60

Sample

247

248

249

250

251

252

253

254

255

256

257

258

259

260

261

262

263

264

265

266

267

268

269

270

271

272

273

274

275

276

277

278

279

280

281

282

283

284

285

286

287

288

289

290

291

292

293

294

295

296

297

298

Depth 

(m)

62.25

62.35

62.45

62.63

62.83

62.95

63.05

63.15

63.25

63.35

63.45

63.55

63.65

63.75

63.85

63.95

64.05

64.15

64.25

64.35

64.45

64.55

64.65

64.75

64.85

64.95

65.05

65.15

65.25

65.35

65.45

65.55

65.65

65.75

65.85

65.95

66.05

66.15

66.25

66.35

66.45

66.55

66.65

66.75

66.85

66.95

67.05

67.15

67.25

67.35

67.45

67.55

Age 

(kyrs)

92.32

92.50

92.67

93.00

93.34

93.55

93.73

93.90

94.09

94.27

94.46

94.65

94.83

95.02

95.21

95.39

95.58

95.77

95.95

96.14

96.33

96.51

96.70

96.89

97.07

97.26

97.45

97.63

97.82

98.01

98.19

98.38

98.57

98.75

98.94

99.13

99.31

99.50

99.69

99.89

100.08

100.28

100.48

100.67

100.87

101.06

101.26

101.46

101.65

101.85

102.05

102.24

§13C

(%o)

2.79

1.13

13.59

13.19

2.50

3.15

3.26

3.69

3.72

3.89

4.57

4.65

3.82

4.14

3.24

2.98

2.84

2.86

2.71

2.52

2.72

2.38

2.85

2.80

2.74

2.56

2.32

3.56

5.39

4.38

4.31

4.06

4.22

4.42

4.25

4.47

3.76

4.24

4.14

4.14

4.01

4.10

4.69

5.10

6.89

7.63

11.61

11.54

9.34

9.53

4.52

4.48

§180

(%o)

-6.53

-9.62

-0.38

0.07

-8.45

-6.63

-5.90

-4.35

-5.62

-5.70

-5.34

-4.88

-5.46

-5.57

-6.64

-6.89

-7.78

-9.31

-10.17

-11.47

-9.95

-11.28

-10.06

-10.95

-10.41

-10.58

-10.14

-5.86

-2.47

-3.73

-4.39

-4.56

-3.20

-3.21

-3.41

-3.40

-3.50

-3.19

-3.20

-3.10

-3.34

-3.36

-2.40

-2.77

-1.87

-1.59

-1.11

-1.16

-1.58

-1.75

-2.82

-2.89
Table 1 continued

Sample

299

300

301

302

303

304

305

306

307

308

309

310

311

312

313

314

315

316

317

318

319

320

321

322

323

324

325

326

327

328

329

330

331

332

333

334

335

336

337

338

339

340

341

342

343

344

345

346

347

348

349

350

351

Depth 

(m)

67.65

67.75

67.85

67.95

68.05

68.15

68.25

68.35

68.45

68.55

68.65

68.75

68.85

68.95

69.05

69.15

69.25

69.35

69.45

69.55

69.65

69.75

69.85

69.95

70.05

70.15

70.25

70.35

70.45

70.55

70.65

70.75

70.85

70.95

71.05

71.15

71.25

71.35

71.45

71.55

71.65

71.75

71.85

71.95

72.05

72.15

72.25

72.35

72.45

72.55

72.65

72.75

72.85

Age 

(kyrs)

102.44

102.63

102.83

103.03

103.22

103.42

103.62

103.81

104.01

104.21

104.40

104.60

104.79

104.99

105.19

105.38

105.58

105.79

105.99

106.20

106.40

106.61

106.81

107.01

107.22

107.42

107.63

107.83

108.04

108.24

108.45

108.65

108.85

109.06

109.26

109.47

109.67

109.88

110.08

110.29

110.49

110.69

110.90

111.10

111.31

111.51

111.72

111.93

112.14

112.35

112.56

112.77

112.99

S13C

(%<>)

3.32

3.30

3.25

4.15

3.81

3.19

2.29

2.63

2.96

2.73

3.07

2.84

2.79

2.62

2.72

5.16

10.01

3.45

5.82

6.84

4.72

4.25

4.77

4.32

3.23

3.97

4.22

4.80

5.13

5.31

5.30

4.10

3.17

4.22

4.73

4.88

4.67

4.57

4.68

5.64

4.44

5.13

4.80

3.26

4.30

4.71

4.41

3.73

4.05

3.68

2.93

3.03

4.27

81*0

(%o)

-3.33

-3.43

-3.26

-2.99

-3.16

-3.50

-3.74

-3.45

-3.44

-3.13

-3.54

-2.92

-2.89

-3.39

-3.32

-2.55

-1.67

-2.95

-2.69

-2.20

-3.40

-3.32

-3.23

-3.46

-3.73

-3.59

-3.87

-3.33

-3.54

-3.57

-3.49

-3.67

-4.77

-4.28

-3.83

-3.76

-4.37

-4.01

-3.69

-3.63

-4.09

-4.33

-3.69

-7.12

-3.90

-3.47

-3.50

-4.09

-3.84

-4.02

-5.19

-4.97

-4.51

Sample

352

353

354

355

356

357

358

359

360

361

362

363

364

365

366

367

368

369

370

371

372

373

374

375

376

377

378

379

380

381

382

383

384

385

386

387

388

389

390

391

392

393

394

395

396

397

398

399

400

401

402

403

404

Depth 

(m)

72.95

73.05

73.15

73.55

73.65

73.75

73.85

73.95

74.05

74.15

74.25

74.35

74.45

74.55

74.65

74.75

74.85

74.95

75.05

75.15

75.25

75.35

75.45

75.55

75.65

75.75

75.85

75.95

76.05

76.15

76.25

76.35

76.45

76.55

76.65

76.75

76.85

76.95

77.05

77.15

77.25

77.35

77.45

77.55

77.65

77.75

77.85

77.95

78.05

78.15

78.25

78.35

78.45

Age 

(kyrs)

113.20

113.41

113.62

114.46

114.67

114.89

115.10

115.31

115.52

115.73

115.94

116.15

116.36

116.57

116.79

117.00

117.21

117.42

117.63

117.84

118.05

118.27

118.49

118.70

118.92

119.13

119.35

119.57

119.78

120.00

120.22

120.43

120.65

121.48

121.30

121.51

121.73

121.95

122.16

122.38

122.59

122.81

123.03

123.24

123.46

123.68

123.89

124.11

124.32

124.54

124.76

124.98

125.20

S13C

(%o)

5.62

4.02

3.87

3.73

4.41

3.12

7.35

8.75

8.44

4.23

2.90

3.65

6.16

4.13

3.85

2.99

2.18

1.61

0.92

nm

nm

-1.33

-0.23

nm

nm

nm

nm

nm

1.31

2.38

3.43

4.31

3.76

5.95

4.41

4.40

4.57

4.93

4.72

6.01

5.14

5.05

4.97

3.77

0.52

5.07

nm

nm

nm

0.42

3.89

3.59

3.55

8^0

(%o)

-3.18

-4.04

-4.39

-4.20

-3.77

-3.83

-2.28

-1.39

-1.70

-5.57

-6.39

-5.21

-2.48

-4.22

-4.81

-5.51

-5.95

-7.81

-7.82

nm

nm

1.07*

-1.03

nm

nm

nm

nm

nm

-1.84

-1.95

-1.07

-0.18

-0.92

-1.27

0.03

-0.28

0.51

-2.12

-1.61

-3.38

-1.38

-2.54

-3.26

-3.75

-4.87

-2.31

nm

nm

nm

2.28*

0.42

1.55*

-1.11
Table 1 continued

Sample

405

406

407

408

409

410

411

412

413

414

415

416

417

418

419

420

421

422

423

424

Depth 

(m)

78.55

78.65

78.75

78.85

78.95

79.05

79.15

79.25

79.35

79.45

79.55

79.65

79.75

79.85

79.95

80.05

80.15

80.25

80.35

80.45

Age 

(kyrs)

125.42

125.64

125.86

126.08

126.30

126.52

126.74

126.97

127.19

127.41

127.63

127.85

128.07

128.29

128.51

128.73

128.95

129.17

129.39

129.61

8l3C 

(% )

nm

3.66

4.10

4.40

3.92

3.59

4.69

4.39

4.54

4.29

2.28

nm

2.86

1.72

3.25

2.77

2.25

2.85

2.82

3.45

81*0

(%o)

nm

-1.76

-5.49

-3.84

-1.68

-4.57

-4.97

-4.63

-3.53

-4.31

4.99*

nm

7.45*

4.13*

1.94*

1.44*

-0.25

-2.37

-3.44

-1.38

Sample

425

426

427

428

429

430

431

432

433

434

435

436

437

438

439

440

441

442

443

444

Depth 

(m)

80.55

80.65

80.75

80.85

80.95

81.05

81.15

81.25

81.35

81.45

81.55

81.65

81.75

81.85

81.95

82.05

82.15

82.25

82.35

82.45

Age 

(kyrs)

129.83

130.05

130.27

130.49

130.71

130.93

131.15

131.38

131.60

**

132.05

132.27

132.50

132.72

132.95

133.17

133.40

133.62

133.84

134.07

8l3C

(%o)

1.89

1.18

2.51

2.32

1.16

1.23

-2.25

2.18

1.39

**

0.33

-1.38

1.76

1.69

-0.48

1.05

0.66

0.67

0.84

0.55

51*0 

<% )

-1.13

-3.59

-2.50

-3.85

0.46

-2.62

1.92*

-3.33

-5.90

**

-6.56

-8.40

-6.05

-6.10

-5.95

-7.20

-7.84

-6.05

-7.19

-7.50

nm = not measurable due to too low carbonate contents.

* questionable data, see explanation in text,

** sample lost.
Table 2 Summary of stable isotope data and their paleoenvironmental inferences for interval 32-83 m in core 

Period

Sample No.

Depth (m)

Age (ka)***

Probable age*

Deep-sea 

618O stage

Average 618O 

(%o, PDB)

618O range 

(%c, PDB)

Average 613C 

(%o, PDB)

613C range 

(%c, PDB)

Hydrological 

condition

Lake 

productivity

Climate

I

1-42

32.05-36.95

46.22-54.50

58-66 ka

4

-8.59±1.69

-11. 27 4.68

2.03±1.13

-0.03~5.85

Open lake, 

fresh water

Very low

Wet/Cold

II

43-96

37.95-43.65

56.06-64.45

67-76 ka

5a

-3.10±0.92

-5.40 1.20

5.42±1.32

3.91-10.56

Closed lake, 

saline, alkaline

High

Dry/Warm

m

97-131

43.75-47.55

64.59-69.88

76-81 ka

5b

-9.69±0.76

-10.82 7.01

3.20±0.48

2.52-4.69

Fast throughflow open lake

Low

Very wet/Cold

IV

132-222

47.65-59.75

70.01-87.99

81-99ka

5c

-3.01±0.82

-4.91 1.16

7.3512.21

3.23-12.45

Closed lake, 

saline, alkaline

Very high

Dry/Warm

y*

223-274

59.85-65.15

88.15-97.63

99-1 09 ka

5d

-7.6112.10

-11.28-5.29

3.4412.12

1.13-4.65

Mostly an 

open lake

Low

Wet/Cool

27

65.2

97.82

109

-3.4

-6.3

4.6

2.29

Clo

s

H

Dry

* Isotope data not include those of the two dolomite samples at 62.63 and 62.83 m.

** 618O data not include values greater than 0.5%o.

*** Ages according to the time-depth model of Bischoff et al. (1997b).

* Ages based on assuming that the age boundary between Periods VI and VII correspond to Terminal n (128 
U.S. DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY

Carbonate Mineralogy in Owens Lake, California from 145 to 

45 ka: A Proxy of Lake Hydrology and Productivity

by 

Hong-Chun Li 1 , Teh-Lung Ku1 , and James L. Bischoff2

Open-File Report 98-132 (part 5)

This report is preliminary and has not been reviewed for conformity with U.S. Geological 

Survey editorial standards (or with the North American Stratigraphic Code). Any use of 

trade, product, or firm names is for descriptive purposes only and does not imply 

endorsement by the U.S. Government

1 Department of Earth Sciences, University of Southern California, Los Angeles, 

CA 90089-0740

2 U.S. Geological Survey, Menlo Park, CA 94025

1998
Introduction

Studies of isotopic, chemical, and mineralogical compositions of closed-basin lake 

sediments have provided valuable paleoclimatic and paleoenvironmental information. 

Owens Lake is one of several closed-basin lakes located in east-central California, lakes 

that are the remains of ice-age pluvial lakes in the Great Basin. In 1992, the USGS 

recovered a 323-m-long core, OL-92, from near the depo-center of the lake. It represents a 

continuous record of lacustrine sedimentation spanning the last 800,000 years. Studies 

made on the core have shown that weight percent (wt.%) CaCOs, or total inorganic carbon 

(TIC), in the core may serve as a proxy for lake level oscillations (Smith and Bischoff, 

1997; Benson et al., 1996; Bischoff et al., 1997a, 1997b, 1997c; Menking et al., 1997). 

Calcium and carbonate ions in Owens Lake are trapped under closed-lake conditions, 

whereas during overflow, they are transported downstream to precipitate in the lower 

basins (Bischoff et al., 1997b). Therefore, wt.% CaCOa or TIC in Owens Lake sediments 

was low during wet/cold glacial periods and high during dry/warm interglacial periods. 

This use of the CaCOs-abundance proxy, however, is under the constraint that the source 

and chemistry of the inflow water remain unchanged. If these parameters did change, as in 

Lake Manly (the lake that periodically flooded Death Valley during the late Pleistocene), the 

TIC-lake level relationship would not hold and could even be reversed. For example, in 

Lake Manly sediments Li et al. (1997) found that relatively small amounts of calcite formed 

during dry periods from 10 to 0 ka and 100 to 60 ka and relatively abundant calcite formed 

during wet periods from 10 to 60 ka. To circumvent the inflow problem and to avoid the 

uncertainty whether the TIC proxy can be used when a lake does not experience overflow, 

we attempt here to use aragonite abundance in closed-basin lake sediments as a lake-level 

tracer.

In a reconnaissance study, Bischoff et al. (1997a) carried out XRD analyses of OL92 at about 7000-year intervals. The major carbonate mineral was identified as calcite, with 

minor amounts of aragonite and dolomite. Later, Bischoff et al. (1997b) and Menking et 

al. (1997) studied the core at a higher resolution of -1500 years by measuring the total 

inorganic carbon distribution between 160 and 10 ka. In this report, we present the result 

of our measurements on the calcite, aragonite and dolomite contents in the core between the 

depth interval of 32-83 m, corresponding in age between 145 and 45 ka (Li et al., this 

volume). The measurements were made on 443 samples by XRD. The time resolution 

was about 170 years. Our goal is to use the aragonite variability to deduce lake level 

changes of Owens Lake, as it has been shown by Li (1995) that in sediments of Mono 

Lake, a closed-basin lake located 200 km north of Owens Lake, variations in the aragonite 

concentration strongly correlate with lake level fluctuations. We also intend to examine the 

extent to which the presence of dolomite will affect the use of oxygen and carbon isotope 

compositions of total carbonate in sediments as proxies for lake-level history.

Analytical Method and Results

The XRD analyses were done on sediment samples with interstitial salts having been 

removed by washing with de-ionized water. About 0.2 g of sample material were ground 

into fine power, mixed with 1 ml of acetone and placed on a glass slide where acetone was 

allowed to evaporate before analysis. Measurements of the carbonate minerals and their 

relative abundance were made using a Rikagu D/Max X-ray Diffractometer incorporated 

with a Multi CPU Controller.

The XRD spectra showed the presence of three carbonate minerals: calcite, aragonite 

and dolomite, and quartz as a major detrital mineral. The identification of the X-ray peaks

(CuKa) for these minerals were: aragonite at 33.1°26, quartz at 26.5°20, calcite at

29.5°20, and dolomite at 31.2°2e. The choice of 33.1°20 rather than 26.1020for 

estimating the aragonite peak intensity was to avoid the interference of the quartz peak at 

26.5°2e which was usually rather large. We used the peak intensity of quartz as a 

qualitative measure of the extent of detrital contribution to the sample.
Table 1 lists the XRD results on quartz (Q), calcite (C), aragonite (A) and dolomite 

(D) for the 443 samples analyzed. The peak intensity, expressed numerically in some 

arbitrary units for the area under the peak, was estimated via a computer program supplied 

by the instrument manufacturer. The major uncertainty of such an estimation involves the 

baseline level introduced by clay minerals. Correction for this background is difficult 

because clay contents vary from sample to sample. The data reported here are backgrounduncorrected. Thus the low-intensity peaks will have larger uncertainties than the highintensity peaks. As the characteristic peaks of different minerals have different intensities, 

we made standard curves for calibrating the aragonite and calcite abundance by mixing 

various proportions of pure aragonite and calcite tufas collected from Mono Lake. Figure 1 

shows the standard curves for the two minerals, both giving good linear relationships

between wt.% and the peak intensities at 33.1°20 for aragonite and at 29.5°20 for calcite. 

In a 50-50 wt.% mixture, the standard gives an aragonite peak intensity of about 125 and a 

calcite peak intensity of about 550. The peak intensities of quartz and dolomite are also 

stronger than that of aragonite, e.g., the maximum intensities for quartz and dolomite are 

490 (corresponding to -15 wt.%) and 780 (-80 wt.%), respectively (Tables 1 and 2). 

Therefore, estimates on the aragonite abundance bear relatively large errors due to small 

peak intensity/background ratios in the XRD spectra. For aragonite and calcite with less 

than 5 wt.%, their respective peak intensities of 35 and 100 are close to the baseline value, 

hence are considered undetectable (Fig. 1). For quartz and dolomite, we took a peak 

intensity value of 100 similar to that of calcite as their detection limits of 5 wt.% (see Fig. 

4a for illustration of the detection limit for dolomite).

Figure 2 plots the intensity data for various minerals listed in Table 1 against depth in 

core, with the horizontal dashed lines denoting the detection limits. In order to relate the 

response of carbonate minerals to climate changes, we separate the depth profiles into 

seven periods based on the stable isotope records (Li et al, this volume). It is seen that all 

three carbonate minerals are near or below their detection limits for Periods I and VII. In 

general, calcite is abundant from 38 to 75 m, and its abundance decreases with increasing 

aragonite and dolomite. Aragonite shows high abundance in Period n and late Period VI, 

and moderate abundance in Period IV. Dolomite appears minor only in Periods n and IV 

but exhibits several high but narrow peaks from 38 to 75 m depth. The salient feature for 

the quartz distribution is its low abundance in Period I and high abundance in Period VII. 

Since there are no other detectable carbonate minerals, the total carbonate abundance in a 

sample can be taken as the sum of the peak intensities for calcite (C), aragonite (A) and 

dolomite (D). The peak intensity ratios C/Q, A/Q, and D/Q, where Q is the peak intensity 

of quartz and gives a measure of the detrital contribution to the sample, reflect the 

abundance of carbonate minerals relative to detrital sediments (Fig. 3a).

XRD Analysis as a Quantitative Measure of Carbonate Minerals

Based on the comparison of XRD and chemical analyses on Mono Lake sediments, 

Li (1995) has demonstrated that the XRD method can quantitatively measure the aragonite 

and calcite contents. We have compared the XRD results with the TIC results obtained by 

Bischoff et al. (this volume). The comparison shows an apparent correlation (R = 0.83) 

between the two sets of data (Fig. 3a), suggesting that variations in the ratio (C+A+D)/Q 

may reflect changes in wt.% of total carbonate in Owens Lake sediments. Figure 3b shows 

that the correlation between calcite and TIC has a coefficient of 0.6. The lower correlation 

coefficient (0.6 vs. 0.83) implies that aragonite and dolomite contribute significantly to 

TIC.

In order to assess the extent to which the abundance of dolomite is represented by its 

peak intensity, we performed the following experiment on seven samples having strong 

dolomite peaks (Fig. 2 and Table 2). About 0.5 g of each high-dolomite samples were 

leached with 5 ml of IN HC1 at room temperature. After about 30 minutes when the CC>2 

bubbles subsided (pH of the solution ~7), an additional 0.5 ml of concentrated HC1 was 

added to the solution. It took about another 60 minutes to complete the reaction for all
samples except OL-92-249, which required the addition of another 0.5 ml of concentrated 

HC1. The final pH of the leachate solutions was <1. After centrifugation and decantation 

of the supernatants, the samples were washed three times with 30 ml of de-ionized water 

until the supernatant liquids had a pH of 7. The weight loss of each sample, listed in Table 

2, was estimated after the residues were oven-dried at 70°C. As the samples were removed 

of their salt contents before the leaching, and as little organic matter dissolution is expected 

to have occurred during the leaching process, the weight loss is used to calculate the wt.% 

carbonate. We noted that all 80% of the dolomite in sample OL-92-249 were dissolved in 

cold IN HC1 with ease, in contrast to the common experience that dolomite rocks are 

difficult to dissolve in this concentration. Whether the contrast is caused by a difference in 

structure or grain size between this dolomite and dolomite rocks is not clear.

Figure 4 shows the linear correlations between the XRD and acid leaching results. 

The linear correlation between peak intensity and wt.% loss by acid leaching for dolomite 

in Fig. 4a gives that the peak intensity will be ~100 when wt.% is 5%, a detection limit for 

dolomite discussed above. Since these samples contain mainly dolomite, the low peak 

intensities of calcite and aragonite introduce a fairly large uncertainty into the total carbonate 

abundance estimates. Hence the correlation with wt.% lost using dolomite peaks alone is 

stronger than the correlation using peak intensities of D+A and C+D+A. Figure 4 also 

shows that the peak intensities of carbonate minerals normalized to the quartz peak intensity 

represent the carbonate wt.% better than the carbonate peak intensities without 

normalization, since the wt.% is also related to detrital content. In summary, the strong 

correlations as shown in Fig. 4 indicate that XRD analysis can be used as a quantitative 

method to determine the weight percent of carbonate minerals in sediments.

Data implications

Authigenic Dolomite as an Indicator of Abnormally Dry Climate

We have found that high-dolomite samples generally show heavy 518O and 8 13C 

values which reflect sharp drops in lake level under abnormally dry climates (Table 2). 

Comparisons of the isotopic values and dolomite abundance between these high-dolomite 

samples (e.g., OL-92 153 and 249) and the adjacent low-dolomite samples (OL-92 154 

and 250) indicate that the isotopic fractionation of the dolomite is close to those of calcite 

and aragonite in the lake. If isotopic fractionation of dolomite were very different from 

those of calcite and aragonite, the large difference in dolomite abundance would lead to a 

significant difference in the isotopic values of the two adjacent pairs of sediments. But no 

such a difference is seen in Table 2. Furthermore, the lake 818O and 8 13C values increased 

markedly prior to the formation of the high dolomite layers (Table 2). This means that a 

decrease in lake level lead to an increase in Ca2+, Mg2+, and COs2- concentrations which 

favor dolomite precipitation.

Aragonite Abundance as a Proxy for Lake Hydrology and Productivity

Aragonite formation in a closed-basin lake is a function of lake salinity, alkalinity, 

pH, biological activity, and the supply of Ca2+, Mg2+ and SO42" to the lake, all of which in 

turn depend on lake level and climate changes (Bischoff et al., 1991; Dunn, 1953; Cloud, 

1962; Herbst and Bradley, 1989; Newton, 1994; Scholl and Taft, 1964; Taft, 1962). In 

general, when a lake level declines, increases in salinity, alkalinity, pH, water temperature, 

Mg2+, Sr2+ and biological activities favor the formation of aragonite over calcite. Figure 5 

shows that the aragonite/quartz ratio matches well the total organic carbon concentration, 

indicating that high productivity favors aragonite formation. Figure 6 exhibits a positive 

correlation between the aragonite/quartz ratio and the acid-leachable Sr concentration 

measured by Bischoff et al. (this volume).

As can be seen in Fig. 7, high aragonite contents (A/Q) are found at depths of 38.75- 

44, 52.25-56.35, 59.25, and 65.15-67.65 m, occurring mostly during the closed lake 

Periods n, IV and VI reflected by the 818O curve (Li et al., in this volume). Examining the
corresponding changes in A/Q, C/Q and (C+A+D)/Q ratios to the lake level fluctuations 

reflected by the 818O curve, one may find that the A/Q ratio has a better correlation with 

lake level change than the other two. During Period Vn (corresponding to marine oxygen 

isotope stage 6), the lake was cold and overflowing. Detrital sediments might have been 

carried into the lake by meltwater, and any formation of carbonate in the lake was at an 

undetectable level (Fig. 7). The 818O signals of sediments deposited then do not reflect the 

hydrologic balance of the lake (Li et al., this volume).

Acknowledgements

We thank G. I. Smith and R. Rosenbauer for their helpful reviews of this 

manuscript. Financial support from the USGS and NSF grant ATM-9615875 is gratefully 

acknowledged.

References

Benson, L. V., Burdett, J. W., Kashgarian, M., Lund, S. P., Phillips, F. M., and Rye, 

R. O., 1996. Climatic and hydrologic oscillations in the Owens Lake basin and 

adjacent Sierra Nevada, California. Science, 274: 746-749.

Bischoff, J. L., Chazan, D., and Canavan, R. W. IV, A high-resolution study of 

sediments from the last interglacial at Owens Lake, California: Geochemistry of 

sediments in core OL-92, 83 to 32 m depth. U.S.G.S. Open-File Report 97-xxx (This 

volume).

Bischoff, J. L., Fitts, J. P., and Fitzpatrick, J. A., 1997a. Responses of sediment 

geochemistry to climate change in Owens Lake sediment: An 800 ky record of 

saline/fresh cycles. In: G. I. Smith and J. Bischoff (eds.), An 800,00-year geologic 

and climatic record from Owens Lake, California: Core OL-92. pp. 37-47. Geological 

Society of America Special Paper, 317.

Bischoff, J. L., Menking, K. M., Fitts, J. P., and Fitzpatrick, J. A., 1997b. Climatic 

oscillations 10,000-155,000 yr B.P. at Owens Lake, California reflected in glacial rock 

flour abundance and lake salinity in Core OL-92. Quaternary Research, 48: 313-325.

Bischoff, J. L., Stafford, T. W., Jr., and Rubin, M., 1997c. A time-depth scale for 

Owens Lake sediments of core OL-92: Radiocarbon dates and constant massaccumulation rate. In: G. I. Smith and J. Bischoff (eds.), An 800,00-year geologic and 

climatic record from Owens Lake, California: Core OL-92. pp. 91-98. Geological 

Society of America Special Paper, 317.

Bischoff, J. L., Herbst, D. B. and Rosenbauer, R. J., 1991. Gaylussite formation at 

Mono Lake, California. Geochimica et Cosmochimica Acta, vol. 55, pp. 1743-1747.

Cloud, P. E., 1962. Environment of calcium carbonate deposition west of Andros Island, 

Bahamas. U. S. Geological Survey Prof. Paper 350, 138p.

Dunn, J. R., 1953. The origin of the deposits of tufa at Mono Lake. Journal of 

Sedimentary Petrology, vol. 23, pp. 18-23.

Herbst, D. and Bradley, T., 1989. A Malpighian tubule lime gland in an insect inhabiting 

alkaline salt lakes. Journal of Experimental Biol. vol. 145, pp. 63-78.
Li, H.-C., Ku, T.-L., Bischoff, J. L., and Stott, L. D., Climatic and hydrologic 

conditions in Owens Basin, California between 45 and 140 ka reconstructed from the 

high-resolution stable isotope records. U.S.G.S. Open-File Report 97-132 (part 4, 

This volume).

Li, H.-C., 1995. Isotope Geochemistry of Mono Basin, California: Applications to 

Paleoclimate and Paleohydrology. Ph.D. dissertation, University of Southern 

California, Los Angeles, CA 90089, 244p.

Li, H.-C. and Ku, T.-L., 1997. 613C-618O covariance as a paleohydrological indicator for 

closed-basin lakes. Palaeogeography, Palaeoclimatology, Palaeoecology, 133: 69-80.

Li, J., Lowenstein, T. K., and Blackburn, I. R., 1997. Responses of evaporite 

mineralogy to inflow water sources and climate during the past 100 k.y. in Death 

Valley, California. Geological Society of America Bulletin, 109: 1361-1371.

Menking, K. M., Bischoff, J. L., Fitzpatrick, J. A., Burdette, J. W., and Rye, R. O., 

1997. Climate/hydrologic oscillations since 155,000 yr B.P. at Owens Lake, 

California, reflected in abundance and stable isotope composition of sediment 

carbonate. Quaternary Research, 48: 58-68.

Newton, M. S., 1994. Holocene fluctuations of Mono Lake, California: The sedimentary 

record. In: Sedimentology and Geochemistry of Modern and Ancient Saline Lakes. 

SEPM Special Publication No. 50, pp. 143-157.

Scholl, D. W. and Taft, W. H., 1964. Algae, contributors to the formation of calcareous 

tufa, Mono Lake, California. Journal of Sedimentary Petrology, vol. 34, pp. 309-319.

Smith, G. L. and Bischoff, J. L., 1997. Core OL-92 from Owens Lake: Project rationale, 

geologic setting, drilling procedures, and summary. In: G. I. Smith and J. L. Bischoff 

(eds.), An 800,00-year geologic and climatic record from Owens Lake, California: 

Core OL-92. pp. 1-8. Geological Society of America Special Paper, 317.

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calcite and vaterite, and its control on the precipitation of aragonite (abs.). EOS, 

Transactions, American Geophysical Union, vol. 43, pp. 447.
200

a 150 +

0-

1200

y = 23.283 + 2.0794x R = 1.00

0 20 40 60 80 100 

wt.% Aragonite added

y = 17.446 + 11.768x R2 = 1.00

0 20 40 60 80 100 

wt.% Calcite added

Fig. 1 Working standard curves for XRD analyss of aragonite and calcite in Owens 

Lake sediments. The standards are made from mixtures of pure aragonite and pure 

calcite tufas collected from Mono Lake, CA.
600

50 60 70 

Mid-point depth (m)

Fig. 2 XRD measurements of lake sediments from 32 to 83 m depth in core OL-92, 

showing peak intensities of quartz (a), calcite (b), aragonite (c), and dolomite (d). 

Horizental broken lines indicate the detection limits below which the peak intensities 

have large uncertainties. The sediment core records seven periods of varied climatic 

and hydrologic conditions based on the stable isotope study of Li et al. (this volume).

90
y = 0.522 + 0.476x 

R= 0.83

5 __(b) y = 0.378 +0.21 lx 

R= 0.60

4 

12345 

TIC (Wt.%)

2345 

TIC (Wt.%)

Fig. 3 Plots showing corelations between XRD analyses (calcite, aragonite, 

dolomite, and quartz) and chemical analyses of total inorganic carbon (TIC) in core 

OL-92 from Owens Lake. The correlation shown in (a) serves to validate the XRD 

technique as a semi-quantitative method of determining the carbonate concentration 

in sediments. The plots in (b) gives a correlation coefficient (R) that is lower than 

that of the plots shown in (a), indicating that aragonite and dolomite are not 

negligible compared to calcite.

 y = 269.02 + 6.35x R2 = 0.55

 y = 154.59 + 7.42x R2 = 0.64

 y = 62.91 + S.Olx R = 0.71

 y = -4.98 + 0.191x R =0.88

- -y = -5.41+0.191x R2 = 0.88 

= -5.56 + 0.185x R2 = 0.89

900

300

30 40 50 60 70 80 90

Wt.% loss by IN HC1 leaching

30 40 50 60 70 80 90

Wt.% loss by IN HC1 leaching

Fig. 4 (a) Linear correlations between XRD peak intensities of carbonate minerals and 

the weight % loss by IN HC1 leaching of sediments, (b) Linear correlations between 

intensity ratios of carbonate minerals to quartz determined by XRD and the wt.% loss of 

sediment by IN HC1 leaching. The correlations indicate that the XRD analyses can be a 

semi-quantitative way to determine carbonate contents in sediments. These samples 

contain high dolomite contents. Intensity ratio of carbonate mineral to quartz is better 

proxy for wt.% than intensity of the mineral only.
10 0.8

50 60 70 

Mid-point depth (m)

Fig. 5 Plots showing co-variance between aragonite/quartz ratio and total organic 

carbon content in core OL-92, indicating that aragonite may be used as a proxy for 

lake productivity.

o

30 40 5O 6O 7O SO 90

Mid-point depth (m)

Fig. 6 Comparison of aragonite/quartz ratio with Sr concentration in the sediemnts 

of core OL-92. Similar patterns between the two parameters indicate that Sr 

concentration of lake water strongly influences aragonite formation. Correlation 

coefficient (R) between the two parameters for all data is 0.62, and is 0.65 if the 

data of Period I are excluded.
40 50 60 70 

Mid-point depth (m)

80

Fig. 7 Comparison of 818O record with aragonite/quartz, calcite/quartz and total 

carbonate/quartz ratios in core OL-92 from 32 to 83 m depth. The plots show that 

sediment abundance of aragonite, which is favored to form in a lake with relatively 

high salinity, alkalinity and productivity, may serve to trace past lake level fluctuations. 

The seven divisions of the core shown in the plots are based on interpretation of the 

618O record (Li et al., 1998).
Table 1 Peak intensity values for quartz and carbonate minerals of lake sediments from 

core OL-92. Sampling interval is 10 cm and depth from the core top is at the middle point 

of each interval. Q = quartz, peak at 26.5° 26; C = calcite, peak at 29.5° 28; D = dolomite, 

peak at 31.2° 26; and A = aragonite, peak at 33.1° 26. Baseline values for quartz, calcite 

and dolomite is relatively high. When the peak intensities for these minerals have values 

less than 100, no peaks can be identified. In this case, the intensity for each mineral is 

calculated by taking 0.2° on each side of the designed degrees above.

Samp.

1

2

3

4

5

6

7

8

9

10

11

12

13

14

15

16

17

18

19

20

21

22

23

24

25

26

27

28

29

30

31

32

33

34

35

36

37

38

39

40

41

42

43

44

Depth 

(m)

32.05

32.15

32.25

32.35

32.45

32.55

32.65

32.75

32.85

32.95

33.05

33.15

33.25

33.35

33.45

33.55

33.65

33.75

33.85

34.75

34.85

34.95

35.05

35.15

35.25

35.35

35.45

35.55

35.65

35.75

35.85

35.95

36.05

36.15

36.25

36.35

36.45

36.55

36.65

36.75

36.85

36.95

37.95

38.05

Q

178

131

155

134

153

136

123

127

128

148

167

144

168

149

163

134

126

165

146

160

185

154

144

144

166

146

85

136

152

191

86

159

79

64

106

124

106

105

105

47

121

112

94

84

C

33

30

60

36

33

47

66

72

59

52

34

47

52

44

52

49

44

56

32

28

43

42

34

23

45

38

21

49

50

38

50

61

50

41

83

76

92

89

95

53

122

105

126

115

D

33

30

42

26

24

27

27

39

48

25

48

49

34

28

44

37

37

36

42

33

51

25

41

33

52

24

27

27

23

27

17

25

10

17

25

51

33

41

48

14

21

49

22

27

A

25

22

25

32

35

32

20

34

29

17

18

27

33

26

22

35

30

37

32

29

32

25

29

15

21

16

10

36

20

21

15

29

23

18

28

27

29

25

21

11

28

18

19

23

Samp.

45

46

47

48

49

50

51

52

53

54

55

56

57

58

59

60

61

62

63

64

65

66

67

68

69

70

71

72

73

74

75

76

77

78

79

80

81

82

83

84

85

86

87

88

Depth 

(m)

38.15

38.25

38.35

38.45

38.55

38.65

38.75

38.85

38.95

39.05

39.15

39.25

39.35

39.45

39.55

39.65

39.75

39.90

40.25

40.35

40.45

40.55

40.65

40.75

40.85

40.95

41.03

41.09

41.16

41.25

41.35

41.45

41.55

41.65

41.75

41.85

41.95

42.05

42.15

42.25

42.35

42.45

42.55

42.65

Q

73

90

72

73

87

69

209

193

218

185

206

212

216

229

167

114

218

233

157

137

200

125

210

126

153

156

201

267

154

222

225

272

169

149

204

204

224

239

131

234

126

247

209

521

C

52

65

43

49

73

56

140

130

159

146

143

144

147

157

211

149

340

256

180

123

263

180

280

187

248

183

246

461

92

95

90

252

111

146

192

214

236

277

137

217

187

361

381

377

D

21

19

21

20

16

29

31

49

54

52

56

61

59

47

42

35

72

103

42

62

80

30

164

85

146

122

215

140

440

253

161

251

150

119

184

169

151

185

89

122

50

96

178

163

A

28

31

25

28

28

24

76

58

89

78

63

62

64

86

107

57

89

33

23

36

65

30

79

45

71

51

58

83

71

53

58

81

90

58

79

84

77

75

50

78

32

61

53

49
Table 1 continued

Samp.

89

90

91

92

93

94

95

96

97

98

99

100

101

102

103

104

105

106

107

108

109

110

111

112

113

114

115

116

117

118

119

120

121

122

123

124

125

126

127

128

129

130

131

132

133

134

135

136

137

138

139

140

141

Depth 

(m)

42.75

42.85

43.15

43.25

43.35

43.45

43.55

43.65

43.75

43.85

43.95

44.05

44.15

44.25

44.35

44.45

44.55

44.65

44.75

44.85

44.95

45.05

45.15

45.25

45.35

45.45

45.55

45.65

45.75

45.85

45.95

46.43

46.55

46.65

46.75

46.85

46.95

47.05

47.15

47.25

47.35

47.45

47.55

47.65

47.75

47.85

47.95

49.33

49.45

49.55

49.65

49.75

49.85

Q

253

271

252

254

256

260

222

137

137

211

233

224

135

197

173

200

205

238

226

204

286

227

242

245

249

214

237

222

221

251

191

221

213

194

220

214

194

236

220

222

241

213

205

254

183

202

197

197

190

179

217

209

260

c

338

354

297

326

294

136

101

100

166

222

246

232

150

234

206

288

225

224

217

240

266

245

254

207

243

215

208

228

230

264

289

236

260

241

264

250

246

232

228

212

255

279

270

186

205

207

271

163

125

149

150

108

164

D

137

174

121

123

115

143

180

164

62

73

82

51

38

98

60

65

50

50

51

65

39

60

38

53

54

73

60

62

43

43

57

48

46

69

51

52

34

42

66

60

53

43

59

61

65

72

131

180

237

272

123

183

242

A

55

61

54

48

63

86

82

42

43

54

63

44

26

58

38

47

51

37

29

46

43

46

45

47

33

36

36

47

55

37

33

45

41

49

43

31

34

43

41

47

51

36

47

55

39

40

44

47

50

76

39

39

48

Samp.

142

143

144

145

146

147

148

149

150

151

152

153

154

155

156

157

158

159

160

161

162

163

164

165

166

167

168

169

170

171

172

173

174

175

176

177

178

179

180

181

182

183

184

185

186

187

188

189

190

191

192

193

194

Depth 

(m)

49.95

50.05

50.15

50.25

50.35

50.45

52.25

52.35

52.45

52.55

52.65

52.75

52.85

52.95

53.05

53.15

53.25

53.35

53.45

53.55

53.65

53.75

53.85

53.95

54.05

54.15

54.25

54.35

54.45

54.55

54.65

54.75

54.85

54.95

55.05

55.15

55.25

55.43

55.55

55.65

55.75

55.85

55.95

56.05

56.15

56.25

56.35

56.45

56.55

56.65

56.75

56.85

56.95

Q

189

189

192

195

211

187

191

200

206

179

194

114

211

210

191

215

236

165

167

151

185

149

170

150

121

153

164

134

163

191

174

181

137

142

160

137

124

167

254

183

215

244

209

196

190

203

191

244

213

234

188

215

204

C

164

204

213

174

208

158

166

154

143

125

191

63

152

179

154

118

126

107

110

125

146

173

133

130

170

178

141

160

155

122

144

113

123

175

192

221

178

195

179

159

212

163

140

164

164

131

149

369

472

292

232

235

185

D

243

47

47

50

49

45

69

71

67

187

104

542

144

68

56

75

85

171

218

96

53

77

160

222

275

130

130

196

139

69

166

147

219

139

96

183

133

136

120

153

130

163

114

108

108

120

122

93

61

115

116

175

241

A

51

49

43

48

47

48

63

68

61

41

46

62

46

42

44

46

36

38

60

57

52

47

53

40

41

40

41

52

45

46

45

50

50

57

56

51

60

49

63

43

48

43

48

50

51

49

52

34

35

32

32

31

47
Table 1 continued

Samp.

195

196

197

198

199

200

201

202

203

204

205

206

207

208

209

210

211

212

213

214

215

216

217

218

219

220

221

222

223

224

225

226

221

228

229

230

231

232

233

234

235

236

237

238

239

240

241

242

243

244

245

246

Depth 

(m)

57.05

57.15

57.25

57.35

57.45

57.55

57.65

57.75

57.85

57.95

58.05

58.15

58.25

58.35

58.45

58.55

58.65

58.75

58.85

58.95

59.05

59.15

59.25

59.35

59.45

59.55

59.65

59.75

59.85

59.95

60.05

60.15

60.25

60.35

60.45

60.55

60.65

60.75

60.85

60.95

61.05

61.15

61.25

61.35

61.45

61.55

61.65

61.75

61.85

61.95

62.05

62.15

Q

224

228

239

253

182

233

291

216

216

222

197

229

178

188

231

193

185

256

180

237

209

224

228

257

193

199

215

186

244

265

208

226

260

271

261

242

254

219

230

215

268

276

201

224

261

235

196

269

221

198

203

229

C

154

151

155

193

242

249

302

225

245

150

195

213

204

105

169

164

133

133

102

166

152

101

135

115

122

158

200

214

262

245

248

266

229

226

209

195

205

259

238

262

250

254

218

271

255

230

195

197

185

186

195

269

D

199

168

242

49

99

111

55

131

302

355

170

149

176

383

229

169

182

192

307

157

223

194

193

219

254

200

238

308

66

51

53

55

40

43

47

43

48

47

44

37

62

42

38

36

43

50

35

57

57

43

54

44

A

39

41

46

34

38

39

30

37

44

51

32

30

29

28

37

30

25

31

30

27

24

42

131

44

32

34

31

54

35

24

38

50

40

53

27

24

35

27

22

39

26

20

27

35

39

31

28

38

29

25

39

36

Samp.

247

248

249

250

251

252

253

254

255

256

257

258

259

260

261

262

263

264

265

266

267

268

269

270

271

272

273

274

275

276

277

278

279

280

281

282

283

284

285

286

287

288

289

290

291

292

293

294

295

296

297

298

Depth 

(m)

62.25

62.35

62.45

62.63

62.83

62.95

63.05

63.15

63.25

63.35

63.45

63.55

63.65

63.75

63.85

63.95

64.05

64.15

64.25

64.35

64.45

64.55

64.65

64.75

64.85

64.95

65.05

65.15

65.25

65.35

65.45

65.55

65.65

65.75

65.85

65.95

66.05

66.15

66.25

66.35

66.45

66.55

66.65

66.75

66.85

66.95

67.05

67.15

67.25

67.35

67.45

67.55

Q

194

306

77

309

202

178

239

201

155

218

203

203

185

178

211

149

162

149

235

224

212

227

212

292

207

228

187

263

167

196

244

189

181

145

215

222

214

216

176

207

167

162

248

187

205

174

146

188

233

119

176

207

C

205

70

28

48

259

241

274

237

329

317

290

293

336

408

230

353

359

302

266

242

312

262

256

252

250

240

263

210

102

118

169

148

151

151

93

114

92

124

109

115

95

126

102

90

47

71

35

67

87

93

140

179

D

33

54

787

110

37

38

73

67

82

65

100

98

85

60

73

52

54

43

55

51

46

62

48

40

45

72

55

36

45

36

69

38

43

34

41

55

48

58

45

52

56

50

53

53

152

315

405

416

255

297

41

44

A

28

44

51

46

38

25

38

31

27

40

33

33

42

43

58

55

41

52

51

60

47

45

56

36

32

24

35

55

71

66

53

51

42

76

50

65

49

60

49

54

58

65

56

54

97

94

77

74

55

56

42

43
Table 1 continued

Samp.

299

300

301

302

303

304

305

306

307

308

309

310

311

312

313

314

315

316

317

318

319

320

321

322

323

324

325

326

327

328

329

330

331

332

333

334

335

336

337

338

339

340

341

342

343

344

345

346

347

348

349

350

351

Depth 

(m)

67.65

67.75

67.85

67.95

68.05

68.15

68.25

68.35

68.45

68.55

68.65

68.75

68.85

68.95

69.05

69.15

69.25

69.35

69.45

69.55

69.65

69.75

69.85

69.95

70.05

70.15

70.25

70.35

70.45

70.55

70.65

70.75

70.85

70.95

71.05

71.15

71.25

71.35

71.45

71.55

71.65

71.75

71.85

71.95

72.05

72.15

72.25

72.35

72.45

72.55

72.65

72.75

72.85

Q

270

359

257

266

235

251

351

258

347

358

271

275

241

216

305

275

227

317

323

270

275

491

221

222

215

205

178

230

207

240

192

244

183

216

208

216

185

253

194

192

187

180

177

235

111

203

207

185

193

227

162

242

203

c

208

218

203

179

190

184

195

144

226

167

200

174

188

197

206

132

61

241

153

160

106

110

171

146

171

144

113

76

114

69

101

109

108

105

118

78

83

127

163

94

110

96

86

120

82

110

123

127

141

159

121

143

103

D

25

54

27

32

105

68

29

35

27

25

36

24

34

29

29

76

272

29

124

95

39

38

81

87

51

87

77

33

91

131

158

50

71

83

90

33

45

90

65

114

74

73

75

79

83

100

87

65

73

56

47

51

71

A

63

35

37

29

34

37

25

34

25

21

25

15

21

23

24

22

22

26

26

24

49

27

38

33

26

30

26

36

35

33

40

31

33

42

24

24

25

36

37

38

37

32

24

32

25

38

45

33

36

35

29

29

20

Samp.

352

353

354

355

356

357

358

359

360

361

362

363

364

365

366

367

368

369

370

371

372

373

374

375

376

377

378

379

380

381

382

383

384

385

386

387

388

389

390

391

392

393

394

395

396

397

398

399

400

401

402

403

404

Depth

(m)

72.95

73.05

73.15

73.55

73.65

73.75

73.85

73.95

74.05

74.15

74.25

74.35

74.45

74.55

74.65

74.75

74.85

74.95

75.05

75.15

75.25

75.35

75.45

75.55

75.65

75.75

75.85

75.95

76.05

76.15

76.25

76.35

76.45

76.55

76.65

76.75

76.85

76.95

77.05

77.15

77.25

77.35

77.45

77.55

77.65

77.75

77.85

77.95

78.05

78.15

78.25

78.35

78.45

Q

189

249

203

234

203

261

213

176

198

200

231

227

84

177

172

191

162

214

355

279

354

319

339

298

378

392

344

296

284

282

336

198

296

242

295

277

277

299

337

259

282

314

269

339

304

303

317

307

318

280

283

320

357

C

107

91

145

179

202

221

94

72

99

97

83

113

41

69

90

217

317

294

75

93

80

80

94

100

96

100

96

84

93

61

76

53

85

100

97

97

93

70

63

72

52

55

59

71

107

79

86

76

92

81

87

84

108

D

91

61

97

76

99

39

177

369

290

29

27

36

500

24

47

38

19

21

42

39

47

30

45

57

46

47

45

36

49

43

31

23

24

32

42

37

37

30

38

59

36

48

44

52

36

22

41

40

34

42

34

40

32

A

39

23

31

27

34

33

31

18

40

42

52

22

46

57

62

40

23

45

51

37

33

33

29

46

57

50

43

35

43

34

40

23

31

67

40

31

36

25

33

28

36

40

33

41

39

31

32

36

35

33

28

34

43
Table 1 continued

Samp.

405

406

407

408

409

410

411

412

413

414

415

416

417

418

419

420

421

422

423

424

Depth 

(m)

78.55

78.65

78.75

78.85

78.95

79.05

79.15

79.25

79.35

79.45

79.55

79.65

79.75

79.85

79.95

80.05

80.15

80.25

80.35

80.45

Q

309

298

286

329

322

301

310

354

382

355

286

325

273

334

294

290

268

287

305

333

C

95

85

112

105

98

119

102

46

103

91

65

118

94

98

96

94

76

74

99

106

D

24

24

27

44

54

47

44

32

53

32

31

43

40

43

46

45

41

44

31

30

A

41

30

40

36

36

45

45

48

42

39

35

29

24

32

34

43

33

30

34

24

Samp.

425

426

427

428

429

430

431

432

433

434

435

436

437

438

439

440

441

442

443

444

Depth 

(m)

80.55

80.65

80.75

80.85

80.95

81.05

81.15

81.25

81.35

81.45

81.55

81.65

81.75

81.85

81.95

82.05

82.15

82.25

82.35

82.45

Q

317

298

291

314

295

288

294

283

265

351

446

275

307

316

277

302

259

288

264

C

88

97

92

109

108

102

100

111

90

67

132

92

126

104

123

108

69

114

106

D

30

21

34

32

47

35

39

34

23

34

42

33

45

41

48

34

26

40

37

A

32

26

25

30

27

37

36

30

31

32

31

24

33

36

40

33

39

36

30
Table 2 Comparison of XRD results with chemical and stable isotope analyses on several high dolomite and th

core OL-92. Q, C, D and A represent peak intensity of quartz, calcite, dolomite and aragonite, respectively. C

from the weight loss of samples by IN HC1 leaching. Except for OL-92 251, dolomite to calcite+aragonite rat

from 0.7 to 10. There is no correlation between this ratio and the 618O value, indicating that the isotopic comp

reflects lake history. The 818O value increases from -8.45 to 0.07%o between OL-92 251 and 250, indicating a 

level. Following this decline, a 10-cm thick of dolomitic layer formed.

Sample

OL-92 73

OL-92 74

OL-92 153

OL-92 154

OL-92 249

OL-92 250

OL-92 251

OL-92 293

OL-92 294

OL-92 295

OL-92 296

OL-92 358

OL-92 359

OL-92 360

OL-92 364

Depth 

(m)

41.16

41.25

52.75

52.85

62.45

62.63

62.83

67.05

67.15

67.25

67.35

73.85

73.95

74.05

74.45

Q

154

222

114

211

77

309

202

146

188

233

119

213

176

198

84

C

92

95

63

152

28

48

259

35

67

87

93

94

72

99

41

D

440

253

542

144

787

110

37

405

416

255

297

177

369

290

500

A

71

53

62

46

51

46

38

77

74

55

56

31

38

40

46

CaCO3

wt.%

44

52

80

47

37

49

68

CaC03*

wt.%

47

36

57

35

85

30

35

45

42

35

46

33

40

37

63

D/(C+A) 

ratio

2.7

1.7

4.3

0.7

10.0

1.2

0.1

3.6

3.0

1.8

2.0

1.4

3.4

2.1

5.7

613C (%o, 

PDB)

10.56

9.78

12.45

11.25

13.59

13.19

2.50

11.61

11.54

9.34

9.53

7.35

8.75

8.44

6.16

* CaCOs wt.% in this column is calculated from the relationship between (C+D+A)/Q and wt.% loss shown 

have about 10% uncertainty from the measurements.
U.S. DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY

Sediment Magnetic Data (83-18 m depth) and XRF Geochemical Data 

(83-32 m depth) from Lacustrine Sediment in Core OL-92 from

Owens Lake, California

by

Richard L. Reynolds 1, Joseph G. Rosenbaum^, Nilah Mazza*, 

Willie Rivers 1 and Fred Luiszer2

Open-File Report 98-132 (part 6)

This report is preliminary and has not been reviewed for conformity with U.S. Geological Survey 

editorial standards (or with the North American Stratigraphic Code). Any use of trade, product, or 

firm names is for descriptive purposes only and does not imply endorsement by the U.S. 

Government

*U.S. Geological Survey, Denver, Colorado, 80225 

2University of Colorado, Boulder, Colorado, 80309

1998

/Ofi
INTRODUCTION

This report presents data and describes methods of sediment magnetic and geochemical 

measurements on dominantly silty clay lacustrine lake sediments recovered in a portion of a 323-mdeep core (OL-92) from Owens Lake, California. The core, drilled in 1992 near the depositional 

center of the basin, records climatic cycles of mainly precipitation, reflected by alternating closed 

and overflowing lake conditions, over the past 800,000 years (Smith and Bischoff, 1997; Bischoff 

and others, 1997a).

This report is one in a group that lists data from a depth interval of 83 to 32 m. This 

interval corresponds to the time period between about 134 to 46 kyr (estimated by Bischoff and 

others, 1997b) and thereby encompasses marine oxygen isotope stage 5 (OIS-5, the last 

interglaciation) as well as OIS-4 (about 65 to 50 kyr, a glacial stage) and the latter part of OIS-6 

(the penultimate glaciation). For this report we also present sediment magnetic data from 32 to 18 

m, corresponding in time to about 46 to 26.4 kyr, a period that encompasses most of OIS-3.

METHODS AND RESULTS

Sampling: Samples used for magnetic susceptibility and laboratory induced 

magnetizations were taken in continuous channels, each 10 cm in length. According to the timedepth age model by Bischoff and others (1997b) for the 83 to 32 m depth interval, this 10-cm

depth span corresponds to about 170 years. The samples were dried, lightly disaggregated and

3 homogenized , and then packed into plastic cubes, each having a volume of 3.2 cm . A total of

537 samples were measured for magnetic properties and 164 samples for geochemistry.

Magnetic Susceptibility (Table 1): Magnetic susceptibility (MS) was measured using a

-7 3 susceptometer with a sensitivity better than about 4 x 10 m /kg. Samples were measured in a

0.1 mT (milliTesla) induction at a low frequency of 600 Hz (MSif) and high frequency of 6000 Hz 

(MShf). Each MS value was determined as the mean of four measurements.

Laboratory induced magnetization (Table 1): Anhysteretic remanent magnetization 

(ARM) and isothermal remanent magnetization (IRM) were measured with a high speed spinner 

magnetometer. ARM was imparted in a decreasing alternating field from a peak induction of 100 

mT and a DC bias of 0.1 mT. After ARM acquisition, IRM magnetizations were generated at room 

temperature using an impulse magnetizer. First IRM was imparted in a 1.2T induction (IRM1.2T)- 

The samples were then magnetized in the opposite direction using an induction of 0.3T (IRM0.3T)- Hard isothermal remanent magnetization (HIRM) and the S-parameter were calculated as 

follows (King and Channel, 1991):

HIRM=(IRMi.2T-IRM.o.3T)/2;

S=IRM_0.3T/IRMi.2T..

Minor-element and Trace-element Geochemistry (Table 2): Elemental abundance was 

determined on selected samples using energy-dispersive X-ray fluorescence analysis at the 

University of Colorado's Department of Geological Sciences. Contents of Ba, Ce, Cr, Cs, Cu, Fe, 

La, Mn, Mo, Nb, Ni, Rb, Sb, Sn, Sr, Ti, V, Y, Zn, and Zr were measured.

Variations in Magnetic and Chemical Properties: Depth profiles of MS and IRM/MS 

reveal strong variations in the amounts and magnetic grain size of magnetic minerals (Fig. 1). 

Preliminary petrographic analysis from a few samples indicate that the variations in magnetic 

property data arise from varying distributions of different magnetic minerals. Identified minerals 

include varieties of detrital iron and iron-titanium oxides, as well as greigite. The Fe and Fe-Ti
oxides occur in a number of different textures and associations, from which their different origins 

can be interpreted. For example, in one sample (75.3-75.4 m), the magnetic mineral population is 

dominated by poorly sorted, silt-sized angular grains of optically homogeneous magnetite, 

apparently derived from granitic rocks. In another interval (comprising two channel samples at 

64.8-64.9 m and 65.0-65.1 m), the magnetic signal appears to be dominated by very small oxides 

(<1 |Lim) that occur in large (coarse silt) volcanic rock fragments; greigite is also present in this 

sample. Petrographic observations of varying distribution of different detrital Fe-Ti oxide minerals 

are consistent with strong variations in Zr/Ti that imply changes in provenance. Moreover, sulfidic 

diagenesis has in some intervals produced pyrite that formed at the expense of detrital magnetite. 

These cursory observations indicate that changes in erosional, depositional, and diagenetic 

processes, along with intermittent shifts in provenance, have produced changes in the magnetic 

mineralogy. Magnetic property variations are also related to the effects of dilution by chemically 

precipitated minerals.

Evidence for glacial activity in the Sierra Nevada might be found in magnetic properties of 

Owens Lake sediment (see Benson and others, 1996). For this reason, our preliminary 

petrographic analysis focused on a few intervals that might have diagnostic magnetic and chemical 

records of glacial sediment or water chemistry. Indicators of water chemistry (reflecting open, or 

closed to intermediate, hydrologic conditions) might be found in the absence, or presence and 

types, of iron sulfide minerals. As an example using the interval between 83 and 76.2 m, the high 

content of ferrimagnetic minerals (high MS), with coarse magnetic grain size (low values of 

IRM/MS), results from input of detrital magnetite from Sierran granitic rocks, apparently 

weathered mechanically by glaciers and carried in rivers to the lake as glacial flour. This interval is 

characterized chemically by high Ti and Fe contents and low Zr/Ti values (Fig. 1). In contrast, the 

combination of moderate to high MS and small magnetic grain size (high values of IRM/MS and 

ARM/MS) reflects either very fine grained detrital magnetite or diagenetic greigite (FesS^ magnetic 

sulfide; Reynolds and others, 1994). Such intervals that are dominated by abundant greigite, as 

confirmed petrographically, are indicated in the dark shaded pattern in figure 1. Other zones of 

abundant greigite may be present but have not been examined. Examined intervals that do not 

contain greigite, or in which greigite is present in minor amounts with little contribution to the 

magnetic signal, are shown in a lighter shaded pattern.

The presence of greigite in OIS-3 equivalent sediments from a different core at Owens Lake 

was inferred by Benson and others (1996). They considered the greigite to indicate the intensity of 

glacial erosion, assuming that the greigite formed as a post-depositional replacement of glacially 

derived magnetite. Benson and others (1996) did not confirm the identity of either mineral or such 

origins. Although this hypothesis may be valid, other possibilities should be examined. One 

possibility is that greigite formed in this lake during conditions intermediate between closed and 

stagnant vis-a-vis open and through flowing. Such greigite might then represent conditions of 

increased freshness in an otherwise saline environment, or it might represent conditions of 

increased salinity in an otherwise fresh, open setting. The production of greigite at the boundary 

zone (about 75 m) between OIS-6 and OIS-5 sediments might reflect the transition from fresh to 

saline waters. Saline conditions would promote pyrite formation, given sufficient sulfur, organic 

matter, and iron in the system. A magnetic-mineral separate from two samples encompassing 

72.15-72.35 m contains pyrite, some of which has replaced large detrital magnetite grains, and 

lacks greigite. Another example comes from the occurrence of greigite that yields the high MS and 

high IRM/MS values near 46.8 m depth. Samples below and above this depth (about 55.9 m and 

41.9 m) lack greigite but contain pyrite, some of which has replaced detrital Fe-Ti oxide minerals.

In contrast to the greigite-bearing interval near 46.8 m, the greigite occurrence centered at 

36.65 m is different in some important ways. First, it is within sediment that is enriched in Fe and 

Ti relative to most of the underlying OIS-5 deposits. Second, samples below (38.8-39.2 m) and 

above (33.1-33.4 m) the greigite-bearing interval lack pyrite and contain large, rounded to 

subrounded, detrital Fe-Ti oxides, including magnetic ilmenite varieties. Third, the greigitebearing sample contains sparse, small (fine silt size), angular particles of ilmenite that might 

represent glacial flour. These very preliminary observations suggest that this greigite occurrence is 

bounded by sediments representing relatively more open conditions, perhaps preceding and
postdating an influx of minor amounts of glacial flour under conditions that also promoted greigite 

formation. Whereas iron is certainly not a limiting factor in the production of iron sulfide minerals 

in these OIS-5 sediments, perhaps the surface area provided by fine-grained iron oxides increased 

iron availability.

REFERENCES

Benson, L.V., Burdett, J.W., Kashgarian, M., Lund, S.P., Phillips, P.M., and Rye, R.O., 

1996, Climatic and hydrologic oscillations in the Owens Lake basin and adjacent Sierra Nevada, 

California: Science, v. 274, p. 746-749.

Bischoff, J.L., Fitts, J.P., and Fitzpatrick, J.A., 1997a, Responses of sediment geochemistry to 

climate change in Owens Lake sediment: An 800-ky record of saline/fresh cycles, In Smith, 

G.I. and Bischoff, J.L., eds. "An 800,000-year geologic and climatic record from Owens 

Lake, California: Core OL-92": Geological Society of America Special Paper 317, p. 37-47.

Bischoff, J.L., Stafford, T.W., and Rubin, M., 1997b, A time-depth scale for Owens Lake 

sediments of core OL-92: Radiocarbon dates and constant mass-accumulation rate, In Smith, 

G.I. and Bischoff, J.L., eds. An 800,000-year geologic and climatic record from Owens Lake, 

California: Core OL-92: Geological Society of America Special Paper 317, p. 91-98.

King, J.W., and Channel, J.E.T., 1991, Sedimentary magnetism, environmental magnetism, and 

magnetostratigraphy: Reviews of Geophysics, Supplement, p. 358-370.

Reynolds, R.L., Tuttle, M.L., Rice, C, Karachewski, J., and Sherman, D., 1994, Magnetization 

and geochemistry of greigite-bearing Cretaceous strata, North Slope, Alaska: American Journal 

of Science, v. 294, p. 485-528.

Smith, G.I. and Bischoff, J.L., 1997, Core OL-92 from Owens Lake: Project rationale, geologic 

setting, drilling procedures, and summary, In Smith, G.I. and Bischoff, J.L., eds. An 

800,000-year geologic and climatic record from Owens Lake, California: Core OL-92: 

Geological Society of America Special Paper 317, p. 1-8.
TABLE 1. Sediment Magnetic Data

Sample number.: A unique sample number assigned to samples that are placed into plastic cubes 

for magnetic mineral studies.

Depth (m): Depth of sample in centimeters from top of core. The depth shown is the midpoint of 

a channel sample that encompasses a 10-cm depth interval.

MSLF: Low-frequency magnetic susceptibility in m3/kg.

fy

ARM: Anhysteretic remanent magnetization in Am /kg.

IRM 1.2T: Isothermal remanent magnetization imparted by a 1.2 Tesla induction at room 

temperature. Expressed in Am2/kg.

IRM 0.3T: Isothermal remanent magnetization imparted by a -0.3 Tesla induction at room 

temperature, following the acquisition and measurement of IRM at 1.2 T. Expressed in Air

FflRM: Hard isothermal remanent magnetization: HIRM is calculated as: 

(IRMi.2T-IRM_o 3T)/2 and expressed in Am2/kg.

S: (S Ratio) calculated as: IRM.0.3T^RMi.2T-
Sample No.

18.05

18.15

18.25

18.35

18.45

18.55

18.65

18.75

18.85

18.95

19.025

20.25

20.35

20.45

20.55

20.65

20.75

20.85

20.95

21.05

21.15

21.25

21.35

21.45

21.75

21.85

21.95

22.05

22.15

22.25

22.35

22.45

22.55

22.65

22.75

22.85

22.95

23.05

23.15

23.25

23.35

23.45

23.55

23.65

23.75

23.85

23.95

24.05

24.15

24.25

24.35

Depth

(m)

18.05

18.15

18.25

18.35

18.45

18.55

18.65

18.75

18.85

18.95

19.025

20.25

20.35

20.45

20.55

20.65

20.75

20.85

20.95

21.05

21.15

21.25

21.35

21.45

21.75

21.85

21.95

22.05

22.15

22.25

22.35

22.45

22.55

22.65

22.75

22.85

22.95

23.05

23.15

23.25

23.35

23.45

23.55

23.65

23.75

23.85

23.95

24.05

24.15

24.25

24.35

MSLF

(m3/kg)

2.03E-07

2.10E-07

2.01 E-07

1.57E-07

1.06E-07

1.08E-07

8.73E-08

8.13E-08

7.29E-08

5.94E-08

4.07E-08

5.97E-08

3.65E-08

4.72E-08

6.50E-08

4.61 E-08

3.79E-08

3.99E-08

1.09E-08

1.09E-08

4.10E-08

2.31 E-08

1.95E-08

4.78E-08

5.78E-08

2.57E-08

4.52E-08

1.14E-08

-1.22E-08

1.72E-08

3.00E-08

2.11 E-08

4.25E-08

3.51 E-08

4.51 E-08

5.79E-08

4.90E-08

7.74E-08

1.30E-07

5.33E-08

1.03E-07

1.72E-08

4.91 E-08

5.04E-08

3.99E-08

5.93E-08

3.04E-08

3.57E-08

3.49E-08

6.58E-08

6.02E-08

ARM

(Am2/kg)

2.94E-05

2.52E-05

2.16E-05

2.61 E-05

2.31 E-05

2.43E-05

2.27E-05

1.99E-05

1.87E-05

2.19E-05

2.15E-05

1.99E-05

2.43E-05

2.18E-05

2.04E-05

2.56E-05

2.31 E-05

2.25E-05

2.01 E-05

2.29E-05

1.66E-05

1.98E-05

1.96E-05

1.92E-05

2.00E-05

2.59E-05

2.31 E-05

2.69E-05

2.75E-05

2.29E-05

2.12E-05

2.16E-05

2.06E-05

2.25E-05

2.10E-05

2.07E-05

2.21 E-05

4.02E-05

1.15E-04

2.88E-05

2.46E-05

2.42E-05

2.50E-05

2.23E-05

2.28E-05

2.60E-05

2.90E-05

2.76E-05

2.56E-05

2.71 E-05

2.25E-05

IRM1.2T

(Am2/kg)

8.03E-04

6.58E-04

5.74E-04

4.70E-04

4.02E-04

4.38E-04

4.44E-04

3.86E-04

3.43E-04

4.12E-04

4.08E-04

3.43E-04

4.10E-04

3.82E-04

3.59E-04

4.06E-04

3.41 E-04

3.57E-04

3.46E-04

3.81 E-04

2.92E-04

3.89E-04

3.81 E-04

3.20E-04

4.12E-04

4.22E-04

3.20E-04

4.23E-04

4.29E-04

3.48E-04

3.45E-04

3.33E-04

3. 31 E-04

3.49E-04

3.51 E-04

3.23E-04

3.60E-04

1.30E-03

5.38E-03

4.73E-04

4.49E-04

4.45E-04

4.62E-04

3.64E-04

3.47E-04

3.83E-04

4.02E-04

4.14E-04

3.83E-04

3.69E-04

3.34E-04

IRM 0.3T

(Am2/kg)

7.48E-04

6.00E-04

5.26E-04

4.18E-04

3.56E-04

3.91 E-04

3.99E-04

3.41 E-04

3.02E-04

3.66E-04

3.70E-04

2.97E-04

3.64E-04

3.38E-04

3.10E-04

3.61 E-04

3.08E-04

3.24E-04

3.16E-04

3.45E-04

2.60E-04

3.60E-04

3.44E-04

2.86E-04

3.74E-04

3.83E-04

2.81 E-04

3.89E-04

3.98E-04

3.12E-04

3.07E-04

3.01 E-04

2.92E-04

3.10E-04

3.11 E-04

2.75E-04

3.06E-04

1.07E-03

4.60E-03

4.23E-04

3.99E-04

3.75E-04

4.08E-04

3.31 E-04

3.14E-04

3.43E-04

3.70E-04

3.79E-04

3.47E-04

3.28E-04

2.99E-04

HIRM

(Am2/kg)

2.73E-05

2.89E-05

2.42E-05

2.60E-05

2.32E-05

2.33E-05

2.22E-05

2.27E-05

2.03E-05

2.27E-05

1.92E-05

2.29E-05

2.32E-05

2.20E-05

2.45E-05

2.26E-05

1.66E-05

1.65E-05

1.51 E-05

1.81 E-05

1.61 E-05

1.43E-05

1.86E-05

1.74E-05

1.93E-05

1.96E-05

1.96E-05

1.69E-05

1.59E-05

1.76E-05

1.89E-05

1.61 E-05

1.99E-05

1.96E-05

2.01 E-05

2.36E-05

2.72E-05

1.15E-04

3.88E-04

2.54E-05

2.52E-05

3.50E-05

2.70E-05

1.68 E-05

1.65E-05

1.96E-05

1.62E-05

1.77E-05

1.82E-05

2.06E-05

1.77E-05

S

0.93

0.91

0.92

0.89

0.88

0.89

0.90

0.88

0.88

0.89

0.91

0.87

0.89

0.88

0.86

0.89

0.90

0.91

0.91

0.91

0.89

0.93

0.90

0.89

0.91

0.91

0.88

0.92

0.93

0.90

0.89

0.90

0.88

0.89

0.89

0.85

0.85

0.82

0.86

0.89

0.89

0.84

0.88

0.91

0.90

0.90

0.92

0.91

0.91

0.89

0.89
Sample No.

24.45

24.55

24.65

24.75

24.85

24.95

25.05

25.15

25.25

25.35

25.45

25.55

25.65

25.75

25.85

25.95

26.05

26.15

26.25

26.35

26.45

26.55

26.65

26.75

26.85

26.95

27.05

27.15

27.25

27.35

27.45

27.55

27.65

27.75

30.9

31

31.1

31.2

31.3

31.4

31.5

31.6

31.7

31.8

31.9

32

1

2

3

4

5

Depth

(m)

24.45

24.55

24.65

24.75

24.85

24.95

25.05

25.15

25.25

25.35

25.45

25.55

25.65

25.75

25.85

25.95

26.05

26.15

26.25

26.35

26.45

26.55

26.65

26.75

26.85

26.95

27.05

27.15

27.25

27.35

27.45

27.55

27.65

27.75

30.9

31

31.1

31.2

31.3

31.4

31.5

31.6

31.7

31.8

31.9

32

32.05

32.15

32.25

32.35

32.45

MSLF

(m3/kg)

7.65E-08

8.26E-08

7.88E-08

7.20E-08

1.08E-07

7.76E-08

8.31 E-08

6.03E-08

8.45E-08

7.85E-08

6.60E-08

8.56E-08

9.82E-08

1.22E-07

8.37E-08

7.51 E-08

9.66E-08

1.16E-07

9.78E-08

6.30E-08

8.70E-08

7.21 E-08

6.40E-08

5.84E-08

6.88E-08

6.48E-08

6.72E-08

7.82E-08

8.46E-08

8.18E-08

9.27E-08

1.25E-07

1.46E-07

1.82E-07

1.37E-07

1.79E-07

1.73E-07

8.34E-08

1.23E-07

1.22E-07

1.62E-07

1.73E-07

1.61E-07

1.51E-07

1.66E-07

1.29E-07

1.89E-07

2.23E-07

1.23E-07

1.06E-07

9.79E-08

ARM

(Am2/kg)

2.58E-05

2.56E-05

2.67E-05

2.21 E-05

2.33E-05

2.22E-05

2.35E-05

2.23E-05

2.09E-05

2.56E-05

2.41 E-05

2.69E-05

2.41 E-05

3.51 E-05

3.24E-05

3.14E-05

2.88E-05

3.32E-05

2.43E-05

2.33E-05

2JOE-05

2.24E-05

2.47E-05

3.13E-05

2.92E-05

3.10E-05

2.83E-05

2.40E-05

2.27E-05

2.65E-05

2.38E-05

2.47E-05

2.63E-05

2.66E-05

2.87E-05

2.75E-05

2.51 E-05

2.32E-05

2.63E-05

3.04E-05

3.34E-05

3.78E-05

3.49E-05

3.40E-05

3.29E-05

2.89E-05

6.49E-05

5.94E-05

4.35E-05

4.15E-05

3.90E-05

IRM1.2T

(Am2/kg)

3.93E-04

3.91 E-04

4.71 E-04

3.42E-04

5.24E-04

3.71 E-04

3.78E-04

3.82E-04

3.38E-04

4.15E-04

3.45E-04

4.42E-04

4.50E-04

7.84E-04

5.00E-04

4.57E-04

4.86E-04

5.98E-04

3.97E-04

3.68E-04

4.40E-04

3.78E-04

3.93E-04

4.86E-04

4.76E-04

5.23E-04

4.80E-04

4.02E-04

3.98E-04

4.92E-04

4.25E-04

4.39E-04

5.34E-04

6.42E-04

9.85E-04

7.03E-04

1.07E-03

4.55E-04

5.63E-04

6.47E-04

7.90E-04

9.80E-04

8.43E-04

8.31 E-04

8.23E-04

6.74E-04

2.01 E-03

2.25E-03

1.12E-03

9.92E-04

9.62E-04

IRM 0.3T

(Am2/kg)

3.52E-04

3.53E-04

4.27E-04

3.06E-04

4.78E-04

3.34E-04

3.36E-04

3.49E-04

3.04E-04

3.79E-04

3.10E-04

4.00E-04

4.07E-04

7.32E-04

4.52E-04

4.10E-04

4.32E-04

5.46E-04

3.52E-04

3.33E-04

3.98E-04

3.45E-04

3.49E-04

4.39E-04

4.33E-04

4.74E-04

4.36E-04

3.60E-04

3.53E-04

4.37E-04

3.77E-04

3.93E-04

4.83E-04

5.93E-04

9.46E-04

6.50E-04

1.02E-03

4.09E-04

5.07E-04

5.77E-04

7.12E-04

8.81 E-04

7.56E-04

7.43E-04

7.41 E-04

6.03E-04

1.82E-03

2.07E-03

9.80E-04

8.71 E-04

8.44E-04

HIRM

(Am2/kg)

2.03E-05

1.89E-05

2.17E-05

1.83E-05

2.27E-05

1.85E-05

2.12E-05

1.63E-05

1.69E-05

1.77E-05

1.74E-05

2.09E-05

2.15E-05

2.59E-05

2.41 E-05

2.31 E-05

2.69E-05

2.64E-05

2.21 E-05

1.79E-05

2.10E-05

1.67E-05

2.22E-05

2.35E-05

2.14E-05

2.46E-05

2.19E-05

2.10E-05

2.21 E-05

2.75E-05

2.38E-05

2.34E-05

2.54E-05

2.45E-05

1.95E-05

2.67E-05

2.38E-05

2.30E-05

2.79.E-05

3.50E-05

3.88E-05

4.95E-05

4.35E-05

4.43E-05

4.14E-05

3.58E-05

9.16E-05

8.89E-05

6.99E-05

6.04E-05

5.92E-05

S

0.90

0.90

0.91

0.89

0.91

0.90

0.89

0.91

0.90

0.91

0.90

0.91

0.90

0.93

0.90

0.90

0.89

0.91

0.89

0.90

0.90

0.91

0.89

0.90

0.91

0.91

0.91

0.90

0.89

0.89

0.89

0.89

0.90

0.92

0.96

0.92

0.96

0.90

0.90

0.89

0.90

0.90

0.90

0.89

0.90

0.89

0.91

0.92

0.88

0.88

0.88
Sample No.

6

7

8

9

10

11

12

13

14

15

16

17

18

19

20

21

22

23

24

25

26

27

28

29

30

31

32

33

34

35

36

37

38

39

40

41

42

43

44

45

46

47

48

49

50

51

52

53

54

55

56

Depth

(m)

32.55

32.65

32.75

32.85

32.95

33.05

33.15

33.25

33.35

33.45

33.55

33.65

33.75

33.85

34.75

34.85

34.95

35.05

35.15

35.25

35.35

35.45

35.55

35.65

35.75

35.85

35.95

36.05

36.15

36.25

36.35

36.45

36.55

36.65

36.75

36.85

36.95

37.95

38.05

38.15

38.25

38.35

38.45

38.55

38.65

38.75

38.85

38.95

39.05

39.15

39.25

MSLF

(m3/kg)

8.72E-08

8.48E-08

8.10E-08

7.73E-08

7.80E-08

9.43E-08

1.35E-07

1.79E-07

2.14E-07

1.79E-07

1.96E-07

2.23E-07

2.02E-07

2.30E-07

2.74E-07

2.61E-07

2.82E-07

2J3E-07

2.50E-07

2.82E-07

2.33E-07

2.61 E-07

2.58E-07

2.24E-07

2.91 E-07

2.44E-07

2.20E-07

2.34E-07

2.00E-07

1.71 E-07

1.76E-07

2.03E-07

3.23E-07

2.73E-07

1 .89E-07

2.50E-07

1.82E-07

1.02E-07

9.90E-08

8.53E-08

8.67E-08

7.98E-08

8.09E-08

7.57E-08

8.09E-08

9.45E-08

9.32E-08

8.55E-08

8.98E-08

8.87E-08

8.60E-08

ARM

(Am2/kg)

3.28E-05

8.76E-07

3.55E-05

4.37E-05

3.94E-05

3.93E-05

5.27E-05

6.67E-05

6.62E-05

7.23E-05

7.29E-05

8.12E-05

8.18E-05

9.26E-05

1.03E-04

1.02E-04

1.15E-04

1.20E-04

9.58E-05

1.15E-04

1.05E-04

1.02E-04

1 .05E-04

1.09E-04

1.39E-04

1 .48E-04

1.81E-04

2.37E-04

2.49E-04

2.00E-04

2.29E-04

2J6E-04

5.54E-04

4.71 E-04

2.81 E-04

4.27E-04

2.45E-04

7.12E-05

7.06E-05

5.58E-05

3.92E-05

3.46E-05

3.45E-05

3.31 E-05

3.82E-05

4.26E-05

3.47E-05

3.03E-05

2.72E-05

3.07E-05

2.81 E-05

IRM1.2T

(Am2/kg)

8.10E-04

7.80E-04

6.91 E-04

7.49E-04

7.29E-04

7.19E-04

1.09E-03

1.51E-03

1.58E-03

1.76E-03

1.80E-03

2.19E-03

2.15E-03

2.61 E-03

3.60E-03

3.77E-03

3.84E-03

5.68E-03

2.89E-03

3.84E-03

4.30E-03

4.25E-03

4.54E-03

4.60E-03

7.13E-03

9.35E-03

1 .40E-02

2.50E-02

2.44E-02

1 .78E-02

1.94E-02

2.67E-02

6.85E-02

6.08E-02

2.80E-02

4.50E-02

2.37E-02

3.50E-03

3.56E-03

2.41 E-03

1.17E-03

7.68E-04

6.67E-04

7.39E-04

9.63E-04

1.35E-03

1.23E-03

9.43E-04

9.43E-04

9.44E-04

6.34E-04

IRM 0.3T

(Am2/kg)

7.06E-04

6.80E-04

6.08E-04

6.64E-04

6.40E-04

6.30E-04

9.56E-04

1.31 E-03

1.42E-03

1.58E-03

1.63E-03

2.01 E-03

1.98E-03

2.41 E-03

3.39E-03

3.56E-03

3.58E-03

5.44E-03

2.69E-03

3.61 E-03

4.09E-03

4.06E-03

4.33E-03

4.38E-03

6.87E-03

9.12E-03

1 .38E-02

2.49E-02

2.41 E-02

1.76E-02

1.93E-02

2.66E-02

6.82E-02

6.09E-02

2.78E-02

4.48E-02

2.35E-02

3.42E-03

3.45E-03

2.33E-03

1.10E-03

7.09E-04

6.09E-04

6.86E-04

8.89E-04

1.35E-03

1.16E-03

9.43E-04

8.73E-04

8.66E-04

5.73E-04

HIRM

(Am2/kg)

5.20E-05

4.99E-05

4.17E-05

4.28E-05

4.47E-05

4.48E-05

6.67E-05

9.57E-05

8.02E-05

8.79E-C5

8.72E-05

8.64E-05

8.53E-05

1.01 E-04

1.06E-04

1.04E-04

1.31 E-04

1.20E-04

1.03E-04

1. 14E-04

1.07E-04

9.68E-05

1.08E-04

1.10E-04

1.32E-04

1.14E-04

1.23E-04

3.94E-05

1 .25E-04

8.01 E-05

6.38E-05

5.10E-05

1 .54E-04

-2.12E-05

8.02E-05

7.19E-05

8.78E-05

4.10E-05

5.68.E-05

4.39E-05

3.63E-05

2.98E-05

2.90E-05

2.65E-05

3.68E-05

-2.53E-06

3.56E-05

-2.18E-07

3.50E-05

3.89E-05

3.06E-05

S

0.87

0.87

0.88

0.89

0.88

0.88

0.88

0.87

0.90

0.90

0.90

0.92

0.92

0.92

0.94

0.94

0.93

0.96

0.93

0.94

0.95

0.95

0.95

0.95

0.96

0.98

0.98

1.00

0.99

0.99

0.99

1.00

1.00

1.00

0.99

1.00

0.99

0.98

0.97

0.96

0.94

0.92

0.91

0.93

0.92

1.00

0.94

1.00

0.93

0.92

0.90
Sample No.

57

58

59

60

61

62

63

64

65

66

67

68

69

70

71

72

73

74

75

76

77

78

79

80

81

82

83

84

85

86

87

88

89

90

91

92

93

94

95

96

97

98

99

100

101

102

103

104

105

106

107

Depth

(m)

39.35

39.45

39.55

39.65

39.75

39.9

40.25

40.35

40.45

40.55

40.65

40.75

40.85

40.95

41.03

41.085

41.155

41.25

41.35

41.45

41.55

41.65

41.75

41.85

41.95

42.05

42.15

42.25

42.35

42.45

42.55

42.65

42.75

42.85

43.15

43.25

43.35

43.45

43.55

43.65

43.75

43.85

43.95

44.05

44.15

44.25

44.35

44.45

44.55

44.65

44.75

MSLF

(m3/kg)

9.29E-08

8.86E-08

7.81 E-08

8.20E-08

8.33E-07

1.00E-07

1.02E-07

9.78E-08

8.99E-08

6.06E-08

9.15E-08

7.28E-08

5.60E-08

5.92E-08

5.66E-08

9.77E-08

6.13E-08

2.01 E-07

1.12E-07

1.10E-07

6.41 E-08

7.24E-08

7.12E-08

6.52E-08

7.19E-08

6.79E-08

6.15E-08

6.27E-08

6.32E-08

6.32E-08

6.20E-08

6.21 E-08

5.88E-08

6.51 E-08

7.49E-08

6.81 E-08

6.46E-08

7.05E-08

6.44E-08

6.81 E-08

4.24E-08

5.04E-08

5.98E-08

6.36E-08

5.28E-08

4.54E-08

4.60E-08

5.15E-08

4.82E-08

5.22E-08

6.21 E-08

ARM

(Am2/kg)

2.82E-05

5.68E-05

9.33E-05

8.73E-05

9.49E-04

4.52E-05

4.71 E-05

5.64E-05

7.83E-05

5.36E-05

8.76E-05

6.57E-05

5.89E-05

6.07E-05

6.95E-05

1.19E-04

7.59E-05

2.36E-04

1.70E-04

1.40E-04

3.99E-05

4.65E-05

4.67E-05

4.36E-05

5.60E-05

4.92E-05

3.51 E-05

4.39E-05

3.11 E-05

2.92E-05

2.55E-05

2.02E-05

2.35E-05

2.69E-05

5.70E-05

3.62E-05

4.06E-05

5.30E-05

4.49E-05

6.31 E-05

2.98E-05

4.50E-05

6.33E-05

7.32E-05

4.39E-05

5.23E-05

5.85E-05

6.33E-05

4.49E-05

4.42E-05

5.83E-05

IRM1.2T

(Am2/kg)

7.12E-04

2.82E-03

2.99E-03

2.97E-03

4.77E-02

1.63E-03

1.47E-03

1.31E-03

2.38E-03

1.17E-03

2.75E-03

1.74E-03

1.23E-03

1.15E-03

1.11E-03

2.64E-03

1.26E-03

9.26E-03

4.80E-03

7.99E-03

6.99E-04

9.92E-04

1.25E-03

9.70E-04

1.30E-03

1.43E-03

8.69E-04

1.11E-03

8.38E-04

8.73E-04

6.47E-04

6.32E-04

5.72E-04

7.59E-04

1.26E-03

9.45E-04

7.79E-04

1.13E-03

9.91 E-04

1.30E-03

4.64E-04

6.92E-04

1.36E-03

1.79E-03

5.90E-04

6.98E-04

7.81 E-04

8.83E-04

7.11 E-04

7.75E-04

1.01E-03

IRM 0.3T

(Am2/kg)

6.48E-04

2.74E-03

2.72E-03

2.58E-03

4.74E-02

1.46E-03

1.32E-03

1.13E-03

2.04E-03

9.73E-04

2.38E-03

1.47E-03

1.03E-03

1.15E-03

9.60E-04

2.29E-03

1.12E-03

7.21 E-03

4.28E-03

6.20E-03

6.33E-04

9.06E-04

1.14E-03

8.85E-04

1.14E-03

1.17E-03

7.22E-04

9.03E-04

7.12E-04

7.37E-04

5.77E-04

6.31 E-04

5.12E-04

6.73E-04

1.11 E-03

8.57E-04

6.83E-04

1 .02E-03

9.91 E-04

1.11 E-03

4.21 E-04

6.36E-04

1.20E-03

1.54E-03

5.50E-04

6.56E-04

7.44E-04

8.39E-04

6.68E-04

7.29E-04

9.61 E-04

HIRM

(Am2/kg)

3.21 E-05

3.98E-05

1.35E-04

1.96E-04

1.80E-04

8.44E-05

7.55E-05

9.10E-05

1.71 E-04

9.93E-05

1.86E-04

1 .33E-04

9.68E-05

9.82E-07

7.40E-05

1.76E-04

7.15E-05

1.03E-03

2.63E-04

8.96E-04

3.28E-05

4.32E-05

5.38E-05

4.24E-05

8.12E-05

1.26E-04

7.35E-05

1.03E-04

6.32E-05

6.80E-05

3.51 E-05

6.35E-07

3.01 E-05

4.32E-05

7.55E-05

4.39E-05

4.83E-05

5.90E-05

1.93.E-07

9.27E-05

2.17E-05

2.82E-05

8.08E-05

1.23E-04

2.02E-05

2.07E-05

1.86E-05

2.24E-05

2.18E-05

2.31 E-05

2.53E-05

S

0.91

0.97

0.91

0.87

0.99

0.90

0.90

0.86

0.86

0.83

0.86

0.85

0.84

1.00

0.87

0.87

0.89

0.78

0.89

0.78

0.91

0.91

0.91

0.91

0.88

0.82

0.83

0.81

0.85

0.84

0.89

1.00

0.89

0.89

0.88

0.91

0.88

0.90

1.00

0.86

0.91

0.92

0.88

0.86

0.93

0.94

0.95

0.95

0.94

0.94

0.95
Sample No.

108

109

110

111

112

113

114

115

116

117

118

119

120

121

122

123

124

125

126

127

128

129

130

131

132

133

134

135

136

137

138

139

140

141

142

143

147

148

149

150

151

152

153

154

155

156

157

158

159

160

161

Depth

(m)

44.85

44.95

45.05

45.15

45.25

45.35

45.45

45.55

45.65

45.75

45.85

45.95

46.43

46.55

46.65

46.75

46.85

46.95

47.05

47.15

47.25

47.35

47.45

47.55

47.65

47.75

47.85

47.95

49.325

49.45

49.55

49.65

49.75

49.85

49.95

50.05

50.45

52.25

52.35

52.45

52.55

52.65

52.75

52.85

52.95

53.05

53.15

53.25

53.35

53.45

53.55

MSLF

(m3/kg)

6.56E-08

9.68E-08

1.00E-07

9.45E-08

7.80E-08

8.43E-08

9.61E-08

8.84E-08

1.03E-07

1.31E-07

1.29E-07

1.03E-07

1.18E-07

1.04E-07

1.19E-07

1.36E-07

1.30E-07

1.54E-07

1.18E-07

9.63E-08

1.00E-07

7.88E-08

1.01E-07

1.08E-07

7.09E-08

6.95E-08

6.91 E-08

6.34E-08

5.00E-08

5.20E-08

6.29E-08

7.48E-08

6.79E-08

7.17E-08

5.60E-08

6.80E-08

6.89E-08

8.03E-08

8.04E-08

4.17E-07

6.54E-08

6.79E-08

5.23E-08

6.75E-08

7.15E-08

7.75E-08

7.10E-08

7.89E-08

7.55E-08

6.54E-08

6.63E-08

ARM

(Am2/kg)

7.23E-05

1.49E-04

1.72E-04

1.29E-04

8.83E-05

9.31 E-05

1.16E-04

9.39E-05

1.30E-04

2.19E-04

2.17E-04

1.48E-04

1.63E-04

1.31E-04

1.51E-04

1.98E-04

1.91E-04

1.97E-04

1.07E-04

1.11E-04

1.24E-04

8.73E-05

1.28E-04

1.64E-04

5.06E-05

4.77E-05

4.25E-05

5.30E-05

3.17E-05

3.59E-05

3.98E-05

4.66E-05

3.66E-05

4.15E-05

3.55E-05

4.24E-05

4.11 E-05

2.79E-05

3.43E-05

2.13E-04

3.76E-05

3.27E-05

3.13E-05

4.12E-05

4.07E-05

3.05E-05

4.20E-05

3.67E-05

3.98E-05

4.85E-05

3.87E-05

IRM1.2T

(Am2/kg)

1.28E-03

2.43E-03

3.02E-03

2.51 E-03

1.65E-03

1.99E-03

2.74E-03

2.40E-03

3.23E-03

4.32E-03

4.04E-03

3.05E-03

3.62E-03

3.34E-03

5.05E-03

5.84E-03

5.45E-03

5.36E-03

4.10E-03

4.11 E-03

3.81 E-03

2.69E-03

4.42E-03

5.10E-03

9.75E-04

9.11E-04

8.47E-04

1.32E-03

6.67E-04

7.45E-04

8.39E-04

1.00E-03

8.17E-04

8.66E-04

6.50E-04

8.93E-04

1.01 E-03

5.63E-04

8.45E-04

7.76E-03

8.57E-04

6.34E-04

7.43E-04

8.49E-04

8.97E-04

6.69E-04

8.03E-04

7.19E-04

7.21 E-04

9.88E-04

7.71 E-04

IRM 0.3T

(Am2/kg)

1.22E-03

2.32E-03

2.84E-03

2.32E-03

1.60E-03

1.94E-03

2.69E-03

2.36E-03

3.19E-03

4.25E-03

3.98E-03 -

3.01 E-03

3.56E-03

3.27E-03

5.00E-03

5.76E-03

5.39E-03

5.28E-03

4.05E-03

4.04E-03

3.74E-03

2.64E-03

4.33E-03

5.04E-03

8.79E-04

8.34E-04

7.73E-04

1.17E-03

5.96E-04

6.68E-04

7.61 E-04

9.21 E-04

7.42E-04

7.90E-04

5.87E-04

7.93E-04

9.23E-04

5.18E-04

7.78E-04

7.07E-03

7.81 E-04

5.69E-04

6.92E-04

7.62E-04

7.96E-04

5.93E-04

7.23E-04

6.48E-04

6.46E-04

8.78E-04

6.91 E-04

HIRM

(Am2/kg)

2.93E-05

5.53E-05

9.02E-05

9.53E-05

2.35E-05

2.43E-05

2.71 E-05

2.04E-05

1.95E-05

3.78E-05

2.84E-05

2.34E-05

3.12E-05

3.65E-05

2.73E-05

4.12E-05

3.18E-05

3.86E-05

2.66E-05

3.53E-05

3.56E-05

2.57E-05

4.49E-05

3.02E-05

4.81 E-05

3.89E-05

3.70E-05

7.93E-05

3.55E-05

3.86E-05

3.93E-05

4.18E-05

3.72E-05

3.82E-05

3.15E-05

4.97E-05

4.43E-05

2.22E-05

3.36E-05

3.43E-04

3.80E-05

3.25E-05

2.55E-05

4.34E-05

5.02E-05

3.84E-05

4.00E-05

3.56E-05

3.74E-05

5.50E-05

3.96E-05

S

0.95

0.95

0.94

0.92

0.97

0.98

0.98

0.98

0.99

0.98

0.99

0.98

0.98

0.98

0.99

0.99

0.99

0.99

0.99

0.98

0.98

0.98

0.98

0.99

0.90

0.91

0.91

0.88

0.89

0.90

0.91

0.92

0.91

0.91

0.90

0.89

0.91

0.92

0.92

0.91

0.91

0.90

0.93

0.90

0.89

0.89

0.90

0.90

0.90

0.89

0.90
nple No.

162

163

164

165

166

167

168

169

170

171

172

173

174

175

176

177

178

179

180

181

182

183

184

185

186

187

188

189

190

191

192

193

194

195

196

197

198

199

200

201

202

203

204

205

206

207

208

209

210

211

212

Depth

(m)

53.65

53.75

53.85

53.95

54.05

54.15

54.25

54.35

54.45

54.55

54.65

54.75

54.85

54.95

55.05

55.15

55.25

55.425

55.55

55.65

55.75

55.85

55.95

56.05

56.15

56.25

56.35

56.45

56.55

56.65

56.75

56.85

56.95

57.05

57.15

57.25

57.35

57.45

57.55

57.65

57.75

57.85

57.95

58.05

58.15

58.25

58.35

58.45

58.55

58.65

58.75

MSLF

(m3/kg)

6.92E-08

6.30E-08

6.26E-08

6.45E-08

5.93E-08

6.06E-08

6.61E-08

6.24E-08

6.02E-08

6.41 E-08

6.18E-08

6.38E-08

5.39E-08

5.85E-08

6.43E-08

4.52E-08

4.15E-08

5.28E-08

5.11 E-08

6.25E-08

6.52E-08

5.98E-08

5.88E-08

5.62E-08

6.12E-08

6.63E-08

7.50E-08

6.88E-08

6.21 E-08

6.28E-08

6.80E-08

6.44E-08

6.03E-08

6.00E-08

6.81 E-08

6.30E-08

6.65E-08

6.69E-08

5.64E-08

5.95E-08

6.11 E-08

5.39E-08

5.22E-08

6.17E-08

5.21 E-08

6.38E-08

6.09E-08

6.37E-08

6.57E-08

7.05E-08

7.14E-08

ARM

(Am2/kg)

4.13E-05

3.26E-05

3.97E-05

3.91 E-05

4.28E-05

3.73E-05

4.87E-05

4.79E-05

4.05E-05

3.66E-05

3.44E-05

5.24E-05

5.29E-05

6.07E-05

6.37E-05

4.34E-05

3.87E-05

4.41 E-05

4.05E-05

4.89E-05

5.62E-05

4.26E-05

4.22E-05

4.44E-05

4.44E-05

5.28E-05

7.32E-05

8.02E-05

8.16E-05

5.42E-05

5.55E-05

4.67E-05

4.84E-05

3.92E-05

4.42E-05

3.98E-05

3.66E-05

4.72E-05

3.62E-05

4.72E-05

4.31 E-05

7.37E-05

6.10E-05

5.20E-05

3.28E-05

4.41 E-05

4J8E-05

5.02E-05

4.11 E-05

4.67E-05

4.73E-05

IRM1.2T

(Am2/kg)

8.37E-04

7.62E-04

8.26E-04

8.47E-04

9.82E-04

7.43E-04

1.05E-03

1.10E-03

9.69E-04

1.01E-03

1.18E-03

1.00E-03

1.07E-03

1.27E-03

1.52E-03

8.29E-04

7.95E-04

7.96E-04

7.48E-04

8.85E-04

1.11E-03

8.03E-04

7.74E-04

8.09E-04

7.82E-04

9.10E-04

1.31E-03

1 .56E-03

1 .62E-03

1 .02E-03

8.66E-04

9.13E-04

9.05E-04

7.18E-04

7.72E-04

7.33E-04

6.39E-04

8.00E-04

6.57E-04

8.29E-04

7.51 E-04

1.44E-03

1.15E-03

9.38E-04

6.09E-04

7.54E-04

8.99E-04

1.17E-03

8.09E-04

2.51 E-03

1.31E-03

IRM 0.3T

(Am2/kg)

7.50E-04

6.84E-04

7.39E-04

7.53E-04

8.81 E-04

6.62E-04

9.35E-04

9.39E-04

8.53E-04

8.85E-04

9.95E-04

9.16E-04

9.78E-04

1.14E-03

1.36E-03

7.47E-04

7.24E-04

7.21 E-04

6.76E-04

8.04E-04

9.99E-04

7.24E-04

7.02E-04

7.32E-04

7.13E-04

8.27E-04

1.20E-03

1.41 E-03

1 .46E-03

9.12E-04

7.84E-04

8.38E-04

8.09E-04

6.46E-04

6.98E-04

6.61 E-04

5.77E-04

7.27E-04

5.96E-04

7.47E-04

6.88E-04

1.29E-03

1.02E-03

8.39E-04

5.49E-04

6.94E-04

8.17E-04

1.17E-03

7.27E-04

2.42E-03

1.15E-03

HIRM

(Am2/kg)

4.40E-05

3.89E-05

4.35E-05

4.72E-05

5.08E-05

4.03E-05

5.81 E-05

8.07E-05

5.77E-05

6.18E-05

9.41 E-05

4.39E-05

4.63E-05

6.83E-05

8.27E-05

4.10E-05

3.54E-05

3.76E-05

3.59E-05

4.03E-05

5.75E-05

3.98E-05

3.59E-05

3.86E-05

3.44E-05

4.16E-05

5.78E-05

7.55E-05

8.13E-05

5.38E-05

4.12E-05

3.76E-05

4.80E-05

3.62E-05

3.69E-05

3.60E-05

3.09E-05

3.65E-05

3.02.E-05

4.11 E-05

3.18E-05

7.52E-05

6.13E-05

4.97E-05

2.98E-05

3.03E-05

4.07E-05

-4.75E-08

4.11 E-05

4.23E-05

7.67E-05

S

0.90

0.90

0.89

0.89

0.90

0.89

0.89

0.85

0.88

0.88

0.84

0.91

0.91

0.89

0.89

0.90

0.91

0.91

0.90

0.91

0.90

0.90

0.91

0.90

0.91

0.91

0.91

0.90

0.90

0.89

0.90

0.92

0.89

0.90

0.90

0.90

0.90

0.91

0.91

0.90

0.92

0.90

0.89

0.89

0.90

0.92

0.91

1.00

0.90

0.97

0.88
Sample No.

213

214

215

216

217

218

219

220

221

222

223

224

225

226

227

228

229

230

231

232

233

234

235

236

237

238

239

240

241

242

243

244

245

246

247

248

249

250

251

252

253

254

255

256

257

258

259

260

261

262

263

Depth

(m)

58.85

58.95

59.05

59.15

59.25

59.35

59.45

59.55

59.65

59.75

59.85

59.95

60.05

60.15

60.25

60.35

60.45

60.55

60.65

60.75

60.85

60.95

61.05

61.15

61.25

61.35

61.45

61.55

61.65

61.75

61.85

61.95

62.05

62.15

62.25

62.35

62.45

62.63

62.53

62.95

63.05

63.15

63.25

63.35

63.45

63.55

63.65

63.75

63.85

63.95

64.05

MSLF

(m3/kg)

6.13E-08

7.08E-08

6.77E-08

6.34E-08

7.08E-08

6.56E-08

6.21 E-08

6.53E-08

6.45E-08

5.45E-08

7.13E-08

8.19E-08

1 .09E-07

1.21E-07

1.61E-07

1.16E-07

1.12E-07

1.41E-07

1.99E-07

9.70E-08

7.86E-08

7.79E-08

7.98E-08

7.51 E-08

7.39E-08

7.49E-08

8.53E-08

8.66E-08

7.94E-08

6.99E-08

7.43E-08

7.60E-08

8.07E-08

7.73E-08

7.20E-08

8.84E-08

2.54E-08

8.15E-08

6.51 E-08

7.55E-08

7.92E-08

7.20E-08

6.15E-08

6.43E-08

6.67E-08

6.53E-08

5.97E-08

5.53E-08

6.78E-08

3.78E-08

2.96E-08

ARM

(Am2/kg)

3.50E-05

5.87E-05

4.49E-05

3.35E-05

4.50E-05

3.98E-05

3.46E-05

3.80E-05

3.98E-05

3.50E-05

8.87E-05

1.16E-04

1.94E-04

2.69E-04

2.64E-04

1 .86E-04

1.49E-04

1.92E-04

2.72E-04

7.90E-05

4.11E-05

4.38E-05

5.08E-05

5.54E-05

4.66E-05

4.63E-05

6.87E-05

7.67E-05

5.12E-05

5.13E-05

3.57E-05

4.60E-05

4.91 E-05

5.31E-05

4.57E-05

5.21 E-05

1 .90E-05

5.19E-05

9.52E-05

5.00E-05

4.74E-05

5.10E-05

3.72E-05

4.17E-05

4.17E-05

4.24E-05

4.11 E-05

5.04E-05

4.82E-05

2.72E-05

1.94E-05

IRM1.2T

(Am2/kg)

6.28E-04

1.13E-03

8.18E-04

6.07E-04

8.78E-04

8.47E-04

5.98E-04

7.15E-04

7.30E-04

5.89E-04

1.41E-03

2.36E-03

4.22E-03

5.26E-03

1.06E-02

4.65E-03

4.93E-03

1 .48E-02

3.25E-02

6.52E-03

1.10E-03

1.01E-03

1.07E-03

1 .06E-03

8.97E-04

9.51 E-04

2.15E-03

2.62E-03

1.12E-03

6.47E-04

8.35E-04

9.05E-04

1.07E-03

1.23E-03

1.13E-03

1.14E-03

3.55E-04

9.74E-04

1.43E-03

1.00E-03

9.48E-04

9.79E-04

7.15E-04

7.53E-04

7.48E-04

7.69E-04

7.48E-04

8.67E-04

9.53E-04

6.25E-04

4.21 E-04

IRM 0.3T

(Am2/kg)

5.77E-04

1 .04E-03

7.43E-04

5.60E-04

8.13E-04

7.20E-04

5.49E-04

6.60E-04

6.70E-04

5.45E-04

1.35E-03

2.32E-03

4.14E-03

5.17E-03

1.06E-02

4.55E-03

4.84E-03

1 .47E-02

3.25E-02

6.43E-03

1.02E-03

9.34E-04

9.74E-04

9.52E-04

8.10E-04

8.65E-04

2.04E-03

2.50E-03

1.03E-03

5.84E-04

7.64E-04

8.40E-04

9.83E-04

1.14E-03

1 .05E-03

1 .05E-03

3.22E-04

8.78E-04

1.37E-03

9.24E-04

8.63E-04

8.90E-04

6.53E-04

6.86E-04

6.80E-04

6.99E-04

6.82E-04

7.94E-04

8.70E-04

5.89E-04

3.98E-04

HIRM

(Am2/kg)

2.58E-05

4.64E-05

3.71 E-05

2.37E-05

3.23E-05

6.39E-05

2.42E-05

2.74E-05

3.02E-05

2.23E-05

3.09E-05

2.15E-05

3.93E-05

4.28E-05

-2.76E-05

4.93E-05

4.46E-05

4.28E-05

-7.84E-06

4.70E-05

3.66E-05

3.76E-05

4.58E-05

5.21 E-05

4.39E-05

4.31 E-05

5.72E-05

5.86E-05

4.59E-05

3.15E-05

3.55E-05

3.29E-05

4.27E-05

4.64E-05

4.16E-05

4.86E-05

1.66E-05

4.80E-05

3.10E-05

3.78E-05

4.25E-05

4.44E-05

3.11 E-05

3.38E-05

3.38E-05

3.48E-05

3.29E-05

3.67E-05

4.13E-05

1.78E-05

1.17E-05

S

0.92

0.92

0.91

0.92

0.93

0.85

0.92

0.92

0.92

0.92

0.96

0.98

0.98

0.98

1.01

0.98

0.98

0.99

1.00

0.99

0.93

0.93

0.91

0.90

0.90

0.91

0.95

0.96

0.92

0.90

0.91

0.93

0.92

0.92

0.93

0.92

0.91

0.90

0.96

0.92

0.91

0.91

0.91

0.91

0.91

0.91

0.91

0.92

0.91

0.94

0.94
Sample No.

264

265

266

267

268

269

270

271

272

273

274

275

276

277

278

279

280

281

282

283

284

285

286

287

288

289

290

291

292

293

294

295

296

297

298

299

300

301

302

303

304

305

306

307

308

309

310

311

312

313

314

Depth

(m)

64.15

64.25

64.35

64.45

64.55

64.65

64.75

64.85

64.95

65.05

65.15

65.25

65.35

65.45

65.55

65.65

65.75

65.85

65.95

66.05

66.15

66.25

66.35

66.45

66.55

66.65

66.75

66.85

66.95

67.05

67.15

67.25

67.35

67.45

67.55

67.65

67.75

67.85

67.95

68.05

68.15

68.25

68.35

68.45

68.55

68.65

68.75

68.85

68.95

69.05

69.15

MSLF

(m3/kg)

3.14E-08

4.61 E-08

5.93E-08

6.06E-08

5.90E-08

6.12E-08

7.98E-08

7.75E-08

8.90E-08

7.26E-08

6.14E-08

6.16E-08

6.43E-08

6.69E-08

6.57E-08

6.60E-08

6.29E-08

7.46E-08

7.97E-08

8.88E-08

8.00E-08

7.73E-08

7.48E-08

7.84E-08

7.62E-08

7.47E-08

8.19E-08

2.00E-07

1.84E-07

5.28E-08

7.27E-08

1.05E-07

1.25E-07

2.06E-07

2.48E-07

2.66E-07

2.59E-07

2.65E-07

4.61 E-07

6.85E-07

4.81 E-07

1.30E-07

1.47E-07

1.40E-07

1.45E-07

1.44E-07

1.51 E-07

1.34E-07

1.28E-07

1 .08E-07

9.87E-08

ARM

(Am2/kg)

2.32E-05

4.65E-05

8.18E-05

9.45E-05

7.76E-05

8.72E-05

1.30E-04

1.13E-04

1.67E-04

1.15E-04

5.89E-05

5.17E-05

3.91 E-05

4.34E-05

3.21 E-05

3.71 E-05

3.74E-05

4.23E-05

4.15E-05

4.51 E-05

4.01 E-05

3.62E-05

3.66E-05

4.16E-05

4.24E-05

4.20E-05

4.33E-05

5.99E-05

4.62E-05

3.57E-05

3.32E-05

5.70E-05

4.48E-05

6.74E-05

7.55E-05

1.09E-04

1.03E-04

9.12E-05

1.17E-04

1.30E-04

1.24E-04

9.24E-05

1 .09E-04

1 .23E-04

1 .34E-04

1 .23E-04

1.24E-04

1.21E-04

1.40E-04

1.16E-04

1.11E-04

IRM1.2T

(Am2/kg)

4.33E-04

8.37E-04

1.66E-03

1.85E-03

1.98E-03

2.22E-03

3.18E-03

2.72E-03

3.94E-03

2.32E-03

1.75E-03

8.53E-04

6.60E-04

7.84E-04

6.92E-04

6.46E-04

6.52E-04

7.36E-04

7.22E-04

8.09E-04

7.09E-04

6.31 E-04

6.57E-04

7.47E-04

7.84E-04

7.55E-04

8.62E-04

2.10E-03

1.52E-03

6.07E-04

6.47E-04

1 .03E-03

9.91 E-04

1 .58E-03

1.91E-03

2.79E-03

2.58E-03

2.41 E-03

3.66E-03

4.86E-03

4.24E-03

1.98E-03

2.36E-03

2.50E-03

2.72E-03

2.45E-03

2.56E-03

2.43E-03

2.88E-03

2.22E-03

2.10E-03

IRM 0.3T

(Am2/kg)

4.05E-04

8.01 E-04

1.60E-03

1.80E-03

1.93E-03

2.16E-03

3.12E-03

2.64E-03

3.84E-03

2.25E-03

1 .45E-03

7.83E-04

6.05E-04

7.16E-04

6.32E-04

5.91 E-04

5.99E-04

6.66E-04

6.57E-04

7.34E-04

6.44E-04

5.71 E-04

5.94E-04

6.67E-04

6.87E-04

6.76E-04

7.77E-04

2.02E-03

1.52E-03

5.41 E-04

5.94E-04

9.56E-04

9.39E-04

1.50E-03

1.81 E-03

2.64E-03

2.43E-03

2.30E-03

3.53E-03

4.72E-03

4.08E-03

1.85E-03

2.18E-03

2.32E-03

2.54E-03

2.28E-03

2.37E-03

2.25E-03

2.67E-03

2.03E-03

1.91 E-03

HIRM

(Am2/kg)

1.42E-05

1.84E-05

3.08E-05

2.79E-05

2.41 E-05

3.17E-05

3.18E-05

3.73E-05

5.06E-05

3.32E-05

1.47E-04

3.48E-05

2.75E-05

3.41 E-05

3.01 E-05

2.74E-05

2.63E-05

3.46E-05

3.25E-05

3.73E-05

3.22E-05

3.00E-05

3.15E-05

3.97E-05

4.85E-05

3.96E-05

4.25E-05

3.66E-05

2.24E-06

3.29E-05

2.66E-05

3.75E-05

2.64E-05

3.94E-05

5.34E-05

7.55E-05

7.51 E-05

5.72E-05

6.92E-05

6.69E-05

8.05E-05

6.67E-05

8.92E-05

8.80E-05

9.35E-05

8.64E-05

9.57E-05

8.89E-05

1.07E-04

9.31 E-05

9.55E-05

S

0.93

0.96

0.96

0.97

0.98

0.97

0.98

0.97

0.97

0.97

0.83

0.92

0.92

0.91

0.91

0.92

0.92

0.91

0.91

0.91

0.91

0.90

0.90

0.89

0.88

0.90

0.90

0.97

1.00

0.89

0.92

0.93

0.95

0.95

0.94

0.95

0.94

0.95

0.96

0.97

0.96

0.93

0.92

0.93

0.93

0.93

0.93

0.93

0.93

0.92

0.91
Sample No.

315

316

317

318

319

320

321

322

323

324

325

326

327

328

329

330

331

332

333

334

335

336

337

338

339

340

341

342

343

344

345

346

347

348

349

350

351

352

353

354

355

356

357

358

359

360

361

362

363

364

365

Depth

(m)

69.25

69.35

69.45

69.55

69.65

69.75

69.85

69.95

70.1

70.15

70.25

70.35

70.45

70.55

70.65

70.75

70.85

70.95

71.05

71.15

71.25

71.35

71.45

71.55

71.65

71.75

71.85

71.95

72.05

72.15

72.25

72.35

72.45

72.55

72.65

72.75

72.85

72.95

73.05

73.15

73.55

73.65

73.75

73.85

73.95

74.05

74.15

74.25

74.35

74.45

74.55

MSLF

(m3/kg)

1.02E-07

1.16E-07

1.16E-07

1.15E-07

1.31E-07

1.18E-07

1.67E-07

1.03E-07

9.05E-08

8.09E-08

9.16E-08

8.56E-08

8.03E-08

9.59E-08

7.88E-08

9.07E-08

8.54E-08

8.75E-08

9.51 E-08

1.04E-07

1.02E-07

9.80E-08

9.10E-08

9.83E-08

8.65E-08

9.17E-08

1.30E-07

9.20E-08

9.19E-08

8.61 E-08

8.94E-08

8.94E-08

9.28E-08

9.14E-08

9.33E-08

9.64E-08

9.48E-08

9.41 E-08

9.82E-08

9.27E-08

9.34E-08

8.71 E-08

8.72E-08

9.05E-08

6.63E-08

8.29E-08

7.99E-08

8.22E-08

9.49E-08

4.24E-08

6.54E-08

ARM

(Am2/kg)

9.82E-05

1.40E-04

1.28E-04

1.38E-04

1.76E-04

9.90E-05

1.16E-04

7.40E-05

5.58E-05

4.77E-05

6.44E-05

6.76E-05

4.99E-05

6.70E-05

5.35E-05

6.99E-05

4.71 E-05

6.87E-05

7.38E-05

1.24E-04

9.96E-05

1.04E-04

7.07E-05

8.42E-05

6.14E-05

8.06E-05

8.19E-05

8.15E-05

7.80E-05

6.22E-05

7.17E-05

6.94E-05

6.51 E-05

7.08E-05

6.89E-05

7.78E-05

7.18E-05

8.76E-05

7.24E-05

6.89E-05

6.56E-05

5.65E-05

7.57E-05

7.19E-05

4.56E-05

4.52E-05

5.80E-05

6.28E-05

7.84E-05

3.96E-05

5.13E-05

IRM1.2T

(Am2/kg)

1.90E-03

2.80E-03

2.33E-03

2.51 E-03

3.77E-03

2.10E-03

3.08E-03

1.65E-03

1.14E-03

9.67E-04

1.37E-03

1.58E-03

9.04E-04

1.21 E-03

8.32E-04

1.11 E-03

7.35E-04

1.19E-03

1.24E-03

2.12E-03

1.73E-03

1.78E-03

1.23E-03

1.55E-03

1.02E-03

1.36E-03

1.31 E-03

1.35E-03

1.24E-03

9.87E-04

1.12E-03

1 .09E-03

1.07E-03

1.24E-03

1.38E-03

1.29E-03

1.12E-03

1.32E-03

1.12E-03

1.04E-03

1 .08E-03

9.17E-04

1 .37E-03

1.10E-03

6.85E-04

1.17E-03

8.87E-04

8.40E-04

1.28E-03

5.78E-04

7.14E-04

IRM 0.3T

(Am2/kg)

1.72E-03

2.56E-03

2.17E-03

2.37E-03

3.55E-03

1.98E-03

2.89E-03

1.52E-03

1.05E-03

8.78E-04

1.25E-03

1.37E-03

8.26E-04

1.13E-03

7.63E-04

9.86E-04

6.56E-04

1.07E-03

1.11 E-03

1.90E-03

1.54E-03

1.61 E-03

1.10E-03

1.38E-03

8.97E-04

1.20E-03

1.16E-03

1.20E-03

1.09E-03

8.89E-04

1 .OOE-03

9.71 E-04

9.63E-04

1.12E-03

1 .24E-03

1.17E-03

1.02E-03

1.19E-03

1.01 E-03

9.54E-04

9.86E-04

8.32E-04

1.27E-03

1 .02E-03

6.24E-04

1.12E-03

8.18E-04

7.76E-04

1.19E-03

5.37E-04

6.63E-04

HIRM

(Am2/kg)

9.10E-05

1.20E-04

7.83E-05

6.57E-05

1.14E-04

6.22E-05

9.61 E-05

6.22E-05

4.82E-05

4.48E-05

6.06E-05

1.02E-04

3.94E-05

4.01 E-05

3.45E-05

6.11 E-05

3.95E-05

6.11 E-05

6.35E-05

1.08E-04

9.49E-05

8.57E-05

6.44E-05

8.37E-05

5.93E-05

7.89E-05

7.43E-05

7.33E-05

7.27E-05

4.87E-05

6.11 E-05

5.97E-05

5.36E-05

6.03E-05

6.84E-05

6.17E-05

5.00E-05

6.32E-05

5.68E-05

4.52E-05

4.84E-05

4.22E-05

5.40E-05

3.98E-05

3.03E-05

2.66E-05

3.48E-05

3.18E-05

4.42E-05

2.07E-05

2.57E-05

S

0.90

0.91

0.93

0.95

0.94

0.94

0.94

0.92

0.92

0.91

0.91

0.87

0.91

0.93

0.92

0.89

0.89

0.90

0.90

0.90

0.89

0.90

0.89

0.89

0.88

0.88

0.89

0.89

0.88

0.90

0.89

0.89

0.90

0.90

0.90

0.90

0.91

0.90

0.90

0.91

0.91

0.91

0.92

0.93

0.91

0.95

0.92

0.92

0.93

0.93

0.93
Sample No.

366

367

368

369

370

371

372

373

374

375

376

377

378

379

380

381

382

383

384

385

386

387

388

389

390

391

392

393

394

395

396

397

398

399

400

401

402

403

404

405

406

407

408

409

410

411

412

413

414

415

416

Depth

(m)

74.65

74.75

74.85

74.95

75.05

75.15

75.25

75.35

75.45

75.55

75.65

75.75

75.85

75.95

76.05

76.15

76.25

76.35

76.45

76.65

76.75

76.85

76.95

77.05

77.15

77.25

77.35

77.45

77.55

77.65

77.75

77.85

77.95

78.05

78.15

78.25

78.35

78.45

78.55

78.65

78.75

78.85

78.95

79.05

79.15

79.25

79.35

79.45

79.55

79.65

79.75

MSLF

(m3/kg)

7.78E-08

7.23E-08

2.18E-07

1 .90E-07

1 .09E-07

9.84E-08

1.12E-07

1.18E-07

1.25E-07

1.14E-07

1 .09E-07

1.15E-07

1.19E-07

1.40E-07

1.62E-07

1.84E-07

5.35E-07

8.73E-07

8.50E-07

8.67E-07

1.21E-06

1.11E-06

1 .04E-06

1.11E-06

9.86E-07

9.36E-07

9.96E-07

9.71 E-07

9.88E-07

9.99E-07

9.70E-07

1.03E-06

8.50E-07

1.04E-06

7.99E-07

8.53E-07

7.16E-07

7.29E-07

7.92E-07

8.33E-07

7.09E-07

7.87E-07

7.37E-07

7.24E-07

5.92E-07

7.37E-07

9.10E-07

1.32E-06

1.33E-06

7.48E-07

1.08E-06

ARM

(Am2/kg)

1.03E-04

7.89E-05

5.20E-04

3.16E-04

1.07E-04

8.28E-05

9.85E-05

9.99E-05

1.56E-04

1.10E-04

9.72E-05

1.07E-04

1.07E-04

1.24E-04

1.56E-04

1.82E-04

1.29E-04

1.61E-04

1.74E-04

2.25E-04

2.25E-04

2.53E-04

2.71 E-04

2.77E-04

2.59E-04

2.36E-04

2.75E-04

2.06E-04

2.24E-04

2.22E-04

2.24E-04

2J2E-04

1J2E-04

1.75E-04

2.13E-04

1.85E-04

1.42E-04

1.52E-04

1.71 E-04

1.93E-04

1 .82E-04

1.90E-04

1.59E-04

1.26E-04

1.06E-04

1 .45E-04

1.72E-04

2.39E-04

1.96E-04

1.58E-04

4.06E-04

IRM1.2T

(Am2/kg)

1.43E-03

1.03E-03

7.30E-03

8.34E-03

3.83E-03

1.80E-03

4.67E-03

4.42E-03

7.63E-03

5.91 E-03

4.72E-03

5.14E-03

4.79E-03

7.59E-03

9.89E-03

1.09E-02

6.54E-03

1.10E-02

1.35E-02

1.68E-02

1 .94E-02

2.31 E-02

2.43E-02

2.51 E-02

2.38E-02

2.29E-02

2.76E-02

2.15E-02

2.41 E-02

2.37E-02

2.34E-02

2.67E-02

1.61 E-02

1.55E-02

2.00E-02

1.62E-02

1.08E-02

1.21 E-02

1.51 E-02

1.67E-02

1.54E-02

1.61 E-02

1.18E-02

8.98E-03

7.06E-03

1.25E-02

1.50E-02

2.42E-02

1.81 E-02

1.38E-02

3.10E-02

IRM 0.3T

(Am2/kg)

1.38E-03

9.79E-04

7.19E-03

8.27E-03

3.76E-03

1.72E-03

4.58E-03

4.32E-03

7.50E-03

5.77E-03

4.59E-03

4.97E-03

4.58E-03

7.35E-03

9.52E-03

1.04E-02

6.41 E-03

1 .08E-02

1.34E-02

1 .66E-02

1.93E-02

2.29E-02

2.42E-02

2.50E-02

2.37E-02

2.28E-02

2.74E-02

2.13E-02

2.39E-02

2.37E-02

2.32E-02

2.65E-02

1.59E-02

1.53E-02

1 .97E-02

1.60E-02

1.07E-02

1.19E-02

1.50E-02

1.64E-02

1.52E-02

1.59E-02

1.16E-02

8.86E-03

6.93E-03

1.24E-02

1.49E-02

2.40E-02

1.79E-02

1.36E-02

3.06E-02

HIRM

(Am2/kg)

2.84E-05

2.37E-05

5.61 E-05

3.84E-05

3.14E-05

3.62E-05

4.60E-05

4.88E-05

6.54E-05

6.74E-05

6.46E-05

8.54E-05

1.06E-04

1.19E-04

1.86E-04

2.19E-04

6.52E-05

7.64E-05

8.24E-05

9.49E-05

5.37E-05

9.16E-05

4.38E-05

4.07E-05

8.75E-05

7.34E-05

7.05E-05

7.64E-05

8.24E-05

4.00E-05

8.17E-05

1.11 E-04

8.00E-05

7.51 E-05

1.35E-04

1.02E-04

7.65E-05

7.84E-05

8.8QE-05

1.24E-04

9.94E-05

9.71 E-05

9.01 E-05

5.74E-05

6.35E-05

5.53E-05

6.82E-05

8.66E-05

7.96E-05

9.04E-05

1.63E-04

S

0.96

0.95

0.98

0.99

0.98

0.96

0.98

0.98

0.98

0.98

0.97

0.97

0.96

0.97

0.96

0.96

0.98

0.99

0.99

0.99

0.99

0.99

1.00

1.00

0.99

0.99

0.99

0.99

0.99

1.00

0.99

0.99

0.99

0.99

0.99

0.99

0.99

0.99

0.99

0.99

0.99

0.99

0.98

0.99

0.98

0.99

0.99

0.99

0.99

0.99

0.99
nple No.

417

418

419

420

421

422

423

424

425

426

427

428

429

430

431

432

433

434

435

436

437

438

439

440

441

442

443

444

Depth

(m)

79.85

79.95

80.05

80.15

80.25

80.35

80.45

80.55

80.65

80.75

80.85

80.95

81.05

81.15

81.25

81.35

81.45

81.55

81.65

81.75

81.85

81.95

82.05

82.15

82.25

82.35

82.45

82.55

MSLF

(m3/kg)

1.01E-06

1.48E-06

1 .03E-06

7.83E-07

4.43E-07

4.55E-07

8.77E-07

1.13E-06

1.01E-06

1.10E-06

1.13E-06

1.03E-06

1.12E-06

9.35E-07

1 .02E-06

1.07E-06

9.32E-07

9.07E-07

1.06E-06

1 .90E-06

7.56E-07

7.52E-07

8.20E-07

7.19E-07

7.85E-07

7.72E-07

6.40E-07

8.64E-07

ARM

(Am2/kg)

3.29E-04

3.07E-04

1 .90E-04

1 .67E-04

9.47E-05

8.62E-05

2.81 E-04

2.74E-04

3.59E-04

4.76E-04

3.80E-04

3.40E-04

3.11E-04

2.31 E-04

2.24E-04

2.50E-04

1.93E-04

1.53E-04

1.32E-04

2.72E-04

1.31 E-04

1.33E-04

1 .26E-04

1.31 E-04

1.58E-04

1 .22E-04

1.07E-04

1.16E-04

IRM1.2T

(Am2/kg)

2.64E-02

3.12E-02

1.87E-02

1.43E-02

4.83E-03

3.92E-03

2.33E-02

2.75E-02

3.07E-02

3.60E-02

2.96E-02

3.00E-02

2.68E-02

1 .87E-02

1.87E-02

2.12E-02

1.64E-02

1.23E-02

1.23E-02

2.98E-02

1 .07E-02

1.01E-02

9.89E-03

1.13E-02

1.40E-02

9.08E-03

8.60E-03

8.37E-03

IRM 0.3T

(Am2/kg)

2.61 E-02

3.10E-02

1.85E-02

1.40E-02

4.71 E-03

3.78E-03

2.29E-02

2.70E-02

3.03E-02

3.55E-02

2.91 E-02

2.96E-02

2.65E-02

1 .83E-02

1 .83E-02

2.07E-02

1.61 E-02

1 .20E-02

1.21 E-02

2.97E-02

1.05E-02

9.88E-03

9.74E-03

1.11 E-02

1.38E-02

8.93E-03

8.48E-03

8.21 E-03

HIRM

(Am2/kg)

1.40E-04

1.01 E-04

1.04E-04

1.32E-04

5.91 E-05

7.22E-05

1.73E-04

2.66E-04

2.27E-04

2.75E-04

2.50E-04

2.12E-04

1.30E-04

1 .68E-04

2.27E-04

2.69E-04

1.56E-04

1.21 E-04

1.00E-04

6.39E-05

7.70E-05

9.02E-05

7.80E-05

1.02E-04

9.60E-05

7.54E-05

6.20E-05

8.29E-05

S

0.99

0.99

0.99

0.98

0.98

0.96

0.99

0.98

0.99

0.98

0.98

0.99

0.99

0.98

0.98

0.97

0.98

0.98

0.98

1.00

0.99

0.98

0.98

0.98

0.99

0.98

0.99

0.98
TABLE 2. Elemental Abundance from X-ray Fluorescence

Sample No.: A unique sample number assigned to sediment samples placed in vials.

Depth (cm): Depth of sample in centimeters from top of core. The depth shown is the midpoint 

of a channel sample that encompasses a 10-cm depth interval.

Elements: The elements analyzed are listed below. The units are either weight percent (Wt%) 

or parts per million (ppm).

Ti: Titanium-Wt % V: Vanadium-ppm

Cr: Chromium-ppm Mn: Manganese-ppm

Fe: Iron- Wt% Ni: Nickel-ppm

Cu: Copper-ppm Zn: Zinc-ppm

Rb: Rubidium-ppm Sr: Strontium-ppm

Y: Yttrium-ppm Zr: Zirconium-ppm

Nb: Niobium-ppm Mo: Molybdenum-ppm

Sn: Tin-ppm Sb: Antimony-ppm

Cs: Cesium-ppm Ba: Barium-ppm

La: Lanthanum-ppm Ce: Cerium-ppm
Sample Depth Ti V Cr Mn Fe Ni Cu Zn Rb Sr Y Zr Nb Mo Sn Sb Cs Ba La Ce 

Number (m) wt.% ppm ppm ppm wt. % ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm

1

2

3

5

7

11

13

17

20

23

24

26

29

31

33

35

38

42

45

48

51

53

56

60

61

62

64

65

66

67

69

73

74

76

77

79

82

86

89

91

93

96

97

100

101

104

105

106

110

112

115

117

119

121

123

126

129

131

132

134

135

139

143

147

32.05

32.15

32.25

32.45

32.65

33.05

33.25

33.65

34.75

35.05

35.15

35.35

35.65

35.85

36.05

36.25

36.55

36.95

38.15

38.45

38.75

38.95

39.25

39.65

39.75

39.9

40.35

40.45

40.55

40.65

40.85

41.155

41.25

41.45

41.55

41.75

42.05

42.45

42.75

43.15

43.35

43.65

43.75

44.05

44.15

44.45

44.55

44.85

45.05

45.25

45.55

45.75

45.95

46.55

46.75

47.05

47.35

47.55

47.65

47.85

47.95

49.85

50.05

50.45

0.29

0.30

0.28

0.28

0.25

0.26

0.31

0.31

0.31

0.33

0.33

0.34

0.33

0.33

0.25

0.27

0.3

0.33

0.27

0.28

0.30

0.29

0.30

0.14

0.16

0.33

0.31

0.21

0.18

0.16

0.18

0.18

0.27

0.26

0.24

0.25

0.23

0.18

0.19

0.24

0.22

0.24

0.18

0.22

0.22

0.19

0.19

0.21

0.21

0.21

0.23

0.19

0.18

0.22

0.22

0.20

0.21

0.21

0.25

0.22

0.19

0.25

0.22

0.22

107

72

44

90

72

80

96

127

88

68

73

78

78

70

77

110

19

136

81

101

107

97

124

49

0

87

60

87

94

26

69

56

68

57

64

21

90

42

80

20

70

55

43

27

59

57

59

43

27

75

68

77

66

66

44

66

85

53

70

92

72

88

88

74

0

0

0

39

0

0

0

17

0

38

32

55

24

47

30

21

49

10

10

20

0

0

0

0

0

0

0

0

0

15

5

0

37

31

33

49

0

0

0

43

0

31

0

49

46

32

34

24

44

18

34

18

31

25

40

0

22

28

48

0

10

21

0

44

643

651

727

719

740

744

734

871

734

1000

998

1100

895

824

1300

1400

979

949

795

717

745

753

747

356

415

922

774

587

540

409

504

486

628

762

717

748

572

530

558

738

618

837

528

611

879

663

614

576

713

577

559

550

639

662

522

537

619

646

738

600

622

659

624

517

3.74

3.69

3.60

3.39

3.40

3.58

3.90

3.72

3.74

3.89

4.03

3.96

3.88

3.83

3.16

3.18

3.55

3.64

2.98

3.21

3.52

3.47

3.72

1.74

1.92

3.91

3.45

2.78

2.36

1.98

2.2

2.19

2.43

2.64

2.43

2.60

2.55

2.46

2.63

2.72

2.76

2.79

2.54

2.57

2.65

2.25

2.37

2.41

2.51

2.46

2.73

2.62

2.33

2.55

2.61

2.72

2.65

2.49

2.91

2.96

2.29

2.91

2.90

2.60

24

28

27

30

22

31

27

22

35

32

28

30

33

26

25

25

29

28

24

24

23

3

27

20

20

24

27

22

22

15

22

21

20

24

25

31

25

26

26

24

19

23

23

29

21

27

31

29

22

22

24

25

22

22

21

23

20

24

22

26

27

28

28

22

41

41

42

50

35

40

43

52

43

54

49

50

54

51

46

51

52

56

59

60

49

54

50

16

18

52

46

29

36

23

26

20

26

34

43

44

29

25

36

44

38

41

29

39

38

38

35

38

31

33

36

27

35

40

37

34

38

35

44

34

32

45

33

40

104

102

92

110

83

90

105

129

103

137

145

145

141

150

113

117

131

133

115

131

107

116

115

43

53

123

107

60

57

45

53

58

68

84

85

94

67

62

85

91

79

96

61

85

85

74

82

87

84

83

90

63

81

91

93

71

80

86

107

78

71

108

82

94

155

137

121

122

130

129

155

155

168

160

174

155

156

150

132

112

150

141

149

156

186

187

194

66

75

201

174

96

98

81

81

65

90

99

89

97

81

93

93

100

106

94

89

97

95

77

77

78

92

91

98

91

81

101

97

104

99

99

102

109

101

121

128

107

214

211

194

197

235

226

231

225

225

237

234

231

234

234

377

379

406

650

941

794

817

740

519

0

0

705

669

811

746

990

982

806

539

750

970

946

846

681

654

537

723

581

444

359

467

388

364

308

420

332

314

392

363

368

337

345

328

409

350

397

714

510

490

510

19

23

15

19

19

13

16

8

11

27

22

26

7

10

13

2

2

2

10

14

7

1

1

13

16

12

11

9

7

8

1

10

22

7

7

5

8

9

10

14

15

2

9

15

19

5

2

2 .

11

5

14

15

2

8

7

18

15

12

2

6

2

10

7

2

104

112

105

86

101

97

108

115

109

114

101

95

102

107

92

78

68

68

62

45

67

64

57

111

143

73

90

108

93

133

87

118

184

105

43

61

89

93

89

104

88

92

82

85

92

55

64

75

83

72

91

86

69

80

75

97

73

83

69

81

77

58

74

65

14

15

11

11

15

15

15

28

14

14

15

7

28

29

13

31

30

28

20

18

10

13

12

0

1

10

13

14

11

9

11

11

14

21

25

26

3

10

11

27

13

31

9

12

12

25

29

28

23

26

26

3

26

26

26

4

10

26

28

4

27

24

12

25

3

4

3

12

4

4

4

16

2

4

4

4

20

18

5

18

18

41

27

33

6

5

5

2

1

5

4

6

8

7

7

5

14

34

48

42

4

9

8

34

7

39

6

5

5

17

19

20

18

17

16

0

17

17

16

0

4

16

36

5

40

29

7

36

5

4

2

10

3

8

5

16

3

4

4

4

7

7

9

10

23

15

11

14

6

4

1

1

2

2

7

4

5

4

5

4

8

6

5

8

5

2

4

7

5

3

3

12

5

5

5

9

18

17

16

6

11

7

4

5

5

15

8

4

10

16

5

11

4

5

3

4

4

3

4

3

3

2

3

6

2

3

2

5

6

8

7

8

6

4

5

3

2

1

2

1

2

2

1

3

4

3

3

2

2

1

3

2

2

1

0

2

2

2

2

2

2

2

2

3

2

2

1

1

2

2

2

1

3

2

4

3

0

12

0

22

0

0

14

30

15

52

41

73

58

63

49

72

96

23

30

19

13

5

11

10

0

0

0

10

0

0

0

9

42

44

17

37

10

16

0

10

0

0

11

37

18

23

66

9

32

25

50

0

39

44

43

0

20

45

28

10

5

30

0

32

620

803

578

611

501

487

795

751

813

801

892

1000

835

853

660

841

1500

1000

1000

964

948

859

794

706

530

593

549

631

402

435

412

567

781

597

781

681

736

635

446

540

759

524

533

634

467

472

521

461

470

524

571

460

776

552

609

427

356

526

634

687

661

885

494

824

62

232

8

34

51

40

234

25

216

25

16

57

26

47

23

47

62

44

44

22

185

231

201

183

0

17

20

63

31

33

18

199

35

0

18

22

174

226

29

21

169

43

216

47

37

19

20

32

10

20

14

22

52

28

31

0

12

0

23

193

29

59

23

20

33

233

44

57

43

18

245

51

202

50

105

2

38

55

62

61

65

50

38

28

214

203

176

168

34

41

42

182

20

36

40

164

74

22

56

31

197

201

47

46

215

52

222

68

18

40

2

2

28

46

45

26

53

37

2

40

34

66

34

210

2

71

3

52

n
Sample Depth Ti V Cr Mn Fe Ni Cu Zn Rb Sr Y Zr Nb Mo Sn Sb Cs Ba La Ce 

Number (m) wt.% ppm ppm ppm wt. % ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm

148

151

152

156

163

171

176

177

180

180

182

186

190

193

196

200

203

206

211

213

217

222

224

227

229

231

233

237

240

242

246

249

251

253

255

258

258

261

264

267

270

272

276

280

265

288

291

293

297

301

303

305

310

315

317

321

324

326

327

331

334

337

343

347

352

52.25

52.55

52.65

53.05

53.75

54.55

55.05

55.15

55.55

55.55

55.75

56.15

56.55

56.85

57.15

57.55

57.85

58.15

58.65

58.85

59.25

59.75

59.95

60.25

60.45

60.65

60.65

61.25

61.55

61.75

62.15

62.45

62.83

63.05

63.25

63.55

63.55

63.85

64.15

64.45

64.75

64.95

65.35

65.75

68.25

66.55

68.65

67.05

67.45

67.85

68.05

68.25

68.75

69.25

69.45

69.85

70.15

70.35

70.45

70.65

71.15

71.45

72.05

72.45

72.95

0.27

0.21

0.23

0.26

0.21

0.20

0.17

0.17

0.17

0.15

0.2

0.21

0.18

0.22

0.23

0.18

0.21

0.22

0.23

0.23

0.27

0.19

0.24

0.23

0.26

0.28

0.26

0.24

0.27

0.24

0.24

0.11

0.21

0.27

0.21

0.22

0.21

0.22

0.13

0.17

0.18

0.18

0.21

0.20

0.25

0.24

0.08

0.17

0.19

0.23

0.25

0.27

0.25

0.26

0.22

0.25

0.24

0.21

0.24

0.29

0.28

0.26

0.29

0.28

0.27

60

66

64

50

63

59

47

49

57

49

73

15

18

39

65

39

62

76

91

76

87

59

70

44

76

69

99

51

81

80

98

29

55

71

59

47

38

59

22

91

78

57

65

47

93

89

22

73

33

77

57

67

55

96

71

102

93

116

43

77

92

103

91

79

98

41

25

31

42

27

36

29

31

23

0

34

28

36

35

42

37

43

27

27

25

39

23

42

45

42

33

38

52

45

52

41

23

54

63

20

37

10

0

0

0

0

0

0

0

0

0

0

3

0

14

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

699

628

639

643

545

576

514

500

497

467

558

594

577

625

582

574

643

618

619

643

691

664

519

565

524

863

753

684

705

640

639

409

573

700

682

670

577

668

516

495

485

482

691

588

669

649

281

462

488

550

600

642

620

638

551

615

658

596

646

789

725

680

695

790

687

3.37

2.62

2.65

3.27

2.50

2.53

1.87

1.87

2.01

2.16

2.30

2.52

1.79

2.67

2.62

1.89

2.47

2.53

2.85

2.83

3.09

2.37

2.68

2.69

3.04

3.38

3.18

2.96

3.17

3.12

3.02

1.39

2.46

3.18

2.53

2.67

2.77

3.06

2.09

2.40

2.47

2.38

2.87

2.73

3.27

3.17

1.14

2.30

2.37

2.63

2.74

3.13

2.76

2.94

2.41

2.94

3.18

2.71

2.96

3.61

3.29

3.21

3.38

3.54

3.47

23

22

32

22

21

22

19

22

20

26

22

25

20

30

26

18

26

21

24

24

23

31

23

22

25

23

29

32

44

26

31

25

22

32

32

35

27

32

21

20

21

3

21

23

23

26

21

19

22

30

30

25

24

28

24

26

27

35

24

35

27

37

29

30

25

53

44

37

44

36

39

23

31

29

22

35

40

25

36

33

23

36

39

41

43

47

37

43

39

39

46

47

36

45

49

47

14

37

43

33

36

33

36

21

26

25

25

32

33

35

33

8

22

22

27

25

27

24

22

9

23

34

24

30

45

25

44

33

38

34

127

98

102

112

84

82

60

72

62

49

77

88

58

86

86

60

82

90

101

100

107

75

90

89

100

115

104

96

106

100

103

35

88

107

83

87

70

76

51

64

63

65

73

71

90

82

17

56

56

65

67

82

67

68

55

69

85

66

73

98

86

106

91

89

84

127

98

103

137

90

88

71

66

82

71

88

97

73

89

112

75

80

95

121

92

121

83

104

102

100

143

136

116

122

105

122

33

99

118

91

97

102

106

74

86

82

99

93

88

145

125

39

87

75

88

105

128

107

108

90

106

124

83

107

115

133

111

124

132

118

340

566

414

371

576

554

732

769

750

776

652

768

958

564

596

898

599

580

534

573

500

712

379

351

325

557

550

549

544

398

532

0

485

574

718

709

756

568

455

418

341

378

702

793

689

688

0

721

725

698

607

533

662

822

583

549

489

716

662

524

520

611

528

536

528

2

2

2

2

9

2

6

11

13

15

2

9

16

2

10

10

2

2

12

14

19

6

6

10

2

15

6

23

2

2

14

5

18

2

2

21

24

14

3

13

16

15

8

7

10

13

6

7

13 .

13

17

24

18

25

15

16

18

16

11

14

12

16

16

21

11

41

37

57

59

14

48

80

61

70

79

76

77

143

72

93

65

68

51

85

83

102

62

97

101

104

110

77

97

76

95

97

18

97

70

35

100

79

82

60

76

70

90

62

65

62

80

105

69

92

121

138

123

136

117

140

142

104

98

103

95

142

121

119

114

115

25

25

27

22

25

25

23

23

10

1

25

27

21

25

21

21

25

28

23

10

27

25

25

27

31

23

28

14

30

31

21

17

11

30

24

13

4

2

1

2

2

12

11

11

10

4

8

7

15

13

16

6

7

14

4

18

17

5

5

16

6

14

16

16

13

36

38

38

35

40

41

34

38

23

5

35

40

25

38

29

29

37

39

24

18

31

27

21

16

24

20

40

18

36

35

24

17

7

36

25

11

2

2

1

1

0

2

12

10

8

6

2

9

5

4

4

2

1

4

1

5

5

1

2

6

2

5

6

5

6

9

9

12

6

8

12

7

38

23

6

4

10

5

11

6

6

14

8

10

6

31

5

9

4

11

13

10

18

36

15

9

8

7

7

9

11

4

3

5

6

3

3

6

4

6

6

5

5

4

6

2

3

3

6

3

5

3

4

3

3

3

4

2

4

5

3

2

2

2

3

3

3

3

3

2

3

4

3

3

2

2

3

3

2

4

1

5

2

2

3

3

3

3

3

4

2

3

3

2

2

2

3

2

1

3

1

1

3

4

2

2

2

3

3

1

1

2

3

2

2

2

3

1

1

2

1

1

1

1

1

23

36

39

46

12

42

27

13

44

0

36

8

26

28

48

25

57

21

30

56

58

60

25

53

34

40

40

57

0

41

34

26

66

57

39

32

0

13

0

11

0

0

10

0

14

0

0

0

12

0

7

7

0

0

0

0

0

7

0

8

8

0

0

0

0

521

393

549

467

477

533

537

418

722

441

686

625

685

419

537

501

636

564

425

927

708

862

490

504

614

776

607

1000

603

804

605

561

703

695

645

650

504

702

331

554

404

414

693

530

743

548

589

410

691

525

663

834

544

563

580

556

500

814

580

783

850

614

611

624

628

9

28

22

8

0

36

16

17

25

20

24

18

34

13

10

20

5

44

4

50

47

42

32

32

44

63

18

26

19

44

41

52

23

30

0

39

23

231

0

214

15

30

175

33

201

20

209

0

206

21

211

215

19

18

39

36

0

158

24

218

243

26

29

47

34

2

52

31

13

61

32

49

28

36

12

25

77

35

12

22

28

66

62

27

2

52

56

45

42

49

47

32

55

59

64

32

37

57

30

24

36

37

172

3

209

27

3

209

23

164

32

167

26

195

24

187

228

35

21

35

42

46

242

22

203

246

40

57

44

57

n
Sample Depth Ti V Cr Mn Fe Ni Cu Zn Rb Sr Y Zr Nb Mo Sn Sb Cs Ba La Ce 

Number (m) wt.% ppm ppm ppm wt. % ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm ppm

355

361

364

367

369

371

372

374

376

378

381

382

384

386

389

394

397

398

400

402

406

410

413

415

416

419

422

423

426

430

434

436

438

441

443

443

73.55

74.15

74.45

74.75

74.95

75.15

75.25

75.45

75.65

75.65

76.15

76.25

76.45

76.75

77.05

77.55

77.65

77.95

78.15

78.35

78.75

79.15

79.45

79.65

79.75

80.05

80.35

80.45

80.75

81.15

81.55

81.75

81.95

82.25

82.45

82.45

0.29

0.28

0.14

0.24

0.25

0.32

0.32

0.33

0.33

0.33

0.34

0.39

0.41

0.38

0.40

0.43

0.43

0.44

0.45

0.44

0.44

0.44

0.39

0.44

0.42

0.42

0.45

0.45

0.43

0.43

0.44

0.35

0.45

0.46

0.46

0.46

19

114

63

0

119

139

61

63

93

129

72

126

129

124

142

108

41

127

165

118

124

163

77

174

142

97

136

159

109

136

175

87

116

141

138

138

0

0

0

0

22

15

0

0

0

0

0

0

7

0

0

0

0

0

0

0

0

0

0

0

33

0

0

0

0

0

15

0

0

0

5

5

749

703

570

1000

2300

891

711

843

832

820

883

961

1200

934

959

958

941

1200

1300

1300

1400

1500

941

1300

1100

1100

1300

1100

925

1200

1300

747

1400

1300

1300

1300

3.76

3.53

1.95

2.88

3.20

4.66

4.05

4.17

4.06

4.09

4.04

4.55

4.89

4.54

4.82

4.95

5.02

5.45

5.20

5.19

5.37

5.45

4.56

5.17

4.85

4.86

5.23

5.14

4.90

4.96

4.98

3.47

5.30

5.40

5.37

5.37

29

37

21

17

30

22

24

26

19

21

21

34

26

31

3

32

27

31

26

27

3

24

28

32

26

24

25

26

25

24

29

17

27

31

26

26

39

44

17

34

36

36

36

35

40

42

46

48

58

55

51

48

53

49

63

59

54

60

49

55

57

52

57

57

50

59

57

44

55

57

60

60

94

88

44

66

65

90

101

91

102

112

108

138

151

143

151

160

157

158

165

159

160

159

143

159

155

148

154

159

156

190

148

115

151

161

166

166

132

120

47

82

89

134

148

136

175

174

158

232

231

205

228

238

237

242

263

255

254

255

240

249

244

254

254

264

256

242

258

226

241

265

255

255

528

698

0

971

656

247

232

261

277

273

247

298

275

282

277

273

281

280

288

270

298

271

313

282

293

308

300

291

305

304

317

384

314

295

273

273

13

13

9

15

24

21

24

22

15

14

24

15

16

13

13

16

9

21

14

9

17

19

10

14

23

10

22

9

20

18

19

10

21

12

23

23

111

105

62

101

135

127

112

161

107

110

99

84

75

81

73

68

68

62

59

65

61

60

81

64

68

70

59

67

62

66

78

116

61

55

54

54

16

5

1

3

14

18

16

7

14

14

5

15

18

12

15

17

16

16

17

20

17

20

17

19

18

18

15

17

17

15

18

16

15

18

18

18

8

5

1

3

2

3

2

0

1

2

0

2

2

2

2

1

1

2

0

2

1

2

2

1

1

1

1

0

1

2

2

2

2

1

1

1

4

3

5

4

4

3

2

3

3

5

4

4

2

3

5

3

3

3

3

3

4

4

3

5

4

8

3

3

4

4

3

3

4

3

4

4

2

3

1

2

2

1

1

2

3

2

1

1

1

1

2

1

1

2

1

1

1

1

2

1

1

1

1

1

1

1

1

1

3

1

1

1

8

0

10

11

8

0

0

9

0

9

15

0

13

0

0

0

8

8

0

0

0

0

9

7

0

12

0

0

0

10

0

16

0

0

10

10

807

765

796

961

853

604

676

866

697

946

990

1000

1100

1000

1100

1200

1300

1200

1100

1100

1200

1100

1200

1200

1200

1200

1100

1.100

1100

1300

1100

969

1100

1200

1200

1200

214

32

203

231

239

33

28

265

22

229

187

39

198

49

14

231

227

225

52

26

23

19

198

210

29

216

29

18

26

185

0

261

31

52

185

185

240

59

168

199

235

50

46

256

43

226

227

3

217

60

38

216

224

213

48

49

3

29

233

214

55

215

23

67

39

212

25

241

41

47

192

192
0 50 100 150 0.0 0.1 0.2 0.3 0.4 0.5 0 1 2 3 4 5 6 

IRM 03T/MS(x10 3 Am-1 ) Ti (wt. %) Fe (wt. %) 

Figure 1. Depth plots of magnetic susceptibility (MS), isothermal remanent magnetization (IRM) 

titanium (Ti), iron (Fe), and zirconium to Ti (Zr/Ti) ratio. The dark shaded pattern indic

that contain abundant greigite, on the basis of moderately high MS, very high values of I

within each interval, petrographically identified greigite in a magnetic-mineral separate f

sample. Other zones of abundant greigite may be present. The lighter shaded pattern de

examined intervals, in which greigite is absent or is very sparse and thus an unimportant 

magnetic signal.
U.S. DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY

DIATOM COUNT DATA AND OWENS LAKE 

PALEOLIMNOLOGY DURING THE LAST INTERGLACIAL

by 

J. Platt Bradbury1 and Marc Paquette l

Open-File Report 98-132 (part 7)

This report is preliminary and has not been reviewed for conformity with U.S. Geological 

Survey editorial standards (or with the North American Stratigraphic Code). Any use of 

trade, product, or firm names is for descriptive purposes only and does not imply 

endorsement by the U.S. Government

!U.S. Geological Survey, Denver, Colorado 80225

1998
Introduction

This report contains the diatom species count data for samples of cores OL-92/1 and OL92/2 from Owens Lake, Inyo County, California, that encompass depths between 32 and 

83 m. These depths span estimated ages between 46 ka and 137 ka and thereby 

encompass most of marine oxygen isotope stages 3,4, and 5, the last interglacial period. 

Details regarding coring methodology, core curation, and preliminary analytical data 

from these cores can be found in Smith and Bischoff (1993, 1997).

Taxonomy

Diatoms were identified as closely as possible to descriptions and illustrations of taxa in 

standard texts. However, the diatom flora of the western United States is poorly known, 

and some taxa from Quaternary deposits of distinctive paleolimnological environments 

are probably new to science. In some cases such taxa are recorded by "cf." or "aff." (= 

"compare with" or "with affinities to" respectively) in other cases they are lumped 

together with the taxon of closest similar morphological appearance.

The diatom count data appear in a spreadsheet (Table 1) with column headers that 

represent abbreviations of selected species or genera commonly appearing in the analyzed 

sediments. The taxon abbreviations and equivalent names (in italics) are given in the 

explanation preceding Table 1. Diatom taxa of rare occurrence or very restricted 

stratigraphic distribution are not included in this data set. Generic epithets in the Table 1 

explanation followed by "spp." include multiple species included within that genus.

Counts

The numbers in the spreadsheets represent un-modified counts of diatom valves of 

selected, abundant species or species groups in the Owens Lake cores. Diatom 

preservation may be poor in Owens Lake sediment because of breakage and corrosion. 

The counts represent whole valves and (or) large (> 40%) fragments of valves. Samples 

were processed according to the protocol described in Bradbury (1997a). The diatom 

species and group profiles presented in figures 1-3 are expressed in percentages. Because 

counts less than 100 valves are inadequate for establishing ecologically significant 

proportions of diatoms in fossil assemblages, these counts are down-weighted in the 

profiles. The assemblages at those levels will not sum to 100 percent on the figures.

Ecological groups

Diatoms are generally classified into taxa living in, or preferring, fresh (<2 %o tds) and 

saline (>4%o tds) waters. Many species found in the cores overlap in their salinity 

preferences and tolerances, and these guidelines cannot be taken too literally. For 

example, although most of the taxa considered "fresh" have optima well below l%o tds, 

they may inhabit waters 2 to 3 times more saline. "Saline" taxa, on the other hand, often 

tolerate (or even prosper in) a broad range of salinities above 4%o tds, but they may be 

also present in waters below 4 %c tds. Today, the Owens River has a salinity of about 

0.2%o tds (200 ppm), and this salinity level may have been typical of Owens Lake when it 

was overflowing.

The diatoms from Owens Lake can also be grouped into taxa that live in open water 

suspended by turbulence and those that reside on the bottom, moving along or attached to 

various substrates within the illuminated zone of the lake. These groups are referred to as 

planktic (open water) and benthic (bottom dwelling) species respectively. Additional
information about the ecology of the diatoms from Owens Lake cores can be found in 

Bradbury (1997a,b).

Letters in brackets [ ] on the following taxon list (Table 1 explanation) indicate ecological 

grouping of the taxon: S = saline, F = freshwater, p = planktic, b = benthic. 

Tychoplanktic "Fragilaria" and Synedra species have been grouped separately because 

they occupy either benthic or planktic freshwater habitats depending on turbulence. This 

variable ecological classification is represented by [Fb-p] in the Table 1 explanation.

Paleolimnology of Owens Lake during the last interglacial period

This part of the Owens Lake record begins at 83.7 m (136.6 ka) with a dominance of 

planktic freshwater diatoms (Figs. 1 and 2). Spring-blooming taxa are most abundant, 

implying that climatic conditions characteristic of spring-like conditions extended well 

into the summer months, perhaps as a consequence of increased cloudiness and cool 

weather (e.g., Hostetler and Benson, 1990). Between 83.7 m and 75 m (118 ka) the 

spring-blooming Stephanodiscus taxa steadily decline and are replaced by summer-, fall-, 

and winter-blooming diatoms (cold season Aulacoseira species). These assemblages may 

suggest that diatom productivity during the spring was impeded by excessive turbidity 

caused by glacial runoff and that production shifted to seasons later in the year. 

Significant numbers of Cyclostephanos (Fig. 3) imply elevated salinities (about 1000 

mg/L) during winter months following the major seasons of runoff. The abundance of 

cold-season Aulacoseira species at 76 m (120 ka) could indicate a reduction of turbidity 

sufficient to allow these species to prosper in the winter and early spring months. The 

predominant species, Aulacoseira islandica, blooms under ice in southern Canada and the 

Great Lakes today. This part of the core may correlate to the terminal phases of oxygen 

isotope stage 6.

According to the distribution of saline benthic and planktic diatoms (Fig. 1) arid climates 

that resulted in low, saline-water stages of Owens Lake began at about 74 m depth (116 

ka). Although the chronology of core OL-92 remains unconfirmed, freshwater 

environments at Owens Lake documented between 137 and 118 ka coincide with 

uranium-series dates on halite inter-beds in lacustrine muds in Death Valley 146 - 127 ka 

and with bedded salts deposited from a deep saline lake in Death Valley 128 - 120 ka 

(Lowenstein, 1994). This coincidence lends support to the Owens Lake chronology. On 

the other hand, the Devils Hole oxygen isotope record (Winograd et al, 1988) implies 

warmer air temperatures beginning 145 ka and continuing until 118 ka. The relation 

between warmer air temperatures and precipitation remains unclear although it is possible 

 assuming all chronologies are accurate that moisture supplying Owens Lake and 

Death Valley came from lower latitudes of the East Pacific Ocean in circulation patterns 

that resembled the present-day Southwest Monsoon.

Between 74 m and 60 m (116 - 89 ka) there are six well-defined episodes of freshwater 

conditions in Owens Lake that punctuate the generally saline lacustrine environments that 

document arid climates presumed to represent oxygen isotope stage 5. Some of these 

freshwater intervals may correlate with five bedded salt layers (indicating perennial 

saline lake conditions) recognized near the base of the Death Valley core and above or 

below a U-series date of 98.6 ka (Li and others, 1996).

Generally saline conditions persisted at Owens Lake from between 60 and 48 m (89 - 70 

ka). Fluctuations between saline planktic and saline benthic diatoms may indicate subtle 

variations in water depth throughout this period. At 48 m (70 ka), freshwater diatoms
again predominate, indicating a deep, fresh and overflowing lake in the Owens basin. 

This interval persists for about 7 ky and abruptly ends at 43 m depth (63 ka). In timing 

and character, the freshwater lacustrine conditions 70 - 63 ka probably represent oxygen 

isotope stage 4. Following this freshwater diatom assemblage, Owens Lake again 

became saline until 36 m depth (54 ka) when freshwater conditions returned and persisted 

until the Holocene (Bradbury, 1997b).

Overall, the fluctuations between fresh- and saline- water conditions at Owens Lake 

occurred very rapidly, sometimes between adjacent samples that represent only 200 

years. These rapid fluctuations testify to the sensitivity of Owens Lake to climatemediated hydrologic change.

References:

Bischoff, J.L., Stafford, T.W., and Rubin, M., 1997, A time-depth scale for Owens Lake 

sediments of core OL-92: Radiocarbon dates and constant mass-accumulation rate. 

In: Smith, G.I., and Bischoff, J.L. (eds.), An 800,000-year paleoclimatic record 

from core OL-92, Owens Lake, southeast California. Geological Society of America 

Special Paper.

Bradbury, J.P., 1997a, A diatom-based paleohydrologic record of climate change for the 

past 800 k.y. from Owens Lake, California: in Smith, G.I. and Bischoff, J.L. (eds.) 

An 800,000-year paleoclimate record from core OL-92, Owens Lake, southeast 

California: Boulder, Colorado, Geological Society of America Special Paper 317, p. 

99-112.

Bradbury, J.P., 1997b, A diatom record of climate and hydrology for the past 200 ka from 

Owens Lake, California with comparison to other Great Basin records: Quaternary 

Science Reviews, v. 16, p. 203-219.

Hosteller, S., and Benson, L.V., 1990, Paleoclimatic implications of the high stand of 

Lake Lahontan derived from models of evaporation and lake level: Climatic 

Dynamics, v. 4, p. 207-217.

Li, J., Lowenstein, T.K., Brown, C.B., Ku, T-L., Luo, S, 1996, A 100 ka record of water 

tables and paleoclimates from salt cores, Death Valley, California: Paleogeography, 

Paleoclimatology, Paleoecology, v. 123, p. 179-203.

Lowenstein, T.K., 1994, Death Valley salt core: 200,000 year record of closed-basin sub 

environments and climate [abs.]. Geological Society of America, Abstracts with 

Program, A-169.

Smith, G.I., and Bischoff, J.L., eds., 1993, Core OL-92 from Owens Lake, southeast 

California: U.S. Geological Survey Open File Report, OFR 93-683, 398 p.

Smith, G.I. and Bischoff, J.L. (eds.), 1997, An 800,000-year paleoclimate record from 

core OL-92, Owens Lake, southeast California: Boulder, Colorado, Geological 

Society of America Special Paper 317, 165 p.

Winograd, I.J., Szabo, B.J., Coplen, T.B., and Riggs, A.C., 1988, A 250,000 year climatic 

record from Great Basin vein calcite: implications for Milankovitch theory. Science, 

242, 1275-1280.
Figure Captions:

Figure 1. Stratigraphic distribution of saline benthic and planktic diatoms, and of 

freshwater planktic diatoms from Owens Lake cores OL-92/1 and OL-92/2 between the 

depths of 32 m (46 ka) and 83 m (137 ka). Selected ages taken from the age - depth 

model of Bischoff and others, 1997).

Figure 2. Stratigraphic distribution of freshwater diatom ecological groups from Owens 

Lake cores OL-92/1 and OL-92/2 between the depths of 32 m (46 ka) and 83 m (137 ka). 

"planktic (smr)" and "planktic (spg)"= planktic diatoms blooming in the summer to early 

fall and in the spring respectively. "Aulacoseira (wrm)" and " Aulacoseira (eld) = warm 

season [summer] and cold season [winter / early spring] species of Aulacoseira 

respectively.

Figure 3. Stratigraphic distribution of Fragilaria, Cyclostephanos, and Stephanodiscus 

"carconensis" from Owens Lake cores OL-92/1 and OL-92/2 between the depths of 32 m 

(46ka)and83m(137ka).
30 -,

benthic tychoplanktic planktic (smr) Aulacoseira (wrm) planktic (spg) 

0 40 0 

percent

40 0

80 
benthic saline planktic saline freshwater planktic 

30-, -, 30

40-

80-

90

0 perecent 80

0 80

F.J.I
30-i

Fragilaria Cyclostephanos Stephanodiscus "carconensis"

approximate age

 

<- 53 ka

90

80 0

percent

80 0

<- 65 ka

<-89ka 

<-95ka

<-120ka

136.6ka

50
Table 1. Abbreviation codes, species names and ecology of selected diatom taxa 

from Owens Lake cores.

code= taxon ecology

ach = Achnanthes spp. [Fb]

am-cof = Amphora coffaeiformis [Sb]

am-mac = Amphora macilenta [Sb]

am-oval = Amphora ovalis [Fb]

am-per = Amphora perpusilla [Fb]

ano-cos = Anomoeoneis costata [Sb]

ast-form = Asterionellaformosa [Fp]

au-amb = Aulacoseira ambigua [Fp]

au-gr = Aulacoseira granulata [Fp]

au-isl? = Aulacoseira islandica ? [Fp]

au-sarc = Aulacoseira subarctica [Fp]

au-sol = Aulacoseira solida [Fp]

cal = Caloneis spp. [Fb]

cam-cly = Campylodiscus clypeus [Sb]

chaet = Chaetoceros muelleri (usually spores) [Sp]

coc-pla = Cocconeis placentula [Fb]

coc-dim = Cocconeis neodiminuta [Fb]

coc-dis = Cocconeis disculus [Fb]

cyc-bod = Cyclotella bodanica [Fp]

cyc-dist = Cyclotella distinguenda [Fp]

eye-men = Cyclotella meneghiniana [Sp]

cyc-oce = Cyclotella ocellata [Fp]

cyc-quil = Cyclotella quillensis [Sp]

cymb = Cymbella spp. [Fb]

cymb-nz = Cymbellonitzschia diluviana [Fb]

cyst-pit = Cyclostephanos sp. [Fp]

cyst#10 = Cyclostephanos sp. [Fp]

epi = Epithemia spp. [Fb]

fr-brv = Fragilaria (Pseudostaurosira ) brevistriata [Fb-p]

fr-cap = Fragilaria caupucina [Fb-p]

fr-con = Fragilaria (Staurosira) construens + varieties [Fb-p]

fr-crot = Fragilaria crotonensis [Fp]

fr-lepto = Fragilaria (Staurosirella) leptostauron [Fb-p]

fr-pin = Fragilaria (Staurosirella) pinnata [Fb-p]

fr-vau = Fragilaria vaucheriae [Fb-p]

gom = Gomphonema spp. [Fb]

gyro = Gyrosigma spp. [Fb]

hz-am = Hantzschia amphioxys [Fb]

marty = Martyana martyi [Fb]

mel-sp. = Melosira species [Fb]

mel-var = Melosira varians [Fb]

nv-fw = freshwater Navicula spp. [Fb]

nv-sal = saline Navicula spp. [Sb]

nz-fw = freshwater Nitzschia spp. [Fb]

nz-fru = Nitzschia frustulum [Sb]

nz-mon = Nitzschia monoensis [Sb]

nz-pus = Nitzschia pusilla [Sb]

nz-rad = Nitzschia radicula [Fb]

nz-sal = saline Nitzschia spp. [Sb]

nz-sin = Nitzschia sinuata type [Sb}

pin = Pinnularia spp. [Fb]

reim = Reimeria sinuata [Fb]

rho-acu = Rhopalodia acuminata [Sb]

rho-con = Rhopalodia constricta [Sb]
rho-gbr = Rhopalodia gibberula [Sb]

rho-gib = Rhopalodia gibba [Fb]

rhoi = Rhoicosphenia curvata [Fb]

st-ast = Stephanodiscus asteroides [Fp]

st-car = Stephanodiscus sp. cf. St. carconensis [Fp]

st-car/ast = intermediate between S. asteroides and S. carconensis [Fp]

st-min = Stephanodiscus minutulus type [Fp]

st-nia = Stephanodiscus niagarae [Fp]

st-org = Stephanodiscus oregonicus [Fp]

st-ovec = Stephanodiscus sp. (oval and eccentric form) [Fp]

st-prv = Stephanodiscus parvus type [Fp]

su-hof = Surirella hoefleri [Sb]

su-ova = Surirella ovalis type [Sb]

su-str = Surirella striatula [Sb]

sy-acus = Synedra acus [Fp]

sy-bero = Synedra berolinensis [Fb-p]

sy-maz = Synedra mazamaensis [Fb]

sy-rum = Synedra rumpens types [Fb]

sy-uln = Synedra ulna [Fb]

Other column identifiers

z(m) = depth in core in meters.

ka = the estimated ages that correspond to the sample depths for the diatom counts. The age model for

the OL-92 cores is from Bischoff and others (1997).

count = total diatom valve count (includes diatom taxa not represented in spreadsheet).

trav = traverse length in mm on microscope slide along which diatoms were enumerated at 1000 X

magnification.

D/mm = diatom valves per mm of microscope traverse at 1000 X.
OL-92 (5+6) «

z<m)

32.31

32.32

32.72

33.32

33.68

3392

34.52

34.92

35.53

36.12

36.32

36.52

36.72

36.92

37.92

38.12

38.32

38.51

38.82

38.92

39.12

39.52

39.72

40.32

40.52

40.72 

40.92

41.12 

41.32

41.72

41.79

41.92

42.12

A9 19

42.52

42.72

42.92

43.13

43.32

43.52

43.72

43.92

44.12

44.32

44.72

44.92

45.12

45.32

45.38

45.52

45.72

45.92

46.12

46.5

46.52

48.72

47.12

47.32

47.52

47.72

47.02

ka

46.68

47

47.4

48.45

49.08

49.5

50.56

51.26

52.3

53.23

53.543

53.857

54.17

54.4S4

56.05

56.362

56.67

56.96

57.42

57.56S

57.86

58.157 

58.454

58.75

59.63

59.939

60.246 

60.52 

60.57

60.796 

61 .082 

S1.4

61.69

61.79

61.975

62.26

62.827

63.11

63.305

63.696

63.97

64.26

64.546

64. SB 

64.83

65.113

65.396

65.958

66.236

66.51

66.779

66.86

67.049

67.32

67.591

67.863

68.38

68.407

68.68

68.955 

69.231

69.51

69.793

70.077

70.36

ach

0

5

2

3

2

2

0

4

6

2

0

2

0

0

0

0

0

0

1

0

0

0

0

0

0

0 

0

0 

0

0

0

0

0

0

0

1

0

0

0

0

1

0

0

1

2

1

0

2

1

2

0

0

0

1

0

0

1

0

0

0

0

am- cot

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

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0

8

0

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3

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0

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0

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0 

0

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0

0

0

0

0

0

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0

0

0

0

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0

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0

0

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am-mac

0

0

0

0

0

0

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0

0

0

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0

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am- oval

1

0

1

1

3

1

0

1

4

2

1

1

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0

0

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0

2

1

0

1

1

0

2

1

1

0

0

1

1

2

0

0

0

0

2

1

0

am-pw

13

11

6

6

17

6

23

26

16

1

2

0

0

0

0

0

0

0

0

0

0 

0

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5

3

6

2

3

3

2

2

6

1

4

5

0

2

4

3

1

6

0

5

0

0

ano-cos

3

0

0

1

0

0

0

0

0

0

0

2

13

9

2

0

0

3

0

6

25 

2

0

7

3

1

0 

0 

0

0 

0 

0

0

0

0

0

5

5

3

2

2

0

0

0

2

0

0

1

0

0

1

0

0

1

0

0

0

0

0

0

55

55

ast-torm

11

S

0

8

38

3

IB

25

56

36

18

0

0

0

0

0

0

2

0

0

0

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0

0 

0 

0

0 

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10

7

1

5

10

4

21

4

0

5

4

2

3

12 

17

31

35

0

0

au-amb

73

64

164

205

32

6

54

41

24

24

26

1

0

0

0

0

0

0

0

0

0

2

0

0

0 

0 

0

0 

0 

0

1

0

0

0

0

0

1

0

7

4

2

36

58

39

16

21

15

2

41

12

20

37

69

20

IB

40

42

0

0

au-gr

57

SB

14

2

0

4

20

4

2

0

0

6

0

0

0

0

0

0

0

0

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8

3

4

6

2

5

8

6

4

8

24

23 

6

a

5

5

0

0

au-isl?

0

0

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au-sarc

0

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au-sol

0

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cal

0

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2

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1

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2

1

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0

0

0

0

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1

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0

0

1

0

0

0

0

0

0

0

0

0

0

cam-dy

0

0

0

0

0

0

0

0

0

0

1

2

13

6

5

0

1

3

34

1

17

0

58

10

2

0 

0

0

1

0

1

0

104

28

47

79

6

145

0

0

2

0

1

0

0

0

0

0

0

1

0

0

0

0

0

0

1

45

22

enact

0

0

0

0

0

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0

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0

0

0

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0

0

0

0

0

0

L 0

0

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0

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0

0

0

0

5

0

6

0

10

0

0 

0

1

0

0

0

0

1

0

0

0

0

0

0

0

0

0

0

2

38

4

coc-pla

2

1

6

6

7

10

5

6

7

1

5

1

5

6

0

0

1

0

0

0

0 

0

0

22

2

0

0 

0

0

0

0

2

0

1

0

0

5

0

0

2

1

2

5

1

4

3

0

2

1

4

1

0

1

3

1

2

1

3

1

11

coc-dim

0

0

5

0

4

1

5

1

0

1

0

0

0

0

0

0

0

0

0

0

0 

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0

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2

0

0

0

1

0

1

0

2

1

2

0

0

0

0

0

0

coc-dis

0

2

1

0

3

0

0

3

1

0

0

0

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cyc-bod

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0

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1

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cyc-dist

0

0

0

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0

0

0

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cyc-m«n

0

0

0

3

0

0

1

1

0

6

0

12

2

20

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

34

22

8

0

1

0

0

0

0

2

0

1

0

0

0

0

1

0

1

0

0

1

0

0

cyc-oce

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

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0

0

0

0

0

0

eye-quit

4

7

2

17

6

16

6

S3
OL-92 (5+6) *

z(m)

74.715

74.915

75.115

75.315

75.515

75.715

75.6975

76.165

76.365

76.625

76.625

77.025

77.16

77.225

77.425

77.625

77.625

78.025

76.245

76.39

78.445

78.645

76.645

79.045

79.245

79.405

79.465

79.675

79.9

60.075

60.275

60.475

60.675

80.675

81.075

61.275

81.42

61.475

81.675

61.875

62.075

62.275

82.475

82.675

82.875

83.075

83.275

83.475

63.55

83.675

ka

116.92

117.34

117.77

116.19

118.63

119.06

119.45

120.03

120.46

121.03

121.46

121.69

122.15

122.32

122.76

123.19

123.62

124.05

124.53

124.87

124.97

125.41

125.65

126.29

126.73

127.09

127.26

127.68

126.23

126.56

129

129.44

129.66

130.33

130.77

131.21

131.61

131.66

132.11

132.55

133

133.45

133.9

134.35

134.8

135.25

135.69

136.14

136.37

136.59

ach

0

2

2

7

4

5

9

11

11

12

9

12

6

5

4

7

7

5

6

3

4

5

3

0

2

1

1

1

2

2

1

2

4

1

1

5

0

0

0

0

2

1

2

0

1

6

5

2

2

0

am-cof

0

0

0

0

0

0

0

0

0

0

0

0

0

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0

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am -mac

0

0

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am- oval

0

0

0

0

1

0

0

0

2

0

2

2

2

1

0

0

1

0

1

0

0

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0

0

0

0

a

0

0

0

0

0

i

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

am-par

2

5

3

1

5

6

2

6

3

3

3

6

3

0

4

0

6

6

2

3

6

0

0

1

1

2

6

2

3

0

0

2

0

4

0

3

4

6

1

1

3

0

3

0

0

10

0

5

15

11

ano-cos

0

0

0

0

0

0

0

0

1

0

1

0

0

1

0

1

1

1

0

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

ast-form

0

3

0

9

16

9

14

20

6

7

8

2

0

0

0

5

0

3

0

54

17

3

10

5

7

16

7

3

6

0

0

6

0

10

0

16

7

10

5

0

10

18

2

0

0

14

6

20

35

91

au-amb

0

0

1

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

au-gr

0

8

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

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0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

au-lsl?

0

0

25

55

167

110

91

120

44

55

39

38

64

25

24

22

17

30

14

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

au-sarc

0

0

34

74

2

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

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0

0

0

0

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0

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0

0

0

0

0

0

0

0

au-sol

0

0

0

0

0

0

0

0

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0

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cal

0

0

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1

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1

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2

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0

0

0

0

0

0

0

2

0

2

0

0

0

0

0

0

0

0

0

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cam-dy

0

0

0

0

0

0

0

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0

0

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0

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cha*t

3

0

0

0

0

0

0

0

0

0

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0

0

0

0

0

0

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0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

coc-pla

6

1

7

4

9

7

3

6

9

11

6

13

10

9

4

5

6

6

6

9

5

10

5

6

5

4

3

4

3

4

2

5

3

4

2

2

10

5

5

6

6

7

11

9

1

7

2

6

9

5

coc-dim

0

2

5

3

8

4

2

0

2

2

0

1

2

0

1

0

1

0

1

L_ 8

3

0

1

1

0

0

0

1

1

0

0

0

0

0

1

0

0

0

0

0

0

0

3

0

0

0

0

0

1

0

coc-dis

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

0

0

0

0

0

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0

0

0

0

0

0

0

3

0

0

0

0

0

0

0

0

0

0

0

0

0

cyc-bod

0

1

0

20

0

0

0

0

0

0

0

0

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0

0

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cyc-dist

0

96

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

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0

0

0

0

0

0

0

0

0

eye-man

101

0

0

0

0

0

0

0

2

0

0

0

0

0

0

0

0

0

0

0

0

0

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0

0

0

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

cyc-oc*

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

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0

0

0

0

0

0

0

0

0

0

0

cyc-qu
OL-92 (5+6) *

z(m)

32.31

32.32

32.72

33.32

33.68

33.92

34.52

34.92

35.53

38.12

36.32

36.52

38.72

36.92

37.92

38.12

38.32

38.51

38.82

38.92

39.12

39.32

39.52

39.72

40.32

40.52

40.72

40.92

40.96

41.12

41.32

41.52

41.72

41.79

41.92

42.12

42.32

42.52

42.72

42.92

43.13

43.32

43.52

43.72

43.75

43.92

44.12

44.32

44.72

44.92

45.12

45.32

45.38

45.52

45.72

45.92

48.12

48.5

48.52

48.72

48.92

47.12

47.32

47.52

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ftio-co
OL-92 (5+6) *

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40.32

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40.6

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00.38

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0

0

0

0

0

0

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

0

0

0

0

0

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

nv-tw

0

0

3

8

1

0

0

0

2

0

0

1

1

1

0

0

4

0

0

1

0

0

0

2

2

0

2

0

0

0

1

0

0

0

1

1

2

0

0

2

0

2

0

5

0

0

1

4

1

2

4

5

0

4

6

6

3

1

5

3

0

2

2

1

2

1

nv-sal

2

7

2

1

0

0

0

0

0

0

0

0

1

3

1

2

1

0

0

1

12

0

0

0

0

0

1

0

0

0

0

0

7

2

2

4

a

2

i

2

0

26

1

4

4

0

4

0

0

1

3

0

0

1

0

0

0

0

2

47

14

0

0

0

0

1

nz-fw

0

13

6

4

0

0

5

2

6

0

0

1

0

30

3

5

13

0

1

2

4

0

0

0

0

0

1

0

1

0

0

5

20

1

18

7

11

11

11

1

0

27

1

1

0

0

5

2

2

1

4

47

1

2

4

0

2

1

1

36

1

1

2

0

2

4

nz-rad

0

0

0

3

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

nz-sal

0

0

0

0

0

0

0

0

2

0

0

0

0

62

0

0

0

0

0

4

6

0

5

0

0

0

0

0

9

3

0

0

0

0

0

11

2

0

0

0

2

13

2

2

3

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

2

0

0

0

0

0

nz-tru

0

26

5

26

0

0

7

13

10

4

2

3

5

76

14

4

35

0

17

3

3

18

30

15

50

0

0

0

4

4

2

18

66

2

72

30

30

36

16

20

38

at

a

11

10

6

8

6

4

13

2

1

0

0

0

0

4

11

1

3

10

3

0

0

1

3

nz-mon

60

0

0

0

0

0

0

0

0

0

144

65

126

10

32

62

80

170

2

18

37

23

6

0

0

0

56

0

46

8

2

2

4

11

0

7

1

0

2

1

0

4

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

2

0

0

0

0

0

0

rut-pus

0

0

0

0

0

0

0

0

0

0

0

0

0

6

0

0

1t7

16

12

0

aa

45

23

7

0

0

0

0

12

35

115

0

123

0

2

32

11

2

4

0

6

130

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

nz-sin

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

pin

0

0

0

1

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

0

1

0

0

0

0

0

0

0

0

1

0

0

0

0

0

0

0

0

0

0

0

1

1

4

0

1

0

0

0

1

1

0

0

0

0

0

2

1

1

0

0

0

2

0

r»lm

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

rho-acu

0

4

0

0

0

0

0

0

1

0

t

0

0

10

0

5

0

3

0

3

0

17

180

80

0

0

8

0

20

6

0

3

0

2

0

60

36

0

28

23

0

72

14

10

56

22

2

0

4

1

6

2

0

0

0

0

0

0

0

0

14

0

0

0

0

0

rho-co

2

7
OL-92 (5*6) *

z(m)

62.12

62.32

62.52 

62.685

62.72 

82.8

62.925

62.96

63.125

63.325

63.525

63.725

63.925

64.135

64.355

64.555

64.755 

64.94

65.155

65.355

65.555 

65.775

65.94

66.175

66.375

66.575

66.765

66.975

67.145

87.345 

67.49

67.745

67.945

68.145

68.345

68.59

68.745

68.945 

69.145

69.345 

69.545

69.745

70.035

70.235

70.495 

70.695

70.895

71.06

71.295 

71.495

71.695 

71.835

71.985 

72.06

72.135

72.285

72.435

72.585

72.735

72.93

73.695

73.895

74.095

74.295

74.37

74.515

k»

92.1

92.44

92.79 

93.086

93.1 

93.4

93.51

93.56

93.86

94.23

94.6

94.97

95.35

95.55

96.15

96.52

96.89 

97.19

97.64

96.01

98.39

99.07

99.55

99.94

100.33

100.7

101.11

101.45

101.84 

102.11

102.63

103.02

103.41

103.8

104.29

104.59

104.98 

105.37

106.19

106.6

107.19

107.6

108.54

108.95

109.38

109.76 

110.17

110.58 

110.87

111.17 

111.43

111.48

111.79

112.11

112.43

112.74

113.15

114.77

115.19

115.61

116.04

116.2

116.5

fr-c«p

0

0

0 

0

0 

0

0

0

0

0

0

0

0

36

55

135

49

9 4

8

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0 

0

0 

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

fr-con

7

11

15 

10

10 

62

7

3

19

36

6

13

12

16

19

30

11

23

1

0 

2

2

0

0

0

0

0

0

0

0

0

0

0

4

6

1 

0

0

0

0

0

0

0

12

4

0 

0

0 

5

3

4

0

0

2

0

0

14

1

12

14

0

fr-crot

0

0

0 

0

0 

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

fr-lepto

1

0

0 

2

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

fr-pln

2

0

1

1

0 

2

0

1

1

0

0

4

0

4

13

0 

8

3

0

0 

0

0

0

0

0

0

0

0

0

0

2

0

3

2

2 

0

0

0

0

0

0

0

4

1

0

0 

5

0

2

3

0

0

0

0

3

2

0

2

0

fr-v»u

0

2

0

4

0 

8

2

3

0

6

0

10

6

2

0

0 

0

12

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0 

0

0

2

0

0

0

0

0

0

0

0

0

4

gom

0

1

0 

0

0 

0

0

2

0

2

1

1

0

0

0

0

1

0

0 

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

2

0

0

0 

2

0

0

0

0

0

0

0

0

0

0

1

0

gyro

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

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

0

0

0

0

1

0

1

1

0

hi-*m

2

0

0

0 

0

0

0

0

1

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

2

0

0

0 

0

0

0

0

0

0

0

6

0

1

0

0

m«rty

0

0

1

0 

0

1

0

1

0

0

0

0

0

2

0

0 

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

3

0 

0

0

0

0

0

0

0

2

0

0

0

1

1

0

0

0

0

0

0

0

0

1

0

m«l-sp

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

m«l-vv

4

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

nv-fw

1

0

2

2

4

1

1

0

7

1

11

3

0

6

2

2

3

0

1 

0

1

0

0

0

0

0

0

0

2

0

0

0

4

0

1 

0

0

0

0

0

0

0

7

0

0

0 

0

0

0

6

0

0

2

5

2

1

3

2

nv-sal

0

0

2 

0

0 

0

0

0

2

1

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

3

0

65

71

2

62

0

0 

10

31 

0

0

0

2

0

2

0

0

4

0

0 

0

0

3

2

0

0

2

8

176

75

4

0

nz-fw

1

3

0 

3

3 

2

0

5

0

77

36

3

2

3

7

4

5

3

0

1 

0

1

0

0

0

0

0

0 

0

1

0

0

0

2

2

0

0

0

0

0

0

0

0

1

1

0 

0

0 

6

0

0

s

1

4

0

1

2

0

1

4

0

nz-r*d

0

0

0 

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0 

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

nz-Ml

0

0

0 

0

0 

0

0

0

6

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0 

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

nz-fru

7

2

0 

0

1

0

0

0

1

4

4

0

0

0

0

0

2

0

0 

0

4

0

0

0

0

0

0

5

7

0

0

8

0

0

0

0

0

0

0 

0

0

2

0

2

4

0 

20

0

0

0

0

0

2

12

0

2

0

0

0

nz-mon

1

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

2

0

0

0

0

0

0

0

0

2

0

1

1

0

1

0

0

0

2

4

1

7

0

0

0

0 

42

3 

207

0

10

1

0

7

3

0

7

4

1

0

0

nz-pu*

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

17

0

15

24

6

16

0

4

9 

87

0

0

3

0

8

0

0

16

0 

30

29

12

4

0

12

25

20

38

10

6

64

111

7

0

nz-iln

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

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

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

pin

0

0

0 

0

0

1

0

0

0

0

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

0

0 

0

0

0

1

0

0 

0

1

2

0

0

0

0

0

0

0

0

0

0

0

0

reim

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0 

0

0 

0

0 

0

0

0

0

0

0

0

0

1

0

0

0

0

rho-*cu

0

0

0 

0

0

3

0

3

2

1

3

0

0

1

0

0

2

5

39 

19

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

0

0

0

3

0

4

1 

0 

0

1 

0

1

1

0

0

0

1

0

0

0

0

0

0

rho-con
OL-02 (5+6) #

z(m)

74.715

74.015

75.115

75.315

75.515

75.715

75.8075

76.165

76.365

76.625

76.825

77.025

77.16

77.225

77.425

77.625

77.825

78.025

78.245

78.30

78.445

78.645

76.845

70.045

70.245

70.405

70.485

70.675

70.0

80.075

80.275

80.475

80.675

80.875

61.075

61.275

81.42

81.475

81.675

81.875

82.075

82.275

82.475

82.675

82.675

83.075

83.275

83.475

83.55

63.675

ka

116.02

117.34

117.77

118.10

116.63

110.06

110.45

120.03

120.46

121.03

121.46

121.80

122.15

122.32

122.76

123.10

123.62

124.05

124.53

124.87

124.07

125.41

125.65

126.20

126.73

127.00

127.26

127.68

128.23

128.56

120

120.44

120.88

130.33

130.77

131.21

131.61

131.66

132.11

132.55

133

133.45

133.0

134.35

134.8

135.25

135.60

136.14

136.37

136.50

fr-cap

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

fr-con

2

15

18

26

6

10

24

7

5

33

10

25

5

0

3

0

1

5

8

2

3

3

0

5

5

10

1

4

0

2

2

0

2

0

0

0

0

2

3

0

2

0

2

6

1

6

3

8

7

6

fr-crot

0

56

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

tr-lepto

0

0

0

0

1

0

0

0

0

0

0

0

2

0

0

0

0

0

0

2

0

0

0

0

0

0

0

0

 2

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

fr-pin

0

0

11

2

2

1

8

4

4

2

14

6

8

0

2

1

0

0

3

4

2

1

0

0

2

0

0

1

0

0

0

0

0

0

2

0

1

0

0

0

0

0

2

0

0

0

0

2

3

0

fr-vau

2

0

2

2

5

2

5

0

1

0

0

0

2

0

2

0

0

0

0

6

0

0

0

2

0

0

0

0

2

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

1

0

0

0

2

0

gom

0

1

0

0

2

2

0

0

1

0

1

1

4

2

0

1

0

0

0

0

0

1

1

0

0

0

0

0

1

2

1

0

0

1

0

0

2

0

4

0

0

0

0

0

0

0

4

1

2

0

gyro

0

1

3

1

1

1

0

5

0

1

0

0

0

0

0

0

1

0

0

0

0

3

1

0

0

1

0

0

0

0

0

1

2

0

0

0

0

0

0

0

0

1

0

0

0

0

1

1

1

0

hz-am

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

1

0

0

0

0

0

0

0

1

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

marty

0

1

0

3

6

0

2

2

2

8

6

3

2

6

4

5

6

4

7

0

0

2

2

0

2

0

2

2

0

0

0

1

0

0

0

,__ 0

0

1

0

0

2

0

0

1

0

1

2

1

0

0

mel-ap

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

mel-var

0

0

0

0

0

0

0

0

0

0

0

0

2

2

0

2

0

0

0

0

0

1

0

1

0

0

2

1

0

0

0

5

t

1

2

6

2

3

4

5

6

0

25

12

6

7

12

11

10

11

nv-fw

4

12

to

15

7

6

23

11

18

13

6

8

18

13

11

3

4

0

IB

25

2

12

2

3

4

5

1

5

14

0

0

3

0

7

2

5

5

3

8

1

6

3

6

4

5

6

6

7

12

0

nv-Ml

0

0

0

0

1

0

0

0

0

0

1

0

0

0

0

0

0

0

0

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

0

0

0

0

2

nz-tw

64

5

2

1

12

13

6

3

8

18

0

0

13

11

6

3

10

7

0

10

7

2

1

5

5

2

4

4

16

2

0

2

2

12

6

4

20

4

2

2

7

3

8

2

1

6

2

11

20

6

nz-rad

77

0

0

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

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

nz-Ml

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

nz-fru

0

3

0

0

0

0

0

0

0

0

2

0

4

0

0

0

0

4

0

0

2

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

2

0

nz-mon

0

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

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

nz-pus

0

0

0

0

0

0

0

0

0

0

0

0

2

0

0

0

0

0

0

0

0

0

0

0

0

0

2

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

nz-sin

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

pin

0

0

0

0

1

0

0

0

1

0

0

0

4

0

1

0

2

1

0

0

0

0

0

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

2

1

2

0

reim

0

0

1

0

0

0

0

1

1

0

0

1

0

1

0

0

0

0

0

0

0

1

0

0

0

0

0

3

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

2

0

rho-acu

0

0

0

0

0

1

0

0

0

1

0

1

0

5

1

1

0

0

0

0

0

0

1

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

rtiO'Co
OL-92 (5+6) »

z(m)

32.31

32.32

32.72

33.32

33.68

33.92

34.52

34.02

35.53

36.12

36.32

36.52

36.72

36.02

37.02

38.12

38.32

38.51

38.82

38.92

39.12

39.32

30.52

30.72

40.32

40.52

40.72

40.92

40.06

41.12

41.32

41.52

41.72

41.79

41.92

42.12

42.32

42.52

42.72

42.92

43.13

43.32

43.52

43.72

43.75

43.92

44.12

44.32

44.72

44.92

45.12

45.32

45.38

45.52

45.72

45.92

48.12

46.5

46.52

46.72

46.92

47.12

47.32

47.52

47.72

47.02

k*

46.68

47

47.4

48.45

49.08

49.5

50.56

51.26

52.3

53.23

53.543

53.857

54.17

64.484

56.05

56.362

56.67

56.98

57.42

57.566

57.86

58.157

58.454

58.75

50.63

50.939

60.246

60.52

60.57

60.796

61.092

61.4

61.69

61.79

61.075

62.26

82.544

62.827

63.11

63.395

63.896

63.07

64.26

64.548

64.59

64.83

65.113

65.396

65.058

66.236

66.51

66.779

66.86

67.049

67.32

67.501

67.863

68.30

68.407

68.60

68.055

69.231

60.51

60.703

70.077

70.36

st-min

1

1

0

4

4

0

0

0

6

0

15

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

7

0

6

60

13

0

1

0

0

0

2

0

0

0

3

0

0

3

0

1

0

5

3

0

0

st-nii

60

51

50

60

69

7

73

73

26

72

72

0

1

1

1

0

0

0

2

0

0

0

0

5

0

0

0

0

1

1

0

0

1

0

1

0

0

0

2

1

42

3

2

65

70

65

106

59

66

42

70

77

40

53

24

30

62

70

103

35

49

36

57

110

0

4

st-org

13

a

2

6

5

6

7

7

0

21

8

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

3

0

0

2

2

0

7

3

0

0

1

0

2

0

3

0

5

0

5

0

0

7

5

0

IS

28

0

1

st-ov»c

1

0

0

1

0

1

2

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

0

0

0

0

0

st-prv

0

0

0

0

0

0

0

0

3

16

0

0

0

0

0

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

0

0

0

0

18

2

1

0

0

22

0

0

0

8

6

0

0

0

0

3

0

0

0

0

0

su-hof

0

0

0

0

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

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

13

0

Ht-OVI

1

0

0

0

0

0

2

1

0

1

4

33

13

110

3

0

0

3

0

1

4

0

0

5

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

2

4

3

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

0

16

6

su-*tr

0

0

0

0

1

0

0

0

0

6

0

0

20

28

1

0

0

3

0

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

6

3

8

14

15

26

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

i 0

6

0

0

0

0

sy-icus

7

15

5

5

2

1

14

16

a

9

1

2

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

5

0

1

1

0

1

0

0

0

sy-bwo

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

sy-maz

0

0

0

0

0

2

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

sy-rum

0

0

0

0

3

0

0

0

0

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

0

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

sy-uln

0

0

1

4

6

0

2

1

1

1

1

2

0

0

0

0

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

1

1

2

0

1

0

0

0

1

0

1

0

0

1

0

0

2

0

0

0

0

1

0

1

0

0

count

497

447

449

495

458

287

551

525

484

511

418

385

139

268

16

1

2

31

95

14

89

13

0

142

51

4

0

0

1

1

0

0

15

0

15

0

0

297

161

247

361

353

241

488

502

384

501

511

474

480

480

487

472

467

476

484

501

402

501

427

496

480

434

480

288

102

trav

5

10

5

10.8

7

17.6

17

14

14

10

12

a

35

35

35

35

35

35

35

35

35

36

36

35

35

35

36

35

36

36

36

35

37

36

36

35

36

36

35

17.5

35

17

36

13

5

13

9

8.5

13.5

a. s

12

12

5

8

a

a

6.5

a

10

7

7

7

8.1

12

38

34

D/mm

99.4

44.7

89. a

45.8

_ 65.4

16.3

32.4

37.5

34.6

51

34. a

48.1

3.9

7.7

0.5

0.03

0.06

0.09

2.7

0.04

2.5

0.4

0

4.1

1.5

0.1

0

0

0.03

0.03

0

0

0.4

0

0.4

0

0

8.3

4.6

14.1

10.3

20.8

6.7

37.5

100.4

29.5

55.7

60.1

35.1

56.5

40

40.6

94.4

58.4

50.5

60.5

77.1

50.3

50.1

61

70.0

68.4

53.6

40

a

5.6
OL-92 (5+6) »

z(m)

47.00

40.32

40.52

40.6

40.72

40.82

40.02

50.12

50.32

50.40

52.2

52.5

52.72

52.02

53.12

53.32

53.35

63.52

53.72

53.02

54.12

54.32

54.52

54.7

54.8

54.02

55.52

55.72

55.02

56.32

56.5

56.72

56.02

57.12

57.32

57.52

57.72

57.76

57.02 

58.12

58.32

58.52

58.72

58.02

58.05

50.12

50.32

50.52

50.72

50.02

60.12

60.32

60.52

60.63

60.72

60.02

61.12

61.32

61.32

61.52

61.72

61.73

61.02

ka

70.458

72.334

72.63

72.75

72.021

73.061

73.2

73.470

73.76

74

76.411

76.83

77.136

77.417

77.7

77.086

76.03

78.260

78.55

78.842

70.14

70.44

70.74

80.016

80.17

80.36

81.27

81.577

81.884

82.40

82.76

83.1

83.410

83.743

84.07

84.308

84.724

84.70

85.360

85.680

86.012

86.338

86.67

86.72

87.000

87.340

87.680

88.020

66.360

88.700

80.040

60.34

80.53

80.60

00.03

00.38

00.500

00.7

01.07

01.41

01.43

01.76

st-mln

0

0

0

2

0

0

1

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

0 

0

0

0

0

0 

0

0

3

0

0

0

0

0

1

0

0

0

0

0

2

0

0

1

15

0

15

2

21

20

0

0

0

0

0

0

0

0

1

«t-nla

2

1

1

6

5

1

4

6

2

0

1

0

0

5

2

4

2

4

5

0

1

1

2

0

1

0

0

1 

0

1

5

4

0

4

2

1

1

0

1

1

0

6

1

4

0

0

0

0

1

0

70

57

77

1

3

0

0

3

2

1

2

2

st-org

2

0

0

0

0

1

0

0

0

0

0

0

1

0

1

0

0

1

0

0

0

1

0

0

1

1

1

0

3

0

1

0

0

0

1

1

1

0

1

3

2

1

2

5

0

1

40

7

0

3

0

0

0

0

1

0

0

0

0

»t-ov»c

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

*t-prv

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

2

0

1

7

0

0

0

0

0

0

0

0

0

 u-hof

0

11

0

0

0

0

58

6

0

2

1

0

0

0

0

0

0

0

0

0

1

5

2

1

0

0

0

0

0

15

42

27

31

32

31

32

10

12 

6

4

1

3

0

0

0

0

0

0

0

0

0

0

0

5

0

8

0

0

1

0

0

0

su-ova

0

0

11

22

3

1

0

2

0

0

0

0

0

5

1

0

0

0

1

2

0

14

0

0

0

0

2

0

0

15

1

20

21

0

2

1

3

0

1

4

5

1

2

1

1

0

0

0

1

2

1

0

0

0

1

6

0

1

0

1

0

su-str

2

0

0

0

68

2

0

0

0

0

2

0

0

1

0

1

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

1

1

0

0

0

0

0

1

0

12

3

4

1

5

5

7

0

0

0

0

0

0

0

0

0

0

1

0

3

10

«y-acus

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

1

0

0

0

0

0

0

3

1

0

0

0

2

0

0

0

0

0

1

1

0

0

0

sy-bwo

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

sy-maz

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

2

0

0

0

0

0

0

0

0 

2

0

0

0

0

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

sy-rum

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0 

0

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

5

0

0

0

0

1

0

0

0

0

sy-uln

0

0

0

0

0

0

0

0

0

0

1

0

1

0

0

0

0

0

2

2

0

0

1

1

0

2

0

0

1 

1

0

0

1

2

1

0

1

2

2

0

4

0

3

0

3

1

0

3

0

0

1

0

2

0

0

0

1

1

2

2

3

2

1

count

202

316

232

263

272

213

151

161

384

63

207

120

216

505

133

184

387

270

67

173

305

230

370

183

84

0

7

178

101

47

383

222

308

547

260

260

181

06

221

250

318

376

204

308

333

432

508

523

440

522

450

418

624

143

165

334

100

88

166

75

100

220

trav

36

36

17.5

34.0

35

2.5

35

36

35

35

36

35

36

17.5

35

36

35.6

36

35

36

36

35

18

36

34

35

35

36

36

36

28.3

35.7

36

36

34.8

36

36

35

36

36

36

36

36

17.6

6.1

11

18

11

7

4

0

18

7.4

36

36

34.7

36

34.8

36

34.4

35

35.6

D/mm

5.6

8.8

13.3

8.1

7.8

85.2

4.3

4.5

11

1.8

5.8

3.7

6.1

34

3.8

5.1

10.0

7.5

1.0

4.0

8.5

6.6

20.6

5.1

2.5

0

0.2

4.0

2.8

1.3

13.5

6.2

11.1

15.2

6.3

7.5

5

2.7

12.2 

6.1

5.7

8.8

10.4

8.2

22.8

54.6

30.3

33.2

47.5

64

130.5

50

23.2

84.3

4

4.6

0.6

5.5

2.5

4.6

2.2

5.4

6.2
OL-92 (5+6) #

z(m)

62.12

62.32

62.52

62.685

62.72

62.8

62.925

62.96

63.125

63.325

63.525

63.725

63.925

64.135

64.355

64.555

64.755

64.94

65.155

65.355

65.555

65.775

65.94

66.175

66.375

66.576

66.765

66.975

67.146

67.345

67.49

67.745

67.945

68.145

68.345

66.59

66.745

66.945

69.146

69.345

69.545

69.745

70.035

70.235

70.496

70.695

70.896

71.06

71.295

71.495

71.695

71.835

71.985

72.06

72.136

72.286

72.435

72.585

72.735

72.93

73.695

73.895

74.096

74.295

74.37

74.616

ka

92.1

92.44

92.79

93.086

93.1

93.4

93.51

93.56

93.86

94.23

94.6

94.97

95.35

95.55

96.15

96.52

96.69

97.19

97.64

96.01

96.39

98.6

99.07

99.55

99.94

100.33

100.7

101.11

101.45

101.84

102.11

102.63

103.02

103.41

103.8

104.29

104.59

104.96

105.37

105.78

106.19

106.6

107.19

107.6

108.13

108.54

106.95

109.38

109.76

110.17

LllO.58

110.87

111.17

111.43

111.48

111.79

112.11

112.43

112.74

113.15

114.77

115.19

116.61

116.04

116.2

116.5

st-min

0

0

0

3

0

7

7

0

0

15

2

4

15

4

6

4

1

0

77

0

3

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

3

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

2

1

0

0

0

2

0

0

0

0

st-nfa

0

2

4

0

0

3

0

0

3

1

2

76

9

37

35

28

29

31

5

4

2

1

1

1

1

0

1

0

0

2

0

1

4

4

5

26

17

10

7

3

0

0

0

0

0

3

2

13

17

5

2

4

2

15

6

7

8

9

6

4

1

43

1

6

3

1

st-org

1

0

1

4

6

19

9

0

0

7

0

7

0

5

13

19

8

4

2

1

1

0

2

0

0

0

0

0

0

0

0

1

0

4

0

1

1

3

0

0

0

0

0

0

0

0

1

3

3

0

0

0

0

3

0

0

0

1

0

0

0

1

0

0

1

0

st-ov«c

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

2

0

0

0

0

0

0

0

0

0

0

0

0

st-prv

0

0

0

0

0

0

0

0

0

4

0

0

0

13

10

6

1

0

17

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

2

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

7

0

0

3

4

0

0

0

12

0

0

0

40

tu-hof

6

1

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

3

3

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

2

0

0

0

2

0

su-ova

1

1

4

0

1

0

3

4

4

13

29

2

1

0

2

0

0

0

15

29

35

13

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

4

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

3

0

0

1

3

0

6

41

0

0

3

0

10

*u-str

24

15

3

0

0

0

14

2

7

3

16

10

0

0

0

0

0

0

1

0

0

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

sy-acus

0

0

0

0

0

0

1

0

0

0

0

8

6

7

1

12

4

1

5

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

1

20

6

5

0

0

0

0

0

0

0

0

0

2

3

0

0

0

0

11

0

0

3

3

0

1

0

5

0

2

0

131

sy-b«ro

0

0

0

0

0

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

0

0

0

0

0

0

0

0

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

0

sy-maz

0

0

0

0

0

0

0

0

0

0

0

0

8

7

0

2

0

0

0

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

sy-rum

0

1

0

4

0

0

0

0

0

0

0

0

1

0

0

0

0

0

15

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

2

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

sy-uln

0

0

1

0

0

0

0

3

0

1

0

0

0

1

0

0

1

1

1

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

1

0

1

0

0

0

0

0

0

0

0

0

3

1

0

1

0

0

0

1

1

4

1

0

1

1

2

1

1

1

0

count

262

315

391

450

362

519

395

369

334

561

332

617

507

492

461

512

520

386

426

99

171

65

47

6

5

0

6

2

21

4

4

99

120

27

121

340

109

77

144

20

0

6

11

2

0

28

10

236

136

25

5

97

39

495

26

47

131

126

65

92

131

314

328

350

86

418

trav

36

35

17.6

9.5

12.5

6.1

18

10.1

36

18

36

18

5

6

6

5.7

4

4

5

36

36

36

35

36

36

35

36

36

36

36

35

36

36

36

36

37

38

36

36

36

36

36

36

36

36

36

36

35

36

36

36

36

36

31.4

36

36

36

36

36

36

36

36

18

36

36

3

D/mm

7.3

9

22.2

47.4

29

85.1

21.9

36.5

9.3

31.2

9.2

34.3

101.4

82

80.2

89.8

130

97

85.6

2.75

4.75

1.8

1.3

0.17

0.1

0

0.2

0.06

0.6

0.1

0.1

2.75

3.3

0.8

3.4

9.2

3

2.1

4

0.6

0

0.2

0.3

0.06

0

0.8

0.3

6.7

3.8

0.7

0.1

2.7

1.1

15.8

0.7

1.3

3.6

3.5

1.8

2.6

3.6

8.7

18.2

9.7

2.4

139.3
OL-92 (5+6) »

z(m)

74.715

74.915

75.115

75.315

75.515

75.715

75.8975

76.165

76.365

76.625

76.825

77.025

77.16

77.225

77.425

77.625

77.825

78.025

78.245

78.39

78.445

78.645

78.845

79.045

79.245

79.405

79.485

79.675

79.9

80.075

80.275

80.475

80.675

60.875

61.075

61.275

61.42

81.475

81.675

81.875

82.075

82.275

82.475

62.675

82.875

83.075

83.275

83.475

83.55

83.675

ka

116.92

117.34

117.77

116.19

118.63

119.06

119.45

120.03

120.46

121.03

121.46

121.89

122.15

122.32

122.76

123.19

123.62

124.05

124.53

124.87

124.97

125.41

125.65

126.29

126.73

127.09

127.26

127.68

128.23

128.56

129

129.44

129.88

130.33

130.77

131.21

131.61

131.66

132.11

132.55

133

133.45

133.9

134.35

134.6

135.25

135.69

136.14

136.37

136.59

ct-mln

0

2

0

4

0

2

2

3

4

0

0

5

0

1

6

2

2

1

14

0

2

0

0

1

3

0

1

1

0

0

3

1

0

7

0

2

0

6

4

6

6

7

0

0

0

12

8

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17.2
U.S. DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY

OSTRACODES FROM OWENS LAKE CORE OL-92 AND THE 

PALEOENVIRONMENT OF THE LAST INTERGLACIAL

by 

Richard M. Forester 1 and Claire Carter^

Open-File Report 98-132 (part 8)

This report is preliminary and has not been reviewed for conformity with U.S. Geological Survey 

editorial standards (or with the North American Stratigraphic Code). Any use of trade, product, or 

firm names is for descriptive purposes only and does not imply endorsement by the U.S. 

Government.

!U.S. Geological Survey, Denver, Colorado 80225 

2U.S. Geological Survey, Menlo Park, CA 94025

1998
ABSTRACT

The Owens Lake core taken by the U. S. Geological Survey in 1992 (OL-92) was sampled at 20 

cm intervals in the section from 32 m to 89.6 m deep (46 ka to about 150 ka) in order to establish the 

nature of short-term limnologic and climatic variability within this system. Ostracode species were 

found in most samples including the environmentally well- known Cytherissa lacustris, Candona 

caudata, Limnocythere ceriotuberosa, and L. sappaensis. These species show that the 

paleoenvironment varied from a freshwater boreal-forest like lake to a high-alkalinity saline lake. 

Those environments appear to be associated with known changes in regional climate and can be 

related to the magnitude and persistence of surface versus base flow in the Owens River. The timing 

of polar air retreat from this region using the Owens Lake age model is consistent with the timing of 

that event in Devils Hole. The penultimate interglacial apparently was much wetter than the Holocene 

and may have been cooler.

INTRODUCTION

A long sedimentary core was taken from Owens Lake, California in 1992 by the U.S.Geological 

Survey in order to acquire a continuous climate record of the last 800,000 years (Smith and Bischoff, 

1993). Results from studies of that core are described in Smith and Bischoff (1997a). Recently the 

core was sampled for ostracodes in more detail in the interval from the penultimate glacial (oxygen 

isotope stage 6, about 135-170 ka) to about 46 ka to obtain a better understanding of the variability of 

the paleoenvironment and to better understand the nature of the previous interglacial (oxygen isotope 

stage 5, about 70-135 ka). This report focuses on the general nature of the ostracode data in those 

samples and provides a preliminary interpretation of the ostracode data (see section on ostracodes 

and their environmental preferences, below).

MATERIALS AND METHODS

Ostracodes were sampled by taking 5-cm-thick samples, usually weighing 50 to 80 g, every 20 

cm. Each sample was then split into two fractions. The first fraction, weighing about 15 g, was 

processed to obtain an ostracode species valve count. The remaining material was used in other 

studies such as stable-isotope analysis of the ostracode shells. Sample preparation followed a 

standard procedure (Forester, 1991; Carter, 1997). The prepared sediment was then examined for 

ostracodes and any adult valves were counted. The resulting valve counts are presented in tabular 

form in Table 1 and in graphic form in Fig. 1.

OSTRACODES AND THEIR ENVIRONMENTAL PREFERENCES

Ostracodes are small bivalved crustaceans having a carapace consisting of two valves (shells) made 

of calcite. The ostracode valve can be easily identified to species by its distinctive ornamentation and 

shape. Ostracodes live in many continental aquatic environments including ground water, springs 

and seeps, streams, wetlands, and lakes (Forester, 1987, 1991). In fact, many ostracode species are 

limited to a particular hydrological environment such as a spring or a lake, and as such, provide 

environmental information.

Ostracode species are also sensitive to the temperature of the water in which they live. As a 

consequence of their temperature sensitivity, ostracode species have discrete biogeographic 

distributions. In the case of lacustrine species, their biogeographic distributions may be described in 

climate terms. Similarly, ostracode species are sensitive to the chemistry of their environment 

(Delorme, 1969, 1989; Forester, 1983, 1986, 1987), particularly the ratio of alkalinity to calcium in 

their environment (Forester, 1991).

When an ostracode species' environmental preference (e.g. spring or lake) and its temperature and 

chemistry requirements are both known, the identification of that species provides detailed 

paleoenvironmental information. Ground-water and ground-water-discharge ostracodes provide 

information about past hydrology. In the case of lacustrine and, to some extent, wetland taxa, they 

give information on climate (Forester and Smith, 1994; Forester and others, 1994).

SUMMARY PALEOENVIRONMENTAL HISTORY, 65-150 KA

Table 1 shows the abundance, expressed in adult valves per sample, of ostracode species found in
each sample from the Owens Lake core between 32 m and 89.6 m below the surface. The most 

common ostracodes in this interval are Limnocythere ceriotuberosa Delorme and L. sappaensis 

Staplin. Candona caudata Kaufmann and Cytherissa lacustris (Sars) are also present. The 

stratigraphic distribution of these four species, expressed in valves per gram of raw sediment, is 

graphically depicted in Fig. 1. Other species identified from these samples (see table 1) are either rare 

or are taxa with little environmental data. These other taxa are not considered further in this report.

The following paleoenvironmental interpretation of Owens Lake is based on the biogeographic 

distribution and chemical preferences of these species derived from largely unpublished ostracode 

and chemical data. These data were collected from springs, wetlands, lakes, and a few streams at 

about 800 localities throughout the United States by Don Palmer and Alison Smith (Kent State 

University), Brandon Curry (Dlinois State Geological Survey), and many people from the USGS. 

L. Denis Delorme (1989) collected ostracodes and environmental data from over 3500 sites in 

Canada.

Cytherissa lacustris, Candona caudata, Limnocythere ceriotuberosa, and L. sappaensis all live in 

lakes, but the chemical and thermal characteristics of the lakes inhabited by these species are quite 

different (Delorme, 1989; Forester, 1986, 1987, unpublished data). In addition, C. caudata is a 

common inhabitant of streams and L. sappaensis occurs in some spring pools and wetlands. 

Limnocythere ceriotuberosa and L. sappaensis commonly live in slightly saline to saline water 

having a high alkalinity to calcium ion (alk / Ca) ratio (Forester, 1983, 1986).

Within the Owens Lake drainage, C. caudata presently lives in the Owens River and in a number 

of lakes at up to about 3,000 m elevation in the Sierra Nevada mountains. Limnocythere sappaensis 

lives in slightly saline to saline springs, such as Dirty Sock, and in wetlands having high alk/Ca 

(meq/L) ratios (> 7) along the Owens River. Limnocythere ceriotuberosa lives in Diaz Reservoir, 

which varies seasonally in volume and total dissolved solids (TDS) and has a moderately elevated 

alk/Ca ratio of just over 3, but it has not been found elsewhere in the Owens River drainage.

Cytherissa lacustris does not live in the Owens River drainage, nor in any lake south of Canada 

with the exception of rare occurrences in the Great Lakes and in Yellowstone Lake. In Canada and 

Alaska, C. lacustris lives in dilute cold lakes in the boreal forest and northward into the arctic circle. 

Delorme (1989) reports the upper TDS tolerance of C. lacustris at 300 mg/L. TDS alone, however, 

does not account for the distribution of C. lacustris. It is a species of both cold lakes and lakes that 

are chemically and thermally stable from season to season, either not changing or changing 

gradually.

The biogeographic distribution and temperature and chemical preferences of these four ostracode 

species provide a means of understanding the probable climate history of the Owens Lake area from 

46-150 ka. A preliminary and simplified interpretation of the ostracode data is as follows: the 

presence of C. lacustris implies the residence of polar-air in the Owens Lake region, the same air 

mass found today in the boreal regions of Canada and southern Alaska. The residence of polar air in 

the Owens Lake drainage implies the existence of continental ice sheets on the North American 

landscape that force and maintain polar air to the south. When C. lacustris disappears from the 

Owens Lake fossil record (the core), it suggests that the polar air has retreated northward, and further 

implies the initiation of deglaciation.

Candona caudata co-occurs with C. lacustris in the fossil and modern-day records, but also lives 

in lakes and streams well south of Alaska and Canada. In fact, the southern-most distribution of this 

species is in southern Nevada (Forester, unpublished data). Its upper TDS limit is about 3,000 

mg/L, so the presence of C. caudata and the absence of C. lacustris implies freshwater, but probably 

with higher air temperatures. For these ostracodes to survive, flow in the Owens River must also 

have been sufficient on a seasonal basis to maintain freshwater, river-like, conditions within the lake 

basin. Because evaporation on the valley bottom today is quite high (Smith and Bischoff, 1997b) 

and the lake basin is saucer shaped, which promotes evaporation, flow in the Owens River would 

presumably have to be higher and/or evaporation lower than today to maintain a C. caudata 

environment.

Limnocythere ceriotuberosa typically lives in lakes that exhibit strong seasonality in volume and
associated chemistry. It is has been found living in lakes with a TDS as low as 400 mg/L and as 

high as 12,000 mg/L (unpublished data). A common setting for this species would be a lake that 

becomes larger and is freshened by a seasonal gain in surface water flow, but that later becomes 

smaller and more saline when the stream returns to base-flow. Typically, such lakes are found in 

semi-arid settings located within the temperate latitudes. When the abundance of L. ceriotuberosa 

increases in the Owens Lake core, it implies seasonality in surface water discharge in the river. 

Limnocythere ceriotuberosa often appears in the Owens Lake record during climate transitions, such 

as those from or to (inter)glacial conditions or during wet phases within the interglacial.

Limnocythere sappaensis commonly lives in wetlands and lakes that remain saline or maintain a 

saline, alkaline-enriched solute composition (Forester, 1983,1986) throughout the year. It has been 

found living in wetlands and lakes with a salinity as low as 650 mg/L and as high as 110,000 mg/L 

(unpublished data). Its solute and salinity preferences suggest it would live in Owens Lake during 

the drier phases within interglacials, when baseflow predominated in the Owens River during a 

typical year. The presence of L. sappaensis does not imply the absence of seasonal surface water 

flow, but only that such flow didn't dominate the lake's volume and chemistry. Present day flow, if 

it were allowed to enter Owens Lake, would likely support a L. sappaensis environment.

The relative abundances, over time, of the four species discussed above provide an insight into the 

environmental history of Owens Lake. A C. lacustris-dominated ostracode assemblage implies a 

glacial climate with cool to cold summers and moderately high flow in the Owens River. As the 

assemblage abundances shift away from C. lacustris toward C. caudata, glacial conditions are 

waning, summers are likely warmer, but flow remains high in the Owens River. Similarly, as L. 

ceriotuberosa becomes common, so does climatic and limnologic seasonality, signaling a transition 

into a glacial from an interglacial or from an interglacial into a glacial or a wet phase within an 

interglacial. Finally, as L. sappaensis dominates, it identifies a lake that is saline throughout the year 

and is largely supported by baseflow in the Owens River with limited surface-water-discharge 

events. Limnocythere sappaensis identifies the drier phases within the interglacial climate state.

The abundance and stratigraphic succession of these species, along with the core chronology 

(Bischoff and others, 1997), provide a means of assessing the rates, durations, and magnitudes of 

past climate events on glacial-interglacial and stadial-interstadial time scales. Cytherissa lacustris is 

relatively abundant at the base of the core segment in this study, presumably reflecting the 

penultimate glacial (oxygen isotope stage 6), but then its abundance tails off dramatically around 138- 

136 ka. Spotty occurrences of C. lacustris in sediments younger than about 138 ka may represent 

reworking of older shells into younger sediments or an environment only marginally favorable to this 

taxon. The timing of deglaciation as implied by the loss of C. lacustris from the Owens Lake record 

is quite similar to the timing of the stable isotope record from Devils Hole (Winograd and others, 

1992). Providing both records are synchronous, then the loss of C. lacustris at this time implies that 

the change was due to the retreat of the polar front from this region.

Candona caudata-dominated assemblages with varying numbers of L. ceriotuberosa typify the 

Owens Lake ostracode record from about 135-85 ka. Their occurrences are not continuous, but are 

persistent. The presence of those ostracodes and the absence of L. sappaensis implies that this 

interval was wetter and perhaps cooler than the intervals where L. sappaensis was a dominant 

species.

Limnocythere sappaensis dominates the interval from about 85-70 ka. The presence of this taxon 

implies predominantly baseflow in the Owens River as defined above. The lake was saline and had a 

very high alk/Ca ratio. The presence of L. sappaensis and absence through most of the interval of L 

ceriotuberosa or other ostracodes suggest the lake's TDS was typically above about 15,000 mg/L. 

Limnocythere sappaensis exhibits a continuous distribution through this interval, suggesting that 

although the climate was dry, there was sufficient flow in the Owens River to sustain a saline lake 

throughout the interval. By contrast, there are intervals within the Holocene when no ostracodes are 

present, possibly representing very low or no flow in the Owens River.

Candona caudata occurs in the lake from about 70 ka to 65 ka, implying cooler and wetter climates 

that supported moderately high flow in the Owens River. The rarity of C. lacustris suggests that,
unlike in the penultimate glacial, year round polar conditions were infrequent.

Limnocythere ceriotuberosa appeared around 65 ka and was followed at about 60 ka by 

Limnocythere sappaensis, which was abundant until about 52 ka. At 52 ka, L. ceriotuberosa 

reappeared followed by abundant Candona caudata, which remained abundant to the top of the 

interval of interest (46 ka, 32 m). The transition from C. caudata to L. ceriotuberosa and then to L. 

sappaensis implies a change from a large fresh-water lake to one with seasonal changes in lake-level 

to a low-level saline lake. Then the lake shifts from a low-level saline lake back to a large freshwater lake, even supporting Cytherissa lacustris for a brief period. Such systematic and rapid 

changes in the environmental characteristics of Owens Lake indicates a transition to interglacial like 

climate and then a progressive shift back to glacial climate. Such changes were likely controlled by 

the relative persistence of polar air mass activity in the region.

SUMMARY

The high resolution ostracode record from 150 ka to 65 ka shows dramatic changes in Owens Lake 

environments. Those changes appear to be climate driven and may be understood from the changes 

in atmospheric circulation associated with glacial and interglacial climates. The last interglacial 

appears to have been wetter and perhaps cooler than the current interglacial.

REFERENCES CITED

Bischoff, J. L., Stafford, T. W., and Rubin, M., 1997, A time-depth scale for Owens Lake 

sediments of core OL-92: Radiocarbon dates and constant mass-accumulation rate, in Smith, 

G. L., and Bischoff, J. L., eds., An 800,000-Year Paleoclimatic Record from Core OL-92, 

Owens Lake, Southeast California: Boulder, Colorado, Geological Society of America 

Special Paper 317, p. 91-98.

Carter, Claire, 1997, Ostracodes in Owens Lake core OL-92: Alternation of saline and freshwater 

forms through time, in Smith, G. L., and Bischoff, J. L., eds., An 800,000-Year 

Paleoclimatic Record from Core OL-92, Owens Lake, Southeast California: Boulder, 

Colorado, Geological Society of America Special Paper 317, p. 113-119.

Delorme, L. D., 1969, Ostracodes as Quaternary paleoecological indicators: Canadian Journal of 

Earth Sciences, v. 6, p. 1471-1476

___, 1989, Methods in Quaternary ecology 7. Fresh-water Ostracodes: Geoscience Canada, v. 16, 

p. 85-90.

Forester, R. M, 1983, Relationship of two lacustrine ostracode species to solute composition and 

salinity: Implications for paleohydrochemistry: Geology, v. 11, p. 435-438.

___, 1986, Determination of the dissolved anion composition of ancient lakes from fossil 

Ostracodes: Geology, v. 14, p. 796-798.

___, 1987, Late Quaternary paleoclimate records from lacustrine ostracodes, in Ruddiman, W.F., 

and Wright, H.E., Jr., eds., North America and adjacent oceans during the last deglaciation: 

Boulder, Colorado, Geological Society of America, The Geology of North America, v. K-3, 

p. 261-276.

___, 1991, Ostracode Assemblages from Springs in the Western United States: Implications for 

Paleohydrology. Memoirs of the Entomological Society of Canada, V. 155: p. 181-201.

Forester, R. M., and Smith, A. J., 1994, Late glacial climate estimates for southern Nevada, the 

ostracode fossil record: The 5th annual International High-Level Radioactive Waste

Icl7
Management Conference and Exposition, May 22-26, Las Vegas, Nevada, p. 2553-2561.

Forester, R. M., Coleman, S. M., Reynolds, R. L., and Keigwin, L. D., 1994, Lake Michigan's 

late Quaternary limnological and climate history from ostracode, oxygen isotope, and 

magnetic susceptibility: Journal of Great Lakes Research, v. 20, no. 1, p. 93-107.

Smith, G. L, and Bischoff, J. L., eds., 1993, Core OL-92 from Owens Lake, southeast California: 

U.S. Geological Survey Open-File Report 93-683, 398 p.

Smith, G. L, and Bischoff, J. L., eds., 1997a, An 800,000-Year Paleoclimatic Record from Core 

OL-92, Owens Lake, Southeast California: Boulder, Colorado, Geological Society of 

America Special Paper 317,165 p.

Smith, G. I., and Bischoff, J. L., 1997b, Core OL-92 from Owens Lake: Project rationale, geologic 

setting, drilling procedures, and summary. In Smith, G. L, and Bischoff, J. L., eds., 1997, 

An 800,000-Year Paleoclimatic Record from Core OL-92, Owens Lake, Southeast 

California: Boulder, Colorado, Geological Society of America Special Paper 317, p. 1-8..

Winograd, I. J., Coplen, T.B., Landwehr, J. M., Riggs, A. C., Ludwig, K.R., Szabo, B. J., 

Kolesar, P. T., and Revesz, K. M., 1992, Continuous 500,000-year climate record from 

vein calcite in Devils Hole, Nevada: Science, v. 258, p. 255-260.
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Table 1.

Drive#

Owens Lake

Sample #

(cm)

Core OL-92-1

17A

17A

17A

17A

17A

17B

17B

17B

17B

17B

18B

18B

18B

18B

18B

18B

18B

18C

18C

18C

18C

18C

18C

19A

19A

19A

19A

19A

19B

19B

19B

19B

19B

19B

19B

20A

52-57

72-77

92-97

112-117

132-137

0-5

20-25

40-45

60-65

80-85

9-14

29-34

49-54

69-74

89-94

109-114

129-134

0-5

20-35

40-45

60-65

80-85

100-105

21-26

61-66

101-106

121-126

141-146

10-15

30-35

50-55

70-75

90-95

110-115

130-135

43-48

Interval Depth

(m)

31.99-32.04

32.19-32.24

32.39-32.44

32.59-32.64

32.79-32.84

32.97-33.02

33.17-33.22

33.37-33.42

33.57-33.62

33.77-33.82

34.55-34.60

34.75-34.80

34.95-35.00

35.15-35.20

35.35-35.40

35.55-35.60

35.75-35.80

35.97-36.02

36.17-36.22

36.37-36.42

36.57-36.62

36.72-36.77

36.82-36.87

37.17-37.22

37.57-37.62

37.97-38.02

38.17-38.22

38.37-38.42

38.47-38.52

38.67-38.72

38.87-38.92

39.07-39.12

39.27-39.32

39.47-39.52

39.67-39.72

40.44-40.49

Interval

midpoint

32.015H

32.215

32.415

32.615

32.815

32.995

33.195

33.395

33.595

33.795

34.575

34.775

34.975

35.175

35.375

35.575

35.775

35.995

36.195

36.395

36.595

36.745

36.845

37.195

37.595

37.995

38.195

38.395

38.495

38.695

38.895

39.095

39.295

39.495

39.695

40.465

Age (ka)

46.154

46.514

46.873

47.233

47.593

47.916

48.264

48.602

48.94

49.278

50.597

50.935

51.273

51.611

51.949

52.287

52.625

52.997

53.322

53.634

53.947

54.181

54.337

54.884

55.508

56.133

56.445

56.758

56.914

57.226

57.539

57.851

58.145

58.439

58.732

59.862

Weight

(g)

14.2

14.1

58.2

15.6

15

55.9

51.2

15

15

15

66.7

15

14.9

14.5

15

14.2

14.9

14.8

14.2

15

15.6

15

15.2

17.7

13.5

12.2

14.2

15.2

14.9

14.9

14.5

13.7

42.7

15

14.4

15.4

L. cerio

0

0

0

0

1

0

4

0

2

21

4

1

12

5

36

7

24

72

230

135

309

834

171

34

172

3

0

0

j

0

0

3

j

48

393

6

C. caud

0

0

1

0

26

2

15

0

10

30

12

8

15

8

48

35

27

33

36

38

0

0

0

9

6

0

0

0

0

0

0

0

0

0

0

j

C. lacust

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

Oj

0

0

0

Oj

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

L. sappa

0

0

0

0

0

0

0

0

0

0

i

0

0

0

0

0

0

j

0

0

6

236

5

2

52

799

137

298

582

218

225

58

29

2156

145

_ 1178

L.aff.ita
Drive#

20A

20A

20A

20A

20A

20B

20B

20B

20B

20B

20B

20B

21A

21A

21A

21A

21A

21A

21A

21B

21B

21B

21B

21B

21B

21B

21C

22A

22A

22A

22A

22A

22A

22A

22B

22B

23A

23A

23A

23A

Sample #

63-68

83-88

103-108

123-128

143-148

10-15

30-35

50-55

70-75

90-95

110-115

130-135

15-20

35-40

55-60

75-80

95-100

115-120

135-140

6-11

26-31

46-51

66-71

86-91

106-111

126-131

5-10

9-14

29-34

49-54

69-74

89-94

109-114

129-134

1-6

21-26

12-17

32-37

52-57

72-77

Interval Depth

40.64-40.69

40.84-40.89

41.04-41.09

41.24-41.29

41.44-41.49

41.64-41.69

41.84-41.89

42.04-42.09

42.24-42.29

42.44-42.49

42.64-42.69

42.84-42.89

43.20-43.25

43.40-43.45

43.60-43.65

43.80-43.85

44.00-44.05

44.20-44.25

44.40-44.45

44.64-44.69

44.84-44.89

45.04-45.09

45.24-45.29

45.44-45.49

45.64-45.69

45.84-45.89

46.15-46.20

46.19-46.24

46.39-46.44

46.59-46.64

46.79-46.84

46.99-47.04

47.19-47.24

47.39-47.44

47.63-47.68

47.83-47.88

49.27-49.32

49.47-49.52

49.67-49.72

49.87-49.92

Interval

40.665

40.865

41.065

41.265

41.465

41.665

41.865

42.065

42.265

42.465

42.665

42.865

43.225

43.425

43.625

43.825

44.025

44.225

44.425

44.665

44.865

45.065

45.265

45.465

45.665

45.865

46.175

46.215

46.415

46.615

46.815

47.015

47.215

47.415

47.655

47.855

49.295

49.495

49.695

49.895

Age(ka)

60.156

60.449

60.743

61.036

61.33

61.623

61.917

62.21

62.495

62.776

63.058

63.339

63.846

64.128

64.409

64.691

64.973

65.254

65.536

65.874

66.155

66.437

66.715

66.991

67.268

67.545

67.973

68.029

68.305

68.582

68.859

69.135

69.412

69.689

70.021

70.297

72.3

72.579

72.858

73.136

Weight

15.1

15

14.6

14.6

14.3

15.3

13.1

14.5

15

15

14.4

14.8

15.1

15

14.9

60.2

50.8

65.1

14.3

14.8

53.6

60.7

36.4

35.4

53.5

53.6

53.7

66.1

51.4

54.3

84.8

67.3

53.3

55.7

15.6

15.9

15.3

15.5

15.2

15.1

L. cer/o

0

0

26

1

0

i

0

i

6

52

20

933

309

679

1520

j

J

1

2

j

15

3

2

10

2

j

21

1

4

2

2

7

5

J

2

0

4

3

26

51

C. caud

0

0

0

0

0

0

0

0

0

0

0

1

2

1

44

2

4

2

2

i

11

5

1

1

1

5

7

4

2

j

i

i

i

1

0

0

i

0

0

0

C. lacust

0

0

0

0

0

0

0

0

0

0

2

0

3

0

0

0

0

0

0

0

0

0

0

0

j

0

1

i

i

0

0

0

0

0

0

0

0

0

0

0

L. sappa

8554

1773

2623

559

634

267

2556

961

692

6

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

i

j

2

3

1

5

2

4

7

1393

593

568

180

12

461

L.aff.ita
Drive#

23A

23A

23A

24A

25A

25A

25A

25A

25A

25A

25A

25A

25B

Drive*

25B

25B

25B

25B

25B

26A

26A

26A

26A

26A

26A

26A

26A

26B

26B

26B

26B

26B

26B

26B

26C

27A

27A

27A

27A

Sample #

92-97

112-117

132-137

0-5

0-5

20-25

40-45

60-65

80-85

100-105

120-125

140-145

10-15

Sample #

(cm)

30-35

50-55

70-75

90-95

110-115

6-11

26-31

46-51

66-71

86-91

106-111

126-131

146-151

13-18

33-38

53-58

73-78

93-98

113-118

133-138

7-12

9-14

29-34

49-54

69-74

Interval Depth

50.07-50.12

50.27-50.32

50.47-50.52

52.20-52.25

52.50-52.55

52.70-52.75

52.90-52.95

53.10-53.15

53.30-53.35

53.50-53.55

53.70-53.75

53.90-53.95

54.10-54.15

Interval Depth

(m)

54.30-54.35

54.50-54.55

54.70-54.75

54.90-54.95

55.10-55.15

55.31-55.36

55.51-55.56

55.71-55.76

55.91-55.96

56.11-56.16

56.31-56.36

56.51-56.56

56.71-56.76

56.89-56.94

57.09-57.14

57.29-57.34

57.49-57.54

57.69-57.74

57.89-57.94

58.09-58.14

58.28-58.33

58.38-58.43

58.58-58.63

58.78-58.83

58.98-59.03

Interval

50.095

50.295

50.495

52.225

52.525

52.725

52.925

53.125

53.325

53.525

53.725

53.925

54.125

Interval

midpoint

54.325

54.525

54.725

54.925

55.125

55.335

55.535

55.735

55.935

56.135

56.335

56.535

56.735

56.915

57.115

57.315

57.515

57.715

57.915

58.115

58.305

58.405

58.605

58.805

59.005

Age (ka)

73.415

73.693

73.972

76.43

76.862

77.149

77.437

77.724

78.012

78.3

78.587

78.875

79.162

Age (ka)

79.463

79.767

80.07

80.374

80.677

80.996

81.299

81.602

81.906

82.209

82.513

82.816

83.12

83.393

83.696

84.017

84.343

84.669

84.995

85.321

85.631

85.794

86.12

86.446

86.772

Weight

15.2

15.1

13.7

15

15.4

15.2

15.4

15.7

15.4

15.1

15.5

15.2

15.1

Weight

(g)

14.5

14.4

15.4

15.4

15.1

15.2

15.8

15.4

15.5

15.2

15.1

15.5

15.7

15.9

15.7

15.1

15.3

15.2

15.9

15.5

15.7

15.9

15.4

15.3

15.5

L. cer/o

0

0

0

0

0

0

0

0

0

0

0

0

0

L. cer/o

0

0

0

0

0

j

0

0

0

0

1

2

0

1

0

0

0

0

2704

114

71

1595

61

40

39

C. caud

0

0

0

0

0

0

0

0

0

0

0

0

0

C. caucf

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

C. lacust

0

0

0

0

0

0

0

0

0

0

0

0

0

C. lacust

0

i

i

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

L. sappa

1090

216

242

326

5543

44

658

1581

151

120

619

212

905

L. sappa

438

151

484

93

488

881

982

4053

99

230

379

6985

130

1504

149

147

460

208

0

0

0

0

0

2

0

L.aff.it

L.aff.ita
Drive#

27A

27A

27A

27A&B

27B

27B

27B

27B

27B

27B

27B

Sample #

89-94

109-114

129-134

149-1 50, CM

19-24

39-44

59-64

79-84

99-104

119-124

139-144

Core OL-92-2

1A

1A

1A

1A

1A

1A

1A

1A

1B

1B

1B

1B

1B

1B

1B&2A

2A

2A

2A

2A

2A

2A

2A

2B

2B

2B

2B

0-5

20-25

40-45

60-65

80-85

100-105

120-125

140-145

14-19

34-39

54-59

74-79

94-99

114-119

134-135,0-4

19-24

39-44

59-64

79-84

99-104

119-124

139-144

11-16

31-36

51-56

71-76

interval Depth

59.18-59.23

59.38-59.43

59.58-59.63

59.78-59.83

59.98-60.03

60.18-60.23

60.38-60.43

60.58-60.63

60.78-60.83

60.98-61.03

61.18-61.23

61.26-61.31

61.46-61.51

61.66-61.71

61.86-61.91

62.06-62.11

62.26-62.31

62.46-62.51

62.66-62.71

62.90-62.95

63.10-63.15

63.30-63.35

63.50-63.55

63.70-63.75

63.90-63.95

64.01-64.06

64.33-64.38

64.53-64.58

64.73-64.78

64.93-64.98

65.13-65.18

65.33-65.38

65.53-65.58

65.75-65.80

65.95-66.00

66.15-66.20

66.35-66.40

interval 

59.205

59.405

59.605

59.805

60.005

60.205

60.405

60.605

60.805

61.005

61.205

61.285

61.485

61.685

61.885

62.085

62.285

62.485

62.685

62.925

63.125

63.325

63.525

63.725

63.925

64.035

64.355

64.555

64.755

64.955

65.155

65.355

65.555

65.775

65.975

66.175

66.375

Age (ka) 

87.098

87.424

87.751

88.085

88.403

88.733

89.084

89.435

89.786

90.137

90.488

90.629

90.98

91.331

91.682

92.033

92.384

92.735

93.086

93.507

93.858

94.225

94.598

94.972

95.345

95.55

96.148

96.521

96.894

97.268

97.641

98.014

98.388

98.798

99.172

I 99.545

I 99.936

Weight

15.4

15.4

15.3

15.3

15.5

15.7

78.7

15.8

15.5

15.5

_ 15

15.9

15.2

15.5

15.2 

15.6

15.6

15.4

54.5

15.1

15.3

15

15.5

15.2

66.2

15.1

15.7

55.8

58.6

14.8

15.8

14.5

15.3

15.1

15.2

15.3 

53.7

L. cerio

290

148

76

344

449

9

12

270

41

61

11

15

211

243

21

345

321

1

33

1044

336

709

229

2103

2

69

14

17

5

48

762

7

13

10

3

0

1

C. caud

0

0

0

i

10

3

14

1

0

0

0

0

0

i

0

0

0

0

3

i

4

28

40

81

7

2

4

3

1

i

0

0

1

i

0

0

0

C. lacust

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

L. sappa

0

0

0

0

0

0

22

0

0

2

0

0

0

5

1

0

1

0

0

2

0

0

0

1

i

0

0

0

0

2

4

103

125

69

47

13

8

L.aff.ita
Drive#

2B

2B

2B

3A

3A

3A

3A

3A

3A

3A

3B

3B

3B

3B

3B

3B

3B

3C

3C

4A

4A *

4A

4A

4A

4A

4A

4B

4B

4B

4B

4B

4B

4B

4B&5A

5A

5A

5A

5A

6A

6A

Sample #

91-96

110-116

131-136

13-18

33738

53-58

73-78

93-98

113-118,

133-138

3-8

23-28

43-48

63-68

83-88

103-108

123-128

2-7

22-27

1-6

21-26

41-46

61-66

81-86

101-106

121-126

5-10

25-30

45-50

65-70

85-90

105-110

125-130

145-149,0-1

16-21

36-41

56-61

76-81

7-12

27-32

Interval Depth

66.55-66.60

66.74-66.79

66.95-67.00

67.12-67.17

67.32-67.37

67.52-67.57

67.72-67.77

67.92-67.97

68.12-68.17

68.32-68.37

68.52-68.57

68.72-68.77

68.92-68.97

69.12-69.17

69.32-69.37

69.52-69.57

69.72-69.77

70.01-70.06

70.21-70.26

70.47-70.52

70.67-70.72

70.87-70.92

71.07-71.12

71.27-71.32

71.47-71.52

71.67-71.72

71.51-71.56

71.71-71.76

72.11-72.16

72.26-72.31

72.31-72.36

72.56-72.61

72.71-72.76

72.91-72.95

73.67-73.72

73.87-73.92

74.07-74.12

74.27-74.32

74.49-74.54

74.69-74.74

Interval

i 66.575

' 66.765

66.975

67.145

67.345

67.545

67.745

67.945

68.145

68.345

68.545

68.745

68.945

69.145

69.345

69.545

69.745

70.035

70.235

70.495

70.695

70.895

71.095

71.295

71.495

71.695

71.535

71.735

72.135

72.285

72.335

72.585

72.735

72.93

73.695

73.895

74.095

74.295

74.515

74.715

Age (ka)

100.33

100.7

101.11

101.45

101.84

102.23

102.63

103.02

103.41

103.8

104.2

104.59

104.98

105.37

105.78

106.19

106.6

107.19

107.6

108.13

108.54

108.95

109.36

109.76

110.17

110.58

110.87

111.17

111.48

111.79

112.11

112.43

112.74

113.15

114.77

115.19

115.61

116.04

116.5

116.92

Weight

53.1

15.6

15.4

76.3

64.6

38.6

61.1

65.8

15.6

79.2

73.4

15.2

55.7

15.3

67

15

67

15

15.5

61.9

15.1

51.1

15.4

15.1

15.3

15.6

54.1

50.9

15.9

15.5

51.5

15.5

55.2

15.1

15.5

91.5

56.2

88.2

15.4

44.7

L. cer/o

j

0

0

3

7

0

j

2

0

2

0

0

1

0

i

i

j

0

3

1

j

0

3

10

1

j

2

0

0

14

4

5

1

5

208

2

3

11

11

14

C. caud

0

0

0

0

0

0

j

j

0

2

5

0

0

0

I

J

1

0

1

i

i

0

1

0

i

0

0

0

0

i

1

1

0

0

0

1

j

1

6

23

C. lacust

0

0

0

0

0

1

0

i

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

 0

L. sappa

28

204

1926

1

8

0

i

12

12

3

4

0

0

j

7

15

10

12j

23

8

12

3

21

76

16

0

16

13

34

17

6

12

5

10

293

12

1

1

0

0

L.aff.ita
Drive#

6A

6A

6A

6A

6A

6A&B

6B

6B

7A

7A

7A

7A

7A

7A

7A

7A

7B

7B

7B

7B

7B

7B

7B

7C&D

8A

8A

8A

8A

8A

8A

8A

8A

8B

8B

8B

8B

8B

8B

8B

9A

Sample #

47-52

67-72

87-92

107-112

127-132

147-148,0-3

18-23

38-43

4-9

24-29

44-49

64-69

84-89

104-109

124-129

144-149

13-18

33-38

53-58

73-78

93-98

113-118

133-138

2-7

5-10

25-30

45-50

65-70

85-90

105-110

125-130

145-150

13-18

33-38

53-58

73-78

93-98

113-118

133-138

0-5

Interval Depth

74.89-74.94

75.09-75.14

75.29-75.34

75.49-75.54

75.69-75.74

75.89-75.94

76.14-76.19

76.34-76.39

76.60-76.65

76.80-76.85

77.00-77.05

77.20-77.25

77.40-77.45

77.60-77.65

77.80-77.85

78.00-78.05

78.22-78.27

78.42-78.47

78.62-78.67

78.82-78.87

79.02-79.07

79.22-79.27

79.42-79.47

79.46-79.51

79.65-79.70

79.85-79.90

80.05-80.10

80.25-80.30

80.45-80.50

80.65-80.70

80.85-80.90

81.05-81.10

81.25-81.30

81.45-81.50

81.65-81.70

81.85-81.90

82.05-82.10

82.25-82.30

82.45-82.50

82.65-82.70

Interval

74.915

75.115

75.315

75.515

75.715

75.915

76.165

76.365

76.625

76.825

77.025

77.225

77.425

77.625

77.825

78.025

78.245

78.445

78.645

78.845

79.045

79.245

79.445

79.485

79.675

79.875

80.075

80.275

80.475

80.675

80.875

81.075

81.275

81.475

81.675

81.875

82.075

82.275

82.475

82.675

Age (ka)

117.34

117.77

118.19

118.63

119.06

119.45

120.03

120.46

121.03

121.46

121.89

122.32

122.76

123.19

123.62

124.05

124.53

124.97

125.41

125.85

126.29

126.73

127.09

127.26

127.68

128.12

128.56

129

129.44

129.88

130.33

130.77

131.21

131.66

132.11

132.55

133

133.45

133.9

134.35

Weight

15.1

15.5

15.4

15

15.5

15.9

58.5

_ 15.1

76.1

15.1

61

82.1

56.1

15.1

49.8

15.5

78.1

74.9

57.3

70.8

102.5

15.8

74.5

76.1

15

15.7

15.6

81

15.3

89.6

86.1

15.3

74.7

15.7

15.7

15.4

15.5

15.9

80.7

90.7

L. cer/o

1

0

0

0

0

0

6

0

3

0

0

]

1

0

1

1

0

1

1

1

9

0

1

0

0

2

1

0

0

9

2

0

3

1

0

1

0

8

2

7

C. caud

57

0

0

0

0

0

12

0

3

0

1

j

3

0

1

1

1

1

14

0

3

i

0

0

i

1

1

4

0

i

4

0

2

8

7

12

1

12

10

6

C. lacust

0

0

0

0

0

0

1

0

0

0

0

9

3

0

0

8

0

0

6

1

0

0

0

0

1

0

0

1

0

0

1

0

0

1

6

3

0

1

0

j

L. sappa

0

0

0

0

0

0

0

I?

2

0

0

0

1

0

j

0

0

]

0

0

0

0

j

1

i?

2

j

i

j?

2

0

0

0

0

0

0

0

0

0

5

Laff.ita

2
Drive#

9A

9A

9A

9A

9A

9A

9A

9B

9B

9B

9B

9B

9B

9B

9B&10A

10A

10A

10A

10A

10A

10A

10A

10B

10B

10B

10B

10B

10B

10B

10B&C

11A

11A

11A

11A

11A

Sample #

20-25

40-45

60-65

80-85

100-105

120-125

140-145

8-13

28-33

48-53

68-73

88-93

108-113

128-133

148-149.5

18-23

38-43

58-63

78-83

98-103

118-123

138-143

8-13

28-33

48-53

68-73

88-93

108-113

128-133

148-150,0-3

2-7

22-27

42-47

62-67

82-87

Interval Depth

82.85-82.90

83.05-83.10

83.25-83.30

83.45-83.50

83.65-83.70

83.85-83.90

84.05-84.10

84.25-84.30

84.45-84.50

84.65-84.70

84.85-84.90

85.05-85.10

85.25-85.30

85.45-85.50

85.65-85.78

85.93-85.98

86.13-86.18

86.33-86.38

86.53-86.58

86.73-86.78

86.93-86.98

87.13-87.18

87.34-87.39

87.54-87.59

87.74-87.79

87.94-87.99

88.14-88.19

88.34-88.39

88.54-88.59

88.64-88.69

88.77-88.82

88.97-89.02

89.17-89.22

89.37-89.42

89.57-89.62

Interval

82.875

83.075

83.275

83.475

83.675

83.875

84.075

84.275

84.475

84.675

84.875

85.075

85.275

85.475

85.72

85.955

86.155

86.355

86.555

86.755

86.955

87.155

87.365

87.565

87.765

87.965

88.165

88.365

88.565

88.665

88.795

88.995

89.195

89.395

89.595

Age (kaj

134.8

135.25

135.69

136.14

136.59

137.04

137.49

137.94

138.4

138.85

139.31

139.77

140.22

140.68

141.22

141.78

142.23

142.69

143.15

143.61

144.06

144.52

145

145.47

145.93

146.4

146.86

147.33

147.8

148.03

148.33

148.8

149.26

149.73

150.19

Weight

15.4

15.5

15.7

15.1

15.2

15.5

15

73.2

15.4

15.2

48.8

15.7

15.4.

15

15.3

15.5

15.6

15.4

15.1

15.4

15.2

15.6

79.8

15.2

84.5

15.4

96.1

15.9

15.2

15.3

15.6

15.1

15.4

15.3

15.3

L. cer/o

4

20

1

i

0

0

0

0

1

i

0

0

8

16

1

3

7

80

28

93

16

15

7

7

23

5

6

8

0

1

0

0

0

0

1

C. caud

17

16

3

3

13

2

16

11

20

8

4

12

28

17

7

11

3

72

10

50

9

26

6

5

16

7

35

6

7

15

16

8

7

13

8

C. lacust

2

4

1

i

8

2

6

12

52

10

2

6

10

4

3

7

6

12

7

4

6

6

3

1

9

7

23

4

2

6

12

10

16

15

5

L. sappa

0

0

0

0

0

0

0

0

0

0

Oj

0

i?

0

j

j

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

L.aff.ita
U.S. DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY

TESTING CLIMATE STABILITY DURING THE LAST INTERGLACIAL 

INTERVAL: POLLEN EVIDENCE FROM CORE OL-92

by 

Ronald J. Litwin1

Open-File Report 98-132 (part 9)

This report is preliminary and has not been reviewed for conformity with U.S. Geological 

Survey editorial standards (or with the North American Stratigraphic Code). Any use of 

trade, product, or firm names is for descriptive purposes only and does not imply 

endorsement by the U.S. Government.

iU.S. Geological Survey, Reston VA 20192

1998
Abstract

Pollen evidence analyzed at decimeter-scale resolution through a 30-m interval in core 

OL-92, from Owens Lake in the westernmost Great Basin, suggests that the last interglacial 

period was a time of strongly fluctuating climate, despite also being a time of greatly 

increased insolation. The "last interglacial" is used here in its most restricted sense: i.e., 

the terrestrial equivalent of the European Eemian, or the 'pollen-interval' equivalent of 

marine oxygen isotope (OIS) substage 5e. Fossil pollen assemblages from this interval in 

core OL-92 show evidence of multiple climatic shifts, and three strong but relatively brief 

cooling events can be identified. Given the conspicuous and recurrent nature of the climate 

variability documented in the Great Basin for the last interglacial, it would appear to be 

premature to characterize the last interglacial as a time of monotonously stable warm 

climate.

Introduction

Documenting the past relative stability or instability of terrestrial climate (especially at a 

millennial- or submillennial-scale) through time sequences that predate or filter out humaninduced effects on climate such as the increase in atmospheric CO2 levels from increasing 

industrialization is an important prerequisite for accurately assessing trends in present day 

short-term climatic changes. Such documentation provides a basis for determining whether 

current human-induced (atmospheric) effects on climate are being superimposed on a mostly 

static or mostly dynamic baseline of natural climate variability.

This study is one such test of climate stability: an assessment of the character and 

relative magnitude of pollen assemblage (proxy vegetation) changes, at submillenmal 

resolution, in a climatically sensitive area (the northern edge of the Mojave Desert), through 

a period of proposed high insolation (~ marine oxygen-isotope substage 5e). These 

conditions make it a suitable geologic interval for assessing short-term relative stability of 

climate before and during a "warm climate" period.

Materials and Methods

The following parameters bound this study. The Owens Lake samples used here are a 

subset of a suite that covers the climatic equivalent of marine oxygen-isotope (OIS) stage 5, 

taken at 10 cm increments by J.L. Bischoff (Bischoff, this volume). The balance of those 

samples currently are being analyzed, so that ultimately they will span the entire terrestrial 

equivalent of OIS 5.

Warm and cold climate intervals in core OL-92~as determined by pollen assemblage 

characteristics ~ were assigned to numbered "pollen intervals" (Litwin et al., 1997; Litwin 

et al., submitted). These pollen intervals approximately parallel the marine oxygen-isotope 

stages, but because they were not derived specifically from marine isotopic data, they have 

been assigned a qualifying symbol in their notation. Pollen intervals within the Owens

Lake record therefore are appended here by the superscript "A" (to designate each as a 

pollen-based interval and not an isotopically-based interval). For example, the interval in

OL-92 that is believed to correspond to OIS 5 is referenced herein as 5A, with subdivisions

5aA, 5bA, 5cA, 5dA, and 5eA.

The stratigraphic interval examined here from Owens Lake core OL-92 (Fig.l) 

comprised 85 m to 55 m depth. This correlates to pollen intervals spanning the middle of

interval 6A to the middle of 5cA (Fig. 2). Direct age control was absent between -30 ka

(the maximum 14C age deemed reliable in OL-92; Bischoff et al., 1993) and -759 ka (the 

age of the Bishop Ash bed, which was penetrated near the base of core OL-92; SarnaWojcicki and Pringle, 1992, Sarna-Wojcicki et al., 1997) . Because of this, results of the
pollen analyses are plotted here against core depth; ages bounding this stratigraphic 

interval, here derived from the mass accumulation rate model for OL-92 (Bischoff, 1993; 

Bischoff et al., 1997a), are presented along the bottom (x-) axis of Figures 2 and 3 for 

reference to other proxy records. The sampling interval chosen for this study was 20 cm, 

with a total of 165 + samples. More than 49,500 specimens were identified to establish the 

baseline for this study; a census of the samples from core OL-92 is provided in Appendix I. 

Powdering of the core samples prior to their distribution introduced several 

complications for pollen analysis. The first was a coarser sample depth-averaging (here, 

10 cm vs ~2 cm averaging for other palynological samples), which buffered changes in the 

pollen response, especially where averaged across sedimentologically heterogeneous 

intervals. Accordingly, the depth of sampling given here is arbitrarily placed at the midpoint of the sampled interval. Crushing of samples also created substantial breakage in the 

pollen fraction. This thoroughly disaggregated most colonies of the thin-walled alga 

Pediastrum, which increased the difficulty in counting and identifying all pollen grains. 

Fully disaggregated but intact Pediastrum cells bore resemblance to TCT grains 

(Taxodiaceae-Cupressaceae-Taxaceae, here mostly Juniperus species) and visually 

obscured other pollen taxa in the sample preparations by their abundance. To counteract 

this, samples suffering the worst effects, especially those with abundant Pediastrum, were 

counted multiple times on different slide transects to confirm the pollen taxa assemblage 

composition of those intervals. Below -79.5 m depth, the R5258 sample series of 

Bischoff was substituted by 'point' samples taken from an earlier (separate) sampling by

the author (designated R5171 series), due to low productivity, insufficient sample volume,

2 and pollen breakage in the former sample suite .

Cold excursions

The results of these pollen analyses suggest that the terrestrial climate through the peak

insolation interval (5eA) predominantly was dynamic in nature and experienced several 

episodes of strong cooling (at least in the southwestern Great Basin, Fig. 2), on the basis 

of increased juniper (TCT) abundance. Although intra-Eemian cooling has been noted in 

other records (Sarnthein and Tiedemann, 1990; Pinchon et al., 1992; Anklin et al., 1993; 

Dansgaard et al., 1993; Field et al., 1994; Thouveny et al., 1994; Maslin et al, 1996; 

Seidenkrantz and Knudsen, 1997; White et al., 1997), it has been reported variously as a 

single mid-Eemian cold episode (Maslin and Tzedakis, 1996) or as multiple cold pulses 

within the Eemian (Anklin et al., 1993; Thouveny et al., 1994).

Pollen evidence from the Great Basin examined here strongly supports multiple

episodes of cooling within interval 5eA. In this core, the terrestrial climate of interval 5eA 

was divided into three main warm events that alternated with two major cool events (plus

-3

one minor one) . Only a few sustained intervals of relatively "static" climate (either warm 

or cold) were indicated by the pollen assemblage data. The thickest core interval of

relatively unchanging warm pollen assemblages occurred late in subinterval 5e5A (between 

-69 and -72.5 m depth, as indicated by the pollen response of the junipers (TCT)), shortly 

after the insolation maximum (Figs. 2, 3, as determined by total arboreal pollen, 

composites, chenopods, amaranths, and greasewood). However, the beginning of this 

"static" warm interval is separated from the insolation peak by an apparently brief but

moderately strong cold pulse (Fig. 2, asterisk), that effectively divided subinterval 5e5A.

Subinterval 5el comprised the second thickest core interval of relatively stable warm 

pollen assemblages.

Of the three cold events noted in interval 5e , the oldest also is apparently the thinnest

(shortest?); it occurred immediately after the insolation peak and divided subinterval 5e5A 

(above). The second of these cold pulses (and the most strongly sustained one, based on
stratigraphic thickness) is labelled here as subinterval 5e4A. It occurred between -69 m

and 67.7 m core depth. The last of these cold pulses is labelled as 5e2A, and occurred 

between -66.5 m and -64.8 m core depth. Although the current chronology of this 

stratigraphic interval in core OL-92 suggests that these three cold pulses are all geologically 

brief, their strength appears to be significant. All three cold pulses in the OL-92 record had 

TCT values that ranged from nearly 50% to more than 60% of their full-glacial magnitude.

Conclusions

The conclusions from these new analyses are: 1.) the pollen serial record through

terrestrial interval 5eA in core OL-92 suggests that the last interglacial had a dynamic 

climate that can be divided into 6 parts: three longer warm intervals (of differing duration) 

and three shorter cold excursions (also of differing duration); and 2.) abrupt 

sedimentological change and abrupt vegetational change (in several biological indicators)

through the transition from interval 6A to interval 5eA suggests that the climate history 

record across the termination n transition in OL-92 (at -75 m) is unconformable, although 

the duration of this hiatus appears to be relatively short. Further work on comparison of 

this climate record to other climate records through the last interglacial interval (from other 

geographic sites) is in progress.

Acknowledgements

The author gratefully acknowledges R.Z. Poore, J.L. Bischoff, J.P. Smoot, and N.J. 

Durika (USGS), and P. Lamos (Lake Minerals Corp.) for operational, logistical, and 

technical support during this study, and J.A. Barren and J.L. Bischoff for helpful reviews 

of this manuscript. This report is a contribution of the USGS Global Climate Change/ 

Global Hazards Program.

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America Abstracts with Programs, 29, 7:A-340.

Endnotes

1 Although within-Brunhes magnetic reversals were reported in this core (Glen et al., 1993; Glen and Coe, 

1997) more recent examination of these excursions (J. Rosenbaum, R. Reynolds, and J. Smoot, USGS) has 

discovered that some to perhaps most of these may be artifacts that are depth-coincident with core drive-top
slumping and core section spinoffs. Accordingly, these paleomagnetic excursions presently are considered 

to be suspect until they can be reexamined and confirmed.

2 In addition, four other samples of the R5171 series were used for this study. Those samples are from the 

following depths: 62.57 m, 62.72 m, 73.0 m, and 74.5 m.

3 The notation for these sub-portions of the last interglacial interval follow the precedent of Anklin et al. 

(1993) and are designated here as 5el A, 5e2A, 5e3A, 5e4A, and 5e5A. Because of the relative thinness of 

the first cool interval in comparison to the two later cold pulses observed in this record, it was not assigned 

as a separate subinterval of 5eA. This conforms to the precedent used for the oldest subinterval of the 

Eemian in other climate records (e.g., Anklin et al., 1993).

FIGURE CAPTIONS

1. Generalized map of southeastern California, showing location of the Owens Valley 

drainage system, the southern Sierra Nevada, Owens Lake (core OL-92), and the lakes it in 

turn fed during the late Pleistocene: China Lake, Searles Lake, Panamint, and Lake Manly 

(Death Valley). Question marks denote probable drainage paths from Searles Lake into 

Panamint Valley and Death Valley during times of spill in Searles Lake.

2. Percent juniper (TCT, or Taxodeaceae-Cupressaceae-Taxaceae) as a relative indicator of 

climatic change along the eastern flank of the southern Sierra Nevada, core OL-92, Owens 

Lake, California. Increased abundance of juniper pollen denotes intervals of colder 

climate. Three cold pulses are observed in the last interglacial interval of the OL-92 core.

An asterisk marks the oldest of these cold pulses, that occurs within sub-interval 5e5 . 

Ages derived from mass accumulation rate model of Bischoff et al. (1997) are shown along 

bottom axis, for reference (-94 ka, ~118 ka). "A" and "B" denote two possible placements 

for termination II. The shallower position ("A") is placed at the greatest change in percent 

arboreal pollen; this also coincides with the point of greatest lithologic change. The deeper 

position ("B") is placed at the estimated midpoint along the extended transition from fullglacial to full-interglacial juniper abundances. Interval between these two positions

tentatively is assigned to interval 6A, but noted with a dark hatchured line. Percent arboreal 

pollen also indicates probable depth interval of maximum insolation during the last 

interglacial period (i.e., here marked by the greatest sustained minimum of arboreal pollen, 

i.e., maximum desert conditions within the lake basin).

3. Selected desertscrub taxa in core OL-92. Percent greasewood pollen (Sarcobatus) 

shown on upper graph; composites, chenopods, and amaranths shown on lower graph. 

Both indicators are desertscrub taxa whose greatest abundance indicates the maximum

insolation interval within 5eA . Ages derived from mass accumulation rate model of 

Bischoff et al. (1997) shown along bottom axis, for reference (-94 ka, -118 ka). "A" 

denotes one of two possible placements for termination II- the one that more closely 

conforms to the sedimentary structures within this core (see Smoot, this volume). Shaded 

areas denote extent of the last interglacial interval within core OL-92. Shaded portions 

indicate warmest subintervals, with the two shorter, interspersed unshaded areas 

representing intervals of cold climate within the last interglacial period (per Figure 2).
Figure 1. Owens Valley drainage system (southern part)
55

2 100

85

[-94 ka] [~118ka] 

Figure 2. Owens Lake interval 5eA (last interglacial period): %TCT and % arboreal pollen
70 

DEPTH (m)

Figure 3. Selected desertscrub vegetation indicating insolation maximum

US'
Appendix 1. OL-92 pollen counts

Sample Depth(m) Sacci/2 Pinus TPine TCT Abies Alnus Artemisia Car/a ChenAm SCmp LnqCmp LiqCmp Corylus Ephedra

R5258 FS

R5258 FU

R5258 FW

R5258 FY

R5258 GA

R5258 GC

R5258 GE

R5258 GG

R5258 Gl

R5258 GK

R5258 GM

R5258 GO

R5258 GO

R5258 GS

R5258 GU

R5258 GV

R5258 GY

R5258 HA

R5258 HC

R5258 HE

R5258 HG

R5258 HI

R5258 HK

R5258 HM

R5258 HO

R5258 HQ

R5258 HS

R5258 HU

R5258 HW

R5258 HY

R5258 IA

R5258 1C

R5258 IE

R5258 IG

R5258 II

R5258 IK

R5258 IL

R5258 IM

R5258 IO

R5171 GX

R5258 IP

R5171 GY

R5258 IQ

R5258 IR

R5258 IS

R5258 IU

R5258 IW

R5258 IZ

R5258 JA

R5258 JC

R5258 JE

R5258 JG

R5258 Jl

R5258 JK

R5258 JM

R5258 JO

54.95 63.00 188.00 251.00 13.00

55.15 60.00 209.00 269.00 4.00

55.42 72.00 188.00 260.00 10.00

55.65 74.00 178.00 252.00 20.00

55.85 55.00 193.00 248.00 13.00

56.05 71.00 179.00 250.00 17.00

56.25 75.00 176.00 251.00 17.00

56.45 49.00 221.00 270.00 11.00

56.65 40.00 238.00 278.00 5.00

56.85 63.00 210.00 273.00 7.00

57.05 36.00 234.00 270.00 7.00

57.25 38.00 228.00 266.00 14.00

57.45 53.00 213.00 266.00 8.00

57.65 79.00 201.00 280.00 5.00

57.85 66.00 208.00 274.00 5.00

57.95 51.00 234.00 285.00 2.00

58.25 45.00 235.00 280.00 0.00

58.45 54.00 222.00 276.00 2.00

58.65 85.00 200.00 285.00 3.00

58.85 95.00 177.00 272.00 1.00

59.05 68.00 208.00 276.00 13.00

59.25 64.00 197.00 261.00 5.00

59.45 90.00 184.00 274.00 10.00

59.65 54.00 219.00 273.00 13.00

59.85 131.00 123.00 254.00 22.00

60.05 99.00 112.00 211.00 47.00

60.25 63.00 195.00 258.00 23.00

60.45 57.00 195.00 252.00 20.00

60.65 59.00 193.00 252.00 11.00

60.85 50.00 204.00 254.00 22.00

61.05 70.00 192.00 262.00 22.00

61.25 44.00 231.00 275.00 10.00

61.45 53.00 207.00 260.00 19.00

61.65 65.00 212.00 277.00 9.00

61.85 75.00 197.00 272.00 12.00

62.05 40.00 206.00 246.00 17.00

62.15 31.00 209.00 240.00 26.00

62.25 37.00 232.00 269.00 12.00

62.45 52.00 209.00 261.00 23.00

62.57 28.00 179.00 207.00 56.00

62.63 55.00 196.00 251.00 18.00

62.72 50.00 163.00 213.00 73.00

62.83 31.00 187.00 218.00 42.00

62.95 76.00 165.00 241.00 38.00

63.05 64.00 194.00 258.00 22.00

63.25 73.00 208.00 281.00 12.00

63.45 72.00 205.00 277.00 11.00

63.75 61.00 190.00 251.00 10.00

63.85 88.00 165.00 253.00 8.00

64.05 110.00 154.00 264.00 5.00

64.25 156.00 119.00 275.00 5.00

64.45 112.00 126.00 238.00 17.00

64.65 145.00 121.00 266.00 8.00

64.85 108.00 173.00 281.00 3.00

65.05 139.00 128.00 267.00 15.00

65.25 78.00 188.00 266.00 11.00

17.00

8.00

7.00

5.00

13.00

5.00

11.00

6.00

9.00

2.00

8.00

5.00

7.00

7.00

11.00

4.00

6.00

4.00

1.00

4.00

4.00

3.00

3.00

2.00

5.00

2.00

3.00

1.00

0.00

4.00

1.00

8.00

1.00

1.00

3.00

2.00

2.00

2.00

3.00

3.00

5.00

3.00

3.00

1.00

3.00

2.00

2.00

1.00

3.00

2.00

5.00

4.00

3.00

7.00

3.00

4.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

6.00

7.00

10.00

8.00

11.00

4.00

3.00

1.00

1.00

0.00

1.00

1.00

0.00

0.00

0.00

0.00

3.00

2.00

5.00

1.00

9.00

2.00

1.00

2.00

12.00

3.00

3.00

5.00

0.00

3.00

1.00

6.00

4.00

0.00

19.00

10.00

2.00

1.00

13.00

4.00

3.00

12.00

2.00

3.00

0.00

0.00

9.00

9.00

1.00

2.00

16.00

4.00

1.00

6.00

2.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

2.00

4.00

2.00

5.00

7.00

4.00

3.00

3.00

8.00

3.00

6.00

7.00

2.00

4.00

5.00

4.00

3.00

1.00

4.00

0.00

4.00

1.00

2.00

2.00

6.00

1.00

6.00

5.00

11.00

7.00

0.00

4.00

6.00

0.00

3.00

3.00

5.00

0.00

5.00

2.00

1.00

5.00

7.00

2.00

0.00

2.00

7.00

8.00

10.00

3.00

8.00

3.00

0.00

3.00

7.00

0.00

1.00

2.00

1.00

0.00

2.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

3.00

0.00

0.00

4.00

0.00

1.00

1.00

5.00

1.00

2.00

1.00

3.00

1.00

4.00

7.00

1.00

2.00

0.00

4.00

1.00

6.00

2.00

3.00

2.00

0.00

3.00

3.00

3.00

3.00

1.00

1.00

2.00

2.00

2.00

2.00

1.00

1.00

2.00

4.00

1.00

1.00

2.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

1.00

0.00

1.00

0.00

0.00

0.00

1.00

1.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

0.00

0.00

3.00

3.00

0.00

1.00

0.00

2.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

1.00

2.00

1.00

1.00

1.00

0.00

3.00

3.00

0.00

1.00

2.00

0.00

1.00

3.00

2.00

0.00

1.00

1.00

3.00

1.00

0.00

3.00

0.00

5.00

0.00

0.00

2.00

1.00

0.00

1.00

1.00

3.00

3.00

3.00

4.00

2.00

4.00

3.00

2.00

4.00

3.00

2.00

1.00

0.00

4.00

3.00

2.00

1.00

1.00

0.00

0.00

0.00

2.00
Appendix 1. OL-92 pollen counts

Samole Poaceae Larx/Ps Picea Pooulus Ouercus Salix Sarc Sheph Tmert UK/Otht Sum Cyper Typ/Spc %AP %TCT

R5258 FS

R5258 FU

R5258 FW

R5258 FY

R5258 GA

R5258 GC

R5258 GE

R5258 GG

R5258 Gl

R5258 GK

R5258 GM

R5258 GO

R5258 GQ

R5258 GS

R5258 GU

R5258 GV

R5258 GY

R5258 HA

R5258 HC

R5258 HE

R5258 HG

R5258 HI

R5258 HK

R5258 HM

R5258 HO

R5258 HQ

R5258 HS

R5258 HU

R5258 HW

R5258 HY

R5258 IA

R5258 1C

R5258 IE

R5258 IG

R5258 II

R5258 IK

R5258 IL

R5258 IM

R5258 IO

R5171 GX

R5258 IP

R5171 GY

R5258 IQ

R5258 IR

R5258 IS

R5258 IU

R5258 IW

R5258 IZ

R5258 JA

R5258 JC

R5258 JE

R5258 JG

R5258 Jl

R5258 JK

R5258 JM

R5258 JO

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

2.00

1.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

2.00

0.00

0.00

0.00

2.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

1.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

1.00

0.00

2.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

1.00

1.00

3.00

1.00

2.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

12.00

7.00

5.00

3.00

7.00

3.00

8.00

5.00

3.00

5.00

4.00

4.00

7.00

3.00

3.00

2.00

3.00

2.00

3.00

9.00

4.00

5.00

5.00

3.00

5.00

10.00

2.00

8.00

11.00

4.00

1.00

5.00

1.00

0.00

3.00

2.00

9.00

2.00

5.00

5.00

6.00

2.00

8.00

4.00

5.00

1.00

3.00

8.00

7.00

8.00

2.00

9.00

5.00

2.00

1.00

5.00

1.00

1.00

0.00

3.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

1.00

1.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

2.00

0.00

0.00

0.00

0.00

1.00

0.00

1.00

2.00

1.00

0.00

0.00

0.00

1.00

2.00

2.00

0.00

3.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

0.00

1.00

2.00

0.00

0.00

1.00

2.00

0.00

1.00

3.00

2.00

4.00

2.00

3.00

2.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

2.00

1.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

1.00

0.00

0.00

1.00

1.00

2.00

2.00

2.00

3.00

3.00

1.00

1.00

0.00

3.00

2.00

1.00

1.00

0.00

0.00

2.00

1.00

1.00

1.00

0.00

1.00

3.00

3.00

0.00

2.00

1.00

1.00

5.00

1.00

0.00

1.00

2.00

1.00

1.00

3.00

3.00

2.00

5.00

1.00

5.00

0.00

0.00

1.00

1.00

1.00

1.00

1.00

1.00

0.00

0.00

0.00

0.00

2.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

1.00

0.00

0.00

1.00

0.00

0.00

1.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

1.00

0.00

0.00

1.00

0.00

1.00

1.00

1.00

1.00

0.00

1.00

2.00

0.00

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

1.00

0.00

0.00

1.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

3.00

4.00

3.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

4.00

1.00

0.00

0.00

0.00

1.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

4.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

4.00

0.00

0.00

0.00

0.00

4.00

0.00

6.00

0.00

0.00

0.00

0.00

0.00

4.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

4.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

4.00

0.00

0.00

6.00

98.67

97.00

95.00

95.33

94.33

93.00

98.33

97.67

98.67

95.67

97.67

97.00

96.67

98.67

97.67

97.67

97.33

95.67

97.67

95.67

99.00

91.00

98.33

98.00

95.67

91.33

96.00

94.00

93.00

95.33

95.67

99.67

94.67

96.00

97.00

90.00

93.33

95.67

99.00

91.00

95.33

97.00

91.00

95.67

96.67

99.00

98.00

90.67

91.00

93.00

96.00

90.00

95.00

98.67

96.00

95.67

4.33

1.33

3.33

6.67

4.33

5.67

5.67

3.67

1.67

2.33

2.33

4.67

2.67

1.67

1.67

0.67

0.00

0.67

1.00

0.33

4.33

1.67

3.33

4.33

7.33

15.67

7.67

6.67

3.67

7.33

7.33

3.33

6.33

3.00

4.00

5.67

8.67

4.00

7.67

18.67

6.00

24.33

14.00

12.67

7.33

4.00

3.67

3.33

2.67

1.67

1.67

5.67

2.67

1.00

5.00

3.67

/67
Appendix 1. OL-92 pollen counts

Samole Deothfm) Sacci/2 Pinus TPine TCT Abies Alnus Artemisia Carya C hen Am SCmp LnqCmp LigCmp Corylus Ephedra

R5258 JQ

R5258 JS

R5258 JU

R5258 JV

R5258 JW

R5258 JY

R5258 KA

R5258 KB

R5258 KE

R5258 KG

R5258 Kl

R5258 KK

R5258 KM

R5258 KO

R5258 KQ

R5258 KS

R5258 KT

R5258 KU

R5258 KV

R5258 KW

R5258 KX

R5258 KY

R5258 KZ

R5258 LA

R5258 LC

R5258 LE

R5258 LI

R5258 LK

R5258 LM

R5258 LO

R5258 LP

R5258 LQ

R5258 LS

R5258 LU

R5258 LW

R5258 LY

R5258 MA

R5258 MC

R5258 ME

R5258 MG

R5258 Ml

R5258 MK

R5258 MM

R5171 IR

R5258 MO

R5258 MQ

R5258 MS

R5258 MU

R5258 MW

R5258 MY

R5171 IX

R5258 NA

R5258 NC

R5258 NE

R5258 NG

65.45

65.65

65.85

65.95

66.05

66.25

66.45

66.55

66.85

67.05

67.25

67.45

67.65

67.85

68.05

68.25

68.35

68.45

68.55

68.65

68.75

68.85

68.95

69.05

69.25

69.45

69.85

70.05

70.25

70.45

70.55

70.65

70.85

71.15

71.25

71.45

71.65

71.85

72.05

72.25

72.45

72.65

72.85

73.00

73.05

73.55

73.75

73.95

74.15

74.35

74.50

74.55

74.85

74.95

75.15

75.00 188.00

69.00 182.00

88.00 167.00

75.00 193.00

40.00 223.00

92.00 172.00

56.00 126.00

67.00 202.00

94.00 184.00

32.00 230.00

27.00 247.00

66.00 201.00

59.00 181.00

26.00 190.00

57.00 198.0

72.00 161.00

82.00 141.00

94.00 165.00

76.00 142.00

86.00 145.00

57.00 178.00

35.00 158.00

56.00 147.00

115.00 141.00

39.00 223.00

42.00 210.00

61.00 186.00

53.00 186.00

32.00 222.00

113.00 135.00

52.00 182.00

54.00 180.00

46.00 222.00

31.00 198.00

38.00 202.00

52.00 188.00

52.00 211.00

69.00 189.00

55.00 224.00

44.00 208.00

91.00 169.00

83.00 167.00

72.00 169.00

21.00 126.00

46.00 209.00

54.00 191.00

43.00 208.00

102.00 159.00

116.00 119.00

96.00 114.00

47.00 110.00

50.00 108.00

70.00 108.00

66.00 155.00

82.00 184.00

263.00

251.00

255.00

268.00

263.00

264.00

182.00

269.00

278.00

262.00

274.00

267.00

240.00

216.00

255.00

233.00

223.00

259.00

218.00

231.00

235.00

193.00

203.00

256.00

262.00

252.00

247.00

239.00

254.00

248.00

234.00

234.00

268.00

229.00

240.00

240.00

263.00

258.00

279.00

252.00

260.00

250.00

241.00

147.00

255.00

245.00

251.00

261.00

235.00

210.00

157.00

158.00

178.00

221.00

266.00

17.00

20.00

34.00

22.00

25.00

21.00

64.00

13.00

7.00

16.00

15.00

3.00

37.00

25.00

18.0

35.00

34.00

21.00

53.00

39.00

42.00

71.00

63.00

15.00

14.00

22.00

16.00

16.00

12.00

23.00

15.00

19.00

8.00

13.00

19.00

17.00

8.00

13.00

5.00

18.00

18.00

16.00

23.00

51.00

13.00

18.00

12.00

5.00

11.00

24.00

6.00

11.00

8.00

7.00

6.00

1.00

6.00

2.00

2.00

2.00

3.00

1.00

2.00

5.00

3.00

5.00

9.00

2.00

1.00

3.00

9.00

5.00

6.00

4.00

10.00

4.00

3.00

3.00

3.00

1.00

3.00

4.00

3.00

0.00

3.00

5.00

5.00

1.00

1.00

2.00

3.00

1.00

3.00

3.00

2.00

1.00

3.00

3.00

1.00

3.00

4.00

2.00

1.00

1.00

3.00

4.00

7.00

3.00

5.00

7.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

6.00

7.00

1.00

0.00

3.00

1.00

16.00

5.00

1.00

6.00

2.00

11.00

13.00

36.00

1.00

9.00

0.00

2.00

1.00

4.00

5.00

1.00

0.00

1.00

2.00

3.00

2.00

19.00

8.00

0.00

20.00

9.00

5.00

10.00

5.00

8.00

6.00

4.00

1.00

7.00

3.00

11.00

15.00

30.00

4.00

4.00

6.00

7.00

6.00

5.00

36.00

14.00

29.00

25.00

7.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

6.00

2.00

2.00

0.00

2.00

4.00

11.00

3.00

2.00

6.00

0.00

0.00

1.00

9.00

7.00

1.00

13.00

0.00

3.00

4.00

4.00

16.00

10.00

6.00

5.00

2.00

4.00

9.00

8.00

6.00

8.00

7.00

3.00

20.00

17.00

17.00

6.00

5.00

2.00

9.00

3.00

8.00

5.00

33.00

7.00

6.00

2.00

5.00

11.00

10.00

20.00

29.00

26.00

9.00

1.00

1.00

1.00

0.00

0.00

1.00

1.00

4.00

1.00

2.00

1.00

0.00

3.00

2.00

2.00

2.00

1.00

0.00

3.00

2.00

3.00

9.00

0.00

2.00

6.00

5.00

8.00

1.00

4.00

8.00

6.00

3.00

1.00

0.00

7.00

1.00

2.00

2.00

2.00

1.00

1.00

3.00

1.00

3.00

6.00

2.00

3.00

9.00

4.00

7.00

12.00

24.00

18.00

7.00

7.00

2.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

2.00

1.00

1.00

0.00

0.00

0.00

2.00

0.00

1.00

1.00

2.00

0.00

3.00

2.00

1.00

0.00

0.00

0.00

0.00

0.00

2.00

4.00

3.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

4.00

2.00

2.00

0.00

1.00

5.00

2.00

2.00

2.00

0.00

2.00

1.00

6.00

3.00

5.00

4.00

2.00

7.00

6.00

0.00

9.00

8.00

9.00

9.00

3.00

18.00

7.00

1.00

4.00

8.00

6.00

3.00

7.00

4.00

0.00

2.00

3.00

1.00

1.00

5.00

2.00

2.00

3.00

5.00

4.00

4.00

6.00

4.00

10.00

4.00

3.00

3.00

3.00

0.00

teg
Appendix 1. OL-92 pollen counts

Samole Poaceae Larx/Ps Picea Pooulus Quercus Salix Sarc Sheph Tmert UK/Otht Sum Cyper Typ/Spc %AP %TCT

R5258 JQ

R5258 JS

R5258 JU

R5258 JV

R5258 JW

R5258 JY

R5258 KA

R5258 KB

R5258 KE

R5258 KG

R5258 Kl

R5258 KK

R5258 KM

R5258 KO

R5258 KQ

R5258 KS

R5258 KT

R5258 KU

R5258 KV

R5258 KW

R5258 KX

R5258 KY

R5258 KZ

R5258 LA

R5258 LC

R5258 LE

R5258 LI

R5258 LK

R5258 LM

R5258 LO

R5258 LP

R5258 LQ

R5258 LS

R5258 LU

R5258 LW

R5258 LY

R5258 MA

R5258 MC

R5258 ME

R5258 MG

R5258 Ml

R5258 MK

R5258 MM

R5171 IR

R5258 MO

R5258 MQ

R5258 MS

R5258 MU

R5258 MW

R5258 MY

R5171 IX

R5258 NA

R5258 NC

R5258 NE

R5258 NG

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

1.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

1.00

1.00

2.00

0.00

0.00

0.00

1.00

1.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

3.00

1.00

0.00

0.00

0.00

0.00

1.00

1.00

1.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

1.00

1.00

0.00

1.00

1.00

1.00

0.00

1.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

1.00

1.00

2.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

1.00

2.00

4.00

2.00

1.00

9.00

0.00

2.00

0.00

2.00

2.00

2.00

2.00

4.00

1.00

0.00

3.00

4.00

2.00

1.00

1.00

1.00

2.00

2.00

3.00

6.00

2.00

8.00

6.00

3.00

16.00

8.00

11.00

3.00

5.00

7.00

4.00

6.00

5.00

1.00

6.00

5.00

21.00

5.00

11.00

5.00

6.00

17.00

21.00

43.00

51.00

35.00

18.00

10.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

1.00

1.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

1.00

0.00

1.00

1.00

3.00

2.00

0.00

2.00

0.00

2.00

1.00

0.00

0.00

2.00

0.00

2.00

3.00

1.00

5.00

3.00

4.00

4.00

1.00

1.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

5.00

2.00

2.00

2.00

3.00

6.00

2.00

0.00

3.00

2.00

3.00

2.00

3.00

4.00

2.00

17.00

4.00

5.00

1.00

0.00

3.00

9.00

0.00

0.00

3.00

1.00

1.00

1.00

2.00

1.00

0.00

1.00

0.00

4.00

5.00

4.00

4.00

1.00

1.00

3.00

1.00

3.00

0.00

2.00

1.00

4.00

4.00

2.00

1.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

3.00

1.00

0.00

0.00

0.00

0.00

0.00

3.00

1.00

3.00

0.00

3.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

2.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

2.00

1.00

1.00

1.00

0.00

1.00

0.00

0.00

0.00

3.00

0.00

0.00

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

0.00

1.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

1.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

2.00

0.00

0.00

2.00

0.00

5.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

4.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

4.00

3.00

1.00

94.67

95.00

98.33

99.33

98.00

97.67

87.67

95.33

97.33

95.00

99.33

94.67

94.33

82.33

94.67

94.33

93.33

97.67

94.67

94.33

94.00

90.67

93.33

92.33

93.00

94.33

91.67

87.00

91.67

94.00

86.33

91.67

95.67

84.67

89.67

90.33

94.67

94.00

98.33

92.67

94.67

92.00

91.67

73.33

92.67

93.00

91.67

92.33

88.67

86.33

70.67

76.67

75.67

84.00

96.33

5.67

6.67

11.33

7.33

8.33

7.00

21.33

4.33

2.33

5.33

5.00

1.00

12.33

8.33

6.00

11.67

11.33

7.00

17.67

13.00

14.00

23.67

21.00

5.00

4.67

7.33

5.33

5.33

4.00

7.67

5.00

6.33

2.67

4.33

6.33

5.67

2.67

4.33

1.67

6.00

6.00

5.33

7.67

17.00

4.33

6.00

4.00

1.67

3.67

8.00

2.00

3.67

2.67

2.33

2.00
Appendix 1. OL-92 pollen counts

Samole Deothfnrt Sacci/2 Pinus TPine TCT Abies Alnus Artemlsia Carya ChenAm SCmp LngCmp LJgCmp Corylus Ephedra

R5258 Nl

R5258 NK

R5258 NM

R5258 NO

R5258 NO

R5258 NR

R5258 NS

R5258 NT

R5258 NU

R5258 NW

R5258 NY

R5258 OA

R5258 OB

R5258 OC

R5258 OE

R5258 OG

R5258 OH

R5258 OK

R5258 OM

R5258 OO

R5258 OQ

R5258 OR

R5258 OS

R5258 OU

R5258 OW

R5171 JR

R5258 OY

R5258 PA

R5171 JT

R5258 PE

R5258 PG

R5171 JV

R5258 PI

R5171 JW

R5258 PK

R5171 JX

R5258 PM

R5171 JY

R5171 JZ

R5171 KA

R5171 KB

R5171 KC

R5171 KD

R5171 KE

R5171 KF

R5171 KG

R5171 KH

R5171 Kl

R5171 KJ

R5171 KK

R5171 KL

R5171 KM

R5171 KN

75.35

75.55

75.75

75.95

76.15

76.25

76.35

76.45

76.65

76.85

77.05

77.25

77.35

77.45

77.65

77.85

77.95

78.25

78.50

78.65

78.85

78.95

79.05

79.25

79.45

79.50

79.65

79.85

80.00

80.25

80.45

80.50

80.65

80.75

80.85

81.00

81.05

81.25

81.50

81.75

82.00

82.25

82.50

82.75

83.00

83.25

83.50

83.75

84.00

84.25

84.50

84.75

85.00

61.00

63.00

30.00

60.00

54.00

44.00

34.00

38.00

54.00

52.00

43.00

38.00

57.00

51.00

42.00

34.00

55.00

52.00

45.00

36.00

52.00

46.00

42.00

40.00

39.00

26.00

38.00

44.00

13.00

39.00

52.00

11.00

25.00

22.00

41.00

10.00

24.00

22.00

15.00

25.00

24.00

26.00

14.00

19.00

20.00

11.00

6.00

7.00

14.00

2.00

11.00

5.00

11.00

214.00

211.00

236.00

212.00

202.00

204.00

167.00

209.00

188.00

220.00

196.00

190.00

198.00

185.00

159.00

217.00

193.00

197.00

157.00

154.00

203.00

215.00

192.00

203.00

209.00

179.00

172.00

180.00

165.00

203.00

175.00

157.00

199.00

206.00

187.00

113.00

190.00

173.00

141.00

200.00

219.00

195.00

170.00

171.00

137.00

142.00

129.00

165.00

151.00

181.00

140.00

213.00

202.00

275.00

274.00

266.00

272.00

256.00

248.00

201.00

247.00

242.00

272.00

239.00

228.00

255.00

236.00

201.00

251.00

248.00

249.00

202.00

190.00

255.00

261.00

234.00

243.00

248.00

205.00

210.00

224.00

178.00

242.00

227.00

168.00

224.00

228.00

228.00

123.00

214.00

195.00

156.00

225.00

243.00

221.00

184.00

190.00

157.00

153.00

135.00

172.00

165.00

183.00

151.00

218.00

213.00

9.00

14.00

20.00

17.00

28.00

32.00

77.00

35.00

31.00

15.00

43.00

57.00

37.00

58.00

84.00

45.00

34.00

23.00

86.00

92.00

34.00

30.00

52.00

39.00

44.00

76.00

75.00

69.00

80.00

45.00

65.00

81.00

65.00

42.00

58.00

105.0

78.00

78.00

112.0

47.00

36.00

54.00

87.00

89.00

112.0

93.00

111.0

91.00

97.00

87.00

109.0

51.00

60.00

3.00

0.00

1.00

1.00

4.00

2.00

2.00

2.00

4.00

0.00

0.00

1.00

2.00

0.00

2.00

1.00

1.00

2.00

3.00

2.00

2.00

6.00

5.00

3.00

1.00

0.00

4.00

0.00

1.00

1.00

3.00

1.00

0.00

0.00

1.00

0.00

1.00

0.00

0.00

1.00

0.00

0.00

2.00

2.00

0.00

4.00

0.00

4.00

1.00

5.00

0.00

6.00

3.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

5.00

0.00

5.00

1.00

2.00

2.00

0.00

1.00

5.00

2.00

6.00

1.00

0.00

0.00

4.00

0.00

0.00

4.00

1.00

0.00

3.00

1.00

2.00

0.00

2.00

6.00

3.00

1.00

9.00

0.00

1.00

13.00

0.00

3.00

0.00

10.00

0.00

3.00

8.00

6.00

2.00

0.00

7.00

0.00

4.00

6.00

14.00

0.00

9.00

0.00

11.00

1.00

3.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

1.00

3.00

0.00

0.00

0.00

3.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

0.00

4.00

1.00

2.00

1.00

0.00

0.00

1.00

2.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

1.00

1.00

1.00

4.00

0.00

0.00

1.00

3.00

0.00

1.00

3.00

1.00

8.00

0.00

5.00

1.00

3.00

0.00

4.00

1.00

3.00

2.00

2.00

3.00

1.00

0.00

0.00

0.00

2.00

2.00

1.00

1.00

2.00

0.00

0.00

5.00

1.00

1.00

1.00

3.00

5.00

1.00

0.00

1.00

3.00

1.00

5.00

1.00

1.00

6.00

2.00

1.00

4.00

2.00

1.00

1.00

10.00

0.00

4.00

4.00

2.00

1.00

1.00

0.00

1.00

6.00

10.00

7.00

5.00

6.00

4.00

6.00

10.00

2.00

1.00

0.00

1.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

3.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

1.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

0.00

1.00

1.00

0.00

2.00

1.00

0.00

2.00

1.00

1.00

2.00

1.00

0.00

0.00

2.00

2.00

1.00

0.00

1.00

0.00

0.00

0.00
Appendix 1. OL-92 pollen counts

Sample Poaceae Larx/Ps Picea Populus Quercus Salix Sarc Sheph Tmert UK/Othi Sum Cyper Typ/Sps %AP %TCT

R5258 Nl

R5258 NK

R5258 NM

R5258 NO

R5258 NQ

R5258 NR

R5258 NS

R5258 NT

R5258 NU

R5258 NW

R5258 NY

R5258 OA

R5258 OB

R5258 OC

R5258 OE

R5258 OG

R5258 OH

R5258 OK

R5258 OM

R5258 OO

R5258 OQ

R5258 OR

R5258 OS

R5258 OU

R5258 OW

R5171 JR

R5258 OY

R5258 PA

R5171 JT

R5258 PE

R5258 PG

R5171 JV

R5258 PI

R5171 JW

R5258 PK

R5171 JX

R5258 PM

R5171 JY

R5171 JZ

R5171 KA

R5171 KB

R5171 KC

R5171 KD

R5171 KE

R5171 KF

R5171 KG

R5171 KH

R5171 Kl

R5171 KJ

R5171 KK

R5171 KL

R5171 KM

R5171 KN

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

1.00

2.00

0.00

0.00

1.00

1.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

1.00

1.00

3.00

2.00

2.00

1.00

2.00

5.00

4.00

1.00

1.00

0.00

0.00

1.00

2.00

1.00

0.00

2.00

1.00

0.00

2.00

1.00

0.00

0.00

3.00

1.00

0.00

0.00

1.00

0.00

1.00

0.00

1.00

2.00

0.00

1.00

2.00

0.00

0.00

3.00

0.00

2.00

0.00

3.00

3.00

3.00

3.00

1.00

2.00

1.00

4.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

4.00

7.00

2.00

2.00

1.00

9.00

10.00

4.00

9.00

1.00

3.00

3.00

2.00

0.00

0.00

0.00

11.00

9.00

1.00

1.00

1.00

0.00

0.00

0.00

0.00

4.00

2.00

1.00

15.00

3.00

0.00

26.00

0.00

8.00

2.00

33.00

1.00

0.00

12.00

3.00

9.00

6.00

6.00

4.00

3.00

5.00

16.00

3.00

6.00

2.00

8.00

2.00

2.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

OJ0*

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

1.00

1.00

1.00

2.00

4.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

4.00

1.00

0.00

4.00

0.00

2.00

0.00

2.00

0.00

2.00

0.00

0.00

2.00

1.00

1.00

0.00

0.00

3.00

0.00

1.00

1.00

0.00

1.00

0.00

1.00

1.00

1.00

1.00

1.00

4.00

1.00

1.00

1.00

1.00

3.00

4.00

1.00

2.00

1.00

7.00

3.00

6.00

1.00

9.00

1.00

6.00

1.00

2.00

5.00

7.00

3.00

14.00

3.00

8.00

1.00

8.00

1.00

7.00

2.00

0.00

0.00

0.00

1.00

1.00

3.00

3.00

1.00

0.00

3.00

4.00

2.00

1.00

1.00

3.00

1.00

1.00

5.00

2.00

5.00

0.00

0.00

3.00

4.00

1.00

3.00

1.00

2.00

4.00

3.00

0.00

3.00

4.00

6.00

5.00

5.00

3.00

9.00

2.00

6.00

6.00

9.00

5.00

4.00

7.00

10.00

2.00

7.00

8.00

4.00

3.00

3.00

6.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

300

0.00

1.00

1.00

4.00

1.00

3.00

5.00

1.00

4.00

0.00

3.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

2.00

0.00

0.00

2.00

2.00

0.00

0.00

0.00

1.00

0.00

0.00

0.00

1.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

4.00

1.00

0.00

0.00

2.00

5.00

1.00

1.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

1.00

0.00

0.00

1.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

97.00 3.00

98.33 4.67

96.67 6.67

98.00 5.67

97.67 9.33

98.67 10.67

98.33 25.67

97.33 11.67

96.00 10.33

98.67 5.00

97.67 14.33

97.33 19.00

99.33 12.33

98.67 19.33

96.67 28.00

99.67 15.00

99.00 11.33

96.67 7.67

98.00 28.67

97.33 30.67

97.67 11.33

99.00 10.00

98.67 17.33

96.67 13.00

98.00 14.67

96.00 25.33

98.33 25.00

99.00 23.00

92.67 26.67

98.00 15.00

98.67 21.67

93.00 27.00

98.00 21.67

94.67 14.00

99.00 17.67

89.33 35.00

99.00 26.00

94.33 26.00

94.67 37.33

94.00 15.67

98.33 11.33

97.67 18.00

94.67 29.00

97.00 29.67

93.00 37.33

89.33 31.00

89.00 37.00

93.33 30.33

93.33 32.33

94.00 29.00

91.00 36.33

93.67 17.00

96.00 20.00
U.S. DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY

THERMOLUMINESCENCE AND OPTICAL DATING OF FINE SILT-SIZE 

FELDSPARS FROM MUD FROM OWENS LAKE, CALIFORNIA CORE OL-92

by 

Glenn W. Berger1

Open-File Report 98-132 (part 10)

This report is preliminary and has not been reviewed for conformity with U.S. Geological 

Survey editorial standards (or with the North American Stratigraphic Code). Any use of 

trade, product, or firm names is for descriptive purposes only and does not imply 

endorsement by the U.S. Government

Desert Research Institute, Reno NV 89512

1998
Introduction

The thermoluminescence (TL) signal from most polymineral fine-silt-size samples is 

dominated by the signal from the feldspar family. As well, the particular optical-dating method 

employed here (IR-OSL, see below) produces a signal from only the feldspars within a 

polymineral sample. Thus, this project essentially dates fine-silt-size feldspars.

Preliminary results are reported here for samples collected from the upper 80 m of the 323- 

m deep core OL-92 from Owens Lake. Based on prior experience (e.g., Berger, 1988, 1990, 

1995; Berger and Easterbrook, 1993; Berger and Anderson, 1994) with dating lake sediments by 

TL, only fine-grained beds were targeted for sampling. These horizons are believed to be most 

likely to contain the maximum fraction of feldspar grains that have been exposed to daylight before 

burial. Uniform exposure of all grains to daylight is required to meet the principal assumption of 

zeroing of luminescence sediment dating. A good basic discussion of other assumptions and 

principles is provided by Aitken (1985).

A primary objective of this study is to provide the first numeric dating of horizons beyond 

the usual radiocarbon ( 14C) limit of -30 ka, and spanning the time interval of the last 

interglaciation, inferred to be represented in the upper -80 m of Core OL-92 (Bischoff et al., 

1997). For the purposes of this study, the newer optical dating (Huntley et al., 1985) technique is 

also employed, to attempt to attain a higher resolution than that which traditionally has been 

provided by the TL method. For this purpose, only the infrared-stimulation version (IR-OSL) 

(e.g., Berger, 1995; Ollerhead et al., 1994; Wintle, 1994) of optical dating is used, wherein -880- 

nm light from light-emitting diodes produces a shorter-wavelength (ultraviolet to red) 

luminescence. The main advantage of IR-OSL over TL is that the former arises only from the 

feldspars within a polymineral sample, and the former is far more sensitive to zeroing than is TL, 

potentially facilitating greater precision in age determination.

Sampling

Samples reported here (Table 1) were collected by the author at Menlo Park under darkroom conditions, transported to the Desert Research Institute (DRI), and analyses begun. Samples 

for luminescence work were collected in light-tight tins, after removal under dim amber light of a 

3-mm thick zone from the face of the core split. Smaller samples for dosimetry measurements were 

collected subadjacent to the main samples, also in the form of cohesive chunks. Laboratory 

sample-preparation procedures have been outlined elsewhere (e.g., Berger, 1990; Wintle and 

Huntley, 1980).

Analytical Techniques

A luminescence age t = DE/DR> where DE is the so-called "equivalent dose", or sometimes 

called the paleodose (units Gy, 1 Gy = 100 rads). This is a measure of the post-depositional 

absorbed ambient ionizing radiation dose, and is derived from luminescence measurements. The 

term DR is the effective dose rate (units Gy/ka), and is derived from measurements of U, Th, K 

and water concentration. For U and Th measurements, the thick-source-alpha-particle-counting 

(TSAC) technique (Huntley and Wintle, 1981) was used. K was determined by commercial atomic 

absorption spectrophotometry. Radioactive secular equilibrium is assumed, an assumption 

confirmed by previous age-check studies with such lake sediments (cited above).

For both TL and IR-OSL measurements, the deep-blue luminescence near the known 410- 

nm emission from most K-rich feldspars was detected (e.g., Krbetschek et al., 1998). To convert 

the sample's fossil light to an absorbed-energy equivalent, calibrated laboratory beta (90Sr-90Y) and 

alpha ( Am) sources were used. Luminescence signal was recorded with an automated, highcapacity Daybreak Nuclear Model 1150 reader. Dose-response curves and other data were 

processed with author-produced software (e.g., Berger et al., 1987).

/73
Results and Comments

Dosimetry data are listed in Table 2. Ages and related luminescence data are listed in Table 

3. Many more analyses (on some of these and additional samples) remain to be completed before 

confident interpretation can be made. Of immediate interest are the high Th and U concentrations in 

some samples (Table 2). At first this was thought to indicate samples having post-depositional 

enrichments, but a comparison of the ages for samples 22 and 31 and for samples 35 and 37 (Table 

3) suggest that these relatively high U and/or Th values do not necessarily manifest such an opensystem (hence disequilibrium) behavior.

A second prominent feature of these results is the occurrence of an age reversal for samples 

31 and 35. Interpretation of and speculation about these results must await completion the full data 

set. For example, it is possible that significant age underestimation manifests the presence of 

malign (anomalous-fading luminescence) plagioclase feldspars. However, it is noteworthy that the 

IR-OSL ages for the three youngest samples and the TL age for sample 37 all fall closely on the 

inferred age-depth curve (Fig. 1) of Bischoff et al. (1997).

References

Aitken, M.J., 1985, Thermoluminescence Dating: Academic Press, San Diego, 351 p.

Berger, G.W., 1988, Dating Quaternary events by luminescence, in Easterbrook, D.J.,ed., Dating 

Quaternary Sediments: Geological Society of America, Special Paper 227, p. 13-50.

Berger, G.W., 1990, Effectiveness of natural zeroing of the thermoluminescence in sediments: 

Journal of Geophysical Research, v. 95, p. 12,375-12,397.

Berger, G.W., 1994, Thermoluminescence dating of sediments older than -100 ka. Quaternary 

Science Reviews, 13(5-7), 445-455.

Berger, G.W., 1995. Progress in luminescence dating methods for Quaternary sediments. In: 

N.W. Rutter and N. Catto (Editors), Dating methods for Quaternary deposits. Geological 

Association of Canada, GEOtextno. 2, 81-103.

Berger, G.W., and Anderson, P.M., 1994, Thermoluminescence dating of an Arctic lake core 

from Alaska: Quaternary Science Reviews, v. 13, p. 497-501.

Berger, G.W., and Easterbrook, D.J., 1993, Thermoluminescence dating tests for lacustrine, 

glaciomarine and floodplain sediments from western Washington and British Columbia. 

Canadian Journal of Earth Sciences, 30, 1815-1828.

Berger, G.W., Lockhart, R.A., and Kuo, J., 1987, Regression and error analysis applied to the 

dose-response curves in thermoluminescence dating: Nuclear Tracks and Radiation 

Measurements, v. 13, p. 177-184.

Bischoff, J.L., Stafford, Jr., T.W., and Meyer, R., 1997, A time-depth scale for Owens Lake

sediments of core OL-92: Radiocarbon dates and constant mass-accumulation rate, in 

Smith, G.I., and Bischoff, J.L., eds., An 800,000-Year Paleoclimate Record from Core 

OL-92, Owens Lake, Southeast California: Boulder, Colorado, Geological Society of 

America Special Paper 317, p.91-98

Huntley, D.J., and A.G. Wintle. 1981. The use of alpha scintillation counting for measuring 

Th-230 and Pa-231 contents of ocean sediments, Can. J. Earth Sci., 18,419-432.
Huntley, D.J., Godfrey-Smith, D.I., and Thewalt, M.L.W., 1985, Optical dating of sediments: 

Nature, v. 313, p. 105-107.

Krbetschek, M.R., Gotze, J., Dietrich, A., and Trautmann, T. 1998. Spectral information from 

minerals relevant for luminescence dating. Radiation Measurements (in press).

Ollerhead, J., Huntley, D.J., and Berger, G.W., 1994, Luminescence dating of the Buctouche 

Spit, New Brunswick: Canadian Journal of Earth Sciences, v. 31, p. 523-531.

Prescott, J.R., and Hutton, J.T., 1988, Cosmic ray and gamma ray dosimetry for TL and ESR: 

Nuclear Tracks and Radiation Measurements, v. 14, p. 223-227.

Wintle, A.G., 1994, Infrared-stimulated luminescence dating of sediments: Radiation 

Measurements, v. 23, p. 607-612.

Wintle, A.G., and Huntley, D.J., 1980, Thermoluminescence dating of ocean sediments: 

Canadian Journal of Earth Sciences, v. 17, p. 348-360.

ns~
TABLE 1.

Sample

OWN97-1 ti

tt

H

tt

H

If

-3

-5

-22

-31

-37

-35

Samples from Core OL-92

Slug Top 

(m)

5.49

9.45

20.19

64.14

74.42

75.96

79.60

Core/Drive/Slug/Depth 

(cm)

92-1/6/A/30.0-34.0

" /8/B/68.5-72.5

" /12/A/131.5-135.5

92-2/2/A/123.0-127.0

" /6/A/16.0-20.0

" /6/B/31. 0-35.0

" /8/A/l 15.5-1 19.5

Total Depth Texture 

(m)

5.81

10.16

21.51

65.39

74.60

76.29

80.78

silty mud

green clay

silty mud

laminated silty clay

silty mud

silty mud

green clay
Table 2. Dosimetry Data For Core OL-92

Sample

OWN97-1

OWN97-3

OWN97-5

OWN97-22

OWN97-31

OWN97-35

OWN97-37

Water"

(±0.05)

1.62

0.84

1.97

2.09

0.89

0.55

0.53

K2 O 

wt.%

(±0.05)

2.42

3.99

1.75

2.15

2.18

3.73

3.47

p*

M

ks" 1 cm"2

0.9436±0.0087

1.306±0.010

0.9101±0.0088

2.464±0.019

2.315±0.021

1.685±0.019

1.558±0.018

c *

^Th

ks" 1 cm"2

0.294±0.025

0.519±0.034

0.289±0.025

0.320±0.053

0.443±0.064

0.655±0.063

0.706±0.062

Th 

ppm

7.89±0.67

13.94±0.91

7.77±0.67

8.6±1.4

11.9±1.7

17.6±1.7

19.0±1.7

U 

ppm

5.08±0.21

6.15±0.28

4.85±0.21

16.75±0.44

14.62±0.53

8.05±0.51

6.66±0.51

b value

pGym

0.615±0

0.600±0

0.60±0.

1.10±0.

0.90±0.

1.0±0.2

1.0±0.2

" Measured saturation value for ratio of weight of water/weight of dry sample. Uncertainties here and elsewh

* Total and thorium count rates from finely powdered samples for thick-source-alpha-particle-counting (TSAC

1981]. C.-Qc Alpha effectiveness factor [Huntley et al., 1988; Berger, 1988].

d Estimated from the data of Prescott and Hutton [1988].

e Calculated with the conversion factors given by Berger [1988] and includes the cosmic ray component.
TABLE 3. TL and IR-OSL Data and Ages for Core OL-92"

Sample

OWN97-1

OWN97-3

OWN97-5

OWN97-22

OWN97-31

OWN97-37

OWN97-35

Mode

TL 

IRSL 

IRSL

TL 

IRSL 

IRSL

IRSL 

IRSL

IRSL 

IRSL

TL

TL

TL

Preheat* Bleachc

120°C/3d PB/560(3d) 

130°C/3d TB/780(4h) 

150°C/3d TB/780(4h) 

Average IRSL DE =

130°C/3d TB/400(3d) 

130°C/3d TB/780(4h) 

150°C/3d TB/780(4h) 

Average IRSL DE =

130°C/3d TB/780(4h) 

150°C/3d TB/780(4h) 

Average IRSL DE =

140°C/3d TB/FSL(3h) 

160°C/3d TB/FSL(3h) 

Average IRSL DE =

145°C/3d TB/400(3d)

150°C/3d TB/400(3d)

150°C/3d TB/400(3d)

IV

(Gy)

12.8±1.8 

18.5±2.5 

16.3±2.2 

17.4±2.0

53.1±2.0 

58.2±3.8 

57.9±3.4 

58.0±3.0

36.7±2.0 

32.9±2.1 

34.8±2.0

243 ±23 

280±31 

260±20

318±27

628 ±82'

3 19 ±40

Temp. /Time'

220-3 10°C 

l-35s 

l-15s

200-280°C 

l-95s 

l-95s

l-65s 

l-30s

l-65s 

l-35s

230-380°C

330-400°C

240-380°C

Age 

(ka)

6.9±1.

9.4±1.

14.24±0

15.6±1

26.3±1

87.2±8.

69.0±7

122 ±17

58.5±8.

a For all TL runs, the heating rate was 5C°/sec. The polymineral 4-11 /an size fraction was used 

measurements. Both TL and IRSL were detected at the 420±20 nm spectral region (bandpass 390
* The chosen pre-readout annealing (see Berger and Anderson, 1994; Berger, 1994; Ollerhead et 

rationale).

c The value in parentheses specifies the optical bleaching time. PB = "partial-bleach" protocol; 

method. Different optical-filter bandpasses were used for bleaching, as follows: 560 = 560-800 n

= 390-740 nm at 5% cut; 780 = >780 nm solar spectrum passed; FSL = full solar spectrum.

d Weighted mean equivalent dose plus average error over temperature or time interval in next col

saturating-exponential regression model (Berger et al., 1987) was employed for all samples.

e The temperature (TL) or time (IRSL) interval for which DE is calculated.

f The DE values show a detectable monotonic rise with readout temperature, indicating that a hig

temperature should have been used. The estimated DE average may underestimate somewhat the c
0

20

40

Q_ 

CD

60

80

age-depth curve of 

Bischoff et al (1997)

100

0 20 40 60 80 100 120 140 160

age ky

Fig. 1 

TL and IR-OSL dates for core OL-92

ISO
U.S. DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY

A TEST OF URANIUM SERIES DATING OF OSTRACODE SHELLS FROM 

THE LAST INTERGLACIATION AT OWENS LAKE, CALIFORNIA, CORE

OL-92

by

James L. Bischoff1 , Thomas D. Bullen 1 , Richard W. Canavan IV2, and Richard. M.

Forester3

Open-File Report 98-132 (part 11)

This report is preliminary and has not been reviewed for conformity with U.S. Geological 

Survey editorial standards (or with the North American Stratigraphic Code). Any use of 

trade, product, or firm names is for descriptive purposes only and does not imply 

endorsement by the U.S. Government

!U.S. Geological Survey, Menlo Park, California, 94025 

Connecticut College, New London CT 06320 

3U.S. Geological Survey, Denver Colorado 80225

1998
INTRODUCTION

A major deficiency in most paleoclimatic studies is the lack of good time calibration. 

Good dates are extremely rare for the time gap between the radiocarbon limit at about 35 

kyrs and the Brunhes-Matuyama magnetic reversal at 780 kyrs. This lack makes regional 

or world-wide correlation of short-lived climatic events from record to record extremely 

tenuous.

Such is the case at Owens Lake, California, where sediments of the time gap in 

question show a continuous record with clearly defined short and long-term climate 

cycling. The time-depth scale for Owens Lake core OL-92 (Bischoff et al., 1997b) is 

based on radiocarbon control for the uppermost 24 m (to 30,000 yrs), the Bishop ash bed 

at 304 m (at 759,000 yrs) and the inference of a constant mass-accumulation rate of 51.4 

g/cm2/1000 yr. The justification for using a constant mass-accumulation rate for the 

extrapolation is because the average mass-accumulation rate calculated for the 

radiocarbon-dated segment, using bulk densities derived from pore-water measurements, 

was found to be essentially the same as for the entire core down to the Bishop Ash, 

suggesting that an approximately constant accumulation rate prevailed throughout the last 

759,000 yrs. The resulting time-depth curve is reasonably robust back to about 50,000 

yrs, but is essentially extrapolated beyond. The position of Termination II (MIS 5/6 

boundary) based on the abrupt change in TIC, for example, appears at about 118,000 yrs 

(Bischoff et at., 1997a) instead of about 128,000 yrs predicted from orbital tuning 

(Martinson et al., 1987), and about 140,000 yrs B.P. as seen in the nearby Devils Hole 

record (Winograd et al., 1992). Thus, the time-depth model may be as much as 10 

percent in error at around 100,000 yrs, and is subject to modification as future progress is 

made on absolute dating of the core.

The time interval in question spans the range of U-series dating, which offers the 

possibility of providing chronological control back to 350 kyrs. Saline phases yielded 

excellent results on sediments from a drill core taken in downstream Searles Lake 

(Bischoff, et al. 1985). We had hoped to apply U-series dating to similar material in core 

O1-92, but saline minerals are lacking. Therefore, we attempted to apply the technique to 

ostracode shells. Ostracode shells are found throughout lacustrine sediments and present 

a heretofore untested material for U-series dating. Ostracodes are microscopic (adults 

about 0.2 to 3 mm in length) crustaceans having a shell (carapace composed of two 

valves) made of calcite. Like other arthropods they grow by molting and so produce a 

number of juvenile (instars) shells in addition to the adult shells. They commonly live in 

all but highly ephemeral surface water bodies and in oxygenated ground water. They are 

predominately benthic organisms, but many species can swim from spot to spot on the 

substrate and a few can be fully nektonic. Their shells are readily preserved as fossils in 

most sediments deposited in circumneutral to alkaline water bodies.

Ostracode shells have not been tested before because of their small size, their dispersal, 

and low concentration in a clay matrix presents difficulty in isolating a sufficient amount 

for analysis (50 mg). The requirement for successful dating is that the shells take up 

dissolved uranium (but not thorium) from lake water as they are grow. Uranium is 

generally soluble in natural waters, whereas thorium is insoluble. After death and burial, 

the shells must be closed to further uptake or loss or uranium. The age is determined by 

the build-up of 230Th which derives from the decay of 238U and 234U. We report here on 

the separation technique which yields sufficient sample for analysis, and on the results of 

uranium-series analyses by thermal ionization mass spectrometry (TIMS) for 6 samples 

from core OL-92. The results are generally encouraging and yield ages in the expected 

range, but indicate that the shells take up some initial thorium rendering ages somewhat 

too old.
METHODS

Sampling and separation/purification

We chose 6 ostracode-rich horizons from the interval 30 to 90 m based on Carter's 

(1997) reports on ostracode abundance in core OL-92. Samples of about 50 grams dry 

weight were taken at depths of 36.7 m, 40.6 m, 52.5 m, 55.7 m, 57.9 m, and 63.7 m, 

representing an approximate age range of 50 to 100 kyrs before present. Samples were 

frozen overnight, thawed, and suspended in 300 mis of hot distilled water to which 10 

grams of sodium bicarbonate were added. After cooling, about 60 grams of Calgon 

(sodium hexametaphospate, sodium carbonate, and soap) were stirred into the solution, 

and the suspension was allowed to sit for 24 hours. The suspension was then washed 

through a 100-mesh sieve, the fine fraction discarded and the coarser residue was retained 

and dried at room temperature. This residue, the sand fraction, contained the ostracode 

shells along with detrital sand grains. Ostracode shells were then separated from the sand 

by a combination of mica table, heavy liquids, and magnetic separator. The sample was 

first placed on a mica table, a vibrating inclined plate used to isolate mica grains. Equantshaped sand grains like quartz and feldspar tend to roll directly down the vibrating plate 

whereas platy minerals like micas and ostracode shells traverse a diagonal path. Thus, 

micas and ostracode shells were caught in a metal cup hung just below the exit point of 

the platy minerals. Samples were further cleaned using a heavy liquid. Samples were 

place in tubes filled with varying concentrations of methyliodine and acetone to produce 

a density gradient. The ostracode shells and contaminants sank to different levels in the 

column depending on their density. Shells were collected from the solution by filtering 

and the methyliodine was removed by washing with acetone. And finally, samples were 

passed through a Frantz magnetic-separator (vibrating inclined plane passing through a 

magnetic field). Microscopic examination indicated the samples at this stage were 

essentially 100% ostracode shells. The procedure was repeated once again for splits of 

samples at 40.6 m, and 55.7 m to determine if increased purification yielded cleaner 

isotopic results. 

TIMS analysis

Samples for thermal ionization mass spectrometry (TIMS) were fired at 600° to 

remove the organic matrix of the shells, and then dissolved in 7N HNOs and spiked with 

236U and 229Th and passed through anion exchange columns equilibrated with 7n HNOs. 

Th was stripped from the column using 6N HC1, and U was then stripped using Teflondistilled H2O. lOul of 0.15N HsPO4 was added to the Th fraction. Both Th and U 

fractions were evaporated to dryness, converted to nitrate form using 8N HNOs, and 

loaded onto the sample side of a double-Re filament for analysis on a Finnigan MAT 261 

solid-source mass spectrometer configured with adjustable faraday collectors and an ion 

counter. U isotopes were measured using a peak-hopping mode, using the sequence 

234U-238U, 235U, 236TJ.238TJ. Ion currents on the 238U beam were generally greater than 

10-12 a. Th isotopes were measured using a peak-hopping mode on the ion counter. 

Count rates for the 229Th and 230Th peaks were generally greater than 100 cps, and 

occasionally reached 500 cps which represents excellent ionization efficiency for the 1 to 

5 pg Th loads measured here. *

Dates were calculated from the resulting isotopic abundances and activities using age 

equations and half-lives given in Bischoff et al ( 1995).

RESULTS

Isotopic analyses (Table 1) show that the ostracode shells contain very high levels of 

uranium, ranging from 5 to 58 ppm. Thorium ratios (230Th/232Th) range from 3.3 to 5.5, 

and derived ages range from 75 to 155 kyrs, which are within the expected age range of 

the age-depth model. Analyses of the replicate samples at 40.6 m and 55.7 m for which
the purification process was repeated show no significant improvement and indicate no 

significant extraneous contamination. Ages are shown plotted against depth in Fig. 1.

DISCUSSION

The nominal dates of 4 of the six samples (36.7 m, 40.6 m, 55.7 m, and 57.9 m, Fig. 1) 

plot in stratigraphic order on a trend close to that predicted for a SPECMAP predicted age 

for Termination II. Samples at 52.5 m and 63.7 m, however, plot about 50 kyrs too old 

for either trend. Although the systematic relations of the 4 samples might suggest the 

SPECMAP trend is correct, the thorium ratios suggest these ages are somewhat too old 

by having initial 230Th.

The index of detrital contamination is given by the 230Th/232Th ratio (thorium ratio). 

Ratios less than about 20 (Bischoff and Fitzpatrick, 1991) generally indicate the presence 

of excessive extraneous Th, normally harbored by detrital clays that are mechanically 

inseparable from the authigenic phase. The ostracode shells have thorium rations of 3.3 

to 5.5, indicating the presence of significant non-radiogenic thorium. Such thorium 

generally renders the calculated age somewhat too old. Because the re-purified samples 

showed no improvement in the thorium ratio, the extraneous thorium must have been 

accumulated into the shell while the organism was alive. In marine and lake waters, 

thorium is concentrated on suspended particles, such as fecal pellets. It is likely, 

therefore, that the ostracodes ingested thorium while grazing on such particles, and 

incorporated it into their shells or into the organic matrix of the shells. Thus, at death the 

shells likely had an initial content of 230Th, and therefore, an initial "finite" 230Th age. 

This initial age depends on the initial 230Th/232Th, a value which cannot be 

unequivocally estimated. Detritus from a wide variety of sources including eolian dust, 

soils, and alluvial sediments have thorium ratios ranging from 0.25 to 1.25 (Szabo and 

Rosholt, 1982). Using the extremes of this range shows the effects of this initial thorium 

on the calculated age. The sample at 36.7 m has a nominal age of 78.5 kyrs, and a 

thorium ratio of 4.0. An initial ratio 0.25 results in a corrected age of 71.7 kyrs, closer to 

the model age of 53 kyr. An initial ratio of 1.5, however, results in a corrected age of 

42.7 kyrs, too young to be reasonable. Thus, it is not possible to make a general 

correction for initial thorium.

The results, therefore, although encouraging, are not sufficiently robust to yield highresolution calibration of OL-92 for MISD 5. They do, however, give ages in the expected 

range, and in approximate stratigraphic order. Therefore, ostracode dating may be useful 

and worth the effort to provide approximate ages for packages of outcroping lacustrine 

sediments, for which no other age indicators are available.

REFERENCES

Bischoff, J.L., Fitts, J.P., and Fitzpatrick, J.A. (1997a). Responses of sediment 

geochemistry to climate change in Owens Lake sediment: An 800 ky record of 

saline/fresh cycles. In "An 800,000-year geologic and climatic record from Owens 

Lake, California: Core OL-92" (G.I. Smith and J. Bischoff, Eds.), pp. 37-47. 

Geological Society of America Special Paper 317.

Bischoff, J.L., Stafford, T.W., Jr., and Rubin, M. (1997b). A time-depth scale for Owens 

Lake sediments of core OL-92: Radiocarbon dates and constant mass-accumulation 

rate. In "An 800,000-year geologic and climatic record from Owens Lake, California: 

Core OL-92" (G.I. Smith and J. Bischoff, Eds.), pp. 91-98. Geological Society of 

America Special Paper 317.
Bischoff, J.L., Rosenbauer, R.J., and Smith, G.I. (1985). Uranium-series dating of 

sediments from Searles Lake, California: differences between continental and marine 

climate records. Science 227, 1222-1221.

Bischoff J.L. and Fitzpatrick J. A., 1991. U-series dating of impure carbonates: An 

isochron technique using total-sample dissolution. Geochimica et Cosmochimica Acta, 

55, 543-554.

Carter, C. (1997). Ostracodes in Owens Lake sediments of core OL-92: Alternation of 

saline and fresh water forms through time. In "An 800,000-year geologic and climatic 

record from Owens Lake, California: Core OL-92" (G.I. Smith and J. Bischoff, Eds.), 

pp. 113-120. Geological Society of America Special Paper 317.

Martinson, D.G., Pisias, N.G., Hays, J.D., Imbrie, J., Moore, T.C., Jr., and Shackleton, 

N.J. (1987). Age dating and the orbital theory of the ice ages; development of a highresolution 0 to 300,000-year chronostratigraphy. Quaternary Research 27, 1-29.

Szabo, B.J., and Rosholt, J.N. (1982). Surficial continental sediments. In Uranium Series 

Disequilibrium: Applications to Environmental Problems (eds. M. Ivanovich and R.S. 

Haraion), pp. 246-267. Clarendon Press

Winograd, I.J., Coplen, T.B., Landwehr, J.M., Riggs, A.C., Ludwig, K.L., Szabo, B.J., 

Kolesar, P.T., and Revesz, K.M. (1992). Continuous 500,000-year climate record 

from vein calcite in Devils Hole, Nevada. Science 258 255-260.
Table 1 

U-series analyses and derived nominal ages of ostracod shells from Owens Lake core OL-92*

Sample depth 

(m)

36.7

40.6

it

52.5

55.7

n

57.9

63.7

U 

(ppm)

29.710.7

53.810.6 

57.810.7

20.310.2

24.210.3 

26.010.3

7.910.1

5.010.1

234y/238j

1.2610.06

1.2110.02 

1.2110.02

1.2410.02

1.2110.02 

1.2310.02

1.2110.02

1.2010.02

230Th/232Th

4.0

4.6 

4.1

3.2

5.3 

5.5

3.3

3.7

230Th/234Th

0.5310.03

0.5110.02 

0.4810.02

0.7910.03

0.6210.02 

0.5910.02

0.6310.02

0.7910.03

Udate 

(ka)

78.516.2

75.513.6 

69.513.3

155.1110.8

100.315.4 

92.315.0

104.615.8

155.2111.1

* Isotope ratios are in terms of activities (dpm/g); ditto marks (") refer to replicate analyses on 

aliquots purified a second time.
Figure 1

Depth plot of U-series ages of ostracode 

shells from Owens Lake core OL-92.

0

-20

CO

CD »-« 

0)

E

Q. 

0)

-40

-60

-80

-100

0

time-depth curve of 

Bischoff et al (1997b)

0-

Termination II

50 100 

Age, kyrs

150

111