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United States Department of the Interior Geological UNITED STATES DEPARTMENT OF THE INTERIOR GEOLOGICAL SURVEY ISOSTATIC EFFECTS OF THE LAST GLACIATION IN THE PUGET LOWLAND, WASHINGTON By Robert M. Thorson Open-File Report 81-370 This report is preliminary and has not been edited or reviewed for conformity with Geological Survey standards or nomenclature. ABSTRACT During the Vashon Stade of the late Pleistocene Fraser Glaciation, the Puget lobe of the Cordilleran Ice Sheet advanced into western Washington, inundating the Puget lowland between the Cascade Range and Olympic Mountains. During the systematic recession of the Puget lobe between about 14,000 and 13,000 years B. P., a complex system of proglacial lakes formed in the troughs of the Puget Sound region. Initially the lakes drained south via the Chehalis River to the Pacific Ocean, but lake drainage was later directed northward to the Strait of Juan de Fuca. Following deglaciation of the lowland about 13,000 years ago, marine waters invaded the areas formerly occupied by proglacial lakes. The surfaces of the proglacial lakes (water planes) that formerly occupied the Puget lowland can be reconstructed from lake spillways that controlled the height of the lakes, and from outwash deltas built at the lake surfaces. The marine limit in the northern Puget lowland is also a nearly isochronous water plane, and can be reconstructed from the distribution of raised marine deltas and glacial-marine drift and of meltwater channels. The ancient marine and lacustrine water planes were determined independently, yet both indicate a regional gradual northward increase in the amount of postglacial deformation, reaching a maximum of about 140m in the northern Puget lowland. The major cause of postglacial deformation in the Puget lowland was a return to isostatic equilibrium following deglaciation. At least one, and possibly three, significant departures from the regional pattern of uplift near Seattle were probably caused by Holocene tectonic warping and (or) possibly by variations in the rate of glacier retreat. Comparison of the predicted and observed isostatic responses indicates that the substratum below the Puget lowland responded rapidly to the mass imbalance caused by ice-sheet glaciation. As much as 35 to 70 percent of isostatic equilibrium apparently was attained at the glacial maximum, which occurred less than several thousand years after glaciers invaded the Puget lowland. This inferred rapid response is supported by relatively low estimates for the effective viscosity of the substratum obtained from minimum uplift rates following deglaciation (3 cm/yr). The large amount and rapid rate of isostatic rebound in the Puget lowland within the last 13,000 years may relate to regional crustal structure, Quaternary faulting, and recent seismicity. ACKNOWLEDGEMENTS I wish to thank the staff of the Puget Sound Earth Science Applications Project for their consistent help during this investigation. I would especially like to thank Fred Pessl, Jr., who originated and administered this research, and provided encouragement and guidance during the entire study. This research also profited from informal discussions with M. D. Crittenden, A. S. Post, R. B. Waitt, Jr., and J. C. Yount of the U. S. Geological Survey. This study greatly benefited from close cooperation with the Department of Geological Sciences at the University of Washington. S. C. Porter provided valuable advice and encouragement on many occasions. R. C. Bostrom, R. S. Crosson, E. B. Leopold, C. R. Raymond and A. L. Washburn also gave me helpful suggestions and support. S. C. Porter, A. S. Post, W. A. Long (U. S. Forest Service) and G. W. Thorson (Washington Division Geology & Earth Resources) generously allowed me to use their unpublished data. I wish to thank R. C. Bostrom, Fred Pessl, Jr., S. C. Porter, R. B. Waitt, Jr., and J. L. Yount for their thoughtful reviews of this report. TABLE OF CONTENTS Page INTRODUCTION I RECONSTRUCTION OF THE PUGET LOBE DURING THE VASHON STADE 10 DEGLACIATION OF THE PUGET LOWLAND 16 Pattern of Ice Retreat 16 Previous Studies Regional Distribution of Glacial Features Theoretical Ice Marginal Configurations Deglaciation of the Northwest Puget Lowland Radiocarbon Chronology of the Puget Lobe 27 PATTERN OF POSTGLACIAL DEFORMATION IN THE PUGET LOWLAND 28 Lake Shoreline (Water-Plane) Data 28 Lake Sequence Proglacial Lake Deposits Marine Limit Data 55 Relative Sea Level Global (Eustatic) Sea Level Pattern of Postglacial Deformation 64 Integration of Lacustrine and Marine Data Potential Error Inferred Pattern CAUSES OF POSTGLACIAL DEFORMATION 71 Dominant Pattern 71 Inflections 75 RATES OF ISOSTATIC UPLIFT 79 Northern Puget Lowland 79 Western Washington and Southwestern British Columbia 80 COMPARISON OF OBSERVED AND PREDICTED ISOSTATIC DEFORMATION 86 Comparison by Mass Compensation 86 Measured Anomaly Predicted Anomaly Page Comparison by Depth of Compensation 89 Restrained Rebound 90 Relative Isostatic Compensation 91 IMPLICATIONS 92 CONCLUSIONS 93 REFERENCES CITED 95 LIST OF FIGURES Page Figure I. Map of the Puget lowland, Washington, showing 3 localities mentioned in the text and the maximum extent of the Puget lobe during the Vashon Stade. 2. Radiocarbon dates pertaining to the Vashon 8 advance of the Puget lobe in the Puget lowland, Washington. 3. Diagram showing the maximum and minimum ages for 9 the advance and retreat of the Puget lobe during the Vashon and Everson Stades. 4. Map showing the maximum extent of the Puget lobe I I and the direction of flow at the base of the glacier, as inferred from ice-flow indicators. 5. Longitudinal profiles of the Puget lobe compared 13 to a theoretical equilibrium glacier profile and to the present longitudinal profile of Malaspina Glacier, Alaska. 6. Contour map of the reconstructed ice surfaces of 15 the Puget lobe during the Vashon Stade. 7. Generalized geologic map of the Puget lowland 17 showing landforms and sediments related to retreat of the Puget lobe. 8. Map of the Puget lobe showing successive 20 configurations of the ice margin during glacial retreat. 9. Map showing deposits and features formed during 22 deglaciation in the northwestern Puget lowland. 10. Bouldery ice-contact stratified drift near 25 Center, WA. I I. Inferred sequence of proglacial lakes in the 29 Puget lowland, based on the assumption that no postglacial warping or spillway erosion occurred. 12. South end of Clifton channel near Belfair showing 30 typical channel form. Page Figure 13. Si I ty lake clay near Eldon along west shore of 35 Hood Canal. 14. Generalized diagram showing relation of pro- 36 glacial lake features to the lake surface. 15. View of Redmond delta. 39 16. Topset-foreset contact in the Steilacoom delta. 41 17. Profile of water-planes associated with deglacia- 46 tion of the Puget lowland plotted along line A-A1 of Figure 23. 18. Deformation in ice-contact strata within the 48 McKenna Falls delta. 19. Geologic features used to reconstruct position of 56 relative sea level in the northern Puget lowland. 20. Typical appearance of pebbly glacial-marine silt 57 in northern part of study area. 21. Contour maps showing types of meltwater channels 60 common in the northern Puget lowland. 22. Map showing inferred location of Everson-age 63 marine limit in the northern Puget lowland. 23. Contour map showing inferred postglacial 65 deformation in the Puget lowland. 24. North-south profile of inferred net postglacial 66 deformation parallel to the axis of the Puget lowland along line A-A1 (Fig. 23). 25. East-west profile of inferred postglacial 67 deformation plotted normal to the axis of the Puget lowland along line B-B1 (Fig. 23). 26. Smoothed isopach map of the Puget lobe. 72 27. Relation between the inferred mass of the Puget 73 lobe and the distance north of the Vashon limit. 28. Relation between inferred postglacial deformation 74 and inferred mass of the Puget lobe south of control point. Page Figure 29. Map showing boundaries of crustal blocks in the 76 Puget lowland inferred from geophysical data (from Gower, 1978). 30. Radiocarbon-dated sea-level relations in the 82 Fraser lowland, B.C. 31. Hypothetical pattern of isostatic deformation 87 beyond the margin of the Puget lowland. LIST OF TABLES Page Table I. Late Quaternary geologic climate units for western 4 Washington 2. Radiocarbon dates pertaining to glaciation of the 6-7 Puget lowland during the Vashon Stade. 3. Lacustrine features used to reconstruct proglacial 40 lake surfaces associated with deglaciation of the Puget lowland. 4. Everson-age deposits in the northern Puget lowland 58 inferred to be glacial-marine in origin. 5. Radiocarbon dates from the Fraser lowland, B.C. 81 associated with postglacial emergence. 6. Minimum postglacial isostatic uplift rates for the 85 northern Puget lowland, Washington, and the Fraser lowland, B. C. 7. Comparison between the masses of the measured post- 88 glacial isostatic anomaly and the expected equili­ brium anomaly at the Vashon maximum. LIST OF PLATES Plate I. Map of the Puget lowland, Washington, showing selected lacustrine and marine features formed during deglaciation (in pocket). INTRODUCTION Much attention is currently being focused on the tectonic behavior of western Washington. Recent studies have attempted to characterize the nature and rate of regional uplift, as well as the pattern of recent faulting and seismicity (Crosson, 1973, 1977; Gower, 1978; Moen, 1971). A thorough understanding of Quaternary deformation in the Puget lowland is needed, particularly where it affects the rates of sea-level change and the potential for causing damaging earthquakes. Such an understanding requires that the character, rates, and causes of postglacial defor­ mation be determined as accurately as possible. Glacial isostatic rebound has been a major cause of postglacial deformation in the Puget lowland. Broad uplift occurred in response to loading and unloading of the region by the advance and retreat of the Cordilleran Ice Sheet. Isostatic uplift may also have set up stresses large enough to have caused displacement or warping along major tectonic structures and along small faults in the surficial sediments.
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