Of the Lower Alaska Peninsula

•

The Ar~hae()logy 1.1 , of the Lower Alaska Peninsula

" J

H'erbert D. G. Maschner, Ph.D. James W. Jordan, M.A. B~ian W. Hoffman, M.A. ~ Tina M. Dochat, Ph.D. ARCHAEOLOGY OF THE LOWER ALASKA PENINSULA: FIELD REPORT OF THE 1995 AND 1996 UNIVERSITY OF WISCONSIN ARCHAEOLOGICAL AND GEOLOGICAL SURVEY OF THE IZEMBEK NATIONAL WILDLIFE REFUGE AND ADJACENT LANDS

BY 1 2 HERBERT D.G. MASCHNER , Ph.D. JAMES W. JORDAN , MA. 3 BRIAN W. HOFFMAN , MA, AND TINA M. DOCHAT\ Ph.D.

WITH THE ASSISTANCE OF 5 6 JESSICA CZEDERPll..TZ , MEGAN PARTLOW , MA, 7 8 9 KATHERINE L. REEDy , BA, ANDY ZEIGERT , CAROLINE L. FUNK , MA, lO ll BRIAN J. VAN PAY , BA AND TY BECK

REPORT 4 OF THE LABORATORY OF ARCTIC AND NORTH PACIFIC ARCHAEOLOG~UNIVERSITYOF WISCONSIN-MADISON

SUMBITTED TO: THE UNITED STATES FISH AND WILDLIFE SERVICE; THE NATIONAL SCIENCE FOUNDATION; THE ALEUT CORPORATION; THE ALEUTIANS EAST BOROUGH; THE COMMUNITITIES OF COLD BA~ FALSE PASS, AND KING COVE; THE ALASKA STATE HISTORIC PRESERVATION OFFICE; AND THE GREATER ALASKA ARCHAEOLOGICALCOMMUNITY; 15 MAY 1997

Reference as: Maschner, Herbert D. G., James W. Jordan, Brian W. Hoffman, and Tina M. Dochat (1997). The Archaeology ofthe Lower Alaska Peninsula. Report 4 of the Laboratory of Arctic and North Pacific Archaeology, University ofWisconsin - Madison.

1,3,5,6,7,8,9,11 Department of Anthropology, 5240 Social Science, University ofWisconsin, Madison, WI 53706. 2 Department of Geography, University of Wisconsin, Madison, WI 53706. 4 Department of Geology and Geophysics, University of Wisconsin, Madison, WI 53706. 10 Environmental Remote Sensing Center, University ofWisconsin, Madison, WI 53706. PREFACE AND ACKNOWLEDGEMENTS

This report represents our fIrst attempt to consolidate and summarize the available archaeological data from the lower Alaska Peninsula. To do this we have drawn heavily on the field notes and map data collected over the last two field seasons, on the geological and geomorphological observations made by TIna Dochat (1997), James Jordan (1997), and James Funk (1973), on previous archaeological reports by Allen McCartney (1974), Steve Klingler (n.d.), Michael Yarborough (n.d.), and the BIA-ANCSA (US BIA 1991). For the sites that were discovered prior to our investigations, or were only briefly visited by our project, the site descriptions already in the literature are the most complete. Thus, many ofthe site descriptions presented inthis report for sites originally investigated by the USFWS (Klingler and Yarborough) and the BIA ANCSA (US BlA 1991), are either paraphrases, direct quotes, or summaries ofthese previous, well organized descriptions. We have done this so that all ofthe critical information about the sites in the project area can be found in a single document. The BIA data collected and described by Joseph D. Bartolini, D. Randall Cooper,

Brian W. Hoffman, and David P. Staley have been critical to the success ofthis project, both in presenting the site descriptions and in the analysis and interpretation ofthe findings.

Throughout we have used standard Alaska State Historic Preservation Office (SHPO) nomenclature

(AHRS#) for the archaeological sites. The site numbers used by the BIA ANCSA and other, previously used numbers, are reported where applicable. In some cases descriptive, native, or idiosyncratic site names have been assigned and are used as welL As the reader will become aware, this is a report in progress. We are in the midst ofplanning the 1997 field season, completing the GIS and photogrammetric research, and preparing for a five-year excavation program that will begin in

1998. Papers on specific aspects ofthis project will be presented at the 1998 Annual Meeting ofthe

Alaska Anthropological Association. TIna Dochat's dissertation on the glacial history ofthe lower

2 Alaska Peninsula is now complete. Dissertations by Brian Hoffman on late Aleut household

organization and by Jim Jordan on the coastal geomorphology ofthe region will be completed in

1998.

- The 1995-1996 fieldwork was done by archaeologists Herbert Maschner, Caroline Funk, Kate Reedy,

Izaak Sawyer, Neal Endacott, Brian Van Pay, Trent Deboer, Abe Smith, and geologists Tina Dochat

and Jim Jordan. Portions ofthe data presented in this report were collected as part ofthe BlA

ANSCA 14(h)1 surveys, and we would especially like to thank Ken Pratt, Randy Cooper, and Steve

Street ofthe BlA-ANSCA office for providing critical data and reports. We would like to thank Steve

Klingler for access to data from the 1979 Izembek survey that was led by Michael Yarborough.

Jessica Czederpiltz analyzed the fish and bird remains from a number ofsites. Andy Zeigert sorted

and described bulk samples from three sites. Katherine Reedy and Erin Kester analyzed the largest

shellfish collections and cataloged many ofthe remains. Megan Partlow analyzed most ofthe

mammalian fauna. Brian Van Pay did analyses oflithic raw materials and is now organizing the

geographic information system. Hee-Bum Lee did most ofthe photogrammetric work which will be

presented inthe next version ofthis report. David McJunkin ofthe OW radiocarbon facility prepared

many ofour samples for accelerator mass spectrometer dating and arranged for their analysis at the

University ofArizona and at Lawrence Livermore Laboratory. Elizabeth Pillart, Director ofthe OW

Department ofZoology comparative collection graciously provided access to her research collections

for our faunal analyses. Brian Hoffman assisted with many aspects ofthis project, provided critical

data, and directed student research in the lab.

3 Much appreciation is given to The Aleut Corporation and the Isanotski Corporation ofFalse Pass for access to their lands and sites. Debbie Corbett and Chuck Diters ofthe US Fish and Wildlife Service

(Anchorage) and the entire staff ofthe Izernbek National Wildlife Refuge, Cold Bay (Greg Siekaniec,

Bob Schulmeister, Sue Schulmeister, Chris Dau, and Kathryn Hermann) who contributed in so many ways that this project would have been a complete failure without their assistance and we shall be forever grateful for their encouragement. Carole Seyfrit, Noel Broadbent, Douglas Seigel-Causey, all ofthe Office ofPolar Programs at the National Science Foundation, provided critical and important advice and assistance throughout the last two years; we are lucky to have such great people at NSF.

The field data described in this paper were collected with support from the U.S. Fish and Wildlife

Service, the Graduate School ofthe University ofWisconsin, an EPA Dissertation Fellowship awarded to Jim Jordan, National Geographic Society grant 5728-96 awarded to Dave Mickelson and

Tina Dochat, NSF Grant OPP-9630072 awarded to Maschner, and NSF Grant OPP-9629992 awarded to Maschner and Hoffman. The entire cast ofproject would like to thank Debbie Corbett for letting us sleep on her floor, use her house as a base ofoperations before Cold Bay, and for the general good nature she puts forward when 14 people and 6000 pounds ofgear appear on her door step once a year. Finally, Maschner would like to specifically acknowledge Brian Hoffman, an extraordinary student and friend, who introduced him to the lower Alaska Peninsula.

All errors, omissions, and faults oflogic are Maschner's (but you can blame Jordan, Hoffman,

Dochat, Dave McMahan, Debbie Corbett, Steve Street, Owen Mason, or any other ofmy friends if they are closer at hand).

4 TABLE OF CONTENTS

lltlePage 1 Preface and Acknowledgments 2 Table of Contents 5 List ofFigures 8 - List ofTables 9 Introduction 10 Background 17 Regional Environment 17 Previous Archaeological Research 20 The Lower Alaska Peninsula Project 23 Field Methods 23 Field Results 28 Glacial History 28 Coastal Geomorphology 37 Archaeology 47 Site Recording and Methods 52 Radiocarbon dating 53 Geographic Summary ofthe Survey Locales 57 Moffet Lagoon- Joshua Green River 57 Izembek Lagoon 58 Kinzarof Lagoon- West Cold Bay 59 Morzhovoi Bay- Little, Middle, and Big Lagoons 60 Settlement History and Initial Observations ofVillage Evolution 62 Russell Creek Phase? 63 Moffet Phase 63 Kinzerof Phase 71 Early Izembek Phase 74 Late Izembek Phase 76 Cape Glazenap Phase 79 Big Lagoon Phase 82 Morzhovoi Phase 85 Trends is Settlement and Village Organization 87 Conclusion 91 Investigations at Previously Recorded Archaeological Sites 93 XCB-OOI 94 XCB-002 97 XCB-003 100 XCB-004 103 XCB-005 107 XCB-006 109 XCB-021 112 XCB-022 116 XCB-023 118 XCB-024 122 XCB-025 124 5 XCB-026 127 XCB-027 129 XCB-028 132 XCB-029 137 XCB-030 142 XCB-031 149 XCB-032 151 XCB-033 151 XCB-036 151 XCB-037 152 XCB-038 152 XCB-039 153 XCB-040 154 XCB-041 155 XCB-042 155 XCB-043 157 XCB-044 157 XCB-045 158 XCB-046 158 XCB-047 162 XCB-048 162 XCB-049 163 XCB-050 163 XCB-051 164 XCB-052 165 XCB-053 165 XCB-054 166 XCB-055 169 XCB-On 169 XCB-073 169 XCB-074 169 XCB-075 169 XCB-076 169 XCB-077 169 XCB-078 169 XCB-120 170 XCB-121 172 XCB-122 175 Investigations at Newly Recorded Archaeological Sites 177 XCB-079 177 XCB-080 177 XCB-081 177 XCB-082 179 XCB-083 179 XCB-084 182 XCB-085 182 XCB-086 182 XCB-087 184 6 !s,_~

XCB-088 184 XCB-089 184 XCB-091 184 XCB-092 184 ~ XCB-093 185 XCB-094 185 XCB-095 190 XCB-096 190 XCB-097 194 XCB-098 194 -~ XCB-099 197 XCB-lOO 200 XCB-lOl 200 ~ XCB-102 203 XCB-103 203 XCB-I04 205 XCB-105 205 XCB-106 208 XCB-I07 208 XCB-I08 208 XCB-109 208 XCB-110 211 XCB-lll 214 XCB-112 214 XCB-113 214 XCB-114 214 XCB-115 216 XCB-116 216 XCB-117 /-., 216 XCB-118 217 XCB-119 217 XCB-122 217 L:'" References Cited 218

7 LIST OF FIGURES

1. Map of the North Pacific showing the project area. 10 2. Map ofthe lower Alaska Peninsula showing regional geographic features 12 and place names. 3. Map ofthe lower Alaska Peninsula showing surveyed areas and projects. 16 4. Map ofthe lower Alaska Peninsula showing all archaeological sites by 48 project. 5. Radiocarbon Chronology for the Lower Alaska Peninsula and Unimak 55 Island. 6. Map ofall sites dating to the Moffet, Kinzerof, and Izembek Phases. 65 7. Map ofXCB-054, the Cove Island Site. 66 8. Model for Sedentism in Island Settings 68 9. Map ofXCB-103, Dark Side ofthe Lagoon. 73 10. Map ofXCB-005. 75 11. Map ofXCB-003 77 12. Map ofXCB-121. 78 13. Map of all sites dating to the Cape Glazenap, Big, Lagoon, and 80 Morzhovoi Phases. 14. Map ofXCB-001. 81 15. Map ofXCB-094. 84 16. Map ofall sites with nucleus-satellite houses and showing major salmon 86 stream drainages. 17. Map ofXCB-001. 96 18. Map ofXCB-002. 99 19. Map ofXCB-003. 101 20. Map ofXCB-004. 106 21. Map ofXCB-005. 108 22. Map ofXCB-006. 111 23. Map ofXCB-021. 115 24. Map ofXCB-022. 117 25. Map ofXCB-023. 120 26. Stratigraphic profile for XCB-023. 121 27. Map ofXCB-024. 123 28. Map ofXCB-025. 126 29. Map ofXCB-026. 128 30. Map ofXCB-027. 131 31. Map ofXCB-028, Section 1. 134 32. Stratigraphic profile for XCB-028 135 33. Map ofXCB-028, Section 2. 136 34. Map ofXCB-029. 140 35. Stratigraphic profile for XCB-029. 141 36. Map ofXCB-030. 148 37. Map ofXCB-031. 150 38. Map ofXCB-040. 156 39. Map ofXCB-046, Section 1. 160 40. Map ofXCB-046, Section 2. 161 41. Map ofXCB-054. 167 8 42. Stratigraphic profile from XCB-054. 168 43. Map ofXCB-120. 171 44. Map ofXCB-121. 174 45. Map ofXCB-123. 176 46. Map ofXCB-081. 178 47. Map ofXCB-082 (not yet drafted). 180 48. Map ofXCB-083. 181 49. Map ofXCB-084. 183 50. Map ofXCB-094. 188 51. Stratigraphic profile oftest excavations done at XCB-094. 189 52. Map ofXCB-096. 192 53. Stratigraphic profiles oftest excavations done at XCB-096. 193 54. Map ofXCB-097. 195 55. Map ofXCB-098. 196 56. Map ofXCB-099. 198 57. Stratigraphic profile oftest excavations done at XCB-099. 199 58. Map ofXCB-101. 201 59. Stratigraphic profile oftest excavations done at XCB-101. 202 60. Map ofXCB-103. 204 61. Map ofXCB-1 04. 206 62. Stratigraphic profile oftest excavations done at XCB-104. 207 63. Map ofXCB-108. 209 64. Map ofXCB-109. 210 65. Map ofXCB-IlO. 212 66. Stratigraphic profile oftest excavations done at XCB-llO. 213 67. Map of XCB-l13. 215

LIST OF TABLES

1. Geological radiocarbon dates onthe lower Alaska Peninsula. 46 2. Sites found during the 1995-1996 archaeological survey. 49 3. Sites found on previous archaeological surveys. Many have been 50 reinvestigated by this project. 4. Archaeological radiocarbon dates for all archaeological sites on Dnimak 56 Island and the lower Alaska Peninsula 5. Archaeological phase chronology for the lower Alaska Peninsula. 63

9 INTRODUCTION

The lower Alaska Peninsula (Figure 1), specifically the region incorporated by, and immediately surrounding the Izembek National Wildlife Refuge, is critical to the investigation ofa number of issues that have dominated the anthropological literature in the last 30 years. Izembek Lagoon is the largest and western-most lagoon system on the Bering Sea coast ofthe Alaska Peninsula It is located just north ofCold Bay, Alaska, about 1000 km southwest ofAnchorage. The lagoon extends nearly

55 km from north to south, including Moffet Lagoon, and is a maximum ofabout 10 km wide. The ultimate boundaries ofthis project extend from Moffet Lagoon on the northeast to Bechevin Bay on the southwest shore ofthe peninsula.

Alaska

Bering Sea o

"'. 0\ 0 project area GulfofAlaska

... I)"",~ ~ . ,-..,."" ...:v."'" 0 ... 11> LPr;;../ ~ eLttian Archipe\ago Aleut Yupik (approximate boUndary) I~ Pacific Ocean n .-100 2W !1m FIGURE 1: Map ofthe North Pacific showing the project area.

Located on the eastern frontier ofthe boundary that separates the Aleut of the Aleutian arclJipelago from the Alutiiq and Yupik speakers to the northeast, the lower Alaska Peninsula is one ofthe more important areas in Alaska for the investigation ofprehistoric economies, political organization, and regional interaction. The long history ofearthquakes, tsunamis, volcanic eruptions, climate change, and sea-level adjustments contributes to the study ofhuman responses to global change. A long

10 archaeological sequence oflarge, sedentary villages allows for the exploration ofthe processes that led mobile hunters and fishers to settle into permanent communities. The dense resource base, particularly salmon, waterfowl, and sea mammals, leads to the examination oftechnological change and development, especially with regards to the harvesting, processing, and storing ofseasonally available foodstuffs.

At historic contact, this region supported some ofthe most politically complex and fully sedentary hunter-gatherers known to anthropology. These peoples lived on one ofthe earth's most tectonically, volcanically, and climatically dynamic landscapes. The relationship between prehistoric Aleut settlement systems and socio-political organization on the one hand, and this volatile and dynamic landscape on the other, is the focus ofthis study.

This project was designed as the frrst phase of a multi-year project intended to identify the specific variables that influenced village site location through field survey and the analysis of glacial geology, coastal geomorphology, satellite images, aerial photographs, and statistical models. These models would be used to identify undocumented sites, to construct a long-term field survey sampling strategy, and to reconstruct the landscape at different sea-levels. The ultimate goal is the investigation oflong-term and short-term responses to global change and local catastrophic events.

During the 1995 field season, we conducted an archaeological and geomorphological survey in

Moffet Lagoon, along the Joshua Green River, and in portions ofKinzarof Lagoon (Figure 2). With

NSF funding, the 1996 survey included Morzhovoi Bay and the adjacent Middle and Big Lagoons, western Izembek Lagoon, central Izembek Lagoon, the Cold Bay area and geological surveys ofmost ofthe region byhelicopter provided by the USGS.

11 N ~

Amaklsland MoffetPt.

o D

~-- o 10 20 30 kilometers

FIGURE 2. Map ofthe lowerAlaska Peninsula showing regional geographic features and place names. The importance ofregional analysis for investigations ofthe relationships between the origins of

sedentism, the rise ofsocio-political complexity, subsistence change, trade and exchange, and global

climatic change and landscape evolution cannot be underestimated. Yet, these types ofprojects have

seldom been attempted in Alaska and the Arctic because ofthe immense costs involved in both

transportation and field support.

The use ofremotely sensed data for archaeological research has a long history in archaeology (Ebert "'~ and Lyons 1983; Gumermanand Lyons 1971; Lyons and Avery 1977; Lyons and Mathien 1980). At

the time when remote sensing techniques were frrst being introduced to archaeology, they were

applied to arctic archaeological problems as well (Ebert 1980; Brown and Ebert 1980; Stringer and

Cook 1974; Harp 1974). These projects met with only limited success primarily because the scale of

the data available in the 1970s was too gross for most applications and because there were

technological limits on hardware and software-- neither ofwhich is an issue today. Despite

substantial technological advances our ability to process remotely sensed data, few projects were

carried out in the 1980s and 1990s, probably as a result ofthese early experiences (see Sheets and

McKee 1994 for one ofthe few recent examples; see also Brooks and Johannes 1990 for a review).

-~ In this project we have been testing the applicability ofusing LANDSAT TM multispectral imagery,

high-altitude aerial color IR photographs, and low altitude black and white photography for the

discovery ofarchaeological sites and geomorphological mapping on the lower Alaska Peninsula and

Unimak Island, focusing initially on the Izembek Lagoon region (Figure 2).

Although still in progress, we have begun identifying signatures for vegetation, soils, landform and

elevation, shorelines and other characteristics of archaeological site locations, and the feasibility of

conducting large-scale archaeological survey in this region has been subsequently enhanced. We have

--_r------been successful for a number ofreasons. First, the size ofmost village sites in the area greatly

exceed the resolution ofthe satellite images and the high altitude photographs. Second, there are

visible differences between the vegetation growing on and off known archaeological sites in the

region. Spring and early summer lushness differences are evident between on and off-site areas at

villages as young as 400 years BP and at villages as old as 5000 years BP (Maschner 1995). Third,

there were many known sites in the area prior to our intensive survey. Fourth, the available digital

data for the region are reasonably good and mostly available. Fifth, we have had access to the

Department ofEngineerings system for creating a 2m contour map ofthe project area from stereo

pairs of 1:20000 B&W images, and last, the cooperation of many different agencies and

organizations who have contributed greatly to the data collection efforts.

More importantly, through multivariate statistical modeling oflandscape attributes, we have begun to

reconstruct prehistoric ecosystems by changing the relative sea-level elevation to account for eustatic,

tectonic, and isostatic displacements. Thus, not only will we be able to describe the modem

characteristics ofsite locations, but we will be able to reconstruct the prehistoric characteristics as

well. The importance ofincorporating environmental variables and modeling inthis type ofproject

has not been overlooked. Dumond notes that:

an additional complicating factor rests inlandform changes over time, particularly as related

to the relative level ofthe sea, for as the sea-level has changed so have the favored locations

for sites and, probably, the habitats of sea manunals... Thus, perfection ofthe ability to

predict prehistoric settlement locations must depend upon the improvement ofknowledge in

a number of other directions (1987:106).

Ok These directions include the ability to model prehistoric landscapes and the distribution ofprehistoric resources. When cultural and behavioral data are incorporated, these models provide a contextual screen onto which the archaeology can be projected. We suggest that the evolution ofthe lower

Alaska Peninsula landscape has had a dramatic influence on the evolution ofAleut society. Further, we expect that changes in the distribution ofprehistoric villages and changes inthe distribution and use ofnatural resources occurred in accordance with these landscape changes.

To date, we have completed a study ofthe Pleistocene-Holocene glacial geology which can be found in TIna Dochat's dissertation (1997) and summarized below. The coastal mapping and geomorphic analysis being conducted by James Jordan is nearly complete. The archaeological survey has covered nearly 140 square kilometers, concentrating on modern or relic shorelines (Figure 3). Conventional or accelerator mass spectrometer radiocarbon dates have been obtained on 25 samples from 22 archaeological sites and 16 samples from geological deposits. The 2m digital elevation model is complete for approximately 75 % ofthe project area, and the final GPS points will be gathered in the

1997 season. Analyses in progress include the laboratory-based paleoecological analysis, the artifact analysis, the GIS construction, and the analysis ofthe multi-spectral images. These will be complete by January 1998.

This report is the first attempt at summarizing these studies. A final report will be produced in early

1998 with more data, a complete analysis ofthe artifact collections, the geographic information system and the photograrnrnetric research results, and with the 1997 summer investigations included.

15 _ 1995-96 Lower Alaska Peninsula Project .. 1995-96 Lower Alaska Peninsula Project and 1979 USFWS Survey ~ 1971 McCartney Survey _ 1985 BIA-ANCSA Sites

Amaklsland

~ Ocea{\ o o paC\\\"'c o D

e.-.- o 10 20 30 kilometers

FIGURE 3. Map ofthe lower Alaska Peninsula showing surveyed areas and projects.

F BACKGROUND

Regional Environment

The Aleutian arc is the westernmost extension ofthe Pacific Mountain physiographic province of northwest North America (Warhaftig 1965) and spans the north Pacific Ocean between Alaska and the Kamchatka Peninsula ofthe Russian far east. The Alaska Peninsula and the Aleutian archipelago have formed along one ofthe most seismically active areas in the world (McNutt and Power 1993), developing as an uplifted arc during the late Cretaceous in response to the subduction ofthe North

Pacific plate beneath the North American plate (Nelson et al. 1974).

This chain ofpredominately volcanic islands separates the relatively warm waters ofthe north Pacific

Ocean from the colder shelf waters ofthe eastern Bering Sea. The position ofthe chain between seas with such differing physiographic and climatologic characteristics means that frequent and often violent cyclonic storms are generated along its axis. The Aleutian Low pressure anomaly is centered over the archipelago, and is responsible for much ofthe cyclogenesis over northwest North America

(Hare and Hay 1974). Deep, cold upwelling water ofthe north Pacific generates a productive marine ecosystem that is connected to shallower waters ofthe southern Bering Sea shelf through passes between islands. VVider and deeper passes in the western chain are responsible for most ofthe circulation between basins (Favorite 1974).

The eastern Aleutian Islands and lower Alaska Peninsula have been the most volcanically active portion ofthe arc during late Quaternary time. Caldera-forming eruptions have occurred at 12 of40 volcanic centers in the region during the Holocene (Miller and Smith 1987). The volcanoes of

Unimak Island have been among the most active in historic times (Veniarninov 1984), and have

17 generated volcanically-induced mudflows, lava flows and tephra deposits across the island and onto

the western Alaska Peninsula (Miller and Smith 1987).

The region experiences a maritime climate that supports treeless tundra vegetation. Grasses, sedges,

crowberry and lichen dominate ground cover, with willow, dwarf birch and alder occurring in more

sheltered areas (Viereck and Little 1972; Se1kregg 1976). Most workers recognize a tripartite

succession of broad vegetation associations inthe Aleutians during the post-glacial period (Heusser

1973, 1983; Heusser et al. 1985; Anderson and Brubaker 1993). These changes are probably

associated with regional climatic shifts due to migration ofthe Aleutian Low pressure anomaly and

resulting storm tracks (Kutzbach et al. 1993), although factors such as tephra falls play an important role in local pollen stratigraphy and long-term vegetation succession (Heusser 1985).

'Three broad physiographic zones characterize the lower Alaska Peninsula. A low, gently rolling

coastal plain rises from the Bering Sea coast, and coastal dunes and beach-ridge complexes

commonly occur along the relatively straight, unprotected shoreline. Barrier beaches occasionally

embay shallow lagoon systems. Glacially-derived sediments mantle much ofthe coastal plain (Funk

1973), with end moraines and ice stagnation topography comprising much ofthe local relief. The

coastal plain rises to the interior ofthe peninsula, where peaks ofthe Aleutian Range reach 3,000 to

4,000 meters above sea-level. The Pacific side ofthe peninsula is a steep, rugged cliffed coast with

deep, fiord-like embayments.

The Holocene geomorphic history ofthe Alaska Peninsula coastal plain is complex and dynamic, and

the preservation or destruction ofancient shorelines results primarily from the interaction oftectonic

uplift or subsidence ofthe land, eustatic sea-level change, and isostatic changes due to postglacial

18 rebound (plaiker et al. 1992). In general, the global post-glacial rise ofsea-level decreased exponentially between 8000 and 4000 years ago, following a rapid, linear rise beginning inthe late

Pleistocene (Bloom 1983; Winslow 1991). For much ofthe Aleutian arc, the rate ofsea-level rise during the Pleistocene-Holocene transition outpaced the rate ofuplift due to tectonic activity and isostatic rebound, resulting in the submergence ofpre-early Holocene shorelines.

Geomorphic evidence ofraised marine terraces ofHolocene age is common throughout the archipelago (powers 1961; Plafker 1969; Morris and Bucknan 1972; Black 1976, 1981; Winslow

1991; Johnson and Winslow 1991), but their relationship to eustatic, isostatic, and tectonic controls must be determined from geographic setting and local field data (Gard 1980; Winslow 1991; Plaiker et al. 1992). The tectonic history ofthe lower Alaska Peninsula is still poorly understood, but tectonic uplift rates have been estimated based on dated, emerged strandlines in the Shumagin Islands

(Winslow 1991). Modeling uplift rates and a eustatic-isostatic correction curve, Winslow (1992) suggested that the oldest preserved shorelines (and coastal archaeological sites) on the Alaska

Peninsula adjacent to the Shumagin Islands may date to around 8000 BP.

Marine and terrestrial wildlife are abundant in the region. Terrestrial mammals include brown bear, caribou, wolf, fox, river otter, ground squirrel and porcupine. Avifaunal resources are also plentiful, including ptarmigan, loons, cormorants, gulls, terns, and raptors. The area is remarkable for seasonal migrations of waterfowl, when hundreds ofthousands ofgeese and ducks feed on the rich eel grass beds in Izembek Lagoon each fall (USFWS 1985). Sea mammals and fish include resident and migratory species. Harbor seal, sea otter, sea lion, and whale can be seen in the bays and lagoons, and walrus use Amak Island, about 20 km offshore in the Bering Sea, as a summer haul out. Forty

19 species offISh are found in the lower Alaska Peninsula waters and the larger local streams support large salmon runs.

Previous Archaeological Research

The lower Alaska Peninsula has been recognized as an important region for investigating the eastern frontier ofthe Aleut for many years and it was the question ofthe Yup'ik - Aleut boundary that led

Allen McCartney to conduct the frrst excavations in Izembek Lagoon in 1971 (1974). McCartney excavated at three sites along the southwest shore of Izembek Lagoon. These sites included XCB

001, a large village with dense concentrations ofhouse depressions, XCB-002, a smaller site, and

XCB-003, a site that included a large house with a collapsed whale bone superstructure. All three sites dated to approximately AD 1000 - 1100 (McCartney 1974:64).

The whale bone house was especially unique because is was the only whalebone house yet found in the Aleut region and because this house form seemed to be Eskimo in origin. The house was constructed of34 mandibles ofa very large species ofwhale. McCartney (personal communication) stated that the whale mandibles were much larger than any that are normally hunted by people in the arctic based on his research with bowhead hunting (McCartney and Savelle 1993; Savelle and

McCartney 1991). He believed that they may be as large as adult blue whales. This house was also interesting because, instead ofan Aleutian artifact assemblage, the house contained Eskimo style pottery from the Bering Sea, an abundance ofground slate, and a number of other characteristics that indicated a Bering Sea origin.

From these investigations, McCartney defined the Izembek Phase (McCartney 1974:69). The

Izembek Phase was seen as transitional between the Aleut region and the Bering Sea Eskimo region.

20 The artifact assemblage included a number ofstemmed chipped stone points, ground slate points,

ground slate knives and ulus, and gravel-tempered ceramics. While he recognized that the whale bone

house represented a more permanent structure, he argued that the other sites and depressions resulted

from the seasonal use ofthe lagoons, perhaps during the summer and fall when the salmon or

waterfowl are most abundant (McCartney 1974:65). He speculated that the main winter villages

F'~ would be found outside of the lagoons (McCartney 1974:60) and that the region may have served as

a "kind ofno-man's-land between the warring Aleut, Koniag and Aglegmuit" (McCartney 1974:64).

In 1979, Michael Yarborough led a United States Fish and Wildlife Service (USFWS) survey of

portions ofthe Izembek Lagoon region and tested a number ofsites (Yarborough n.d; Klingler n.d.).

Some ofhis more important findings included another site with pottery, a number ofsites with

ground slate, and the recognition that there were a number ofhuge prehistoric villages in the area. I

am inthe process ofanalyzing the original data and artifacts from this project.

In 1986, Dumond conducted a helicopter survey ofpart ofthe region inthe process ofcreating a

model ofvillage location for the USFWS (Dumond 1987). While he only identified two new sites, he

argued that McCartney's seasonal settlement model for the lagoon systems was not justified given

the abundant resources that live in the area throughout the year. He particularly noted that the caribou

and whale resources could probably sustain a year-round population (Dumond 1987:41). Dumond

has recently continued this line ofreasoning by arguing that the shallow lagoons served as traps for

harvesting large quantities ofwhales (1995). He stated that the initial occupation ofthe lagoons

should have occurred by 4000 BP or even 6000 BP (1987:107) and be related to either the Ocean

Bay Tradition ofthe Kodiak Archipelago (Clark 1993) or to some ofthe earlier Aleutian Traditions

(McCartney 1984). He also argued that the densest concentrations ofsites should be in the lagoon

21 - systems ofthe north side of the Peninsula, not on the Pacific Coast where sea mammal densities are much lower (Dumond 1987:106).

Dumond argued that the majority ofthe items McCartney recovered from the whale bone house, especially the ground slate projectiles and the ceramics, were unique to that structure and not present in his excavations at the other two sites. He stated that these represented a different tradition than the other parts ofthe Izembek Phase with a more Aleut appearance (Dumond 1987:41) indicating a more complicated view ofthe Aleut - Yup'ik frontier.

McCartney revised his view ofthe lower Alaska Peninsula by arguing that the major lagoon systems are actually "ecological hotspots", and suggested that the Bering Sea shore had a "punctuated coast subsistence settlement pattern" (McCartney 1988:46). While Yesner, using McCartney's data, argued that there were few sites on the lower Peninsula because it was an "ecological frontier" (Yesner

1985), McCartney predicted that a large number ofsites might be found in the lagoons with many

"reflecting larger and politically more important settlements" (McCartney 1988:46), once a greater amount ofsurvey was completed (McCartney 1988:47).

In 1988, archaeologists from the Bureau ofIndian Affairs (BIA) investigated 22 sites on the lower

Alaska Peninsula as part ofinvestigation associated the with Alaska Native Claims Settlement Act

(USBIA 1992). The most important findings ofthis study were the identification of a number of villages inthe lagoons with between 200 and 900 surface depressions and a 4500 year occupation history (Cooper and Bartolini 1991). These findings confmned many of Dumond's and McCartney's speculations.

22 Inthe context ofthe BIA investigations, a significant amount ofvariability was recognized in both

the organization ofvillages and in the structure ofhouses (Hoffman 1990). A notable discovery was

a form ofmulti-chambered house with a central room ranging from 8 to 20 meters inlength with one

to 10 attached side rooms, usually from one to three meters in diameter. Termed "nucleus/satellite

complexes" by the BIA investigators (1991 :63), these houses show a significant departure from all

previous houses which generally consist of a single depression.

In 1994, the University ofWisconsin began investigations on the lower Alaska Peninsula and

Unimak Island (Figure 3). This background sets the stage for investigating settlement, sedentism,

and the evolution ofvillages in this region.

THE LOWER ALASKA PENINSULA PROJECT

Our research involves the integration ofgeomorphological and glaciological surveys, archaeological

survey, and the use ofglobal positioning systems, geographic information systems, satellite image

classification, and photogrammetry. Because ofthe active nature ofthe lower Alaska Peninsula

landscape, it was necessary to have a firm control over ofthe geological and coastal histories in order

to place the archaeological data in context.

"'- Field Methods

Previous investigations in the eastern Aleutians have emphasized the need for understanding

geomorphic processes in the interpretation ofthe regional archaeological record (Black 1974, 1975,

1976; Dumond 1987; Johnson and Winslow 1991; Winslow 1991). This component ofthe project is

uses remotely sensed data to identify geomorphic features and interpret evidence ofHolocene

landscape change. Low vegetation cover and distinctness ofsedimentary environments facilitated

23 geomorphic mapping and vegetation-landform classification from aerial photography and satellite imagery.

A primary goal ofthe geomorphic mapping and image classification is to identify landscape elements that are potentially associated with prehistoric settlement ofthe lower Alaska Peninsula. Because regional tectonism, volcanism, and sea-level history are so dynamic in the region (Winslow 1991,

Plafker 1992), the identification offormer shoreline features is critical. These include raised marine terraces, shoreline scarps now inland ofthe present coast, former embayments, and beach-dune ridge

complexes. These data guided field investigation of coastal plain geomorphic environments and aided in our initial models ofthe archaeological settlement patterns.

Alaska High Altitude Photography (AHAP) 1:63000 color-infrared images and 1:36000 black and

white images were be used to identify and map surficial geology ofthe study area. Geomorphic units were defined on the basis of sedimentary provenance. Primary map units consisted of: eolian deposits - - back beach dunes and dune ridge complexes; coastal plain dune field and sand sheet deposits;

alluvial deposits - stream and river floodplains, terraces, and deltas; glacial deposits - till and end

moraines, ice stagnation topography; and volcanic deposits -lava flows and lahar deposits. Map

units were assigned relative ages based on landscape position and apparent vegetation association.

Geologic mapping was done at the 1:60,000 scale.

The archaeological survey was conducted through air photo interpretation, aerial reconnaissance, and

pedestrian survey. Travel to the survey locales was done by boat or by small plane, usually from base

camps in remote locations. The actual foot reconnaissance was done by two to four survey personnel

spread an equal distance across the uplands adjacent to the shoreline. Raised beaches and other

24 prominent features distant from the shoreline where also surveyed. Insome areas soil probes and

shovel tests were used, but the majority offinds were based on surface features.

Sites were mapped with tape measure and compass. Special care was taken to record accurate

measurements on the cultural depressions. Vegetation, site geomorphology, and distance to fresh

water and resources were recorded on site. A shovel test was dug in a depression or a profile was cut

in an erosion cut bank to determine the stratigraphic extent ofthe site and to collect samples for

radiocarbon dating. The site was positioned on an aerial photograph and a GPS reading was taken on

a prominent site feature. Characteristics ofthe nearest marine beach were recorded, as was the nature

ofthe bay or lagoon nearest the site.

We are in the process ofcreating a 2-meter digital elevation model (DEM) ofthe entire research area

from I :20000 black and white photographs (now 75% complete). When completed, this DEM will

give us the micro-topography necessary to investigate variation in the location ofsites and to

reconstruct ancient shorelines, estuaries, and lagoons. We will also use LANDSAT multispectral

imagery to relate vegetation cover types to geomorphic map units and to help assign relative ages to

surficial deposits. An unsupervised classification will be performed initially, and spectral classes will

be assigned to information classes based on known differences in vegetation and on geomorphic

information derived from air photo interpretation. The end product will be a landform/ground cover - classification that will provide data for modeling settlement pattern and predicting site location based on landscape association.

We decided to take a regional approach in our investigations. This is in contrastto the approach that

has prevailed inthe Aleutian - Peninsular region for the last 100 years ofinvestigations. Exceptions

25 to this tendency include the Amchitka study (McCartney 1977) and Dumond's research on the upper

Peninsula -- neither ofthese projects attempted regional analysis or, in the case ofDumond's

predictive model, produced results applicable to more complex analyses.

The regional study had five major goals.

1. To intensely survey three regions for archaeological sites. These three regions are:

a) Moffet Lagoon (including Strawberry Point) and the lower Joshua Green River.

b) Central Izembek to Russell Creek with Applegate Cove as the western border and central

Kinzarof to Blaine Point as the eastern border.

c) Morzhovoi Bay to the Bering Sea with the west shore ofMiddle Lagoon as the western

border and the east shore of Big Lagoon as the eastern border.

2. To investigate the glacial and coastal geomorphology ofthe region in order to build a

model oflandscape change and evolution over the last 12,000 years. These data will be used

to map relict shorelines and other features that could possible have supported settlement

under different geographic conditions than exist today.

3. To gather high precision GPS readings from locales visible on I:30,000 air photographs.

These will be used to produce a 2-3m digital elevation model (DEM). Based on the

geographic data and incorporated into a GIS, the DEM will be used to raise and lower the

shoreline through time thus allowing for a probability-based reconstruction ofthe regional

landscape. This will make sampling of ancient shorelines more productive and allow the

construction ofenvironmentally and behaviorally-based model ofsite location and

variability.

26 4. To map and date all ofthe village sites. Once dated, the maps will be used to investigate

changes in village organization and house form over the last 6000 years. These findings will

then be correlated with our modeled changes in the landscape.

5. To perform a blind test of our model on a previously un-investigated region using satellite

and geographic data.

27 FIELD RESULTS

Glacial History

The present glacial geology research project grew out of a need to establish the environmental changes that have occurred onthe Alaska Peninsula. An understanding ofthe environmental changes was desired by University of'Wisconsin-Mactison anthropologists to assess the effects of environment on human settlement and migration across southern Beringia during the last 5,000 to

6,000 years. The time span for the present geologic study has been increased to accommodate the ages ofall glacial landforms ofthe area and may extend back to at least the start ofmarine oxygen isotope stage 5d.

Uttle detailed mapping ofsurficial deposits and geomorphology had previously been conducted in the Cold Bay region. Early work indicated that a number ofglacial episodes are recorded in the stratigraphy ofthe region (Funk, 1973; Pewe, 1975; Detterman, 1986). More recent study has been by air photograph interpretation (Wilson et al., 1992) and by extrapolation of data from Kodiak

Island and the eastern part ofthe Peninsula, 700 kID east ofCold Bay (Mann and Peteet, 1994). The present study integrates field evidence and air photo interpretation to test the conclusions ofprevious studies and to develop an internally consistent chronology.

Research Objectives. The following four principles have guided this research:

1.) The extent oflate 'Wisconsin ice inthis area can be established. Landform and outcrop

analysis would result in a surficial geology and geomorphology map ofthe region from which ice

mass reconstructions for the last glacial maximum could be made.

28 -

2.) The extent ofNeoglacial ice can be established. While extensive Neoglacial advances have

been mapped for the Cook Inlet region of southeast Alaska, little is known ofcontemporaneous

advances ofalpine glaciers on the Alaska Peninsula. The Neoglacial history is ofinterest because

it could provide an opportunity to study environmental responses to short-term climatic

perturbations. The Neoglacial episode also spans the period oftime when human migration and

occupation were prevalent on the Alaska Peninsula and is thus ofinterest for the archeological

component ofthe overall Alaska Peninsula research project.

3.) The late Wisconsin glacial and Neoglacial records ultimately will be tied to the history of

volcanic eruptions, and these in turn will be tied to vegetation and inhabitation history being

studied by others.

4.) A collaborative effort with a glacial modeler at the University ofBritish Columbia to apply a

numerical ice sheet model to field data generated inthe Cold Bay region would lend support to

the history of glaciation deduced from field studies in this area where datable material tied

-- directly to glaciation is almost nonexistent. This will assist in assessing the feasibility oflate

Wisconsin glaciation proceeding from an ice cap centered on the Pacific continental shelf and

perhaps to distinguishing between hypotheses concerning the general nature ofglaciation.

Research Significance. This research is ofinterest because: 1) it provides the opportunity for further

refining our understanding oflate Wisconsin glaciation by determining how extensive ice cover was - at the western margin ofNorth America [this will contribute to the proper partitioning ofice between the northern and southern hemispheres and perhaps ultimately to determining eustatic sea-level

change [120 + 5 m ofFairbanks (1989) vs 105 m ofPeltier, 1994)]; 2) it will discern the source of

ice in Cold Bay [was the ice from alpine glaciation or from the Cordilleran Ice Sheet as suggested by

Mann and Peteet (1994) or did it have its origins in an ice cap centered on the shallow continental

29 shelf south or southwest of Cold Bay?]; 3) it affords the opportunity to study the interaction between

an ice cap and local alpine glaciers in the area; 4) the occurrence of a Younger Dryas readvance of

alpine glaciers in this region as has been suggested in Peltier's LGM reconstruction (1994) will be

addressed; 5) the response of alpine glaciers (focusing on Fosty glacier) to Holocene climate changes

will be assessed; 6) the Alaska Peninsula is the southern boundary ofBeringia, the proposed

migratory route ofhumans and mammals from Eurasia to North America.

Results ofthe 1995-96 geologic mapping project conducted on the Izembek National Wildlife

Refuge are summarized here and fully expanded upon in Dochat (1997). These results indicate that

alpine glaciers advanced at least 20 kIn from the valley heads sometime prior to the Last Glacial

Maximum (LGM; 21,000 to 18,000 yr BP) . During the LGM, the entire region was glaciated by ice

flowing northward from a center located on the continental shelfperhaps in the vicinity ofSanak

Island. Since the LGM, alpine glaciers have advanced at least six times.

Widely dispersed alpine moraines indicate that glaciers on Frosty Peak, Mount Dutton, and Mount

Emmons extended up to 20 kIn beyond their present margins in the past. Based on cross- cutting

relations, the oldest alpine moraines occur in the Joshua Green River Valley. No correlative glacial

record has been identified for Frosty Peak. Glaciers advancing out ofthe valleys ofMount Emmons

and Mount Dutton deposited Bear Ridge and Ptarmigan Ridge (Dochat 1997).

Bear Ridge is discontinuous and trends offshore. This moraine consists oftill that extends from a

bedrock hillside at an elevation of approximately 80 m as!. The western (proximal) face ofBear

Ridge slopes at 400 to the west. To the east, the ridge abuts bedrock. The moraine extends to the

northwest where it terminates in the Bering Sea.

" West of Bear Ridge, Ptarmigan Ridge is mostly continuous except where dissected by the Joshua

Green River. Where dissected, the ridge is approximately 20 m high. The elevation ofthe base ofthe

ridge is approximately 5 m as!. Subdued hummocks and dry kettles characterize the broad crest of

the ridge. Both the north (distal) and south (proximal) sides have a wave-washed appearance (slopes

of300 to 350). Thus, the ridge is reasonably symmetrical in cross-section. Ptarmigan Ridge is

arcuate and concave to the south.

In one measured section in Ptarmigan Ridge, 1.1 m of soil occur above volcanic ash overlying the till

(A, mixed A and B, 2A, 2A/2B, and 2B12C horizons) (Dochat 1997, appendix m. Within the soil,

cultural artifacts occur which had previously been dated to 5,500 14C yr BP. At other sites along the

ridge crest that lack cultural disturbance, the soil is less well developed (approximately 8 to 10 cm

thick A and B horizons). Along the coastal margin wind-blown sand up to 25 em thick overlies the

till.

Two hummocky moraines surround Cold Bay. The outermost moraine (Cold Bay I of Dochat 1997;

Kvichak ofWilson et al. in prep.) extends northward to the Bering Sea Hills and kettle depressions

frequently occupied by water characterize this area. The hummocks comprising poorly sorted "'- sediment are best preserved at Grant Point. Clasts range from subangular to subrounded. Marine

microfossils including foraminifera, sponge spicules, and probable ostracods occur within the matrix

ofthe till. The relief ofthe hummocks suggests that the moraine was deposited over an ice core.

Hummocks formed as a result of differential melting due to differences in the thickness ofthe - sediment covering the ice. The presence ofmarine microfossils within the till matrix as well as the

31 upper elevationallimit (270 m) ofthe till indicates that grounded ice filled Cold Bay during the

LGM.

Immediately bayward (south ofGrant Point) ofthe Cold Bay I moraine, separating the outer and inner moraines, lies a region ofmore subdued hummocks. The sediment within this intermorainal area is composed ofa better sorted sediment, generally lacking boulders and cobbles. Pebbles are better rounded than those within the moraine.

The sorting and roundness ofthis sediment suggest deposition by meltwater flowing from glacial ice.

The presence ofhummocks within this outwash region suggests that the outwash was deposited over ice that subsequently melted out.

Bayward ofthe outwash surface occurs a second moraine (Cold Bay IT of Dochat 1997; lllianrna of

Wilson et al. in prep.) with high relief hills and kettles. Exposures through this moraine occur along

Cold Bay. The sediment comprising this ridge is similar in all characteristics to the material comprising the Cold Bay I moraine. Thus, both the Cold Bay I and IT moraines were likely deposited over an ice core.

In addition to the numerous volcanic lithologies that in the moraines and outwash, several exotic erratic lithologies have been found. These erratics provide a basis for potentially determining the source area ofthe ice that formed the moraines. Erratics include petrified wood, granidiorite from the

Sanak Island pluton (p. Wilson, pers. cornm.), metaconglomerates from the Belkofski Formation, and red chert. Red chert is perhaps the most significant ofthe erratics because the only known source of red chert in the western Alaska Peninsula region is Long Island. It is not known whether granodiorite

32 or red chert crop out on the sea floor between Sanak Island and Cold Bay. The presence ofred chert

suggests that a component ofice flow must have been from the vicinity ofSanak and Long islands

northward into Cold Bay.

The surficial expression ofthe outwash plane between the two moraines, suggests that the outwash

was deposited on top ofice. Hence it seems likely that ice advanced into the Cold Bay region to a

maximum position and deposited the Cold Bay I moraine. Ice subsequently retreated to a position

south ofthe Kinzarof Lagoon area. Outwash was deposited above stagnant, melting ice as the ice

lobe readvanced to deposit the Cold Bay II moraine.

The ice lobe depositing the Cold Bay I and II moraines likely emanated from an ice cap situated on

the Pacific continental shelf. The idea of an ice cap on the continental shelf is consistent with Funk

(1973) and Detterman (1986) but contrasts with the models ofDenton and Hughes (1981) and of

Mann and Peteet (1994). The latter two models suggest that ice remained centered on the mountains

throughout the last glacial cycle. During the LGM, sea-level was 120 + 5 m lower than present

(Fairbanks, 1989). Both the Bering Sea north ofthe Peninsula and the Pacific continental shelf are

shallow; a 120 m lowering ofsea-level would expose both. It has been proposed that the ice cap

formed from alpine glaciers coalescing on the continental shelf (Dochat 1997). According to this ,~

hypothesis ice initially thickened on the mountains ofthe Alaska Peninsula and likely flowed outward

in all directions. As sea-level lowered, the northern precipitation source was removed and south

flowing glaciers merged on the Pacific continental shelf. As climatic deterioration continued up to the

LGM, the equilibrium line altitude lowered such that ice thickened on the shelf to form a dome

(Dochat 1997). Because the Bering Sea was removed as a source ofmoisture for the north-flowing

alpine glaciers and because these glaciers occur in the lee ofthe ice cap and mountains for moisture

33 originating in the Pacific, it is hypothesized that the north-flowing glaciers had retreated at least to the base of the mountains by the time the ice cap reached its maximum extent (Dochat 1997).

Geomorphic evidence supports the hypothesis that the alpine glaciers retreated by the time the ice cap reached its maximum extent. The Cold Bay II moraine overlies Ptarmigan Ridge. Outwash channels are cut from the Cold Bay II moraine into the flat lying sediments on the ice proximal side ofPtarmigan Ridge. The timing ofthis asynchroneity between the alpine glacier and ice cap maximum extents is unknown.

It is postulated the Morzhovoi and Pavlof bays owe their origin to ice lobes from the same continental shelf ice cap. Similar topography and erratic inclusions (granodiorite from the Sanak

Island pluton, petrified wood, Belkofski Formation metaconglomerates, and red chert) as well as the geographic orientation ofthese bays support the hypothesis that each ofthese bays formed when ice lobes radiated north and northeastward from a single ice cap centered on the continental shelf near the Sanak Island area.

Not until sea-level rose flooding the Bering Sea floor and collapse ofthe continental ice sheet was well underway by 12,000 years ago (AMS date of 11,530 +/- 200 on a leaf at the top ofthe outwash surface indicates that the area was ice free long enough for revegetation by this time) could the alpine glaciers advance. About this time the most extensive, preserved post-LGM advance occurred as

Frosty glacier flowed down Russell Creek valley depositing an alpine moraine over the inner hummocky Cold Bay moraine. This moraine can be seen approximately 8 km upstream from the mouth of Russell Creek. Possibly contemporaneous moraines occur in three other valleys ofFrosty

Peak Volcano. There is no preserved record of contemporaneous advances ofglaciers from Mount

Dutton or Mount Emmons.

34 This alpine advance likely corresponds with a still stand in the retreat ofthe ice lobe filling Cold Bay.

This postulated still stand resulted inthe deposition ofthe moraine that blocks Kinzarof Lagoon. A

second latest Wisconsin alpine advance is recorded by moraines irrnnediately upvalley ofthe earlier

alpine advance. This alpine advance is suggested to correspond with a second still stand during the

retreat ofthe ice lobe from Cold Bay. During the still stand, moraines were deposited at Thinpoint,

darrnning Thinpoint Lake and at Kelp Point. Bathymetric contours suggest that both of these retreat

phase moraines continue underwater water. No evidence ofcontemporaneous continental shelf ice

cap moraines occurs in Morzhovoi or Pavlofbays.

Evidence for one late Holocene alpine advance is preseved as a moraine in Russell Creek Valley. This

alpine advance apparently correlates with the Tunnel I glaciation in southern Alaska (after

approximately 1,200 yr BP). A paleosol buried by a moraine ofthis advance in Russell Creek Valley

yielded a conventional radiocarbon date of 1190 +/- 120 14-C yr BP. Other alpine moraines occur in

Frosty's valleys that are probably contemporaneous. However, only one probable post-LGM moraine

occurs on Mt. Dutton. No evidence for a late Holocene advance has been identified on Mount

Errnnons.

Three more recent, possibly Little Ice Age, less extensive alpine glacier advances are preserved by

moraines farther up-valley in several ofFrosty's valleys including those described above (within

several 100 m ofthe present ice margin) (Funk 1973).

The lack ofcontinuity in what is preserved and where (pre-late WlSconsin alpine moraines from

Dutton and Errnnons; post-glacial maximum moraines from Frosty) hints at the roll that has been

35 - played by the volcanoes ofthe region. Because evidence exists for glacial advances associated with both major (late Wisconsin) and minor climatic changes (late Holocene and Little Ice Age), it is postulated that the volcanic history has had a major impact on either alpine glacial advances or the preservation ofthe record ofthose advances. Volcanic ashes have been collected by all authors ofthis report (chemical analyses ofsome are given in Dochat (1997 Appendix V); these ashes are being analyzed to help establish the Holocene chronology ofthe area. Additional samples will be collected in 1997 and analyzed as part of a Master's thesis byEric Carson.

An ice sheet model used to reconstruct the glacial history ofthe Cold Bay region lacks the resolution to distinguish between the behavior of alpine glaciers during the LGM (to resolve whether they advance synchronously with the ice cap as has been suggested by F. Weber and F. Wilson, pers. - comm. or asynchronously as suggested by Dochat (1997). The model does, however, suggest that ice did accumulate on the continental shelf during the LGM rather than remaining centered on the mountains. The model was created at the University ofBritish Columbia by Shawn Marshall to study ice dynamics ofthe Laurentide Ice Sheet in the Hudson Bay region. The model has been modified to accommodate the smaller grid area ofthe Cold Bay region and to introduce greater variables. While some variables such as ablation may be somewhat insignificant when smoothed over larger areas such as that covered by the Laurentide Ice Sheet, these same variables need to be accounted for when modeling smaller areas. Consequently, more parameters have been specified in the present model to produce a more realistic representation.

36 Coastal Geomorphology

TIlls section summarizes the results ofcoastal geomorphologic fieldwork conducted on the lower

Alaska Peninsula during the summers of 1995-96. The work supports dissertation research that is

aimed at reconstructing the coastal paleogeography ofthe region since the end ofthe late Wisconsin

glacial period. Goals ofthe research are to 1) determine the long term (Holocene) trend ofsea-level

in the context ofisostatic, tectonic, and climatologic controls, and define a local sea-level curve that

will serve as the basis for assessing the geomorphic effects and archaeological implications ofsea

level fluctuation on regional coastlines; 2) determine the magnitude and frequency of

meteorologically- and tectonically-induced coastal floods (storm surges and tsunamis) that occur over

short time scales, and identify the coastal sectors most vulnerable to these events; and 3) provide a

classification and inventory ofregional coastal environments based on present shoreline position,

elevation data, geomorphology, and vegetation cover that will serve as reference layers for analysis of

decadal-scale changes in the coastal ecosystem.

1bree broad physiographic zones characterize the regional landscape. A low, gently rolling coastal

plain rises from the Bering Sea coast, and coastal dunes and beach ridge complexes commonly occur

along the relatively straight, unprotected shoreline. TIlls zone is classified as part ofthe Bristol Bay - Nushagak Lowlands, but can be considered as transitional because ofits considerable local relief and proximity to uplands and mountains ofthe Alaska Peninsula (Gallant et.al., 1995). Barrier beaches - occasionally embay shallow lagoon systems. Glacially-derived sediments underlie much ofthe coastal plain, with end moraines and ice stagnation topography comprising much ofthe local relief.

Elevations range from sea-level to 150 m and drainage is typically poorly integrated across moraine

systems and lake and outwash plains. The coastal plain rises to the interior ofthe peninsula and - island cores, where volcanic peaks ofthe Aleutian Range reach heights of3000 to 4000 meters 37 - above sea-level. The Pacific side ofthe Alaska Peninsula is a steep, rugged cliffed coast with deep, fjord-like embayments and is physiographically classified as part ofthe Alaska Peninsula Mountains

Ecoregion (Gallant et. al., 1995).

During late Wisconsin time, a nearly continuous ice cap was centered on the Pacific side ofthe peninsula and on the eastern Aleutians, retreating fairly rapidly between 14,000 and 11,000 years ago

(Black, 1976; Detterman, 1986; Mann and Peteet, 1994). Evidence oflate Pleistocene glaciers at sea-level comes from extensive lowland drift sheets and pitted outwash on the Bering Sea side of

Frosty Peak (Waldron, 1961; Funk, 1973), and from ice-rafted glacial erratics on the narrow Pacific shelf (Kent et al., 1971). Rapid deglaciation is attributed to warming ofthe North Pacific Ocean following an increase inglobal temperature between 14,000 and 12,000 years ago, with the subsequent rise in sea-level accelerating the disintegration oftidewater glaciers. The highest peaks in the chain carry alpine glaciers today, and likely have supported alpine glaciers throughout most of the Holocene (Black, 1976).

The history ofsea-level fluctuations since the last glacial maximum on the lower Alaska Peninsula

(c. 14,000 yr B.P. to present) is complicated by tectonism, isostatic rebound and changes in coastal meteorological regime through time. Thus the dominant controls on coastal evolution can be generalized at different time scales or frequencies: tectonic displacement is episodic; isostatic compensation is asymptotic; oceanographic and meteorologic controls are cyclic in nature. Tectonic activity has the potential to most dramatically alter coastal environments, both through instantaneous displacement ofthe shoreline and through coastal flooding due to tsunamis. Isostasy exerts less control on coastal morphology through time, as compensation rates are fastest in the centuries and millennia immediately following deglaciation. The prevailing coastal meteorological regime can

38 induce dune stabilization or reactivation, and will also control local sedimentation and erosion in the

littoral zone through its influence on near-shore wave energy.

Coastal Geomorphic systems ofthe lower Alaska Peninsula

A central goal ofthis research is to identify the various mechanisms ofcoastal displacement and

,,- assess their individual contributions to relative sea-level fluctuations. The primary means of

assessing these controls is through obtaining geologic data on regional shoreline deposits. Coastal

geomorphic systems evolve in response to a number of environmental controls; glacial and tectonic

setting, bedrock geology, sediment availability and climatic province all contribute to the long term

development ofcoastal landscapes ofthe lower Alaska Peninsula. Therefore a number ofgeomorphic

features can be investigated for information with which to reconstruct coastal paleogeography and

shoreline processes. Settings that this study focus on include sea cliffs and coastal bluff exposures,

estuarine marsh environments, marine terraces and shore platforms, coastal dune fields, strand plains

- and associated shore zone clastic deposits such as barrier bars, spits and beach berms. This section

presents a summary ofthe main coastal geomorphic systems found on the lower peninsula and

discusses their significance to reconstructing sea-level history.

Glacial and tectonic evidence

A substantial portion ofthe region's coastal geography is inherited from late Pleistocene glaciation of

the Alaska Peninsula. Glacial sediments form the heads ofbays on the Pacific coast, and have been

reworked locally into spits and beach ridge complexes. TIll is extensive and connects former islands

- at Pavlof, Cold, and Morzhovoi bays (Wilson et. al., 1992). Coastal wetlands are inset into low-lying

areas and have expanded and contracted with fluctuations of sea-level. Lag deposits of glacial

cobbles and boulders occur in many intertidal settings and reflect marine erosion ofmoraine and

39 ..... outwash sediments. The Bering Sea coast is predominately erosional, exposing near-vertical cliffs of glacial till and outwash. Retreat ofthe coastal plain that is possibly due to regional subsidence provides fine sediments for littoral transport and deposition as barrier bars and spits that front

Izembek and other lagoon systems along the north shore ofthe peninsula.

It is difficult to estimate the amount ofisostatic depression that the lower Alaska Peninsula experienced because ofdifferences ofopinion on ice volume and thickness, and the possible influence ofvolcanic activity on local ice cover. Ifan estimate for maximum ice sheet thickness ofca.

400 m is used for the Cold - Morzhovoi bay areas (Mann and Peteet, 1994), about a third ofthat figure (ca. 130 m) would approximate crustal subsidence due to ice load. 'This figure is close to the estimate of-120 m (Fairbanks, 1989) for global glacio-eustatic sea-level lowering during the last glacial maximum, and means that regional uplift due to glacio-isostasy alone would result in raised shorelines not higher than a few tens of meters above modem sea-level. A marine limit of 25 m asl presently recognized in the Cold Bay area (Jordan, 1996) provides support for Mann and Peteet's

(1994) estimate ofice thickness, although other field evidence indicates that tectonism plays an important role in shoreline displacement and modification (see below).

The subduction ofthe Pacific plate beneath the North American plate along the axis ofthe Aleutian trench generates seismic activity that occurs at variable depths and intensities along the Alaska

Peninsula. Most seismic activity during the 20th century can be associated with about 12 tectonic blocks along the Aleutian Arc, the Gulf of Alaska and southeast Alaska (Lander, 1996). Blocks range in length from 350 to 700 kIn and major earthquakes occur along the arc with a recurrence interval on the order ofa century to a few hundred years. Seismic gaps (areas that have not had a major earthquake in recorded history) occur between several tectonic blocks and are areas that have a

40 relatively high probability for generating future earthquakes and tsunamis (Lander, 1996). The lower

Alaska Peninsula is located within the Shumagin seismic gap and has not experienced a major

earthquake inrecorded history.

Regional tectonism contributes significantly to the displacement ofthe lower Alaska Peninsula

shoreline. Shore platforms are well-developed at many rocky headlands and isolated dune fields

commonly divert the mouths ofstreams that drain the south face ofFrosty volcano, suggesting that

uplift is ongoing. The stratigraphy ofmany coastal bluffexposures indicates that sudden tectonic

uplift has occurred several times during the Holocene, and that gradual subsidence or uplift also

occurs between seismic events (platker, 1990). Coastal bluffexposures have been examined at the

- heads ofMorzhovoi and Cold bays, and at Kinzarof and Moffet lagoons. The stratigraphy ofthese

sections varies depending on local depositional setting, but all preserve evidence ofmultiple, discrete

horizons ofmarsh peat that are separated by inorganic fine sediments. Investigations ofintertidal

- marsh stratigraphy in south central Alaska (platker, 1990, 1992; Carver and Gilpin, 1993; Barsch

Winkler, 1994~ Mann, 1994) have identified a recurrence interval ofabout 700 yr for major

earthquakes inthe Gulf ofAlaska and Prince William Sound. Local subsidence or uplift occurs

between these events based on proximity to the subduction zone and active faults. Analyses of

intertidal peats on the lower Alaska Peninsula are in progress and will provide valuable information

about relative sea-level changes in the context oftectonic activity along the Shumagin seismic gap. It

appears that there is a general trend ofcoastal emergence throughout the Holocene, with one or more

stillstands that may record episodic attenuation ofthe rate ofuplift. Uplift may also be an episodic

- phenomena, with long periods between tectonic events characterized by subsidence ofmany coastal

,~ sectors.

41 -

----._._._•. ,--- - Peat exposures are also valuable for correlation oftectonic activity and as sources ofpaleoecological information. Insect and plant macrofossils have been recovered from peat horizons exposed in coastal bluffs on Kinzarof Lagoon and Morzhovoi Bay and will aid in reconstructing regional post glacial paleoenvironments. These data are important because they fill a geographic gap in the environmental record ofeastern Beringia (Hu et.al., 1995) and add to our understanding of the dynamic relationship between post-glacial vegetation change and marine climate ofthe Bering Sea

and north Pacific Ocean (cf. Elias, 1992; Short et.al., 1992).

Coastal dune and barrier systems

The distribution ofdune environments gives some indication ofcoastal proximity and dune stratigraphy appears to record fluctuations in regional wind intensity or moisture regime. Dunes cap beach ridges at Big Lagoon on Morzhovoi Bay, Thin Point, Cape Glazenap, and Moffet Point.

Isolated dune fields occur in bluffhead settings at Cold Bay, the head of Kinzarof Lagoon, and at the mouths ofrivers that drain the south face ofFrosty Peak. Blowouts in several dune fields reveal - between two and four weak paleosols that are probably correlative throughout the region. An AMS radiocarbon age of5270±60 yr B.P. (AA-22422) was obtained on a charcoal horizon in a dune ca. 18 m above Russell Creek. About 1.5 m ofpoorly beeded clean sand occurs below this horizon and

above the widely recognized "Fisher Caldera" ash, which suggests that eolian activity was pervasive in near-coast environments during the early Holocene (Mann and Hamilton, 1995). Four paleosols

occur within 2.75 m ofthe section above the charcoal horizon, and while two ofthese may be

pedogenically related to volcanic ash falls (cf. Ping et.al., 1987, 1988), two are probably related to

changes in moisture regime that fostered vegetation growth and surface stability. A bulk soil sample

from a paleosol 1.5 m above the charcoal horizon provided a conventional 14C age of 2805 ±170 yr

B.P. (A-9337). Radiocarbon analyses ofpaleosols from dune fields at the heads of Cold and

; .. ~. Morzhovoi bays, and at Tachilni Creek (informal name) on the Pacific coast south ofFrosty Peak are

in progress and should provide additional information on the response of coastal ecosystems to post

glacial climate change.

A record of coastal climatic regime is reflected in a variety ofrelict and modern coastal landforms

that occur on either side ofthe peninsula. Barrier beaches, spits, and dune-covered beach ridges are

typical mid- to late-Holocene-aged geomorphic elements ofthe outer coast on both sides ofthe

peninsula. An extensive complex ofbeach ridges capped by dunes occurs west ofThin Point, at the

entrance to Cold Bay. This feature is unique among Pacific coast depositional systems ofthe lower

peninsula, and probably reflects the erosion ofheadlands composed ofunconsolidated glacial

materials and reworking ofvolcaniclastic sediments derived from Frosty volcano. A dune field that

caps gravel beach ridges at the head ofMorzhovoi Bay has been deeply incised by north-south

trending blowouts and reflects the dominance ofwinter winds in controlling dune morphology at this

location. Beach berms that underlie the dune field are oriented parallel to the modern shoreline but

have been uplifted 1.5 to 2 m above mean high water. Ages on uplift and the initiation ofdune

formation have yet to be determined but may correlate with the abandonment ofthe 2 - 3 m shoreline

that is recognized elsewhere inthe study area.

Beach ridge plains are commonly mantled by dunes along the Bering Sea coast ofthe peninsula.

Izembek Lagoon is enclosed by a ca. 50 kIn long stretch ofbarrier beaches and dunes bounded by

Cape G1azenap on the west and by Moffet Point on the east. These two spit complexes are attached

to the mainland and consist of 10 to 30 individual ridge/swale sets that have prograded across spit

platforms that are several kilometers in width. Dune heights exceed 20 m in places and reflect intense

erosion and redeposition ofcoastal plain and shelf sediments. The Kudiakof barrier island chain

43 - (Glenn and Operl systems) fronts the central 25 kIn ofIzembek Lagoon. TIlls island chain is younger - than the Glazenap and Moffet beach ridge complexes and is composed ofrelatively low-elevation spits that are capped by one to three dune ridges. Island breaching and inlet migration during storms are common processes and contribute to infilling ofthe lagoon floor. The barrier beaches ofMoffet and Izembek Lagoons and Bechvin Bay (which separates the peninsula from Unimak Island) are important components ofthe modern coastal ecosystem along the north side ofthe peninsula. They probably developed within the last two to three thousand years in response to subsidence and erosion ofthe coastal plain and may have experienced accelerated sedimentation as a result ofepisodic uplift oflagoon floors and the nearshore shelf.

Estuarine marsh environments

During the summer of 1996, several estuarine marsh locales were selected for coring with a manually-operated peat sampler. Locations included a marsh southeast ofthe Cold Bay pier, and two areas in the Grant Point vicinity. The goal was to obtain cores from marshes that have developed in near shore settings so as to track rates of marsh formation as a proxy ofsea-level fluctuation. Core stratigraphy suggests that short-term changes in sea level have occurred during the Holocene. Marsh peat strata are commonly disrupted by sandy horizons, suggesting a record oftsunamis or storm surges. A 2.3 m peat core recovered from below the intertidal zone at Grant Point may indicate a long period of subsidence and coastal transgression along the Bering Sea coast ofthe peninsula. Analyses of cores to determine estuarine ecological zones will aid in reconstructing tectonically-controlled fluctuations of sea-level because ofthe relationship between marsh composition and salt tolerance

(cf., Combellick, 1991; Carver and Gilpin, 1993; Kelsey et.al., 1994; Guilbault et.al., 1995).

Radiocarbon and carbon isotope analyses ofcores obtained in 1996 are in progress. Additional cores will be obtained in 1997 from estuarine settings in Moffet and Kinzarof lagoons.

44 Provisional sea-level record from terrestrial indicators

Terraces uplifted above modern sea-level (asl) due to tectonic and/or isostatic processes provide a

partial record ofpost-glacial sea-level change. Itis possible that seismic subsidence has resulted in

the submergence and transgression ofsome coastal sectors (Reimnitz, 1966; Plafker, 1990). Four

uplifted shorelines are presently recognized in the area. Radiocarbon determinations are pending on

the ages of features that record this record of relative sea-level fluctuation, but provisional ages can

be inferred from stratigraphic relationships and several14C ages obtained thus far (Table 1).

Tentative ages for sea-level stands are given in parentheses following the elevation and location of

features. The marine limit is represented by a 3 kIn long gravel terrace, possibly a bay-head barrier,

that is perched above the head of Kinzarof Lagoon at 25 m asl (late glacial, > c. 11,000 yr BP based

on discontinuous nature offeature and soil development). Subsequent still-stands are recorded as

abandoned marine terraces. A marine scarp and terrace at an elevation of c. 16 m asl is conspicuous

.- around southern Moffet Lagoon and the town ofCold Bay (between 11,000 and 7000 yr BP based on

minimum limiting archaeological age, soil development and stability ofslopes). At the head of

Morzhovoi Bay an eroding coastal bluffexposes glacio-marine and terrestrial sediments that are

truncated by an unconformity at 6 m asl, and terrace remnants are perched at this elevation around

the margins of Big and Middle Lagoons « 9200 yr B.P. based on stratigraphic position above

"Fisher Caldera" ash dated to c. 9200 14C yr B.P.). A 2-3 m asl shoreline is recognized throughout - the eastern Aleutian region (powers,1961; Morris and Bucknam, 1972) and is well preserved as terraces bordering streams that drain coastal lowlands in the USGS Cold Bay and False Pass

quadrangles « c. 3000 yr B.P. based on archaeological limiting ages).

45 - TABLE 1. Project radiocarbon ages from geologic contexts on the lower Alaska Peninsula.

BETA-102185 Mortensens Lagoon, lower intertidal zone 610±70 peat AD 1270 - 1430 - BETA-96827 Russell Creek, paleosol under youngest 1170±120 soil AD 600 -1200 preserved alpine moraine - maximum a e. BETA-96833 Russell Creek Basin, organic matte. 1790±140 organic matte BC 100 - AD 550 BETA-86317 Moffet Lagoon, upper intertidal zone, 191O±60 peat BC32-AD245 s in ondbasin 1!Il!Ii'~ A-9337 Russell Cr. Dunes, middle paleosol 2805±170 soil BC 1450 - 500 BETA-96828 Cold Bay Bluff, peakhorizon near top of 3600±140 peat BC 2500 - 1600 bluffsection. BETA-96826 Little John Lagoon, possible minimum 3850±140 peat BC 2900 - 1900 a e for Little John al ine moraine BETA 96832 Blue Bill Lake basin, base oforganic 4780±160 organic matte BC 4000 - 3100 matte. Maximum age for higher lake level. AA-22422 Russell Cr. Dunes, (archaeological?) 5720±60 charred twigs BC 4250 - 3980 charcoal horizon ~!! BETA-96831 Russell Creek, peat layer between ashes 6070±340 peat BC 5600 - 4240 over! . Cold Ba moraine. BETA-96825 KinzarofLagoon, upper limit for Fisher 791O±160 peat BC 7106 - 6420 ash. BETA-96824 KinzarofLagoon, lower limit for Fisher 9130±140 peat BC 8432 - 7931 ash. A-9338 Morzhovoi Baycoastal bluff, lower limit 9300±80 peat BC 8585 - 8089 """'c for Fisher ash BETA-29390 KinzarofLagoon coastal bluff, lower limit 9380±70 peat BC 8842 - 8197 for Fisher ash BETA-96830 Cold Bay Bluff, thickpeat, infilling 9630±130 peat BC 9055 - 8359 intermorainal pond, minimum age for active ice core. _c BETA-96829 Cold Bay Bluff. Leaflitter on diamicton, 11590±200 leaflitter BC 12083 - 11136 minimum a e ofde aciation.

46 Archaeology

In 1995 portions of the region to the west ofPaul Hansen Lake, the eastern shore of

- Moffet Lagoon, the western half ofKinzarof Lagoon, and unsurveyed areas west and

south ofGrant Point were investigated. Areas surveyed in 1996 include all Middle - Lagoon, the northern, western, and southern shores ofBig Lagoon, Little Lagoon, portions ofthe Bering Sea shore between Cape Glazenap and Hook Bay, and the islands

ofApplegate Cove. Other 1996 investigations included the mapping ofvi11ages discovered

during earlier investigations and the excavation ofseveral test units for charcoal samples in

order to get radiocarbon dates.

- In total, 40 previously unknown archaeological sites have been found (Figure 4, Table 2) and 12 previously known sites have been investigated (Table 3).1n total, over 80

- prehistoric sites are now known in the project area. - -

-~-----_. ------_. __. __._------_.-.._- ---,-,------

Archaeology

In 1995 portions of the region to the west of Paul Hansen Lake, the eastern shore of

Moffet Lagoon, the western half of Kinzarof Lagoon, and unsurveyed areas west and south of Grant Point were investigated. Areas surveyed in 1996 include all Middle

Lagoon, the northern, western, and southern shores ofBig Lagoon, Little Lagoon, portions of the Bering Sea shore between Cape Glazenap and Hook Bay, and the islands of Applegate Cove. Other 1996 investigations included the mapping of villages discovered during earlier investigations and the excavation of several test units for charcoal samples in order to get radiocarbon dates.

In total, 40 previously unknown archaeological sites have been found (Figure 4, Table 2) and 12 previously known sites have been investigated (Table 3).In total, over 80 prehistoric sites are now known in the project area.

48 - A Sites identified by the LowerAlaska Peninsula Project f) Sites identified by the USFWS • Sites recorded or identified by McCartney • Sites recorded or identified by USBIA-ANCSA • Sites identified by other projects

Amak Island

- - -

o - a D

~--- . o 10 20 30 kilometers

,-.. FIGURE 4. Map of the lower Alaska Peninsula showing all archaeological sites by project. -

------"<------TABLE2 Ar h 1 , al S't R d d' 1995 d 1996

79 1995 I amo UW 1995 On the South Shore of the La.oon Drainin. West of Outer Marker Camo 0 0 _. 80 1995-6 South Grant Pt. Fish Camp UW 1995 On a Point in South Grant Point Lagoon VillageiC I 0 amo 81 1996-28 UW 1996 On the West End of Kinzarof La.oon Villa.e 47 0 82 1995-9 Boiler Beach UWl995 Site 200m East ofXCB-021 in KinzarofLa.oon Villa.e 3 0 83 1995-8 First Creek Site UWl995 Site West ofFirst Creek in Kinzarof La.oon Villa.e 201 3 84 1995-7 Second Creek Site UW 1995 On the West Bank ofSecond Creek in Kinzarof Lagoon Village/C 1 0 amD 85 1995-1 Paul Hansen Sod House UWI995 West Shore ofPaul Hansen Lake Sod 1 0 House 86 1995-2 UWI995 NW Shore ofPaul Hansen Lake Villa.e 1 0 87 1995-3 UWI995 1/8 Mile North ofXCB-028 on the East Shore of Moffet La,oDn Villa.e 5 0 88 1995-4 UWl995 1/4 Mile North ofXCB-028 on the East Shore of Moffet La,oDn Midden 0 0 89 1995-11 Moffet Sorin.s UWI995 On the East side ofa Pond in Moffet Sorin.s Villa.e 2 0 91 1995-13 UWI995 On Point in South Swanson La.oon Villa.e ?1 ?1 92 1995-14 UWI995 SW Swanson La.oon Villa.e ?? ?1 93 1996-1 'RusseU Creek Blowout UWl996 West Bank of RusseU Creek Whic 0 0 Scatter 94 1996-2 Point Between Middle and Bi. La'Dons Villa.e 20 0 95 1996-3 Morzhovoi Dunes Blowout UWI996 West Pt Between Middle and Big Lagoons Lithic 0 0 Scatter 96 1996-4 Morzhovoi Dunes Villa.e UW1996 Point Between Middle and Bi. La.oons Villa.e 19 2 97 1996-5 UW1996 East Side ofMiddle La.oon Channel Villa.e 14 0 98 1996-6 UWI996 East Side ofMiddle La.oon Channel Villa.e 12 1 99 1996-7 West Bi. La.oon Villa.e UW1996 On the West Shore ofBi. La.oon Villa.e 27 2 100 1996-8 Middle Lagoon Dunes UW1996 On the East Eud ofthe Outer Middle Lagoon Dunes Lithic 0 () Scatter 101 1996-9 Lillle La.oon Villa.e UW1996 On the East Side ofthe Little La.oon Mouth Villa'e 26 2 102 1996-10 Big Lagooo Cabin #1 UWI996 On the East End ofthe North Shore of Big Lagoon Sod 2 () House 103 1996-11 Dark Side ofthe La.oon UW 1996 On the East Eod ofthe North Shore of Bi. La.oon Villa.e 58 0 104 1996-12 UWI996 East Shore ofUpper Middle La.oon Villa.e 29 () 105 1996-13 Adama.an UWI996 On the West End ofthe North Shore ofBi. La.oon Villa.e 386 5 106 1996-14 Big Lagoon Cabin #2 UW1996 On a Point in the NW Comer of Big Lagoon Sod 1 0 House 107 1996-15 Big Lagoon Cabin #3 UW1996 On a Point in the NW Comer of Big Lagoon Sod I 0 House 108 1996-16 Middle La.oon Fish Camo UWI996 On the West Side ofMiddle La.oon Channel Villa.e 3 () 109 1996-17 UWI996 On the East End ofthe South Shore ofUoner Middle La.oon Villa.e 4 () 110 1996-18 UWI996 South Shore ofUnner Middle Lawon Villa.e 55 0 111 1996-19 UW1996 N. Side ofthe Stream Enterin. Morzhovoi Bav S. of Boiler Pt. Villa.e 15 () - 112 1996-20 UWI996 S. Side ofthe Stream Enterin. Morzhovoi Bay S. ofBoiler PI. Villa.e 12 2 113 1996-22 UWI996 On Apple.ate Cove SW of Grant Point Villa.e 17 0 114 1966-23 UWI996 On Point Across From XCB-054 on Cove Island Lithic 0 0 Scatter 115 1996-24 Swan Lake Road Cut UWI996 10 the Road Cut at the End ofthe Swan Lake Road Lithic 0 0 Scatter 116 1996-25 UW 1996 On the SE Point of the Southern Half ofCove Island Lithic 0 1 Scatter 117 1996-26 UWI996 On a Small Island North ofCove Island Camp 2 () 118 1996-27 UW 1996 On a Small (unchatted) Island SE ofCove Island Lithic 0 0

119 1996-29 UWl996 On Bering Sea Shore NE ofMorzhovoi Lake 25 2 122 Hoffman Glazenao heach rid.es ~ 3-4 0 -

49 TABLE3 P h't Arh 1 . al S' P 1 R d d' h Pr . Ar

1 IZM-1 McCartney-sIZM-1 McCartney 1974. BaseofCapeGlazenap-NormaBay Vdlage 199' 5 BIAANCSA XCB-003 IZM-3 McCartney's IZM-3 McCartney 1974, Unnamed Bay (south Norma I APplegate) Vdlage 0 BIAANCSA XCB-004 Morzhovoi ViIla.e BIAANCSA Middle La.oon Vdla.e 30 5 XCB-5 Klin.ler 1979 S. Entrance to the La'oon SW ofOuter Marker Vdla.e 0 6 XCB-6 Outer Marker Site iKlin.ler 1979 East Side ofthe La.oon East of Outer Marker Vdla.e i=40 4 21 XCB-21 Kinzerof La.oon West BIAANSCA Vdla.e 22 1996-21 Bricker Site UW 1996 South and West of the Russen Creek Mouth Vdla.e 59 0 24 1983 Hook Bav BIAANCSA Ou the NW Tin oflhe AI<. Pen in Hook Bav Vdla·e 79 7 25 PN-97 BIAANSCA Ou the NW Shore ofMorzhovoi Lake Villa'e 60 6 26 PN-96 BIAANSCA On the Berin. Sea SW ofCane Glazenan Vdlaue 37 3 27 XCB-27 Moraine Site Southwest BIAANSCA On a Moraine on the SW side of the Joshua Green River Vdlaue 54 0 28 XCB-28 IMoffet Town BIAANSCA On the Westernmost PI. ofthe East Shore ofMoffet ul~oon Vdlau~ 925 21 29 lXCB-29 Moraine Site Northeast BIAANSCA On a Moraine on the NE side ofthe Joshua Green River Vdbl'e 112 0 30 PN-36, Strawberry Point BIAANSCA On the Point Separating lzembek and Moffet Lagoons Vdlage 213 0 M-12255 123 BIAANCSA Unnamed Bav south Norma I Annle.ate 73 0 121 BIAANCSA Unnamed Bav (south Norma I Annle.ate) 13 0 120 BIAANCSA Unnamed Bav south Norma I Annle.ate) 20 0 31 BIAANCSA Unnamed Bav south Norma I Annleuate e 160 0 32 Dumond 1986 East Shore ofMoffet Lauoon Vill.ue n ?7 33 Dumond 1986 East Shore ofMoffet Lauoon Vdla'e ?? '/? .- 36 XCB-36 USFWS 1979 On a Bluff Across from XCB-OD5 SW nf Outer Marker Lithic 0 0 Scatter 37 XCB-37 USFWS 1979 On a Rid.e in the Marsh Headin. East Outer Marker G'oon Camn I 0 38 XCB-38 USFWS 1979 On a Ridge in the Marsh Heading East Outer Marker Lagoon Lithic 0 0

39 XCB-39 USFWS 1979 On the SW shore ofWest Outer Marker La'oon 3 0 40 XCB-4O Red Saboon Creek USFWS 1979 On the West Side ofthe Stream Emntvin. Hess Saboon) Lake 38 0 41 XCB-41 USFWS 1979 West Side ofHess (Saboon Lake Outlet 2 0 42 XCB-42 USFWS 1979 On a Point SW ofthe Hess (Saboon Lake Outlet 1 0 43 XCB-43 USFWS 1979 East Side ofBlue Bill Creek. 65m Below Outlet 4 0 44 XCB-44 USFWS 1979 On the Terrace NW ofthe Outlet ofBlue Bill Creek IVdlaue 11 0 45 XCB-45 USFWS 1979 South Side ofBlue Bill Creek Mouth Villa'e 2 0 -- 46 XCB-46 USFWS 1979 North Side ofthe Blue Bill Creek Mouth Vi11.ue 42 0 47 XCB-47 USFWS 1979 N. Bank of the Tidal Channel South ofBlue BiD Creek Mouth Villa•• 3 0 48 XCB-48 USFWS 1979 S. Bank of the Twal Channel South of Blue BiD Creek Mouth VJlla.'. 2 0 49 XCB-49 USFWS 1979 Half-wav Between Blue BiD Creek Muuth and OutIet Villa.•• 16 0 50 XCB-50 USFWS 1979 North Bank of the Mouth ofFrost,'Creek Villa•• 20 0 - 51 XCB-51 USFWS 1979 South of Frostv Creek Mouth Vdla.e 21 0 52 XCB-52 USFWS 1979 S. Of Frosty Creek Mouth 150m Lithic 0 0 Scalier 53 XCB-53 USFWS 1979 West Side ofthe Base ofStrawherrv Point Villa'e 3 0 54 XCB-54 USFWS 1979 Southeast End ofCnve Bandin.l Island Villaue 27 0 55 XCB-55 Grant Point USFWS 1979 Grant Point Vdlaue 5 0 72 BIAANCSAI On the North Side ofa Small Lagoon in NE Big Lagoon Lithic 0 0 UW 1996 Scatter 73 =lANCSA South Side ofCreek in Section 14, South Norma Bav Villa..e 1? ?'! 74 XCB-74 Moffet Creek 1 ANCSA North Shore ofMoffet Creek 17 '/? 75 XCB-75 Moffet Creek 2 ANCSA~ Shore of Moffet Creek 11 11 76 XCB-76 Moffet Creek 3 IA ANCSA Shore of Moffet Creek ?? 11 77 XCB-77 Moffet Creek 4 BIA ANCSA rth Shore ofMoffet Creek ~ ?? ?? 78 XCB-78 Moffet Creek 5 BIA ANCSA North Shore ofMoffet Creek Villa.e '/? ??

The newly discovered sites include four site types.

- Historic sites are sites that are the result ofEuropean activities. All of these sites are the remains of small sod houses, one on Paul Hansen Lake and three in Big Lagoon. We conducted little or no

- research at any of these sites

50 Lithic scatters are small concentrations of stone tools or the debitage from their manufacture that are not associated with any surface depressions or other archaeological features. These occur in two forms. The first is in eroding sand dunes and consists of widely scattered remains. These occur primarily in prominent locations where, over many years, activities associated with the search for, hunting, or processing of sea mammals was conducted. The second type is intertidal and consists of a dense concentration of remains in areas that are good for hauling Kayaks out of the water.

These are probably temporary camps were hunters rested, repaired equipment, or did other short term activities. These sites are usually found on small islands or peninsulas.

Villages are large numbers of depressions that are the remains of houses, tents, storage and other facilities. Villages seem to be associated with a number of geographic variables, the most important being a nearby fresh water source. They are more often located where a small lake or pond is near the marine beach. They are secondarily located near springs or small streams. Large villagestend to be located within 2krn of a major salmon system, small villages are less likely to be associated with salmon streams, although many are clearly located on salmon systems.

Camps are sites that consist of 0 to 3 depressions that are intuitively not a village but at the same time are more than a lithic scatter. These are usually found a fish harvesting areas near salmon streams and could probably be considered fish camps. These sites are distinctive in that they usually have 1-3 small depressions «2m in diameter), but sometimes have a single house-sized tent depression. - These classifications are simply for heuristic purposes as we currently have little understanding of either the overall pattern of prehistoric settlement in the region or the temporal variability in its

51 representation on the landscape.

To make the case for full-coverage survey and our decidedly regional approach, a number of - observations should be made. First, while the majority of the large villages had been discovered prior to our investigations, the numbers of smaller sites found during our pedestrian surveys is - greater than the number of smaller villages found over the previous 30 years. There are also numerous medium-sized villages. These are not only the most abundant, but they are also in the

size range that is most often missed in aerial surveys. A similar case can be made for small villages -- and camps. Large and very large villages are commonly identified from the air and, as might be expected, only a few of these villages are newly discovered.

- Second, based on these data, we find that there is a considerable amount of variability in both the size and distribution of villages. For example, we know that the houses identified as nucleus

- satellites all date after approximately AD 1100, with most dating after AD 1500. Within this

narrow time frame villages range from 1 to 30 of these complexes. Some are located adjacent to

salmon streams, some are on the outer coast. Some have numerous large satellites, others have few

,-. or small satellites. All ofthe data are not as yet compiled but at this preliminary stage, a number of

patterns have emerged and will be described in the following sections.

Site Recording and Methods

A number of variables were recorded at each site. In general, much of the data gathered at each

site is reflected in the map. Attributes of site location such as climatic and solar exposure, beach - type (rocky, sandy, etc.), elevation above the beach, defensibility, landform, and distance to fresh water were the primary characteristics recorded. Some attempt was made at describing the site

52 vegetation but the majority ofthe sites had the same plant community that has become known as site vegetation (see Nancy McCartney's dissertation), although they tend to occur in variable percentages. We did note specifically when the vegetation deviated from the expected, such as in

Big Lagoon where a number of old houses are now in crow berry.

The site maps contain an accurate representation of the size of the houses and their spatial arrangement. The actual house dimensions were recorded on each map. Less emphasis was placed on contouring the natural topography except where critical to the spatial organization of the site.

At most sites a test was excavated in order to describe the site stratigraphy and to gathered charcoal for a radiocarbon date. Excavations never exceeded txt meter and the location of the test was usually based on convenience. Collections were made from the beach in front ofthe site where possible. These collections have proven useful in illustrating the range of lithic materials and tool types present at each site. Some sites are highly eroded resulting in large samples, others had no intertidal remains whatsoever.

Radiocarbon Dating

At present, 42 radiocarbon dates have been run on samples from lower Alaska Peninsula and

Unimak Island archaeological sites. The project has contributed 2t AMS and three standard dates while 6 additional AMS dates are in progress. When completed, this region will have the best dated radiocarbon chronology in western Alaska (Table 4, Figure 5).

All dates were run on wood charcoal, many of the AMS dates being run on twigs from floors and ~I hearth areas within houses. The conventional dates were run at Beta Analytic while the AMS dates

53 were prepared to target at the University of Wisconsin Radiocarbon Laboratory and then analyzed

at Lawrence Livermore Laboratory's accelerator. A number of new AMS dates will be from the

University of Arizona.

We believe that there are no inherent problems associated with our dating methods, other than the - possibility of old driftwood. The BIA ANCSA dated a piece of charcoal associated with glass beads at XCB-004 to over 1500 BP, but they believe that this date was ultimately on coa1 brought

in by the Russians since they were testing a Russian-like structure. -

I~ 54 "T1 G5 c :::0m C11 I II , 0 ~ ~ ~ ~ ;::0 J,.. w w w W N N N N ~ ~ ~ ~ N 0 ..... 01 N 0 ..... 01 N 0 ..... 01 N 0 ~ 0. N N 01 ..... 0 N 01 ..... 0 !!. l» 0 01 0 01 0 01 0 01 0 01 0 01 0 01 0 01 01 0 01 0 01 0 01 0 0- 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 a: cr XCB-099 Al ~ CD a- UNI-067 -Q. o C ::::l XCB-025 I» () CD :::r XCB-028 - a UNI-067 ::::lo 6" XCB-046 <0 '< XCB-023 - 0' .., XCB-003 :::r (1) UNI-071 r- ~ XCB-094 .., XCB-094 » XCB-002 -,W Dr fIl @ XCB-001 "U XCB-001 (1) ::::l XCB-006 jj'£Gi 5' fIl c: XCB-001 Dr XCB-001

XCB-121

XCB-003

XCB-025 rn XCB-031 i XCB-040 XCB-040

XCB-003

XCB-104

XCB-031

XCB-004

XCB-005

~ UNI-090

XCB-101

',it. XCB-005

XCB-115 i_ XCB-103 XCB-103

XCB-030

XCB-029

XCB-110

XCB-054

XCB-029

JM TABLE 4: All radiocarbon Dates from the Lower Alaska Peninsula and Unimak Island. ~ CAMS 30623 UNI-067 270±60 AD 1460-1690 BETA 79651 UNI-067 60±50 AD 1690-1815 BETA 79652 UNI-071 550±60 AD 1300-1450 BETA 79653 UNI-090 1680±60 AD 240-535 SI-920 XCB-ool 925±95 AD 950-1270 SI-919 XCB-OOI 905±50 AD 1020-1230 CAMS 30615 XCB-OOI 840±50 AD 1040-1270 CAMS 30608 XCB-ool 79O±60 AD 1040-1290 SI-921 XCB-002 760±9O AD 1040-1400 SI-918 XCB-003 1235±105 AD 630-1000 SI-916 XCB-003 l005±105 AD 790-1240 SI-917 XCB-003 390±95 AD 1390-1680 BETA 29388 XCB-004 15OO±150 AD 200-900 BETA 86320 XCB-005 1870±80 BC 60-AD 350 CAMS 30606 XCB-005 1620±60 AD 320-590 CAMS 30607 XCB-005 1580±50 AD 380-600 CAMS 30610 XCB-006 860±60 AD 1030-1260 BETA 29382 XCB-023 330±100 AD 1400-1700 - BETA 29387 XCB-025 960±160 AD 650-1300 BETA 29386 XCB-025 29O±100 AD 1460-1880 BETA 86320 XCB-028 280±70 AD 1440-1820 BETA 29390 XCB-029 45OO±250 BC 3800-2500 BETA 29381 XCB-029 3370±150 BC 2150-1300 BETA 39381 XCB-030 2990±11O BCI500-900 BETA 29384 XCB-031 1420±130 AD 300-900 BETA 29385 XCB-031 1190±100 AD 640-1030 CAMS 30620 XCB-121 101O±50 AD 890-1160 CAMS 30612 XCB-04O 1190±60 AD 680-970 KLINGLER XCB-040 121O±90 AD 660-990 CAMS 30611 XCB-046 340±60 AD 1440-1660 CAMS 30619 XCB-054 404O±50 BC 2770-2460 CAMS 30618 XCB-054 3980±60 BC 2700-2300 AA-22422 XCB-093 5270±60 BC 4200-4000 CAMS 30605 XCB-094 740±50 AD 1170-1310 CAMS 30604 XCB-094 620±60 AD 1270-1420 CAMS 30621 XCB-099 70±50 AD 1690-1920 CAMS 30609 XCB-101 181O±50 AD 80-340 CAMS 30616 XCB-103 2550±60 BC 830-410 CAMS 30614 XCB-103 2470±60 BC780-41O - CAMS 30617 XCB-I04 13oo±50 AD 640-860 CAMS 30622 XCB-ll0 3460±60 BC -1940-1630 CAMS 30613 XCB-115 1880±50 AD 10-240

56 Geographic Summary ofthe Survey Locales

Moffet Lagoon - Joshua Green River

Moffet Lagoon and the Joshua Green River basin are located in the northeastern portion ofIzembek

National Wildlife Refuge. Moffet Lagoon is an extension ofthe Izembek Lagoon system and is enclosed by a 20 kID long beach ridge plain that has prograded westward from the coastal plain north ofthe Aghileen Pinnacles. This lowland plain consists ofglacial till and outwash; extensive erosion during storms and high tides on the Bering Sea maintains a steep scarp and provides fine sediments for the construction ofbarrier spits and bars that enclose Moffet and Izembek lagoons. hIDer Moffet

Lagoon is exceedingly shallow and channels are poorly integrated across the lagoon floor. Lag deposits ofglacial cobbles and boulders occur inthe near-shore zone and indicate an earlier period of shoreline erosion and greater water depth. The shoreline ofeastern Moffet Lagoon is composed of late Pleistocene moraine renmants that are separated by marsh and pond basins. The southern margin of the lagoon is composed ofdeltaic deposits ofthe Joshua Green River and estuarine marshes.

A prominent moraine separates Moffet Lagoon from the Joshua Green River basin and indicates ice flow from a center on Mt. Dutton or from a larger ice sheet centered south ofthe spine ofthe peninsula. Locally referred to as Ptarmigan Ridge, this moraine is bisected by the river channel and has been trimmed by wave action on its inner and outer margins, indicating that it either dammed a proglaciallake or was an isthmus that confined a paleo-estuary ofthe Bering Sea when sea-level was several meters higher than present. The western limb ofthe moraine system merges with a higher and perhaps younger moraine system that can be traced around the head ofCold Bay. This system forms the western margin ofthe Joshua Green River basin and the shore of Paul Hanson Lake. Drainage is poorly integrated on the upland, which is pitted with kettle lake basins. Several ofthese are drained

57 and expose polygonal ground. Ridge crests support a discontinuous cover of shrub tundra and

surface exposures are common on unprotected sites. Streams are underfit in marsh-filled valleys in

lowland areas and on portions ofthe large delta that the right fork ofthe Joshua Green River has

deposited in the eastern margin ofthe Paul Hanson Lake.

Izembek Lagoon

Izembek Lagoon is enclosed bythe Kudiakof Island chain, a barrier beach system that is composed ..... of Glenn and Oped islands. lhis relatively young barrier chain is frequently overwashed by storm

tides, which contributes to sedimentation ofthe backbarrier platform and infilling ofthe lagoon.

Norma Bay and Applegate Cove are western embayments ofIzembek Lagoon and are protected from

the Bering Sea by the Cape Glazenap beach ridge plain and a broad tidal flat at the western end of

Glenn Island. Water depths are shallow in the Izembek system, although the network oftidal

channels on the lagoon floor are deeper and better established than in Moffet Lagoon. The lagoon

generally shallows to the west, with mud flats typically exposed in Norma Bay and Applegate Cove .... at tidal stages below mean high water (MAW). Several tidal channels trend seaward across the lagoon floor in this sector, possibly indicating the location ofstream courses cut during a period of

lower-than-modem sea-level. The orientation oftidal channels in Izembek Lagoon proper reflects

more dynamic tidal circulation between the inner reaches ofthe lagoon and the Bering Sea.

The landward margin of Izembek Lagoon is formed by headlands composed of glacial till and

outwash and varies in plan morphology from irregular to nearly straight, depending on surface

topography. Small embayments and estuarine marshes are inset into coastal lowlands and have - expanded and contracted with fluctuations of sea-level. Several marsh-filled basins that are presently isolated from the lagoon were probably intertidal estuaries during periods ofhigher sea-level. Terrace

58 .... -

remnants along some stream valleys indicate former sea-level stands at 2-3 m and about 15 m above modern sea-level (asl). An outcrop of marsh peat along the shore at Grant Point extends more than 2 m below MHW, indicating that subsidence ofthe coastal plain has occurred at least locally along the inner shore ofIzembek Lagoon.

Kinzerof Lagoon - West Cold Bay

Kinzarof Lagoon and the northwest margin ofCold Bay preserve a diversity ofpaleoenvironments and record adjustments to post-glacial climate and sea-level changes. The eastern half of Kinzarof

Lagoon is enclosed by a peninsula-shaped remnant ofthe inner margin ofthe Cold Bay moraine, which connects the volcanic massifs ofMt. Dutton and Frosty Peak and separates the Bering Sea from the Pacific Ocean. The western third ofthe lagoon is enclosed by a barrier spit and beach ridge complex that has built atop a shore platform apparently uplifted into the intertidal zone during the late Holocene. The primary tidal exchange occurs within the eastern two-thirds ofthe lagoon, and provides migrating salmon access to stream systems that drain lowlands surrounding its northeast margin.

A wave-cut scarp backs the inner shore of KinzarofLagoon and is actively eroding along its deeper, eastern section. This scarp is stabilized landward ofthe recent spit complex and is separated from the modern shore by a backbarrier lagoon system that impounds Swan Lake. A low angle terrace rises from the head ofthe active scarp to a wave-washed gravel ridge that is presently recognized as the marine limit (25 m asl) in the study area. This feature trends parallel to the modem shore for a distance of about 3 kID and was probably deposited as a bay-head barrier during or shortly following deglaciation ofthe region.

59 Isolated dune fields occur in bluffhead settings above the stabilized marine scarp east ofSwan Lake,

and above the actively eroding scarp north ofthe town of Cold Bay. Blowouts in these dune fields

expose several weakly developed paleosols and at least one volcanic ash that was probably deposited

within the last 200 years, based on its stratigraphic position. Loess deposits also cap bluff edges

around the northwest margin ofCold Bay, and may predate dune formation. The town ofCold Bay is

situated on till ofthe Cold Bay moraine although dune deposits mantle much ofthe area, especially

under the airport. The "Fisher Caldera ash", dated to ca. 9200 14C yr B.P., has been found in dune

settings around Cold Bay, suggesting that eolian activity was common in near-shore settings during

the early Holocene.

Morzhovoi Bay - Middle and Big Lagoons

Morzhovoi Bay is the next major embayment into the Alaska Peninsula west of Cold Bay and shares

the same gross morphology due to scouring by late Pleistocene ice lobes that advanced northward

across the peninsula from a source centered on the shelf ofthe north Pacific. The moraine system that

separates the Bering Sea from the Pacific Ocean at the head ofMorzhovoi bay is probably correlative

with the Cold Bay moraine. Three lagoon systems are inset into coastal lowlands at the head of

Morzhovoi Bay. Big and Middle lagoons are partly enclosed by gravel spits that have been deposited

in westward and eastward directions, respectively, along the head ofthe bay head, and reflect bi

directional circulation within the bay and periods ofintense erosion that have supplied coarse

material for littoral transport. Little Lagoon is an estuary that is enclosed by low headlands ofglacial

till.

Dune deposits mantle all near-shore deposits around the bay head, locally reaching heights of 10 to

30 m. The dune field that caps gravel beach ridges seaward ofBig Lagoon has been deeply incised by

- 60 north-south trending blowouts and reflects the dominance of winter winds in controlling dune morphology at this location. Beach berms that underlie the dune field are oriented parallel to the modern shoreline but have been uplifted 1.5 to 2 m above mean high water. Ages on uplift and the initiation ofdune formation have yet to be determined but may correlate with the abandonment ofthe - 2 - 3 m shoreline that is recognized elsewhere in the study area.

The coastal lowland surrounding the head of Morzhovoi Bay preserves a record of two and possible three former sea-level stands. Terraces are preserved at elevations of 2 - 3 and 6 m asl between Big and Middle lagoons, and till headlands at the western entrances to these lagoon systems may have been wave-cut at 14-16 m as!. Loess deposition and weathering have modified these surfaces, which typically expose lag gravels along their windward edges but grade into deposits ofsilt- and sand supported pebbles and gravels more than a meter in depth, away from bluff edges.

Ponds and poorly integrated stream systems occur across the moraine system between Morzhovoi

Bay and the Bering Sea. Marsh-filled basins, underfit streams and shallow, infilled lagoons backed by stable wave-cut scarps are evidence that sea-level was higher than modern on several occasions throughout the Holocene. It is likely that many stream courses have reversed direction as a result of base level changes accompanying local subsidence, uplift, or deposition ofbarrier bars and dunes along the bay and Bering Sea shorelines.

61 SETTLEMENT mSTORY AND INITIAL OBSERVATIONS

ONVILLAGE EVOLUTION

At present, we have discovered 41 previously unrecorded prehistoric sites. Combined with the known sites, there are approximately 70 village sites, 7 small camps, and 11 lithic scatters. The lithic scatters are all in dune blowouts or in intertidal areas. These sites span the last 5500 years, range in size from a few square meters to over 60,000 square meters, and have from none to over 900 surface depressions.

The preliminary coastal geomorphological investigations indicate that there have been a number of sea-level stands higher than the current shoreline (Jordan 1996). James Jordan has found evidence for 3m, 6rn, and 16m shorelines. Although these have not as yet been fmnly dated, most ofthe sites older than 2000 years are situated on high, stable, landforms. The more recent sites are nearer the modern shoreline. This indicates that there has been serious erosion to both the earlier landscape and to the archaeological sites that may have been located on those landforms.

Based on settlement and house form, we have developed a preliminary chronology for the region divided into six phases (Table 5). The bracketing dates for the early phases should be seen as having fuzzy boundaries as there are not yet sufficient data or resolution to confmn them. Based on research conducted 450krn to the northeast (Dumond 1981, 1988; Henn 1978) and 200krn to the west (Aigner

1976, 1978; Aigner and Del Bene 1982; McCartney and Veltre 1996), I fully expect that earlier phases will be defined but as yet, landforms of earlier ages have not been surveyed and excavations in deeply stratified sites have not been done. Because ofthe quality and number ofthe AMS dates, the last 2000 years are easily defined, although the Izembek Phase may be subdivided in the future.

62 There is indeed a gap in the radiocarbon chronology between 550 BC and AD 100. I will speculate on why this is so in the Discussion.

Table 5: Chronology for the Lower Alaska Peninsula (all dates are approximate). ~,

MORZHOVOI PHASE AD 1550-1804 7 7 BIG LAGOON PHASE AD 1250-1550 4 4 CAPE GLAZENAP PHASE AD 1050-1250 3 6 LATE IZEMBEK PHASE AD 750-1050 7 8 •••••••••• u ••••••••••••••••• u •••••• n n u n n •••••• EARLYIZEMBEKPHASE 200 BC-AD 650 7 9 no sites 500-200 BC 0 0 KINZEROF PHASE 2200-650 BC 4 5 ...... MOFFET PHASE 3800-2400 BC 2 3 RUSSELL CREEKPHASE? 4500-4000 BC 1 1

Russell Creek Phase?

In June, 1996, James Jordan was investigating a dune blowout on the north side of Russell Creek

Mffi'l near the town ofCold Bay. A soil sample collected from a paleosol near the base ofthe dune has been dated to over 6000 BP (calibrated). Around the base ofthis dune and across the surface ofthe blowout were found a number offlakes, retouched flakes, and a single stemmed dart point. The only reasonable association for the artifacts is this 6000 year old paleosol. While tentative and certainly in need offurther investigation, we have preliminarily assigned this site to a hypothetical Russell Creek

Phase.

Moffet Phase

The Moffet Phase extends from 3500 to 1500 BC and is represented by two or three sites scattered

63 across the project area (Figure 6). The Moraine 1 Site (XCB-029) and site XCB-IlO (which dates to

the interface between the Moffet and Kinzerof Phases) are both located on what are now inland

waterways and in association with two ofthe most productive salmon streams on the lower Alaska

Peninsula. The Cove Island Site, XCB-054 (Figure 7) is located on an island inthe middle ofwestern

Izembek Lagoon. At a lower sea-level stand, this site would have formed an island between two of

..- Izembek's most productive salmon streams. All three sites have surface house and cache depressions

that are associated with materials dated to this phase. The houses show no apparent organizational

pattern other than a rather random cluster ofhouses and cache pits.

Moffet Phase lithics are nearly 100% basalt. The technology is bifacial with 3-5cm side-notched dart

points, ovoid knives, a numbered ofhafted knives and scrapers, and occasional unifacially retouched

flakes and blade-like flakes. A single ground slate probable engraving tool was found at Cove Island.

This item has a haft and is less than 2cm in length. No ground slate occurs at this time anywhere in

the Aleutian region and the only ground slate technology in the western north at this time is the

Ocean Bay II Tradition ofthe Kodiak Archipelago and adjacent mainland, but this tradition has

mostly large lances and blades (Clark 1993). A number of notched net sinkers have been found at

two ofthe sites.

2 2 Houses at all three sites range from 9 to 60 m with the majority inthe range of 12 to 30 m • All three

sites have between 1.2 and 2.3 meters of continuous house floors indicating long and stable

occupations. The houses are deep depressions. While the surface depressions are usually between .30

and .70 meters deep. the top house floor is often more than a meter below the current ground surface

indicating unusually deep house depressions.

.------A Moffet Phase Sites • Kinzerof Phase Sites • Izembek Phase Sites

Amaklsland

Q o o D

~-- o - - 10 20 30 kilometers

FIGURE 6. Map ofall sites dating to the Moffet, Kinzerof. and Izembek Phases. XCB-054

- • - • ••• • •• • • • • •• • N~

• o 30 ~ ! ~ meters contours =2m marsh grass

FIGURE 7: Map ofXCB-054, the Cove Island Site. These sites give us a view of early sedentism in this region. Since this region is the terminus ofthe distribution ofterrestrial resources, ifthere was a transition from mobile, terrestrial big-game hunters to sedentary marine oriented strategies, this is where it should have occurred. After surveying over

100 kilometers ofupland moraine and ridge systems - areas that elsewhere inAlaska would be covered with caribou hunting camps, I can finnly announce that not only is there no inland or terrestrial adaptation. When people fIrst arrived on lower Alaska Peninsula they appear to have been marine adapted and sedentary.

The earliest archaeological assemblages found elsewhere in the Aleutian Archipelago are associated with the Anangula Tradition fIrst described by Laughlin (1980), Aigner (1976, 1978; Aigner and Del

Bene 1982) and others in the 1950s and 1960s. The hallmark ofthis tradition is still the Anangula site on Anangula Island in Nikolski Bay, Umnak Island 300 kID west of our research area. This site, dating to between 8600 and 8300 years ago (based on over 40 radiocarbon dates) is spectacular in a number of ways. First, at least fIve houses were uncovered in the most recent excavations. Aigner estimates that given the extent ofthe site, at many as 50 to 60 houses were present at the time of occupation. Second, it manifests the beginning ofa nearly continuous record of early Aleut-like structural. and artifactual elements including red-ochre floors, roof-entrances, stone bowls and oil lamps, and interior storage facilities.

Although several thousand years later, the Moffet Phase sites have the same structure. Small house depressions, red-ochre covered floors, stone lamps, and roof entrances. The presence of a number of widely distributed sites in similar geographic locations allows the construction ofa model of the origins ofsedentism based on resource density and resource distributions. This model is structured as follows.

67 Under conditions ofresource abundance in a redundant landscape, the benefits ofmobility become

irrelevant. For example, in the Aleutian Islands there are no terrestrial resources. The marine

resources occur in the each bay in the same season. Ifone was to be mobile, the only place to be

mobile to is the next bay, which has the same resources in the same seasons as the one you just left. - Thus, the reasons one would be mobile - to take advantage oftemporal and especially spatial variations in resource abundance, are not present. Under these conditions, it is more economically

expensive to be mobile than it is to be sedentary. The relationship between resource abundance and

resource redundancy can be seen in Figure 8. Inthis model, when resource abundance is high and the

resources are temporally and/or spatially redundant, sedentism is the likely outcome. Although there

are other avenues to redundant landscapes (Maschner, in review), this is the only clear path that

explains early Aleutian village sites.

Figure 8: Model for Sedentism in Island Settings.

Redundant Landscape Theory of the Origins of Sedentlsm

High

Resource Abundance

Low

Resource Redundancy

..- It is important to distinguish between sedentism and sedentary villages. I am well aware that there is no reason expect all ofthe people in a region to behave in the same manner and this is discussed in greater detail elsewhere (Maschner, inreview). But this model simply states that beyond social, political, or psychological reasons why it is often difficult to maintain a community, when there are some locations on the landscape where resources are abundant throughout most of the year, and other places on the landscape provide no useful alternatives, we can fully expect that some people will stay and harvest those resources on a continuing basis.

Some may argue that the relationship between the presence of storage facilities and these early houses is meaningful for explaining sedentism. Storage has been seen as a critical aspect ofthe development ofmany societies and its origins and implications are often discussed (Testart 1982). I would like to put storage to rest as an important criteria. There is not a single hunter-gatherer who ever lived in the desert who did not understanding the relationship between desiccation and preservation. There is not a single hunter-gatherer in the north who did not understand the relationship between frozen meat and preservation, and there was never a hunter-gatherer who did not understand that a smoke-filled house preserves meat longer than no smoke. Hunter-gatherers are exceptional at what they do and these are things they would notice in the course of everyday events, at least once the cognitive ability evolved to the point that they would notice. This means that the development ofstorage is irrelevant, it is the initial act ofchoosing to store that is interesting. Using the same criteria as sedentism, people will choose to store foods where they believe it is less expensive than searching for food.

Fitzhugh has recently argued that the earliest north Pacific villages were not sedentary because the size and shape ofthe houses might be simply tent depressions, not more permanent structures

69 (1996), and this might indeed be the case for the earliest communities such as Anangula, although

this argument is open to debate. lbis is definitely not the case for the lower Alaska Peninsula villages

dating after 3000 Be because all ofthese villages have numerous storage facilities. Since this area

has one ofthe highest concentrations of Kodiak Brown Bears on earth, the presence ofstorage

facilities becomes an interesting measure ofsedentism. We have documented bear excavations that

were over 12m2 and 1.0 meter deep that are a result ofbears searching for ground squirrels. We are

also intimately aware ofthe impact a bear can have on anything that smells like food. Since this area

generally does not freeze, and there are no trees or materials to build platforms, any use of storage

facilities requires, by the presence ofbears, sedentism to protect those stores.

To summarize the Moffet Phase, a number of observations can be made. Throughout the Aleutian

region, there is little change in the size or structure of either Aleutian houses or villages between

8000 and 3500 years ago. On the lower Alaska Peninsula these villages appear to be small clusters

ofhouses with each inhabited by a single or extended family. Houses range between 9 and 18 square

meters offloor area. Villages are strategically placed at key subsistence localities. But overall,

villages continue to be rare and populations low. There is no evidence for a more mobile strategy co

occurring with these villages. These small, single family houses were organized into small villages

that ranged from 2000 to 5000 m2 in area.

70 Kinzerof Phase

There are two large sites that fall within the Kinzerof Phase (Figure 6). Strawberry Point is a large village with over 200 depressions spread across approximately 50,000 m2 of site area. The site is located on the point that separates lzembek from Moffet Lagoon. A single date from a cut bank submitted by the BIA calibrates to between 1000 and 600 BC (US BIA 1991:72). Further evidence that this site dates to this age is a whale bone mask collected from this site and donated to the

Anchorage Museum ofHistory and Art. This mask is exactly the same as a number ofmasks found during excavations at Port Moller 150km to the northeast. These masks were all found in the context of Port Moller Phase II deposits (Okada 1989). Nineteen radiocarbon dates from this phase extend from approximately 1500 BC to 0 AD.

Dark Side ofthe Lagoon (XCB-I03) is another KinzerofPhase site located at the head ofBig

Lagoon in Morzhovoi Bay. This site consists ofover 60 depressions scattered along a high, south facing terrace (Figure 9). The lagoon below the site is completely clogged with silt and eel grass, implying that the local ecosystem was much different than it is today. There has been some erosion at the site as nearly 200 artifacts were found on the beach below the site.

The artifact assemblages associated with these two sites are limited to collections from erosion surfaces and a single shovel test. Like the Moffet Phase, the technology is bifacial and composed of local basalts. Projectiles show somewhat more variability in size and shape than in the Moffet Phase and there are a great number oflarge, bifacially flaked tools. Several barbed projectiles were found at

Strawberry Point eroding from a large mussel midden. Both sites are located so as to take advantage ofouter coastal and bay resources, not near primary salmon resources.

71 Kinzerof Phase villages consist ofhouse depressions that range from 30 to 160 square meters of

floor area. Strawberry Point has the largest houses and the most variation in houses. At both sites the

houses are much larger than in the Moffet Phase. It was argued previously that this increase in house

size indicated the transition from single family houses to multi-family and corporate forms of

organization (Maschner and Hoffman 1994). We also argued that the variability in house floor area

seen at Strawberry Point may be indicative of differential corporate group size and thus the potential

for hereditary status differences (Hoffman and Maschner 1994; Maschner and Hoffman 1994; see

also Maschner 1991, 1992). At present, we do not have sufficient data to investigate this hypothesis.

".., • -- - .•. • •••.•••·~·I.·

.~ •• • .\ ..• • '----- ~..... • /• ------marsh ..

meters XCB-103 contours = 2m

FIGURE 9: Map ofXCB-I03, Dark Side ofthe Lagoon.

.~ 1 I j " ~ • Early Izembek Phase

Following a gap between 400 BC and AD 0 to 100, the region is covered with a density ofsites not seen in the previous 3000 years (Figure 6). An interesting aspect ofIzembek Phase villages is that we see the first extensive contacts with cultures to the east, especially the Bering Sea and upper Alaska

Peninsula. It should come as no surprise that these interactions occur during the time ofthe Norton

Tradition (early Eskimo) expansion into the eastern Bering Sea (Dumond 1988) and last through the expansion ofthe Western Thule Tradition after AD 1000. This interaction is seen in the presence of houses with tunnel or ramp entrances, a distinctly Eskimo phenomenon, in the midst ofoval Aleut style houses; the presence ofceramics, another distinctly Eskimo trait; and a number of finished ground slate tools. These houses and artifacts occur within Aleut villages and seem to be contemporaneous with the Aleuts living there.

The best investigated site from the Early Izembek Phase is XCB-005 along the central shore of

Izembek Lagoon (Figure 10). The sites consists of over 65 house and cache depressions in a small cluster on a point that partially faces the outer lagoon and partly a small lagoon that had a salmon stream at one time. The houses are smaller than in the Kinzerof Phase and more densely organized.

There is one larger depression on a hill above the site that may indicate a concern with defense.

Over 2000 artifacts and flaking debris have been recovered from the beach in from of the site. The assemblage includes an incredible variety ofprojectile forms including both bifacially flaked and ground slate points. There are items that seem to be indigenous to the lower peninsula, forms from the upper peninsula, Norton styles from the upper and eastern Bering Sea, and styles more reminiscent ofthe eastern and central Aleutians. There are a number ofrare, non-basalt material types including cherts and chalcedonies apparently from the upper Alaska Peninsula.

74 ,~ ~N

xes-Dos

t:: - 0 0 0) - • (\l • -I ~ Q) - .Q E • Q) • ~ •• • • •• • • -. :. • • • ... •• -. 411' _ •• ••• • • ....• -.•• • • ,--• • • •• .- 0 30 ~ i contours = 1m meters FIGURE 10. Map ofXCB-005. Late lzembek Phase

In the Late Izembek Phase the sites and the houses become somewhat larger, but not as large as the

largest in the Kinzerof Phase. They continue to be specifically associated with salmon streams. The

best known ofthe sites in the Late Izembek Phase XCB-003 (Figure 11) where, in 1971, McCartney

excavated a house constructed of 34 whale mandibles (1974). The artifacts from this excavation

included ceramics ofclear Bering Sea origin, and number ofground slate items and other artifacts

that indicate this house was occupied by peoples from the eastern Bering Sea, not the lower Alaska

Peninsula or eastern Aleutian region. A shovel test at the east end ofthe complex ofsites [lIst

investigated by McCartney and later the BIA ANCSA, produced a radiocarbon date ofthe same

range as the whale-bone house. XCB-121, is clearly defensive in nature and may be indicative of

these changing external relations (Figure 12).

This is the beginning ofthe time ofthe expansion of what has been termed the Western Thule

Tradition out ofBering Straits into the Bering Sea and ultimately the Alaska Peninsula and the

Kodiak Archipelago. This is a tradition that is seen as the technological, economic, and ceremonial

foundation of what today we call the Inupiaq, Yup'ik, and Alutiiq peoples (Dumond 1988). This

tradition is also decidedly not Aleut in origin or association and presents a dynamic view ofthe

Unangax - Yup'ik frontier zone.

-._.-._------~ -----_._._-_...... _--_.... XCB-003 o 30 ••• meters ~.. J. - .. -- .. - • ,. __ .'--"- • • • Unnamed Cove • •• • • •

-- .... - Unnamed Cove

I I

)i;>N .--.

FIGURE 11: XCB-003 (adapted from US BIA 1991:106-108).

, J f f !. t 1 .\

XCB-121

Izembek Lagoon

• I. • N A

30 oe--.- meters contours =1m

FIGURE 12: Map ofXCB-121 (adapted from US BIA 1991:109). Cape Glazenap Phase

After AD 1050 a radical change occurs in both the construction ofhouses and the organization and distribution ofvillages. We call this transition the Cape Glazenap Phase (Figure 13).

At historic contact, the Aleuts ofthe region lived in large communal houses consisting ofa main room (nucleus) for corporate activities and a number ofside rooms (satellites) that were used for storage, sleeping, equipment, and other functions (Hoffman 1995). These types ofhouses, which have been termed nucleus-satellite complexes, are ftrst occupied between AD 1050 and 1225. Two village sites have been dated to this phase, XCB-001 (Figure 14) and XCB-006. Both sites are positioned to take advantage ofboth salmon streams and outer-coastal resources. The artifact assemblages associated with the Cape Glazenap Phase are Aleut in origin and typical ofeastern

Aleut assemblages from late prehistoric times. These include scattered ground slate in a predominately bifacially chipped stone assemblage. The bone tools are typical ofAleut technology as are the scattered fragments ofart and adornment.

The houses are the most spectacular attribute ofthis phase as they are nearly four times the size of

Izembek Phase houses and have a completely different internal organization. It has been argued that this is the clear transition to multi-family corporate groups in this area and probably our fIrst evidence ofthe ranked societies described at historic contact (Hoffman and Maschner). The basis for this argument is that not only are the houses much larger, but that there is also much greater variability in floor areas indicating differential corporate group size. Differential corporate group size being one ofthe critical variables in the development ofhereditary inequality (Maschner 1991, 1992;

Maschner and Hoffman 1994).

79 N

A Cape Glazenap Phase • Big Lagoon Phase • Morzhovoi Phase t • Glazenap or Morzhovoi Phase

Amaklsland

Q o D

~_ .. !WI - o 10 20 30 kilometers

FIGURE 13. Map ofall sites dating to the Cape Glazenap, Big Lagoon, and Morzhovoi Phases. XCB-001 ••••• , • • ~# ' • ..•-1IJ'•.•••... - •• 1# •• •. ;'.~ : . . ...'r..'...". -.. -.' ~ ••• ,-• •• . •....• -I... •".., . ·,N·. '. -,-...." N ..• ';~..- flJit -._~$~'111 ....• fA. I .•• • ••••• , J.Q •••~

~ ... ~ - .~ .,.. o = possible house • , •

oe 30 meters contours = 1m

FIGURE 14. Map ofXCB-001 (adapted from US BIA 1991 :90).. One important characteristic of nucleus-satellite houses is in the location and distribution ofstorage

facilities. In the transition to these larger houses, many ofthe storage facilities become attached to the

house interior as the satellites (Maschner and Hoffman, inreview) and excavated into the house floor

(Hoffman 1996). This is a transition where corporate groups are controlling and protecting storage.

Brian Hoffman and I have argued previously that this transition from external storage to internal

storage may be an important aspect ofthe transition to hereditary status differences among hunters

and gatherers (Maschner and Hoffman, in review).

The earliest Cape Glazenap Phase village site is XCB-OOI, which was tested by McCartney in 1971

and had a single radiocarbon date ofapproximately AD 1100. Because it was unclear exactly where

this sample was collected, two dates collected by our project from a house floor inthis site were

AMS dated. Both fall within 25 years ofMcCartney's original date (Table 4). This site has over 200

depressions organized into 13 nucleus-satellite complexes (Figure 14). The total site area extends for

2 approximately 35,000 m • The site is located on an older beach ridge that is now over one kilometer

from the modern shore line.

Big Lagoon Phase

The Big Lagoon Phase (Figure 13) begins about AD 1225 and is marked by a 300 year

disappearance ofnucleus-satellite houses and the return to large round and oval houses with

unattached cache pits. Three dated sites fall into this phase, XCB-094 in Big Lagoon (Figure 15),

XCB-072 in Moffet Lagoon, and UNI-071 in Peterson Lagoon on Unimak Island. All three villages

are small and positioned to utilize both salmon resources and near coastal waters. Houses mapped at

2 ,~ XCB-094 and UNI-071 range from 40 to 70 m • Excavations conducted at both sites reveal an

internal hearth and external areas ofmussel midden. At XCB-094 a midden deposit was tested that

82 was dominated by mussel with dense quantities ofmigratory waterfowl, salmon, cod, and seal. The artifact assemblage, while substantially basalt, has large quantities of yellow chert and obsidian, materials that are rare at all other investigated sites.

Overall, this is the least known phase on the lower Alaska Peninsula and it is possible that it will be collapsed into either the Cape Glazenap or Morzhovoi Phases with more data.

83 old lake outlet

old pond •• XCB-094

old lagoon

• • o e:. • ~ I • meters A contours = 1m [] Excavation Unit N

FIGURE 15. Map ofXCB-094. Morzhovoi Phase

By AD 1550, there is a dramatic return to nucleus-satellite houses and large villages (Figure 13).

Three large villages are dated to the frrst 50 years ofthe 16th century and another five developed in the next 100 years. The houses are basically the same as in the Cape Glazenap Phase but the villages are different in three areas. First, there are extremely large villages such as Moffet Town (XCB-028) in Moffet Lagoon and Morzhovoi Village (XCB-004) in upper Middle Lagoon. Moffet Town covers

50,000 m2 hectares and has over 900 surface depressions including 20 nucleus-satellite complexes

2 while Morzhovoi Village has nearly 500 depressions, covers 40,000 m , and has 30 nucleus-satellite complexes. The second area ofdivergence is that the very large villages have numerous large house depressions that are not associated with nucleus-satellite houses, indicating either seasonality or time depth. The third area in which the Morzhovoi Phase is different than the Cape Glazenap Phase is the presence of many small villages with 1 to 5 nucleus-satellite houses that are not associated with salmon spawning stream systems. These are the only sites that are found on the outer coastal dune systems and must be less than 500 years old (Figure 16).

The type site for the Morzhovoi Phase is the Morzhovoi Village Site, XCB-004, which is one ofthe late prehistoric-early historic Morzhovoi Village locations. Historic documents indicate that this village was abandoned around AD 1808, although the location continued to be used as a seasonal fish camp until the 20th century (US BIA 1991 :126-127). At least 30 multi-room house depressions were recorded on this site. The house depressions here are huge with many over two meters deep.

One ofthe largest red salmon runs in the region occurs in a small stream that runs directly through the site.

85 .. 10-30 Nucleus-satellite houses .6 5-7 Nucleus-satellite houses • 1-3 Nucleus-satellite houses --J Key Salmon Spawning Drainages

Amaklsland

Q o o D

~-- o 10 20 30 kilometers

FIGURE 16. Map ofall sites with nucleus-satellite houses and showing major salmon stream drainages. InPeterson Lagoon on the north shore of Unimak Island, Brian Hoffinan has been excavating UNI

067, a large Morzhovoi Phase village. He has found that many ofthe artifacts in UNI-067 are exactly

the same as I found in the adjacent site of UNI-071, a Big Lagoon Phase village. This may indicate that the Big Lagoon and later Morzhovoi Phases are closely related aspects ofthe same regional

phenomenon, but why they have different house forms is as yet unclear.

There are a number ofother extremely large sites for which we do not as yet have any data. On the

east shore ofSwanson Lagoon is a village ofnucleus-satellite houses that covers two small hills. This

2 site, estimating from an aerial reconnaissance, has 300 - 400 depressions and covers 50,000 m •

Adamagan, located at the head of Big Lagoon, is another large site. During a briefvisit we recorded

5-7 nucleus-satellite complexes and numerous other depressions, with perhaps 400 in total. There are

also another 15 to 20 small villages from a number oftime periods for which we currently have no

dates. These sites will be investigated in future field seasons.

Trends in Settlement and Village Organization

The earliest known villages on the lower Alaska Peninsula date between 3500-1600 Be and are

associated with what we have termed the Moffet Phase. Villages and houses are small and occur as a

dense cluster ofhouses and cache depressions. These sites are situated on 12 to 16m escarpments, all

of which were probably next to a primary salmon harvesting streams during their occupation but had

easy access to the outer coastal waters as well. These villages were probably sedentary. This early

sedentism is a product ofthe redundant nature ofthe landscape removing any need for a mobile

strategy. I think it is critical to recognize that only one village site exists in each lagoon (Figure 6)

when ,there are numerous locations on the landscape suitable for settlement, and that these three

lagoons have by far the largest salmon runs.

87 Sometime after 1500 BC the Kinzerof Phase ushers in a period ofmuch larger villages, larger

houses, and greater variability in house size. Both ofthe sites that dominate this phase are in

locations that probably did not emphasize salmon harvesting but rather, had an emphasis on

intertidal and outer coastal resources. There are some similarities in house form with Port Moner, the

next large embayment up the Alaska Peninsula, and with the co-occurrence ofa rare form ofwhale

bone mask indicating, at the least, contact along the Bering Sea shore. The size ofthe houses may

indicate a transition to larger social units or corporate groups.

After a 500-600 hiatus inthe radiocarbon chronology, the Early Izembek Phase takes a rather

different tum from the Kinzerof Phase. There are a diversity ofsites and some variability in sites

types, including fish camps without apparent structures. Inthe beginning ofthe Izembek Phase

houses are small and again distributed in clusters rather than a long line along the shore. The artifacts

show contacts with the Aleutian Islands, the upper Alaska Peninsula, and the greater Bering Sea

region. There is evidence ofboth Bering Sea style houses and Aleut style houses, sometimes inthe

same village and, at least on spatial grounds, contemporaneous. The smaller houses at the beginning - ofthe Izembek Phase may indicate a return to smaller socio-economic units, perhaps at the family level. Inthe Late Izembek Phase the houses become larger and more complex. The villages are also

larger and there seems to be a continued reliance on salmon as the primary determinant ofsite

location.

A radical change in household and village organization occurs with the Cape Glazenap Phase. House

floors become as large or larger as they were inthe Kinzerof Phase 2000 years earlier but with the

addition ofattached rooms and storage facilities that often double the floor area ofthe household.

88 These sites are located on landscapes that provide access to both salmon resources and intertidal

outer coastal resources. Inboth village sites dated to this phase, all ofthe large house depressions are

part ofnucleus-satellite complexes.

Hoffman and I have argued that this is the transition to ranked corporate groups based on differential

corporate groups size as seen through house floor area Why this transition occurs is unclear and currently under investig

change may be a response to external political pressures, most notably the expansion ofthe Western

Thule tradition out ofthe Bering Sea onto the Alaska Peninsula and the North Pacific (Hoffman and

Maschner 1994; Maschner and Hoffman 1994, in review). As I have argued for the Northwest Coast,

and as seen in a number ofother areas (Lambert 1994), the formation larger socio-economic groups

and larger villages is often a response to warfare. Ithas been noted that the lower Alaska Peninsula

was, in early historic times, a critical frontier region between the Aleut ofthe Aleutians and the

Yup'ik ofthe Bering Sea (Maschner and Reedy, in review; McCartney 1974; Yesner 1985). This

certainly must have played a significant part in the formation ofthese larger coalitions.

After AD 1250, given the current data, an overall abandonment ofthe region is seen with only three

small sites known. The Big Lagoon Phase shows a return to houses without attached rooms and a

continuation of settlement on landforms that, like the Cape Glazenap Phase, are located to take

advantage ofouter coastal as well as salmon resources. We have no explanation, nor current

hypotheses, to interpret these changes and are pursuing more data. It is possible that when more of

the following Morzhovoi Phase villages are better dated and when we have a better understanding of

why the largest Morzhovoi Phase villages have both nucleus-satellite houses and single room

89 habitations, we may find that the Big Lagoon Phase can be collapsed into the Morzhovoi Phase. At

present, these two house forms are temporally segregated.

The Morzhovoi Phase is the last prehistoric time period identified for the lower Alaska Peninsula.

The hallmark of this phase is the return to large, nucleus-satellite houses and the formation of large - villages. The largest villages are located on the primary salmon streams while a number of smaller villages occur on a diversity of landscapes including, for the first time, outer coastal dune areas.

Unlike the Cape Glazenap Phase, Morzhovoi Phase nucleus-satellite houses exist in the same

villages as numerous houses without attached rooms. Some of these house depressions are similar

to both Big Lagoon and Izembek Phase houses and include a number of Yup'ik style forms from

the Bering Sea region.

The houses of the Cape Glazenap and Morzbovoi Phases are the same. They represent exact

representations of historic Aleut houses as described by Merck (1980), Veniaminov (1984) and

others. They occur across the lower Alaska Peninsula and Unimak Island. They are somewhat

different than houses east along the Pacific shore and different than the ones that occur further out - in the Aleutians (Veltre and McCartney 1988; Hoffman 1997).

- When investigated from a settlement perspective and divided by size, a visual assessment

demonstrates that there is only one large village at the east end of the survey area, one at the west,

and one in Swanson Lagoon on Unimak Island (Figure 16). It was recognized quite early in our

research that large or medium sized nucleus-satellite villages appeared to be associated with the

major salmon producing drainages. To assess the significance of this relationship, site area and

house floor area were plotted against modem data on salmon escapement for eight regions where

90 salmon data are available. The correlation between both site house floor area (~= .94) and overall site area (r2 =.88) are highly significant. Small villages with one to three ofthese houses do not share this relationship. It is possible that the largest villages controlled access to the salmon resources but equally likely that the largest resource patches attracted the largest number of corporate groups.

Important to this settlement study, especially in the context of salmon harvesting, is the recognition that there were probably both winter and summer house forms. Traditional practices in the Aleutian region had the entire corporate group sharing a residence in the winter and then dispersing to single family tents or smaller sod structures during the summer months. This is an important distinction as we may find that the Big Lagoon Phase villages, combined with the non nucleus-satellite houses in the Morzhovoi Phase villages, are simply summer occupations.

Conclusion

This is a preliminary view ofthe archaeology ofthe lower Alaska Peninsula. It is completely based on settlement organization, house form, and radiocarbon dates. At present we have few material remains that allow use to separate these phases, especially the early ones. But a few material-based observations are possible.

In the Moffet Phase, the presence of a minute polished slate end blade in a deposit clearly dated to

2500 Be is odd, although not totally unexpected. But it is also not similar to anything the authors have seen from the Ocean Bay Tradition, the only tradition in the region producing polished slate at this time.

Inthe Kinzarof Phase we have clearer contacts with sites up the peninsula, particularly from the

91 whale-bone mask found at Strawberry Point which is exactly the same as those from the Hot Springs site in Port Moller. Other artifacts look much like the earlier Aleutian Traditions.

The Early Izembek Phase has a number ofartifacts that are distinctly Norton in form. These artifacts are complete, indicating that someone what in an Aleut village using Norton end and side blades.

There are also the tips ofKachemak or similar ground slate harpoons, but no bases, indicating that the tips came in either on wounded sea mammals or perhaps wounded humans. By the Late Izembek

Phase we have pottery, a single whale-bone house, and a number ofother items from the eastern

Bering Sea. We begin to get a few non-projectile pieces ofpolished slate.

In the Cape Glazenap Phase we find for the first time a greater number of domestic items in Bering

Sea styles. These include ulus and knives of ground slate. No other substantial differences are seen until historic contact.

The one area ofinvestigation that is not described here is our integration ofthe regional settlement patterns with the climatological and glaciological data we currently have as well as with other data available for the northern hemisphere. This has not been done because we are waiting on a series of

AMS dates that are specifically oriented towards this issue. This topic will be a major focus of our published report in 1998. In general, our preliminary observations hint that there are significant correlations between gaps in our chronological sequence and changes in climate, storminess, and sea level (in various combinations).

92 INVESTIGATIONS AT PREVIOUSLY RECORDED ARCHAEOLOGICAL SITES

In 1979 a crew from the US Fish and Wildlife Service conducted an archaeological survey ofthe central Izembek Lagoon region. They visited or found over a dozen sites, conducted test excavations and surface collections, and completed the frrst broad survey ofthe region. The site descriptions presented for sites XCB-005, XCB-006, XCB-040 through XCB-056 are taken directly, with some editing from briefreports and field notes by Klingler and Yarborough with the addition ofmore recent data collected by these project. As the maps that were done were not to scale, all ofthe sites found by the 1979 survey have been mapped by our project.

Archaeologists working for the Bureau of Indian Affairs surveyed 16 sites in the Cold Bay area during the summer of 1988. These sites were selected by The Aleut Corporation under section

14(h)(l) ofthe Alaska Native Claims Settlement Act (ANCSA). This legislation allowed the regional corporations created under the act to select land which was considered ofhistorical importance. The BIA ANCSA archaeologists were required to survey the selected lands and gather information necessary to evaluate the site's significance. The criteria used in determining site significance follow those used for the National Registrar ofHistoric Places. An accurate site map depicting surface features, subsurface exposures, disturbance vegetation, and natural topography was the primary goal ofthe BIA archaeologists. The site maps and feature descriptions were made using tape and compass. Subsurface testing ofpreviously uninvestigated sites was undertaken whenever time permitted. Subsurface tests were generally limited to profiling of natural exposures or small test excavations. Site boundaries were established according to legal requirements ofthe

ANCSA legislation. Site boundaries included 360 foot buffer zones around all cultural features and anthropogenic vegetation. Sites were split into parcels whenever cultural remains were separated by

93 more than 720 feet or by a major topographical feature. Thus, the BIA ANCSA sites are often split

into parcels, which do not necessarily represent independent sites.

The results ofthe BIA field work in the Cold Bay area were published in an overview report ofthree

volumes (US BIA 1991). Two conference papers were also presented based substantially on the

results ofthis project (Cooper and Bartolini 1991; Hoffman 1990). The site descriptions from the

BIA Cold Bay overview are presented below for sites XCB-OOl, XCB-004, XCB-021, XCB-022,

XCB-023, XCB-024, XCB-025, XCB-026, XCB-027, XCB-028, XCB-029, andXCB-030. The

BIA crews combine XCB-003, XCB-031, and two other sites into a single application number, these

have been divided below into XCB-003, XCB-031, XCB-120, XCB-121 and XCB-123. Most ofthe

text is quoted directly from the overview report written by Joseph D. Bartolini, D. Randall Cooper,

Brian W Hoffman, and David P. Staley (US BIA 1991). AHRS numbers are substituted for the

ANCSA application numbers used in the BIA report. ANCSA parcels are referred to by separate site

- numbers whenever appropriate. Other minor editing and rewriting was done by Hoffman in order to

standardize the BIA descriptions with this report.

The remainder ofthe site data presented in this section is from AHRS files or from our 1995-1996

investigations.

XCB-OOI BIA ANCSA Site PN 38 (ELM AA 12257): SUMMARYofB/A ANCSA REPORT (B/A

/991:87-91 )

XCB-OOI is located near the head ofNorma Bay at the extreme southwestern end ofIzembek

Lagoon. The site is situated on the edge of a gently rolling uplands, about 1000 meters inland from

the present shoreline ofNorma Bay and 1000 meters inland from the Bering Sea Coast. The cultural

94 remains are concentrated around the tops and sides ofthree knolls and along a lower terrace (Figure

17). At the base of these knolls and the terrace, ancient beach ridges run north ofthe site towards

Cape Glazenap. Most ofthe site is covered with dense disturbance vegetation, which grades into the moist tundra vegetation found throughout the uplands. The beach ridges and surrounding lowlands are covered primarily by grasses and sedges with patches ofwet tundra.

McCartney and his crew investigated XCB 001 in 1971 (A McCartney 1974:61 64). They found approximately 125 depressions and tested two areas ofthe site. Only one test produced cultural materials. It was a 4x4 meter unit that exposed approximately one-third ofa semisubterranean dwelling interior. The feature in which this test was excavated was thought to be a temporary sod structure or tent, rather than a permanent structure (A McCartney 1974:62). Inthe fill above the structure, the excavators found numerous small boulders and a few whale bone fragments. From the - floor area, they recovered nearly 1000 artifacts, primarily lithic tools and debitage. Two charcoal samples (SI 919 and SI 920) were submitted from this test for radiocarbon analysis and produced dates of905 + 50 BP and 925 + 95 BP, respectively (A McCartney 1974:64).

The BIA-ANCSA archaeologists surveyed XCB-OOlon the 28 and 29 July. They identified 199 cultural depressions, including at least 5 nucleus depressions with 33 associated satellite depressions.

Of the remaining 154 features, 123 (80 percent) were 4.0 m or greater in length and are believed to be the remains of dwellings (Figure 17). Artifact and faunal remains noted during the BIA survey included bird, whale and fish bone, mussel and clam shell, flaking debris and fIfe stained rock These materials were generally observed inrodent or bear disturbances.

95 XCB-001 ,.. •• , • II # ' • ...•"'•.~ ., • •eA.-• •• • •. .~.~ . . ,~.; •• _.t ~ ••~ ....,.. •. e.,-...• e.·. el· •••• ~,N._·.·~,. '. ~- .. N ., '.)e • • • A .-I ;-:...•• •- •••••. ~ . ~Q ....~ .... - .~....,.. • • o =possible house ,

oe 30 meters contours = 1m

FIGURE 17. Map ofXCB-OOl (adapted from US BIA 1991:90).. In 1996 two crew members from the University ofWisconsin visited this site to collect further

samples for radiocarbon dating. As it was unclear whether McCartney's dated samples came from the house floor of a nucleus-satellite depression, we wanted another date as, because of McCartney's

dates, this site had the earliest expression ofthese house types in the region. A single .50x.50 meter test unit was dug in the floor ofa large house depression on the south end ofthe site. A clear roof-fall

zone was encountered followed by an obvious, carbon-stained floor covered in whale-bone. Charcoal

samples were collected from both the floor and the roof and were AMS dated at Lawrence Livermore

Laboratory. The dates are 840+/-50 (CAMS 30615) and 790 +/- 60 (CAMS 30608). Calibrated, these dates are very close to the original two dates. When compared with McCartney's dates, this site

now has a ftrmly dated calibrated range between AD 1110 and AD 1165.

XCB-002 BIA ANCSA Site PN 39 (ELM AA 12258): SUMMARYofBfA ANCSA REPORT (BfA

1991:92-98)

XCB-002 is located along the southeastern shore of Norma Bay, on an 8-10 meter high narrow terrace or ridge that is an extension ofthe glacially derived coastal plain The terrace edge follows the shoreline ofthe bay from southeast to northwest, then curves almost due west along an apparent ancient shoreline. A 150 meter wide lowland ofwet tundra and ponds splits the site into a western and eastern ridge. North ofthe terrace is an expansive area less than 2 m high and vegetated almost exclusively by lush grasses. Several low subtle ridges, marked primarily by cow parsnip, project northwesterly from the terrace edge into the grassy flatlands. These subtle ridges are perhaps beach ridges associated with the ancient shoreline. Lush grasses grow north ofthe site in the lowlands, on the flanks of the terrace edge and especially thickly along the shoreline. Much ofthe terrace is covered by mixed species ofon disturbance vegetation, also called "anthropogeneous meadow" (N.

McCartney 1976:340). A portion ofthe site on the northeastern corner ofthe terrace is covered by an

97 oval, 30 x 50 meter, area oflush grasses. All areas ofhigher ground, other than the site area, are

vegetated by moist tundra with patches ofdwarf willow.

McCartney tested this site in 1971, excavating a 4x4 meter area (McCartney 1974:62). The BIA

- ANCSA archaeologists mapped a 5x4 meter rectangular area ofdisturbance, which they believed to

be the remains ofMcCartney's test (Figure 18). An absence ofstructural remains led McCartney to

conclude that his test was located in an area between dwellings (McCartney 1974:62). The

- excavation produced faunal remains (shell and bone) and 227 artifacts, including a pottery sherd ,

notched net sinkers, a stone lamplbowl, slate beads, ground stone adzes, and chipped stone knives

and projectile points (McCartney 1974:Table 2). These artifacts indicate a range ofdomestic and

subsistence activities typical of a main village or base camp. A radiocarbon sample (SI 921) from the - excavation produced an uncorrected date of760 + 90 BP. McCartney characterized the entire site as having 18 to 20 dwelling depressions.

BIA ANCSA archaeologists investigated XCB-002 on 27 July 1988. They identified 73 cultural

features clustered on both the western and eastern ridges, which they believed represented an

estimated 34 former dwellings (US BIA 1991 :97). The feature total included McCartney's test and

eleven satellite depressions associated with two nucleus depressions. Both the western and eastern ,.... ridges had a single nucleus-satellite complex. The remainder ofthe probable dwellings were oval

shaped depressions. Rodent disturbances revealed mussel, clam and cockle shells on the ground

surface.

- 98 N XCB-002 ., Norma Bay o 30 stream -----'------N i ------""'" A meters ",-' ,,- // / I ,I grass grass I I I I lower terrace edge I I I upper terrace edg!...,...-.,.--:----"....-__ lerrare .. :\ .... - "" - \ \ 'Pi ",ge. f" \ . .. - . ~...... , disturbance. vegetation sedges

sedge

Figure 18: Map ofXCB-002 (adapted from US BIA 1991:95-96).

, .~ 1 I. ~ I XCB-003: SUMMARY orBIA ANCSA REPORT(RIA 1991:99-125)

The BIA mapped this area as a complex of six sites (parcels A through F; Site PN 41/PN 42 (BLN

AA 12259/AA 1226) which included XCB-003 and XCB-031. We have divided these six parcels

into five sites - XCB-003, XCB-031, XCB-120, XCB-121, and XCB-123 based on their location

and the distance between them.

XCB-003 is located 9km south-southeast of Cape Glazenap, in an unnamed cove in the southern

portion of Izembek Lagoon, just southwest of Applegate Cove. The cove is very shallow and

muddy with few channels. The air is foul smelling at low tide indicating organic rot and methane

production. The cove is fed by three major streams, the westernmost of which supports the largest

run of salmon.

XCB-003 is located north of the westernmost stream in the cove. The site lies on the cove's

western shore and the stream forms its southern boundary. The site is situated on a point of land

and an adjoining projecting peninsula. The mainland portion has an elevation ranging from 2 m to

12 m above the present shoreline. The peninsula is connected to the mainland point on a low flat

sedge covered isthmus less than 2 m in elevation (Figure 19). The peninsula is vegetated by a cow

parsnip dominated on site community. The majority ofthe site is covered with moist tundra with a

sparse growth of scattered cow parsnip.

A 1971 archeological crew led by Allen McCartney (1974) worked primarily at XCB-003, which

was designated IZM 3 . However, three other site localities, visible from the site were reported. - The area McCartney's crew focused on was described as consisting of approximately 19 scattered depressions, generally located from 5 a to 8 a above sea level. The crew tested one depression and

completely excavated another dwelling (A. McCartney 1974:59-84).

100 XCB-003 a 30 ••• • meters •.. -I • ~ .... I . . I .I. -----.. •• • • ... ---- terr~edge....!-- • • • • Unnamed Cove • • •• • , • • ,

-- .. -- Unnamed Cove

I I

»-N . --. FIGURE 19: XCB-003 (adapted from US BIA 1991:106-108).

~ I t .~ , , 1 "House I" was completely excavated within a 10.0 n x 10.0 m area (A. McCartney 1974:65 70). The

superstructure ofthis regionally unique house was constructed of approximately 34 whale mandibles

and other bones Approximately 1000 boulders were used for the foundation ofthe nearly round

house, 6.0 m x 9 P0 m. Features in the floor included a central rock encircled circular hearth and two

storage pits. A charcoal deposit on the floor was 0.40 m thick, and 25 thin compact floor levels were - reported. The house was apparently built in a previously occupied area. Approximately 10,350 artifacts and fragments were recovered including flaked stone, ground stone, pecked and carved

stone, ceramics, bone tools and faunal remains. The house yielded two radiocarbon dates: a charcoal

sample (SI 916) was dated to 1005 + 105 BP, and wood sample (S1 917) was dated to 390 + 95 BP

(A. McCartney 1974:64). 6 McCartney (1974:60) suggests the site location is in Applegate Cove,

which is incorrect according to published VSGS topographical maps ofthis area. "House 2," a 7.5m

x 7.0m depression, was tested with a 2.0m x 70m trench excavated to a depth of 1.2m (A.

McCartney 1974:62). Small boulders and several whale bone fragments were recovered in the

excavations. Over 1000 artifacts, fragments and chipped stone debitage were uncovered during the

test. A whale bone sample (S1 918) produced a radiocarbon age of 1235 + 105 years BP (A.

McCartney 1974:64).

Nancy McCartney (1976) performed an analysis ofthe effects ofprehistoric occupants upon the soils

and vegetation of a site. A portion ofher data base was derived from eight botanical transects at

Parcel F (N. McCartney 1976: 298 300). Additionally, she collected plants and described nine soil

profiles. Chemical and physical analysis ofthe sediments were run on seven samples.

102

------...... -- Chipped stone tools and debitage, fIre cracked rock, charcoal, shell and faunal remains were scattered across the site at various locations. As with the depressions, however, all ofthe artifacts are situated on a prominent, 10m to 15m high ridge adjacent to the cove.

Artifacts exposed on the surface included many fIne grained black basalt flakes, stone net sinkers with flaked notches, a basalt chipped stone knife, a basalt projectile point base, shell, burned bone, worked antler, whale bone fragments, fIre cracked rock and charcoal. All were observed in sediments disturbed by rodents or' bears.

XCB-004, BIA ANCSA Site PN 43 (ELM AA 12261): SUMMARY orBIA ANeSA REPORTfBIA

1991:126-134)

XCB-004 is located at the north end of an unnamed lagoon, which connects with Morzhovoi Bay. A short stream which flows into the lagoon, bisects the site and drains a large nearby lake. This lake stretches northward nearly to the Bering Sea. XCB-025 sits on a high terrace at the north end ofthe lake approximately 4 km away. The location ofXCB-004 is situated midway between the PacifIc

Ocean and the Bering Sea, with water routes providing easy access to both.

Cultural features are located on a terrace with gently rolling terrain roughly 3 to 8 meters above the lagoon. Disturbance vegetation, mainly grassy areas and patches ofcow parsnip, is associated with the features. Dense raspberry patches line the terrace edge near the lagoon, and elderberry is common across the site. Surrounding vegetation is mostly mosses and sedge. The site's integrity is excellent.

Other than slight bear disturbance and a short stretch of eroding cutbank, the site appeared undisturbed in 1988.

103 XCB-004, Morzhovoi Village, was one ofthe main villages on the lower Alaska Peninsula occupied

into the historic period. According to Father Veniaminov, a Russian Orthodox priest who lived in the

Aleutians between 1824 and 1834, Morzhovoi village was moved three times between the mid-1700s .- and the mid-1800s (Veniaminov 1984:119-120). Morzhovoi village was located on the eastern shore ofBechevin Bay around the time ofinitial contact with the Russians. The village was moved

to XCB-004 near the end ofthe 18th Century, where it remained until around 1808, when the village

was again moved to the vicinity ofXCB-024 in Hook Bay. Joe Bartolini performed a low-level

helicopter survey ofthe eastern shore ofBechevin Bay in July 1988 while with the BIA ANCSA

project. He identified three sites including one which he believed to be the initial contact period

village, and one which he believed to be the post-1808 village, which is not XCB-024 (US BIA

I~ 1991:189). - Ofthe village at XCB-004, Father Veniaminov wrote: "Into the stream flowing from the lake and

discharging into the narrow arm ofsouthern Morzhekoi zaliv [Morzhovoi Bay] enter a great number

ofred salmon which begin to run here from the middle ofAugust and continue even until December.

In 1832 there were so extraordinarily many fish here that the entire stream was so chock full that fish

no longer were able to turn, and it was possible to catch them by hand" (1984:119).

As apparent from the above quote, XCB-004 continued to be used at least as a summer fish camp

..- even after 1808 (US BIA 1991 :127). Archaeological remains observed eroding from the site in 1988

and in 1996 (see below) also suggest a precontact component exists at the site (US BIA 1991 :128).

BIA ANCSA archaeologists identified XCB-004 on 20 July 1988. They returned to map and test the

site from the 6th to the 11 th ofAugust, 1988. They identified 487 depressions, which occur in dense

104 concentrations throughout much ofthe site (Figure 20). Two hundred twenty three ofthe depressions belong to nucleus satellite house complexes, with 30 nucleus depressions and 193 associated satellite depressions. Two other complex features were also found. Both ofthese features consisted ofthree or four aligned rectangular depressions. These linear structures appear to be ofRussian construction.

One was tested and produced historic artifacts (See below). Ofthe remaining features, 239 were described as isolated/independent depressions and 93 were considered to be simple house pits, based on size. Altogether, the remains ofup to 156 former dwellings are represented at the site.

Subsurface remains were noted in a small section ofcutbank by the creek, and cultural material was recovered in a test excavation (Test Pit 1) in Feature 264, one ofthe linear house complexes.

Material in the cutbank included shell, fIre cracked rock, grooved and snapped bird bone, large mammal bone, and charcoal. The test was a 50 cm X 50 cm square unit excavated in 10 cm arbitrary levels. All dirt was screened through 1/4 in. mesh. Materials collected from the test excavation consisted ofbasalt flakes, large mammal bone, wood, small pieces of copper, blue, white and orange glass beads and charcoal. Though the charcoal sample (Beta 29388) has been radiocarbon dated to

1500 +1- 150 years BP, beads found beneath it are thought to date no earlier than the protohistoric period. -

XCB-004 was visited on two occasions in July 1996 by the crew members from the University of

Wisconsin. A number oferosion surfaces were investigated along the creek that flows through the middle ofthe site. Discontinuous deposits nearly 1.3 meters deep were found in a number of areas.

Many ofthe deeper deposits were far below the historic house floors indicating a pre-contact age.

105 - • \ I I } 1 r ,

XCB-004 -"--"--"--"--"--"--"--"--" o 30 i V PS*.- N . meters ~~·]llit····a...... ~ ,- I • ~'.' I ":<.~~.'.. ..~ ··~···S~~...: "" •.•• ~ grass' • • 'cowparsnlp ••.•.• ~ / ' I , ~.: , II , ~~ ...... •.. :,, '. .''.'~.... ' .... ;tI'...... :grass • •••• •• .~. , ~ :~". ••.~...... ·e '.I :- e , ••e...,.: •

XCB-005 is located on the south side of the entrance to a fairly large secondary lagoon within the

Izembek Lagoon system Island. The portion of the site facing Izembek runs roughly north south.

The shore rises from the site's north limit where it is bordered by the narrow lagoon outlet, to a narrow ridge approximately 15m above the beach. Eastward from the beach, the northern portion of the site falls slightly into a rolling topography. The slope is more pronounced from the narrow ridge east. Housepits front both Izembek Lagoon and the entrance channel to the secondary lagoon, with the largest cluster being where the two shores meet (Klingler n.d.).

Vegetation. present at the site includes wild celery (Heracleum lanatum, Anoelica lucida,

Lingusticum hultenii) fireweed (Epilobillm angustifollum), arctic dock (Rumex arcticus), siberian spring beauty (Claytonia sibirica), wild geranium (G. erianthum), buttercup (Ranunculus spp.) and - avens (Geum spp.). From the amount of material on the beach, it appears that the western and northern margins of the site are much eroded. The USFWS crew recovered anifacs from the beach and from where the bluff is slumping along Izembek Lagoon (Klingler n.d.).

Between 1994 and 1996, XCB-005 was visited on five different occasions by the University of

Wisconsin. The site was mapped (Figure 21), two small test units were done. and the anifacts on the beach were collected. Over 3000 surface artifacts have been collected from this site. Three charcoal samples have been dated, one a conventional date, two AMS dates. These dates range from AD 150 to AD 450 (calibrated, see Table 4).

107

lin ~N

xes-Dos

t:: - 0 0 0) - • (tJ • -.J ~ (l) - .Q E • (l) .- • •• • -t:! ... \\ ~ :.~ • • • • •• • ....- ... .- .- ..", ...... -.•. • • ,-- • • •• . - o 30 ~."~~I contours 1m meters = FIGURE 21. Map ofXCB-005. XCB-006 (quoted with revisions and additions from Klingler n.d.)

This is a well defined site located on the eastern side of the entrance to the extensive "outer marker" secondary lagoon, within the Izembek Lagoon system. A major channel of Izembek

Lagoon swings northeast from the outlet, approximately 50m. offshore. From the site the shore of the entrance runs roughly north south, The site sits atop a bluff, at a height ranging from 4m. above the beach at the southern site margin to 8m. high where the bluff turns toward the northeast.

The land rises further to the northeast along the shore and south away from the lagoon. A natural drainage feature, trending northeast from the bluff, separates the southernmost house pit from the remainder. This gully also forms the eastern limit of the southern portion of the site. (Klingler n.d.)

The site is densely vegetated by wild celery (Umbelliferae), siberian spring beauty (Claytonia

Sibirica), wild geranium (Geranium Erianthum), nootka lupine (Lupinus Nootkatensis), and fireweed (Epilobium spp.) along the southeast side of the site the rise is vegetated by grasses, sedges (Carex spp.), horesetail (Equisetum Arvense), with scattered stands of wild celery

(Umbelliferae). The abrupt vegetation change is enhanced by the better drained and enriched soils of the site area, This is suggested by the absence of sedge (Carex spp.), which is a swamp plant, and by the presence of dense stands of nitrogen and phosphate plants, such as wild celery

(Umbelliferae) and siberian spring beauty (Claytonia Sibirica), on the site. Within depressions were found villow (Salix spp.), horsetail (Equisetum Arvense), wild celery (Heracleum Lanatum and Angelica Lucida), nootka lupine (Lupinus Nootkatensis), and siberian spring beauty

(Claytonia Sibirica), On the surrounding rims were found wild celery (Angelica Lucida), fireweed

(Epilobium spp.), siberian spring beauty (Claytonia Sibirica), buttercup (Ranunculus spp.), and wild geranium (Geranium erianthum). Erosion is not as evident as at XCB 005, with fewer artifacts on the beach. A one meter wide bankcut was placed in the second depression from the

109 south, the western end of which had been cut by erosion along the bluff. Other than the distinction

between the sod and the underlying reddish brown silt, there appears to be no stratigraphy, A rock

feature, possibly a structural remnant, extended out ofthe face of the cut. The test was dug to a

depth of58 em. (Klingler n.d.)

This site was visited by the University of Wisconsin in 1995 and 1996. The site was mapped and

shown to have at least four nucleus-satellite depressions (perhaps six) with rather unusual satellites

- (Figure 22). In total, there are 40 depressions at this site. A charcoal sample collected by the

USFWS in 1979 was AMS dated to AD 1145 (calibrated, see Table 4). Only a few artifacts were

found on the beach. -

110 -

xeS-006

•••• • .-.. • • • •• •

o 30 • ~ I I meters • contours =1m

FIGURE 22. Map ofXCB-006. XCB-02l BIA ANCSA Site PN 95CBLM AA 12271): SUMMARY orBIA ANCSA REPORT(BIA

1991:172-177)

XCB-02l is located along the western shore ofKinzarof Lagoon at the head of Cold Bay,

approximately 6.6 km northeast ofthe community ofCold Bay. Itis situated at the tenninus ofa low

ridge, approximately 3.0m above the beach. Kinzarof Lagoon is a small shallow water embayment

separated from Cold Bay by dune grass covered barrier sand spits and bars. Outlets through the

barriers are situated directly across from the sit. There is deep water inthe lagoon at the outlets and

the adjacent inner shoreline. At low tide, however, much ofthe lagoon floor is exposed. Above the - mean high tide line along the western shoreline ofthe lagoon, barnacle encrusted boulders and cobbles cover a sandy beach. Below the tide line, bleached shells of clams and blue mussels litter the

exposed sandy beach. The shoreline of Kinzarof Lagoon is covered with flotsam. Most prominent are

long massive creosote treated poles and timbers, probably from old wharves formerly located along

the shores ofCold Bay. A large metal fuel storage tank has also drifted into the lagoon.

A lush anthropogeneous meadow, dominated by cow parsnip, delimits the slightly raised

occupational mound at the site. The occupational mound is situated on the tenninus of a low ridge

that trends from the northwest to the southeast. North ofthe ridge crest, the terrain drops slightly into

a wide swale. Both the ridge crest and the swale are carpeted by moist tundra. According to Nancy

McCartney (1976:615), who visited the site in the summer of 1971, the heath vegetation was greatly

damaged by a ftre about three years earlier. When she was there, most ofthe burnt area remained

bare ofvegetation except for scattered frreweed and dwarf willows. Seventeen years later there was

no noticeable evidence of a frre. A perennial stream runs alongside the western base ofthe ridge.

Although the stream did not appear to be large enough to support a salmon run, salmon were noted

jumping in the lagoon at the time ofthe 1988 BIA investigation. Approximately 50 m above the

- 112 mouth ofthe stream, on the northern bank, is a lone conifer that was apparently planted by U.S. military personeL Extending southwest from the stream is a low lying terrace covered by wet tundra.

Numerous seeps are present along the edge ofthe terrace southwest ofthe stream. Natural erosion is occurring on the upper bluff slope below the occupational mound.

BIA ANCSA archaeologists surveyedXCB-02l on 5 July 1988. They identified a total of 65 cultural features. All but three features are located on a slightly elevated occupational mound measuring roughly 100 m by 60m. Sixty one features are the remnants of semisubterranean structures, nineteen ofwhich were probable houses (Figure 24). More than half the semisubterranean features are associated with seven nucleus satellite complexes. Three ofthe remaining four features are the remains of historic wood framed structures, probably trapper's cabins built during the 1920s and 1930s. The cabins were occupied by military personnel and others for recreational purposes both during and after WW n according to people interviewed by the BIA. The fire that passed through this site in the late 1960s apparently destroyed the structures. The remaning feature appears to be a 19th century trappers's cabin, based on its method ofconstruction (i.e. sod berms, entrance room). A bluff exposure east ofthe occupation mound revealed a 10 em thick lens of charcoal beneath the sod mat and above a probable paleosol lens. Fire cracked rock, shell and basalt lithic debris were also observed in this exposure. Bird bones, fire cracked rocks, lumps of coal, rusted metal fragments and milled lumber were noted eroding from the occupational mound in 1988. No erosion ofthe occupation mound, however, was observed in 1995.

Hoffman and a crew of UW Madison students returned to XCB-02l in early July 1995. Six lxlm units were excavated in two ofthe nucleus-satellite features in order to assess the research potential ofthis site (Hoffman 1995). Both houses had very thin, indistinct floors. Initially it was

113 - hypothesized that the thin floors indicated the connnunal houses were abandoned after a short occupation (Hoffman 1995). Based on data from excavations on Unimak: Island, Hoffman has more

recently suggested the connnunal house floors were occasionally cleaned by scraping up the organic

rich floor layer and discarding this material outside ofthe houses (Hoffman 1997a, 1997b). 'This

house-cleaning behavior may also explain the archaeological record at XCB-021. A small hearth and

several subfloor pits were encountered in the house excavations. These features were fine screened

and floated. Seeds were recovered from the hearth and one pit feature. Quarter-inch screening was .- used for the rest ofthe excavations. Artifacts recovered from the house floors included an obsidian - projectile point, two ground stone adzes, and a small amount oflithic debitage and other artifacts. Iron and glass fragments were found in the fill above the houses. One small glass bead recovered

- from feature fill was the only historic artifact found inside the houses. -

114 -

------./ / ~,fh ~N ~,(lj /ldf / / / / /' /' / / # ', disturbance vegetation • .. " ~\ •• • ~wet tundra ~. .. . ~I.• ..

• XCB-021 ~I " or-..-_- 30, meters

FIGURE 23: Map ofXCB-021 (adapted from US BIA 1991:175), XCB-022 (the Bricker Site)

This site is located on a 16-20 meter terrace facing Cold Bay on the south site ofthe mouth of

Russell Creek. The site was report but not described in the AHRS files prior to 1996 when it was - visited and mapped by the University ofWisconsin.

The site consists of59 depressions scattered along the highest portion ofthe terrace (Figure 24).

Several ofthese depressions are either ofmilitary origins or have been highly disturbed by military

activity. Most are small and oval. There is lush vegetation along the top ofthe terrace. A number of

basalt flakes were found on an adjacent erosion surface. Although no further investigations have been

done, sites located on these landforms generally date to before 1000 Be. -

-- - -

116 - XCB-022

••______• • e' • • ••••. .. .. • • .• ~..•. •. ••,.e.. •.e- · · •

Russell Creek 30 meters N~ ...... -,.-

opiII_. 30 Cold Bay shoreline W. I meters 600 meters t contours = 2m = depression with military remains

FIGURE 22. Map ofXCB-022, The Bricker Site.

) I I I , II , 1 ~ XCB-023 BIA ANCSA Site PN 37 (BLM AA 12256): SUMMARYorBIA ANCSA REPORT(RIA

1991:126-134)

XCB-023 is located on the northeast shore of an unnamed cove in Izembek Lagoon, approximately

1.5 km due south ofthe tip of Cape Glazenap. The topography surrounding the site is fairly

complicated with prominent ridges and steeply rolling hillocks, some rising up to 50 m above sea.

The cultural features are on relatively level shoreline terrace situated between two ridges (Figure 25). - The cape southwest ofthe site consists of a series of ancient beach ridges and dunes less than 10m above sea level. Accretion ofeolian sand is occurring at a rapid rate over much of the site. A narrow

point ofland extends 75 m from the southeast comer ofthe site into the lagoon. Cultural material

was found eroding from both sides ofthe point. The entire site area is covered with dense moist ,.... tundra vegetation. The lagoon near the site is shallow with a muddy bottom. Numcrous shellfish live

in the area including limpets, razor clans and blue mussels. Amak Island, a kno....ll sca lion and

walrus haul out, is 20 km north in the Bering Sea. XCB-023 is the nearest ofthe laglxm sites to this

resource.

McCartney briefly inspected the site in 1971 and described it simply as a "small eroding site"

(McCartney 1973:9, Map 19; 1974:62). BIAANCSA archaeologists surveyed XCB-021 on 22 July

1988. They encountered dense, chest high vegetation. The surface features wcrc almost unnoticed in

the first walk-over. It was not until after the vegetation was tramped down that thc dcpressions were

easily identified. Aerial photographs ofthe site were taken by BIA Archeologist Stalcy on 30 July

1988.

- The cultural remains at XCB-021 reported by the BIA included surface depressions and stratified subsurface deposits of shell, bone and artifacts exposed in eroded sections ofthe shoreline.

118 - Additional artifacts 'were found on the beach surrounding the site; they apparently had washed out of the shoreline. Twenty-six cultural depressions were identified: 4 nucleus features (2 of which were very indistinct), 21 satellites and 1 isolated/independent depression. Discontinuous subsurface deposits were observed along two stretches of shoreline: one on the north side ofthe point; the other along the south ofthe point. Indistinct nucleus-satellite house complexes were adjacent both deposits. Lenses ofshell with smaller amounts ofbone, charcoal and artifacts were noted. A section ofthe southern exposure was profiled and photographed (Figure 26). The profile had three thick lenses ofshell midden, the deepest lens about 60 cm below the surface. A charcoal sample and chipped stone tool were collected from the middle lens at approximately 48 cm below the surface.

The charcoal sample (Beta 29382) was radiocarbon dated at 330 + 100 BP.

The collected tool is stemmed with prominent shoulders. It was made from a fine grained igneous rock, probably basalt or andesite, and most likely functioned as a knife. Artifacts on the beach included tools and manufacturing debris ofchipped stone, ground stone, ivory, and antler. Among the tools observed, were three ground slate ulu or knife blades, a possible chipped stone burin of basalt, and an ivory labret. The faunal remains included fragments of a walrus skull, a large whale jawbone (probably gray whale), and a beluga skull.

119 XCB-023 N o 30 ~i..• i meters A

- ••

_.. _- .. -_.,--

Izembek Lagoon -

FIGURE 25: Map ofXCB-023 (adapted from US BIA 1991:82).

- oem 20 40 60 oem

10YR 1/2 black silt sand with abundant grass and roots. 20

Mixed midden debris: blue mussel, razor dams, beach pebbles and large mammal bone.

10 YR Black medium coarse sand. 40 Mixed midden debris: blue mussel, razor clams, beach pebbles, large mammal bone, fish, and a walrus skull fragment. Charoal collected. 10 YR Black medium coarse sand. Mixed midden debris: blue mussel, razor clams, beach pebbles and large mammal bone. .~.

60 10 YR 212 coarse black sand with silt.

FlGURE 26: Profile at XCB-023 erosion cut (adapted from US BIA 1991:84). ..,,,' XCB-024 Hook Bay Village. BIA ANCSA Site PN 99 caLM AA 12274): SUMMARY ofBIA

ANCSA REPORT (BIA 1991:188-196)

XCB-024 is located in the extreme northeastern corner of Bechevin Bay, at the head ofa narrow

unnamed embayment formed by the mainland and a long grass covered barrier spit. Most ofthe

cultural features are positioned along the edge of an abandoned and elevated coastline. This former

coastline rises approximately 8 to 10 meters above a low, grass carpeted series of curvilinear beach

ridges. Deeply incised swales isolate segments ofsite terrace into knolls. The front sides ofthe

knolls slope sharply down to the lower beach ridges. Vegetation typical of an anthropogeneous - meadow, such as dune grass, fITeweed and cow parsnip, highlight the knolls where the majority ofthe cUltural remains ofthe site are located. Sedimentation at the head ofthe embayment has resulted in a

shallow water depth. Flotsam and dense mats ofrotting eelgrass cover the shoreline along the

northern edge ofthe embayment at its head. There was no evidence offlowing water in the immediate

site vicinity, although the many ponds surrounding the site provide a source offresh water.

BIA archaeologists recorded a total of79 cultural features at this site (Figure 27). Two features small

pits were found at the base ofthe terrace atop a beach ridge. The remaining features were clustered

on four knolls on the upper terrace. Over two thirds ofthe features found at the site are associated

with seven nucleus satellite complexes. Three other depression have long axes of at least 4.0 meters

and are therefore believed to represent dwellings. The site is marred by numerous surface exposures - caused by burrowing rodents and by bears excavating massive amounts ofsoil, probably in pursuit of the rodents. Cultural materials consisting ofshell, fITe cracked rock charcoal and bone fragments

were noted in several subsurface exposures.

122 • .'" . disturbance .... vegetation 7H' ...... meters

grass

...... •

grass

..... disturbance···· =--. .vegetation f'a : ,.-

• • ~•exposure. , I ... - 1 ...... ••" ••••••• •i~:;:;••••••• ' _•• •

wet tundra

, ._~~ . • ~ "'~-" ~N ...... disturbance .., vegetation

FIGURE 27: Map ofXCB-024 (adapted from US BIA 1991:192-195).

~; BIA archaeologist Joseph Bartolini (US BIA 1991 :188-189), noted that XCB-024 shares some

characteristics with the post-1808 Morzhovoi village described by Father Veniaminov, including its

location "at the head ofthe fIrst northern bay" on the northwest tip ofthe Alaska Peninsula

(Veniaminov 1984:119). The seven "yurtas" (native houses) noted at Morzhovoi by Veniaminov

(1984:119) also coincide with the number ofcommunal houses documented by the BIA at XCB-024.

Bartolini notes, however, that dwellings built after 1805 were suppose to be smaller, single family

structures according to a Russian American Company directive (Veniaminov 1984:264). Bartolini

observed a small site farther to the southewest ofXCB-024 during a low level helicopter

,.... reconnaissance which he believes better fIts the location and description ofthe post-1808 Morzhovoi

village described by Veniaminov (US BIA 1991:189).

- XCB-025 BIA ANCSA Site PN 97 (ELM AA 12273): SUMMARYorBIA ANCSA REPORT(BIA 1991:182-187)

XCB-025 is located on a high terrace along the northwest shore of a large unnamed lake (Morzhovoi

Lake) about 300 meter inland from the Bering Sea. The lake is separated from the Bering Sea by

massive beach dunes roughly 10 meters high and 40 meters wide. The outlet ofthe lake, about 4

kilometers to the south, flows through old Morzhovoi Village (XCB-004) and into Middle Lagoon.

The site is covered by dense disturbance grasses, fringed by cow parsnip and surrounded by moist

tundra vegetation. Waterfowl and the tracks ofbear, fox, wolf and caribou were observed around the

lake. The site appears to be completely undisturbed.

BIA archaeologists identifIed 60 cultural depressions at XCB-025, 45 of which are associated with 5 - nucleus/satellite features (Figure 28). Ofthe 15 depressions not directly associated with these complexes, 2 measured more than 4 meters in maximum dimension and probably represent

124 dwellings; the functions ofthe remaining depressions are unknown. Altogether, the remains of 13 probable dwellings are present at the site. The BIA survey ofthe site was on 23 July. Aerial photographs were taken on 30 July. The site was returned to on 11 August and two 50 x 50 em test pits were excavated. Test pit 1 (TP 1) was dug into the nucleus depression of a house complex, and

TP 2 was excavated into a connected satellite depression. Both tests were excavated in arbitrary 10 cm levels. All dirt was screened through 1/4 inch mesh.

The test pits yielded bird and mammal bone, shell, basalt flaking debris, charcoal, a glass bead, wood fragments, rusted metal fragments, a small whetstone and small amounts of a black brittle material, ~i which was probably coal. A charcoal sample (Beta 29386) recovered from Te-c;;t Pit 2 was radiocarbon dated at 290 + 100 years BP; and a charcoal sample (Beta 29387) recovered from Test it

1 was dated at 960 + 160 3P. The later sample was possibly contaminated by coal and is inconsistent with other dates for Morzhovoi Phase sites. The glass bead strongly suggests the site continued to be occupied into protohistoric times.

125

~, ... XCB-025 ...

... Morzhovoi Lake ...... dune grass ...

......

,~ ... ., ...... • ... .,...... ·aa ... ••• • ... .~:. disturbance vegetation - .. e • , ~•. ••-. ' ... I. • t-.• • moist tundra

N ...... o 30 ...... ,...-.- i A meters

FIGURE 28: Map ofXCB-025 (adapted from US BIA 1991:183).

- XCB-026 BIA ANCSA Site PN 96 (ELM AA 12272): SUMMARYorBIA ANCSA REPORT(BIA

1991:178-181)

XCB-026 is located on the Bering Sea coast ofthe Alaska Peninsula approximately 11 kilometers southwest ofCape Glaznap. The site stands on an elevated coastal plain and behind the extensive

Bering Sea beach ridge deposit, which includes 6 meter high dunes inthe vicinity ofthe site. Just west ofthe site, the sandy Bering Sea beach is interrupted by a rocky spur that extends out into the tidal zone. The topography for the coastal plain surrounding XCB-026 has a characteristic hummocky moraine topography with numerous hills and kettle depressions. The cultural features at

XCB-026 are on top ofthe nobs or hills and bordered by ponds and low lying sedge meadows.

Disturbance vegetation dominated by cow parsnip covers most ofthe site area and on the slopes behind the main site area Moist tundra is found behind the site, and wet tundra grows in all low lying areas.

BIA archaeologists identified 37 cultural features during their site survey on 19 July, including 3 nucleus-satellite complexes and a collapsed historic sod cabin. One ofthe nucleus features was a large "L" shaped depression. This feature was tested with a soil probe. A charcoal lens was noted in two probes. Sea mammal bones were observed in rodent and bear disturbances. Sheet metal, nails and milled lumber were observed within and nearby the collapsed cabin. A buried wooden barrel was noted in a low lying area in the eastern portion ofthe site. Aerial photographs were taken on 30 July

1988.

127 XCB-026 ,," -

.. disturbance vegetation .. ,--~--~.~--.~ I (,·~a~ \ .. I .". ' I •• \ I I ",,-...... /" sedge meadow ...... _-----."." Q •

. . swale o 30 • ~••.. i meters • 4(1!1!••• - • N - moist tundra A

FIGURE 29: Map ofXCB-026 (adapated from US BIA 1991:180). -

-- XCB-027 BIA ANCSA Site PN 94 (BLM AA 12270): SUMMARY ofBfA ANCSA REPORT (BfA

1991:166-17J)

XCB-027 is located on a prominent wave-cut moraine about 100 meters south ofthe Joshua Green

River and 2 kilometers inland (SE) from Moffet Lagoon. The site is on the tip ofthe moraine overlooking the broad flat Joshua Green valley. This setting mirrors that ofXCB-029 onthe opposite side ofthe Joshua Green River. The surface ofthe moraine is rolling tundra covered hills with dense willow thickets on the steeper slopes. Disturbance vegetation such as grass, cow parsnip and frreweed covers most ofthe site. Crowberry and mosses are dominant on the higher ground behind the site. Brown bear, caribou, waterfowl, ptarmigan, ground squirrel, porcupine, fox, birds ofprey and other animals were commonly observed in the area during the investigations ofthis site and others nearby. Ground squirrels were abundant at the site and had done considerable damage to many features. Bears, probably digging for squirrels, had also done some damage to the site. Many features, however, appeared undisturbed.

This site was one ofmany locations reported to the Aleut Corporation by Cold Bay residents (Stein

1977). Dumond noted the site during his 1986 aerial reconnaissance ofthe Izembek National

Wildlife Refuge (Dumond 1987b:143 144).

BIA archaeologists identified 54 depressions and a small earthen mound at XCB-027 during their survey on 19 June. Aerial photographs were taken by the BIA on 30 July. As many as 14 ofthe depressions may be the remains ofdwellings based on their size. The earthen mound was located at the west end ofthe site, approximately 100 meters from the nearest depression. This distinct mound, approximately 1.0 meters high, was surrounded by a large depression (possibly a borrow pit created in constructing the mound). Similar earthen mounds found on Umnak reportedly contain human

129 burials (Aigner and Veltre 1976). These "umagan burials" are noted elsewhere in the eastern

Aleutian Islands, but never before on the Alaska Peninsula. The burial function ofthe mound at

XCB-027 was not conftrmed through subsurface testing. Other explanations for the mound are

possible.

Scattered stone artifacts, charcoal, and fITe cracked rock were noted inrodent disturbances. The

stone artifacts included flakes, flake tools, two biface fragments, and a projectile point/knife. All

artifacts were made ofbasalt. The projectile pointlknife was broad bladed with slight shoulders, a

contracting stem and a slightly indented base; it closely resembles points recovered from sites at

Izembek Lagoon by Allen McCartney (1974). Two flakes were found in shovel tests placed in

indistinct depressions near the site margins, confrrming the cultural origins ofthese features.

In 1995 a crew from the University ofWisconsin investigated this site and excavated a 1.0x1.0 meter

test unit in the floor ofa small house. The unit had poorly deftned stratigraphy. Few flakes and no - artifacts were recovered. We could not find the mound reported by the BIA investigators.

130 ~,

XCB-027

o 30 • grass marsh P'w._-~ meters

, . •.••, .• .--.' ..:.o~ • • ... ~ • ~fli . .- ...... r1 • • .... ~0 ....- CJ0 .... q,~ • .... ~ - ..... ~ .- .. ~ • • • • .- • • " --".,------'a--J • .•..... , - 16m bluff grass marsh ~N

FIGURE 30: Map ofXCB-027 (adapted from US BIA 1991:169). XCB-028. BIA ANCSA Site PN 93 (ELM AA 12269): SUMMARY atRIA ANCSA REPORT(RIA

1991:153-165)

XCB-028 is located on the eastern shore of Moffet Lagoon, about 2 kilometers north ofthe mouth of

the Joshua Green River. The site consists oftwo parcels (A and B) on a low, wave-cut shoreline

bluff, 2 to 4 meters high. Inland from the site is a gently rolling glacial topography of knolls and

kettle ponds. The parcels are separated by a low area ofwet tundra, cut through by a small - intermittent drainage. Parcel A, the southernmost parcel, is near the mouth of an unnamed stream, the frrst stream north ofthe Joshua Green River. Parcel B is centered around a broad promontory, 1000

meters north ofthe stream outlet. Several ponds and wet tundra patches are within the boundaries of

Parcel B. Most of the site, however, is covered with disturbance vegetation mixed with moist tundra

and surrounded by dwarf willow thickets. The willow thickets grade into the moist tundra vegetation,

beyond the boundaries ofthe site. The waters ofthe lagoon are especially shallow and muddy in the

vicinity ofthe site. Only a few inches ofwater cover the entire lagoon between XCB-028 and the

Joshua Green River during low tide. The small unnamed stream near Parcel A is believed to support

a seasonal salmon run and may have been an important resource for the inhabitants ofthe site.

The ANCSA application for XCB-028 was based on a report by Aleut informants living in Cold Bay

(Stein 1977:522). Dumond noted five sites, one ofwhich was apparently Parcel B, during his 1986

aerial survey ofMoffet Lagoon (Dumond 1987b:144 Figure 4.10). He described all five sites as

exhibiting "numerous housepits" (Dumond 1987b:144).

The BIA field investigation ofXCB-028 occurred between 19 June and 11 July 1988. Site work was

performed on 9 full or partial days and required just over 200 person hours during this period. Aerial

photographs ofthe site were taken on 30 July 1988. Additional sites to the southeast were

132 reconnoitered, but they were determined to be outside the application boundaries and were not included as parcels ofthis site. One site was about 200 m from the southern boundary of XCB-028 and distinguished by a 30 m x 40 m patch ofdisturbance vegetation, which contained one or more indistinct depressions. To determine ifthis actually was a cultural site, a shovel test was placed within the most distinct depression. The test revealed fITe cracked rock, charcoal and chipped stone flakes.

The BIA archaeologists identified 925 cultural depressions: 110 at Parcel A (Figure 33) and 815 at

Parcel B. There were at least 21 nucleus features and 128 associated satellite depressions identified, all ofwhich were located in Parcel B (Figure 31). Ofthe remaining 733 depressions, 132 (18 percent) ofthem had a long axis of4.0 m or greater and are believed to be the remains of dwellings.

At the southern end ofParcel A, two rectangular depressions with prominent sod berms were recorded. These features are believed to be the remains oflate nineteenth or early twentieth century trapper's cabins, although they lacked observable modern construction material. One depression in

Parcel B appeared to be a two roomed dwelling, possibly related to the house style introduced by

Russians during the early part ofthe nineteenth century. Numerous subsurface exposures were noted along the bluff edge at Parcel B. Most ofthese exposures were the result of natural erosion and animal disturbance. A few exposures, however, were obviously the remains of excavations by relic collectors. The BIA archaeologists inspected all ofthe subsurface exposures and the beach below the site for archaeological materials. They observed a range of artifacts including bone and ivory tools, chipped stone tools and flaking debris, ground stone tools, and a ceramic rim sherd ofnative manufacture. A 50 em wide profile ofthe eroded bluff near in Parcel B revealed cultural deposits over 1 m deep (Figure 32). Most ofthese remains were of shell, fish bone, and mammal bone

133 -" j I I I

...... ~.~..... ". '...... •...... XCB-028, Section 1 ...... ' :.....,..... - .,...... •..." ...... :"" .,. . . wet tundra .:.,.~...... o 30 ...... N~ e...... : , ...... meters .' •••• •• • • ...... willows ...... willows • Ii • ... , . h~irf \.:~~~ . • • .'., ...... ' .," ...... •..'. I•... • ' ... ,#- -. .. . '. :-'.. " , .. .. ir'ili~(!iii(I:!1 ...... • •• '• \.~..'•••: .. 0 • • • • ....e···.' •·e.. '...... e···...':.. ,. .. ". • i .... -. -. 41 willows :, • . .' \..•••••. .... •• ....A····'• ". wet .....•••••, .., • moist tundra ~ ~,.. ",-"!,,,,.:~ .: •• •••..=--00 .. 0"'"~..•.'i .go • ••••• ••• ..Li • .. • or:...... • .' v.···...... •...• • lj:::" :...•... ~ . . :, .~.". ~" .. ." "0..' :c • .:,.. . : _ ••.',.-!..J ••,." '"E . .: .. :...... willows •.•.•...... 4.: .. .._. dimei"...... "'nd", •••• ••ea., \ ...:' -_ .. __ .. _.... .: , :. . willows •.. - .••• .. ••#! .... moist ~ndra .' '" : : .. . : :-" ... , . :' .•. " .~: Moffet Lagoon .:'..'.,...... '.... .:.. 6m bluff edge

FIGURE 31: Map ofXCB-028, Section 1 (adapted from US BIA 1991: 159-162). o~------.

Root layer with bone.

Silty clay loam, 7.5 YR 3/4.

Fish bone and charcoal. Silty clay loam, 7.5 YR 3/4. Shell fish bone, and flakes. 40 Dense bone and shell.

Sandy clay loam, 10 YR m with numerous discontinUOus 60 lenses of bone, charcoal, and organics.

'bone 80

grooved rock ~ ~ whale bone

Mussel Shell FIGURE 32: Profile from XCB-028 (adapted from US BIA 1992: 163)...... XCB-028, Section 2 • • • ...... , ~ moist tundra , ...... "'~ .., ". ,, ". • .. - '. , . , ••• i , \ ".'• • :". l . , : ..... • , ~::. ~ , _· <:> ". , , .. 0 .... : -.~.•... •...... l " \ '. .. , \

\ \ , , \ , •

\ Moffet Lagoon \ , , "' ...' ..~ ... , • , ...... • , • , moist tundra ,, ,, N , , , , , , 4 , , , , , , o 30 P'w".- i meters

FIGURE 33: Map ofXCB-028, Section 2 (adapted from US BIA 1991:157-158). XCB-029. BIA ANCSA Site PN 92 (ELM AA 12268): SUMMARY orBIA ANCSA REPORT(RIA

1991:146-152)

XCB-029 is located on the tip ofa glacial moraine in the Joshua Green River Valley. It is adjacent to the north bank ofthe river, approximately 2.5 kIn up river from Moffet Lagoon. A moraine adjacent to the south bank ofthe river, where XCB-027 is located, mirrors the one on the north. Since both of the moraines are in alignment and perpendicular to the valley, they are probably part ofa terminal moraine. The moraine top is approximately 30 meters above the valley floor on the north end ofthe site, sloping down to about 5 meters above the valley floor at its southern tip. The outer edge ofthe moraine exhibits a distinct wave-cut slope, indicating this topographical feature was at one time on the Bering Sea coast. Vegetation on the moraine inland ofthe site consists ofmoist tundra dominated by crowberry and deciduous shrubs. The Joshua Green floodplain below the site is covered by wet tundra, particularly grasses and sedges. Levee deposits in the floodplain tend to have more moist tundra species, particularly cow parsnip. Disturbance vegetation grows in the vicinity ofthe features.

Cow parsnip, frreweed, and grasses are particularly lush at the site. The slopes ofthe bluff support frreweed, ferns and horsetails. The site possesses an excellent vantage ofthe river valley and the lowlands surrounding Moffet Lagoon. During the investigation, brown bears, caribou, foxes, cranes, ptarmigan and many migratory birds were observed.

Dumond (1987b:143-144) confirmed reports ofa site inthis area during a 1986 aerial reconnaissance ofthe region. He noted numerous house pits on a grassy rise above the Joshua Green

River Valley. The BIA ANCSA archaeologists investigations at XCB-029 were conducted between the 17th and 19th ofJune. Aerial photographs were taken on 30 July.

137 A total of 113 cultural features were identified by the BIA, 112 depressions and 1 rock cairn (Figure

34). The depressions were predominately oval or irregularly shaped. Twenty one depressions

probably functioned as dwellings based on their size; the functions of the remaining depressions are

less certain. Surface artifacts were observed scattered across the site including chipped stone tools

and debitage, fire cracked rock, worked bone and faunal remains. Stone tools and debitage included

many fine-grained basalt flakes, with several bifacial thinning flakes ofthe same material; a single

jasper flake; three basalt unifacial flake knives; a basalt biface fragment; two hammerstones; and a

pumice abrader. Caribou and whale bones were noted in several locations.

Subsurface testing conducted by the BIA included nine soil probes and a single 50 x 50 centimeter

test unit excavated to a depth of 1.0 m, then probed beneath that level. The soil probes around the

perimeter ofthe features helped establish site boundaries. The test unit (TP 1) was excavated in a

questionable feature at the north end ofthe site and revealed several strata of concentrated charcoal

flecks, possibly representing house floors. Artifacts recovered in the test included basalt retouch and

bifacial thinning flakes, a basalt bifacial tool fragment, and red ochre. Two charcoal samples

recovered from the test unit yielded radiocarbon dates of4500 + 250 BP (Beta 29390) and 3370 +

150 BP (Beta 29391). The older dated sample was obtained from a higher stratigraphic unit. - Although stratigraphically inverted (an indication ofpost depositional transformation) the dates provide a basal age for occupation.

This site was visited in 1995 by the University ofWisconsin crew. A profile was cut in the north

bank and a test unit was dug in a house depression floor. The unit extended 1.2 meters below surface.

The stratigraphy is complicated with multiple house floors and roof fall events (Figure 35). The

138 floors are nearly all covered with dense deposits ofred ochre. Two samples have been submitted for

AMS dating from these floors.

139 : . •... • XCB-029 .: .~

;':derisEf::: :. /i'~~~t~~~ \ · ,,',,', ..'.,'.-"".,.

, , " ~ ,. , , , ,. , , " .. ,-", sedge

• • N

• • ••• A ~. •• o 30 -=:I• •2.__~ l:M,- I meters • -• moist tundra ••• • •, .•...... :. .'• .. 16 m bluff :,': • : ... • '. . : -. • .•...... • :,. .- . . . • \. ,. • •• • -.tI~~~se~·. ::. • ••••• ••• v~et8tion ....'.-...... ------. "...... ' sedge '. ... e,..'• . .. \" •..:-...: . Joshua Green River •••••..".' ••... , • 60 meters)

FIGURE 34: Map ofXCB-029 (adapted from US BIA 1991:149-150). - 0.00 0.20 0.40 0.60 0.80 1.00 1.20

1. Black, greasy, silty surface with hearth, scattered flakes, charcoal sample. 2. Roof fall with some stratigraphy, medium brown, silty. 3. Hearth or dump, filled with charcoal and scattered red ochre. 4. Abrupt line or charcoal and red ochre separates levels 2 and 5. 5. Sandy brown soil with flecks of charcoal and scattered flakes, probable house floor. 6. Silty dark-reddish brown fill, possible between floors. 7. Dark-stained silty sand, flecks of charcoal, possible hearth. 8. Gray-stained sandy soil, another possible floor. 9. Hearth composed primarily of charcoal with some sand. 10. Probably sterile yellowish-brown sand with pebbles. Till below in soil probe.

FIGURE 35: Profile oftest at XCB-029. XCB-030 BIA ANCSA Site PN 36 (BLM AA 12255): SUMMARY orElA ANCSA REPORT(BIA

1991:68-80)

XCB-030 is located on Strawberry Point (USGS Blaine Point). Strawberry Point is a narrow peninsula with rolling topography that separates Izembek Lagoon and Moffet Lagoon. The point

extends about 3 kilometers northeasterly from the mainland. The site encompasses the northern third

ofthe peninsula. A low lying saddle separates the site from the southern two-thirds ofthe peninsula.

A steep bluff, covered with dune grass, defines the western side ofthe peninsula The eastern side of the peninsula consists of a sparsely vegetated, almost vertical, 2 to 3 meter high, escarpment.

Within the site area on the peninsula's eastern side is a low marshy area that is partially silted over.

Presently, this relic tidal lagoon is composed ofthree shallow brackish ponds and a relatively deep outlet channel. The terrain between the tip ofthe peninsula and the relic lagoon is characterized by a ridge with a maximum elevation of approximately 36 m above the beach. On the eastern side ofthe ridge, there is a sharp descent to the escarpment. The slope on the western side ofthe ridge is more gentle and is broken by three wide swales. Another ridge ofsimilar elevation curves around the western and southern margins ofthe relic lagoon. A saddle separates the two ridges

Vegetation onthe peninsula is characterized by moist tundra. Dwarf deciduous shrubs are also present Cow parsnip, wild celery, fireweed, lupiae and wild geranium are the dominant plant species where areas have been disturbed by human activities. Dune grass covers the steep sided western margin ofthe peninsula and the low storm beach terraces. Sedge is present in low wet areas. Near the western side and the tip ofthe peninsula, there is a relatively deep channel in Izembek Lagoon.

Except at the extreme tip, a wide rock covered mud flat separates the channel from the peninsula at low tide. There are no channels in Moffet Lagoon that approach the eastern side of Strawberry Point.

142 Along the western side ofthe tip ofthe peninsula, for a distance ofabout 800 m, the shoreline is very rocky. Boulders encrusted with large barnacles and blue mussels are present along the base ofthe bluff and immediately offshore. Blue mussels are abundant in this rocky portion ofthe peninsula.

The remainder ofthe western shore consists of a cobble and sand beach. A thick drift line ofrotting eelgrass marks the extreme high tide line on this side ofStrawberry Point. The shore and the storm beach terraces are littered with a considerable volume ofdriftwood and debris from fishing vessels.

On the eastern side ofStrawberry Point, the shore is almost devoid ofrocks and flotsam. Erosion along the western shore has abated, but the eastern shore exhibits evidence of active erosion The large quantity ofshell found in middens at the site indicates shellfish, especially clams and cockles, were once abundant in the vicinity. No beds ofclams or of cockles were noted in the site vicinity during the investigation.

The site on Strawberry Point was investigated in July 1979 by a crew ofarcheologists from the

USFWS (Klingler n.d.). They located 150 to 200 cultural features in five distinct clusters. Bluff exposures were examined to ascertain midden characteristics. The site was mapped and the cultural features were described. Approximately 36 items were collected from subsurface tests. There was also evidence ofsouvenir hunting. A fisherman found a whalebone mask on the surface ofthis site in 1975 (Walter Van Horn, personal communication, 16 May 1989). It was presented to the

Anchorage Museum of History and Art in 1981, where it is currently on display. The mask is illustrated by Black (1982:33, Figure 35 d).

The site was identified on 6 July 1988 by BIA ANCSA Archeologists Bartolini, Cooper, Hoffman and Staley. A pedestrian reconnaissance was conducted to determine the extent ofthe site, and visible

143 cultural remains I were flagged. From 11 to 13 July, all identified cultural remains were mapped and described, and bluff exposures and areas ofhuman and animal disturbances were examined for the presence ofcultural materials. Four shovel tests and a profile of a bluff exposure were conducted on

13 July, and artifacts revealed were described in the field. None were collected. A sample ofshell from one test was collected for radiocarbon dating.

The site encompasses the upper 1000 m ofStrawberry Point. A total of 216 cultural features were recorded by the BIA archaeologists during their field investigation ofXCB-030 conducted between

th the 11 th and 13 ofJuly. All but three ofthe features they found are depressions representing remnants ofsemisubterranean structures. The remainder are shell mounds. Five discrete clusters of features (Areas A through E) were noted. One feature cluster is on the tip ofthe peninsula; three are along the western margin ofthe peninsula; and the fifth is in the interior ofthe peninsula, north ofthe relic lagoon Most ofthe cultural depressions have oval outlines. Area A is located at the extreme tip of Strawberry Point and contains the remains of a single semisubterranean structure with an attached entry room. The relatively straight sides and roughly squared shape ofthe feature suggests that it was used during the historic period. A shovel test was excavated into the interior ofthe structure to determine temporal affiliation. The recovery offlat metal fragments (sheet metal7), a rusted nail fragment and pieces oftar paper denote a historical affiliation for this structure.

Area B, which contains two semisubterranean features, is located on elevated ground between two swales, about 150 meters southwest ofArea A on the western edge ofthe peninsula. Both features may be the remains offormer dwellings. A shovel test excavated into an animal burrow revealed intact midden deposits. The profile contained an upper sod mat layer covering a 25 centimeter layer ofsand (two distinct layers ofsand were recognized) followed by a layer ofcompacted shell. Only

144

- ---~------the upper 30 centimeters ofmidden was excavated due to the compactness ofthe shell deposits. An shell sample (Beta 29381) from this excavation yielded a radiocarbon date of 2990 + 110 BP. This date should be used with caution, however, since it was derived from a sample ofmarine shells.

Forty cultural features were identified within Area C, which encompasses a small narrow isolated ridge onthe west side ofthe peninsula. Eight ofthe semisubterranean features within this area are probable dwellings (Figure 36, northeast section). Evidence ofrelic hunting was discovered in eight features and along the upper edge ofthe bluff. Five separate exposures were noted along the 200 meter long bluff edge enclosed by Area C, most of which appear to have resulted from vandalism.

These exposures were up to 15 meters in length and cut back into the bluff as much as 2.5 meters. A total ofnearly 45 linear meters ofsite area was affected by vandalism and natural erosion in 1988.

The BIA archaeologists identified a range of cultural remains in these exposures including blue mussel, cockle and clam shells; fish, bird and mammal bones (including a whale rib and several split long bones); modified antler, pumice, basalt flakes, and burnt rock.

Area D consists of 166 cultural features (Figure 36, west and southwest sections). This area encompasses the entire top and upper slopes ofthe narrow curvilinear ridge located west and south of the tidal lagoon. Cultural features are also present in the two swales at each end ofthis ridge. Over

400 meters ofthe peninsula's western bluff is enclosed by Area D. Three ofthe identified features represent shell mounds; several other similarly shaped mounds were noted but were not mapped or described. All ofthese mounds were located on the back slope ofthe ridge. A shovel test was excavated within the center ofone. Shell deposits in this test extended to a depth of at least 85 centimeters, when the test was terminated. The shell deposits were estimated to continue perhaps another meter, based on the surface contour ofthe mound. The remaining features in this area

145 represent semisubterranean structures. Ninety semisubterranean features, over halfthe cultural

depressions found in Area D, can be described as probable dwellings based on their size. Midden

material is intermittently eroding from the edge ofthe entire bluffin Area D. A segment ofone

exposure was profiled, revealing stratified midden deposits approximately 1meter below the bluff

edge. Midden fill was also noted in several animal burrows and bear tears. All ofthese disturbances

appear to be natural in origin, rather thanthe result of vandalism.

Area E is situated approximately 30 meters inland from the east side ofthe peninsula and

immediately north ofthe relic lagoon. Seven cultural depressions were found in this area, two of

which can be described as probable dwellings (Figure 36, SE section).

A total of 101 cultural depressions were identified as probable prehistoric dwellings hy the BIA at

XCB-030. The probable dwellings from all four prehistoric feature clusters are strikingly similar in

size and shape. The prominent setting and the prodigious quantity ofshell found in Areas B, C and

D suggest Strawberry Point was occupied occurred over a long period oftime. 111is site had the most

shell observed at any site investigated by BIA in the project area, yet shell beds in the two lagoons,

which border it, are now nonexistent. Strawberry Point afforded favorable access to Motfet Lagoon, - Izembek Lagoon, the Joshua Green River valley, the mainland ofthe Alaska Peninsula. the Bering Sea and even the Pacific Ocean. Because ofits elevation, the tip of Strawberry Point provides an

excellent observation post. These and other attributes ofStrawberry Point suggest an ideal location

for a site inhabited by maritime hunters and gatherers. This site could have been occupied on a

continuous basis until the environment became altered to such an extent that the ecosystem could no

longer support large numbers ofhuman inhabitants. Presently, the waters of Moffet Lagoon and

Izembek Lagoon are navigable only through narrow channels, and only during periods ofhigh tide.

146 The impracticality ofboating in Moffet Lagoon at low tide was demonstrated by Hoffman's

unsuccessful attempts to traverse along the eastern shoreline ofthe lagoon in a collapsible kayak

during this investigation. Prehistoric occupation ofthe site may have occurred when it was still

possible to gather sufficient quantities of shellfish and navigate unhindered in Izembek Lagoon, but

not in Moffet Lagoon.

147

liP } r·~,...- .

XCB-030 profile o 4.0 ( meters Izernbek LagoOn ~ ~ ~--"--'" " _.'..--.--.-t' .--..•... --.. --.. --...--....--.. --.. --"--',- ...---- , .••.' .'.,...''" ••. " .:..'#.....•• . ,..-.".'.• . ..• :. ~... .'. . ~.. " ..., ..- ...... ,~~ •••••,..~i:'tUrb~~CEl'!"9"~ti~n ..:• '.. .. ., • •• • I ••• marsh '. • • • • • ' • ...... • .. ' . • • • .' • ...... ~N

FIGURE 36:Partial Map ofXCB-030 (adapted from US BIA 1991:76-77L XCB-031: SUMMARY orBlA ANCSA REPORT(BlA 1991:99-125)

The BIA mapped this selection as a complex of six sites (Parcels A through F; Site PN 41/PN 42 (BLN

AA l2259/AA 1226) which included XCB-003 and XCB-031. We have divided these six parcels into five sites -XCB-003, XCB-031, XCB-120, XCB-121, and XCB-123 based on their location and the distance between them.

XCB-031 is 10cated 9km south-southeast of Cape Glazenap, in an unnamed cove in the southern portion of Izembek Lagoon, just southwest of Applegate Cove. The cove is very shallow and muddy with few channels. The air is foul smelling at low tide indicating organic rot and methane production. The cove is fed by three major streams, the westernmost of which supports the largest run of salmon.

XCB-031 is the largest component of this site complex (Figure 37). It is located in the southwestern comer of the cove between the western and central creeks. The features are concentrated on four northerly sloping ridges, or lobes, that extend down from the coastal plain. Similar to the setting of XCB

120, an area of features at the east end ofXCB-031 is located on a 2 to 3m high terrace adjacent to a stream. Grasses and sedges grow in profusion along the coast and on the floodplain. Wet tundra is found in most low areas and in swales between ridges. The ridges, especially the portions closest to the shoreline, are covered by on site vegetation dominated by cow parsnip. Moist tundra backs all these areas and extends to the south. Two ponds, or small lakes, are found in the western end of the parcel

XCB-03l was dated by the BIA. The site produced inverted radiocarbon dates of 1420 +/- 130 BP and

1190 +/-100 BP, which converts to a corrected calendar dates of AD 555 +/- 132 and AD 782 +/- 105, respectively. The ranges of the dates overlap between AD 600 and AD 850 (Table 4).

149 N XCB-031 lUO A meters \ \

1;,% ' ~ I'~' \,~~$~ -".' unnamed cove "~" ,. - -,I , , " \ ,..-',spring " grasses ~.\ sedges . ....-~~' . /I "

\\ \\ : unnamed cove ~ . .:. ..._"". ~ / ..... sireai; ._, ,... -.. --.. ~ _ ) \~",--, "~- , • . , .- .. ;' '. • .,..- ... . , -----...... , ~.... I " , '-. grasses

"~ • ~: Ill;

FIGURE 37: Map ofXCB-031 (adapted from US BrA 1991:113-116). Four soil probes and a profile were conducted. Three showed evidence of subsurface deposits in the form ofcharcoal flecks. One heavily disturbed feature from bear activity was faced off, and the soil from the bear's activities and from the preparation ofthe profile was screened for artifacts. The bear's back dirt produced 4 projectile point or knife fragments, 1 broken unfinished biface, 3 basalt flakes bearing the collapsed edges ofbifaces, 35 basalt flakes (mostlybifacial thinning), 1 obsidian retouch flake and 1 light brown cryptocrystalline silicate flake. It also revealed charcoal, shell and 9 notched pebble net sinkers. The screened dirt from the profile preparation produced 1 additional net sinker, approximately 50 basalt flakes, 1 unifacia1 knife or scraper fragment and fire cracked rock..

XCB-032

Dumond (1986) noted from a helicopter that a village site with numerous depressions was present on the east shore ofMoffet Lagoon north ofXCB-028. The University ofWisconsin visited this site in

1995 and noted a number ofnucleus-satellite depressions. This site will be mapped and tested in

1997.

XCB-033

Dumond (1986) noted from a helicopter that a village site with numerous depressions was present on the east shore ofMoffet Lagoon north ofXCB-032. This site will be mapped and tested in 1997.

XCB-036

In 1979 the USFWS identified a small lithic scatter in a bear excavation on a bluff across from XCB

005 SW of Outer Marker. A few items were collected. No further work has been done at this site.

151 XCB-037 (quoted with revisions and additions from Klingler n.d.)

This site sits on a low, NW SE tending ridge, 80m by 50m and 5m in elevation, rising from the marsh flats at the head of "East Outer Marker Lagoon". Atop this hill is an ill defined depression, approximately 4x5m. In a test hole within this depression, scattered charcoal and one obsidian flake were encountered. The soil consisted of dark brown silt with a scattering of small cobbles. No stratigraphy was noted in this test, which was dug to a depth of approximately 40cm. Other tests, atop the hill and along the base, were sterile. Vegetation consists of wild celery (Heracleum lanatum)

(Angelica lucida), wild geranium (Geranium erianthum), frreweed (Epilobium spp.), buttercup

(Ranunculus spp.) and various grasses. Similar in form to a glacial drumlin, this hill, which may have at one time been an island when the lagoon was more extensive, may have served as a lookout site for hunting activity (from Klingler n.d.).

XCB-038 (quoted with revisions and additions from Klingler n.d.)

Similar to·and approximately 300m north of XCB 037, this site is located on a 100m long crescent shaped hill about 3m in elevation. The major stream feeding the "East Outer Marker Lagoon" borders the eastern margin of the site. Lithic debitage was found in the back dirt of ground squirrel and bear disturbances. However, a single shovel test atop the hill revealed no stratigraphy. As at XCB 037, the vegetation consists of wild celery (Heracleum lanatum and Angelica lucida), wild geranium (Geranium erianthum), fireweed (Epilobium spp.), buttercup (Ranunculus spp.) and various grasses. Most likely a remnant glacio fluvial feature which may have been an island in the more extensive lagoon, the hill perhaps served as a game lookout (from Klingler n.d.).

152 This site was visited in 1995 by a crew from the University of Wisconsin. A house floor was found situated on glacial gravel approximately 1.1 meters below surface. A charcoal sample has been submitted for AMS dating.

XCB-039 (quoted with revisions and additions from Klingler n.d.)

On the southeast shore of "west outer marker" lagoon, this site lies on the southwest slope of a 4m ridge between the lagoon and the system of lakes at the head of "east outer marker" lagoon. Three depressions, two of which were 3 x3m. and one 6 x 6m. in diameter had depths that varied between 50 and 75cm. were arranged parallel to the lagoon shore, approximately 50m back from its edge. The land along the lagoon is rolling. To the northeast the terrain rises to a slight crest, while to the southeast the land is flat for approximately 200m. before falling to the series of lakes. A shovel test in the most distinct depression reveals three charcoal stained floors at 25 28cm., 30 35cm.. and 50 52cm. below ground surface. These dark stained strata alternate with dark gray silty sand and orange brown possible ash deposits. At a depth of 70cm. the test bottomed on a tan clay deposit. Around the depressions the land, which has a furrowed tundra appearance, is vegetated by crowberry (Enpetrum nigrum) mats with scattered fireweed (Epilobium spp.) and wild geranium (Geranium erianthum), Wild celery

(Heracleum lanatum and Angelica lucida) grow in the deep furrows. A dense stand of scrub willow

(Salix spp.) is located at the northwest comer of the site. Within the depressions is a dense growth consisting primarily of wild celeries (Urnbelliferae), but also including fireweed (Epilobium spp.), and wild geranium (Geranium erianthum). No artifacts were collected (from Klingler n.d.).

153 XCB-040 (quoted with revisions and additions from Klingler n.d.)

This site is located on two remnant terraces on the west side of the stream emptying Lamprey (Hess)

Lake, midway between the lake and "East Outer Marker Lagoon". The site is approximately on the 50

ft. contour, The lower terrace, designated Area 1, is approximately 28m., above the marsh flats. The

upper terrace, designated Area 2, is approximately 10m higher. Area 2 commands an excellent view in

all directions, particularly to the east and northeast over the marsh, and to the east and south up the

narrow stream valley. The marsh is undoubtedly part of a former lagoon system. Presently, salmon run

into Lamprey Lake. The Area 1 vegetation is very dense, consisting of wild celery (Heracleum lanatum

and Angelica lucida), wild geranium (Geranium erianthum), mature salmonberry (Rubus spectabilis)

which is unusual for the area, Geum spp., a few red berried elder (Sambucus racemosa), fireweed

(Epilobium spp.), and a dense understory of siberian spring beauty (Claytonia sibirica) and various

grasses. Within the depressions of Area 2 the dominant vegetation is grasses (Gramineae family), wild

celery (Heracleum lanatum) in somewhat less than usual quantity, frreweed (Epilobium spp.), sedges

(Cyperaceae family), arctic dock (Rumex arcticus), coastal paint brush (Castilleja unalaschcensis),

chocolate lily (Frittilaria camchatcensis), club moss (Lycopodium spp.), wild geranium (Geranium erianthum), horsetail (Equisetum spp.) mosses, monkshood (Aconitum delphinifolium), Geum spp. and buttercup (Ranunculus spp.). The vegetation around the housepits is similar before making an abrupt and distinct transition to furrowed tundra vegetation, which probably delineates the site

boundary. The tundra vegetation is primarily mosses, lichens, crowberry (Empetrum nigrum), and

miscellaneous wildflowers. Two 1m 2 test pits were excavated, one in each area. There was a

pronounced difference in character between these two tests (from Klingler n.d.).

154 This site was mapped by the University of Wisconsin in 1996 (Figure 38). A charcoal sample from this

site was AMS dated to AD 825 (calibrated, see Table 4) which is the same as the conventional date run

by the USFWS ofAD 825 (calibrated, see Table 4).

XCB-041 (quoted with revisions and additions from Klingler n.d.)

XCB-041 On the west side ofthe creek outlet of Lamprey (Hess) Lake is an 8m high grassy knoll. Two depressions, 3 x3m. and 2 x2m., are situated atop this knoll. This site is bordered on the east by the

creek, while to the north, south and west the terrain slopes down to rolling, wet tundra. The vegetation

within the depressions consists of wild celery (Heracleum lanatum), wild geranium (Geranium

erianthum), Geum spp., and grasses. Outside the depressions the primary vegetation is grasses, with

scattered wild celery (Heracleum lanatum and Angelica lucida). No testing was done and no artifacts were recovered (from Klingler n.d.).

XCB-042

A single depression found by the USFWS in 19790n a point SW of the Hess (Salmon) Lake outlet near XCB-041.

155 / I / I J I N 1 I XCB-040 I J ,J I A 1 I, dry tundra I I I I grassland \ I \ marsh \ \ I I I, • • I ,I • I I •• I •• • J grasses and J • I I cow parsnip • I • I ., • J • upper , I terrace I ••• J I • I / J / - / . • J " J" / I I I I , grassland I I marsh I \ fan \ \ \ I \ \ \ \ dry tundra \~ '0- 'ten 10) 1-13 10 l';:) ~() l'@ • ,(1) I'"1 \ \ I I I I 1 I, ,r I, I o 30 I ,....- i , meters I I, I 1 FIGURE 38: Map ofXCB-Q40. XCB-043 (quoted with revisions and additions from Klingler n.d.)

This site is located approximately 65m. downstream from the outlet of Blue Bill Lake, on the east side of the creek. On the fIrst terrace above the creek are situated four depressions two large 6 x 8m pits on the edge of the terrace and two smaller 4 x 4m. pits approximately 15 m. back. The stream, which appears to be navigable for its entire length, presently supports a red salmon run. The vegetation on the site consists of wild celery (Heradeum lanatum and Angelica lucida), fireweed (Epilobium

Angustifollum), wild geranium (Geranium erianthum), siberian spring beauty (Claytonia sibirica),

Geun spp., coastal paintbrush (Castilleja unalaschcensis), horsetail (Eguisetum spp.), and yarrow

(Achillea Borealis). A small shovel test was made in the easternmost of the upper pair of depressions

(from Klingler n.d.).

XCB-044 (quoted with revisions and additions from Klingler n.d.)

North and across the creek from XCB 043, this site is situated on a 6m. terrace located at the juncture of the outlet creek valley and Blue Bill Lake. The lake is to the east of the site, the creek to the south, while to the west is rolling tundra. Four 3m., and, at least, seven 1m. depressions mark the surface 1m. back from the terrace edge. The smaller depressions may be cache pits, but some may also be bear excavations. The vegetation within the depressions consists of a dense undergrowth of grasses, wild celery (Heradeum lanatum), wild geranium (Geranium erianthum), monkshood (Aconitum delphinifolium), lupine (Lupinus nootkatensis), fireweed (Epilobium angustifolium), arctic dock

(Rumex arcticus), coastal paintbrush (Castilleja unalaschcensis), and Geum spp. The limit of the site appears to be indicated by a return to the characteristic rolling furrowed tundra. A shovel test in the southern most large depression encountered a possible slab hearth. Lithics were recovered. A second test of a large depression behind the others revealed a single charcoal stained layer immediately above the basal soil, at 45 em. below the surface (from Klingler n.d.).

157 XCB-045 (quoted with revisions and additions from Klingler n.d.)

This site is located where Blue Bill Creek broadens and empties into Applegate Cove. It is situated on

the south side of the creek, atop the first terrace, about 4 6m above the low, boggy floodplain. The site

is bounded on the northwest, north, and east by this floodplain, and on the south by rolling tundra. The

site consist of one large, roughly rectangular 6 x 8m. depression, a small 1m. cache pit, and a low

mound approximately 6m in diameter. The mound is covered by the typical site vegetation, including

wild celery (Heracleum lanatum and Angelica lucida), monkshood (Aconitum delphinifolium), arctic

dock (Rumex arcticus), wIld geranium (Geranium erianthun), Geum spp., horsetail (Equisetum

arvense), and yarrow (Achillea borealis). The vegetation within the depressions also includes fireweed

(Epilobium spp.). No testing was done and no artifacts were collected (from Klingler n.d.).

XCB-046 (quoted with revisions and additions from Klingler n.d.)

Located where Blue Bill Creek broadens and empties into Applegate Cove, this site is north and across the creek from XCB 045. The site is also situated on the terrace just above the creek, and has as elevation of4 6m. XCB 046 extends for approximately 300m. east west and is 40m. wide. Vegetation on the site is primarily grasses (Graminaea), wild celery (Heracleum lanatum and Angelica lucida), and monkshood (Aconitum delphinifolium). A 1m test was excavated in one of the rectangular depressions with an attached room in Area 1. It would appear that Area 2 is the older of the two, while the large depressions of Area 1 seem to indicate larger, more permanent structures than the summer tent depressions (from Klingler n.d.).

158 This site was mapped in 1996 and found to have approximately 58 depressions, at least two of which are similar to nucleus-satellite houses. Section 1 (or Area 1) has 41 depressions (Figure 39), section

2 (or Area 2) has 17 depressions (Figure 40).

159 I ' . ApPlegate.:::; • " , " " • " ", " , , , , -. \ " , \ , XCB-046 , II \ \ marsh \ Section1 \ , ••• \ o 30 I \ e :~ . e I CD \ ~ ~ ~ .. (J ; I == I •• :m : • • I CD I I;£D:J ,-.' • ; . tundra J .' • ,. . •• .,' I. ~ .I : '. marsh . . , I\, . • . , \\ \ . · , • ,I • I. ·I, , ~, , . . . •• • , , • • tundra , ,,I ..I: •I I J J• ,. , , .

.I II .. I. . • !//~ , 64 meters to Section 2 , , - FIGURE 39: Map ofXCB-046, Section 1. \ , , )i;;>N ,""l64m to Section 1 • •

I I XCB-046 Section 2 marsh •

1 I • tundra ,

marsh

1 1

;~ • ..1 ~(l) ." , () " , J . ;:::. . • tundra ; iii J" 1 J . (l). .. .;;[ .. • 1 .OJ I

J - , , • , I o 30 I , 1 J I I meters

FIGURE 40: Map ofXCB-046, Section 2. XCB-047 (quoted with revisions and additions from Klingler n.d.)

Just south of where the Blue Bill Creek empties into Applegate Cove is a tidal channel which extends

back to a brackish salt water lagoon. XCB 047 is located on the north side at the juncture of the

channel and the lagoon. On a well defmed terrace approximately 10m. above the high tide level are

situated three depressions. Two are located near the point of the juncture, while a third is

approximately 80m. to the east near where a small creek empties into the lagoon from the north. The

latter depression is a deep, well defmed 3 x 4m. rectangle. A piece of sheet metal embedded in its floor

probably indicates a relatively recent, historic origin). Ofthe two depressions at the point, one is

shallow, rectangular, and has dimensions of6 x 7m. The other is a deep, well defined, 5 x 7m,

rectangular structure with an attached 4 x 4m. room on the east wall. This latter depression is open to

the north. A small test ofthe depression with the attached room uncovered evidence of relatively

recent, historic occupation: a door and a small fragment of a cast iron stove, a 6.5mm. cartridge casing,

and a small basalt flake. The flake may be associated with a prehistoric component possibly suggested

by the shallow 6 x 7m. depression. Vegetation on the site includes lyme grass (Elymus spp.), wild

celery (Heracleum lanatum and Angelica lucida), monkshood (Aconitum delphinifolium), wild

geranium (Geranium erianthum), buttercup (Ranunculus uccidentalis), Geum macrophyllum, horsetail

(Equisetum spp.), arctic dock (Rumex arcticus), salmonberry (Rubus spectabilis), fireweed (Epilobium

spp.), and coastal paint brush (Castilleja unalaschcensis) (from Klingler n.d.).

XCB-048 (quoted with revisions and additions from Klingler n.d.)

On the south bank of the tidal inlet just south of where the Blue Bill Creek empties into Applegate

Cove is a 6m. high knoll rising above the surrounding tundra. This 25 x 20m. knoll, most likely glacio

fluvial in origin, is bordered on the north by the tidal inlet and on the west by a small creek which

drains the wet tundra to the south and east. Two deep 6 x 6m. depressions, one with an adjoining room,

162 - are situated on the north end of the knoll. The vegetation on the knoll is primarily furrow tundra vegetation with scattered stands of wild celery (Umbelliferae). The site area, is densely covered with grasses, wild celery (Angelica lucida and a very few Heracleum lanatum). No testing was done and no artifacts were recovered (from Klingler n.d.).

XCB-049 (quoted with revisions and additions from Klingler n.d.)

Perhaps 300m. upstream from XCB 045 and XCB 046, on the east side of Blue Bill Creek, is a 6 Sm. high, north south tending terrace. The site on it is located at the point where the creek runs closest to the terrace, north of the creek's confluence with an unnamed lake's outlet stream. To the north the site is bordered by another valley, drained by a small stream flowing out of the northeast. To the east behind the site is tundra. The creek valley at the site is vide, with several pot hole lakes to the west across the creek. The site extends for approximately 120m. parallel to the terr..tce edge. Nine circular depressions of varying sizes from 3 x 3m. to 6 x Sm., and approximately seven smaller I x 1m. and 2 x

2m, pits are present. Inspection of several bear excavations revealed charcoal but no artifacts. A shovel test adjacent to the southernmost large depression showed patches of charcoal hut no apparent cultural stratigraphy. No artifacts were collected (from Klingler n.d.).

This site will be mapped and tested in 1997.

XCB-050 (quoted with revisions and additions from Klingler n.d.)

This site is located on the north bank of the mouth of Frosty Creek. Approximately 20 depression are situated on a terrace at the juncture of the creek and Applegate Cove. The site is bordered to the south and west by the lagoon, to the east by the creek, and to the north by the wet tundra of the flat of the terrace. The highest point of the site is approximately 6m. above high tide. Frosty Creek presently

163 supports a considerable salmon run. The depressions which are generally placed along the terrace

edge, vary in size, shape, and definition. Those to the north facing the lagoon tend to be vague, 3 to 4

ovals, while those toward the creek are larger more distinct, 6 x 8m. rectangles. There are also a

number of small cache pits. This site has been impacted by erosion, several depressions having lost

their front edge to bluff erosion (from Klingler n.d.).

This site will be mapped and tested in 1997.

XCB-051 (quoted with revisions and additions from Klingler n.d.)

Nearly due south of XCB 050, between the Frosty Creek inlet and the next inlet to the south is a long

north south trending beach. XCB 051 is in a relatively low area, only 2m. above the beach. It extends

the entire 400m. length of the beach, with features situated along the terrace edge. To the north, west,

and south the site is bordered by water, to the northeast by a low marsh and small lakes, and to the

southeast by rolling tundra. Two areas were delineated: the northern portion designated Area 1 and the

southern portion Area 2. The apparent hiatus may be the result of erosion, the impact of which is

evidenced by the loss of the front edge of a number of depressions to beach erosion and by the

considerable amount of lithic materials recovered from the beach. Area 1 contains at least 11 large

depressions, some of which are very large, up to 12m., and irregular shaped. Area 2 contains at least

10 depressions, all roughly rectangular, varying in size from 4 x 4m. to 5 x 10m (from Klingler n.d.).

This site will be mapped and tested in 1996.

164 - XCB-052 (quoted with revisions and additions from Klingler n.d.)

This site is located approximately 150m southeast of XCB 050, on the south side ofFrosty Creek. It is situated on a point of land between the creek and the lagoon, across from a small island in the creek mouth. The site area appears small, about 25m. No surface features were observed, but two basalt flakes were recovered from the back dirt of a rodent disturbance (from Klingler n.d.).

XCB-053 (quoted with revisions and additions from Klingler n.d.)

Located on the west side of Strawberry (Blaine) Point, approximately 500m. south of XCB 030, are three depressions, measuring from 4 x 4m. to 4 x 7m. The site is along a ridge that forms the western bluff of the point. To the east is a low marshy area, probably on extinct lagoon, that drains to the south east. East of the marshy area is another north south trending ridge. The vegetation is primarily grasses, with wild celery (Heracleum lanatum and Angelica lucida) and lupine (Lupinus nootkatensis) within the depressions. Although no depressions are apparent along the 500m. stretch between XCB 030 and

XCB 053, there is considerable flaked material along the beach. No artifacts were collected (from

Klingler n.d.).

165 XCB-054 (quoted with revisions and additions from Klingler n.d.)

On the southeast end of Cove Island, due east of Cape Glazenap, is a small peninsula forming the

southern shore of a small cove. South of the peninsula are eel grass flats of the lagoon, to the east is a

shallow strait separating the site and another small island, and to the west the ground rises to a 30m. ,~

hill. The south edge ofthe peninsula is a steep bluff. A shovel test in one of the larger depressions

revealed a 15cm. thick layer of brown silty sand directly beneath the sod mat. Underlying this were

two lcm.layers of ash, the upper being buff colored, the lower being dark, charcoal colored. Beneath

the ashes, the brown silty sand continued to a depth of 65cm. A second shovel test in a small

depression revealed the same stratigraphic sequence as above to a depth of 70 cm. where the soil

changed to a gray silty sand, with chunks of charcoal at the interface (from Klingler n.d.).

In 1996 the University of Wisconsin conducted investigations at this site. A 2.0 meter deep profile was

cut and the site was mapped (Figure 41). Numerous house floors beginning 1.0 meters below surface

extend to nearly 2.0 meters (Figure 42). Two calibrated AMS dates place this site at approximately

2550 Be. Many basalt flakes and a single basalt projectile were recovered. Also recovered was a

small, stemmed ground slate end blade quite different form anything in Ocean Bay assemblages of - comparable age.

166 XCB-054

• - • •••• • e • • • • •• - • • N~

• o 30 ~ I I meters contours = 2m

marsh grass

FIGURE 41: Map ofXCB-054, the Cove Island Site. 0.0 Humus and roots.

~- Dark brown with dense organics. Much like roof fall in more recent houses.

0.5

Light-brown silty sand with lithics and Light brown clayey silt. charcoal flecks.

Burned silty sand. Some fire-cracked rock and charcoal. Charcoal lens. Medium brown sandy silt with Brown, clay lens charcoal flecks. Mottled black with rown sandy silt with charcoal dense Charcoal. and fire-cracked rock. May be Brown silt r roof fall. Tan, burned silty sand, charcoal. LiQht brown 1 a ouse~oor. sal1d. • rey a aOO sand. ~oLIse oor. Tan sand. Light brown silty sand. Tan sand. House floor. "Ian sand. Tan sand. House floor. 3980+/-60 House Hoor. House oor. House floor.

Tan to brown sand mottled charcoal. Includes pebbles and flakes.

Tan sand mottled House floor. with charcoal. 1.5 ~~t;~~~:;::!~ Tan to brown sand mottled charcoal. Includes pebbles Charcoal lens. and flakes. Medium brown silt. House floor. Ground Slate • Grey ash and sand. HoLfse floor. EndBlade Compacted pebblestgravel. 4040+/-60 Glacial silty sand. Basalt y Projectile Silty ash (volcanic), grey to tan.

Ash and silt, apparently a mixture of glacial silt and 2.0 volcanic ash.

FIGURE 42: Stratigraphic profile from XCB-054. XCB-055 (quoted with revisions and additions from Klingler n.d.)

This site is located on Grant Point on the south shore of Izembek Lagoon. This site was reported in the

AHRS files as a number of Native house depressions in between a number of military depressions. A number of archaeologists have failed to find the Native depressions. We found a scatter of lithics,

including a number of stemmed projectiles, on the beach and bluff above the boat landing at Grant

Point. At present we are unsure of their association (from Klingler n.d.).

XCB-on

This site is located in the northwest corner of Big Lagoon above the north end ofMorzhovoi Bay. This site was recorded by the BIA ANCSA investigators as a small village site seen from a helicopter. We visited their map location in 1996 and found some disturbance vegetation and a lithic scatter on the beach. It was quite possible that they had identified XCB-103 (see below) but placed it nearly Y2 mile from its actual location.

XCB-073

This village site is located on the south side of a creek in Section 14 south of Norma Bay, Village. It

was recorded by the BIA from the helicopter. No other information is available.

XCB-074 through XCB-078

This is a string of house-depression sites along the north shore of Moffet Creek in east Moffet Lagoon.

This sites were found during pedestrian survey by the BIA ANCSA in 1979. These sites will be

mapped and tested by the University of Wisconsin in 1997.

169 XCB-120: SUMMARY orBIA ANCSA REPORT (BIA 1991:99-125)

The BIA mapped this selection as a complex of six sites (parcels A through F; Site PN 41/PN 42

(BLN AA 12259/AA 1226) which included XCB-003 and XCB-031. We have divided these six

parcels into five sites - XCB-003, XCB-031, XCB-120, XCB-121, and XCB-123 based on their

location and the distance between them.

XCB-120 is located 9km south-southeast of Cape Glazenap, in an unnamed cove in the southern

portion of Izembek Lagoon, just southwest of Applegate Cove. The cove is very shallow and muddy

with few channels. The air is foul smelling at low tide indicating organic rot and methane production.

The cove is fed by three major streams, the westernmost of which supports the largest run of salmon.

This site is located near the easternmost stream that discharges into the cove. The site is situated on a 2

m to 3 m high terrace on the edge of the present floodplain. A. wet tundra plant community lies to the north of the terrace, and a moist tundra community backs the site to the east. Thick lush grasses and

sedges grow along the shores of the cove and the floodplain of the creek. The site area is covered by lush grasses on the western end ofthe terrace and by more typical on site vegetation on the eastern portion. The site consists of 19 depressions in a small cluster (Figure 43).

170 XCB-120

I I o 30 I I 1".-.- i ,r meters I I • • grass ...... ",~J : I : disturbance I . I \ vegetation I I ,,I ,'" I I d wet tundra \ ... \ I .- I -- .-I '" ,,,---'"

Unnamed Cove N~

FIGURE 43: Map ofXCB-120 (adapted from US BIA 1991:111). XCB-121: SUMMARY orBIA ANCSA REPORT(BIA 1991:99-125)

The BIA mapped this selection as a complex of six sites (Parcels A through F; Site PN 41/PN 42

(BLN AA 12259/AA 1226) which included XCB-003 and XCB-031. We have divided these six

parcels into five sites - XCB-003, XCB-031, XCB-120, XCB-121, and XCB-123 based on their

location and the distance between them.

XCB-121 is located 9km south-southeast of Cape Glazenap, in an unnamed cove in the southern

portion of Izembek Lagoon, just southwest of Applegate Cove. The cove is very shallow and muddy

with few channels. The air is foul smelling at low tide indicating organic rot and methane production.

The cove is fed by three major streams, the westernmost of which supports the largest run of salmon.

- This site is on a 55m x 60m island, 10 m to 12 m above sea level, which forms the northeast margins ofthe cove. The island is connected to the mainland by a rocky seaweed covered ridge exposed at low

tide. The lower slopes of the island are grassy, and the upper slopes and the top are covered with

typical on site vegetation.

Another group of depressions is located on a point of land east of the island. The highest ground is a

northeast southwest oriented ridge with a primarily western aspect. The ridge parallels the shoreline

east of the cove and gradually slopes down toward the island. The slopes to the south comprise one - side of a swale that drains to the southwest. Typical on site vegetational communities are limited to the area of the point, which is backed on the east by moist tundra. Willows grow in small thickets inside

and outside the site area. The island contains five oval depressions and exposed surface artifacts. The

depressions and artifacts are all located on the top of the island, 10m to 12m above sea level. The

172 depressions were all over 4.0m in length, and all probably functioned as houses. The mainland area has

six small depressions (Figure 44).

In 1996 the University ofWisconsin visited this site to obtain a charcoal sample from the island. An

AMS date of AD 1025 (calibrated, see Table 4) was done on a charcoal sample from a house floor. -

173

Hi ), } "\ 1 } ,

XCB-121

Izembek Lagoon

a.• • N A

30 oe.-w- meters contours =1m

FIGURE 44: Map ofXCB-121 (adapted from US BIA 1991:109). XCB-123: SUMMARYofBIAANCSA REPORT(BIA 1991:99-/25)

The BIA mapped this selection as a complex of six sites (Parcels A through F; Site PN 41/PN 42

(BLN AA 12259/AA 1226) which included XCB-003 and XCB-031. We have divided these six parcels into five sites - XCB-003, XCB-031, XCB-120, XCB-121, and XCB-123 based on their location and the distance between them.

XCB-123 is located 9km south-southeast of Cape Glazenap, in an unnamed cove in the southern portion of Izembek Lagoon, just southwest of Applegate Cove. The cove is very shallow and muddy with few channels. The air is foul smelling at low tide indicating organic rot and methane production.

The cove is fed by three major streams, the westernmost of which supports the largest run of salmon.

This site is situated on a long prominent ridge, 10 m to 15 high, parallel and adjacent to the cove's southeastern shore. The ridge is part ofthe glacially derived coastal plain that descends from the base of Frosty Peak. Large patches of willow grove on the inland slopes and the crest of the ridge; many of these willow patches correspond with an apparent WW IT vintage road. The front of the ridge is vegetated by a dense growth of grasses, and the back is covered by moist tundra with scattered willow thickets. The site area has a lush dense growth of grasses, cow parsnip and other plants. The site has 71 surface depressions (Figure 45).

175 -

.' •...... XCB-123 willow"" .::.. :::-"

, I moist tundra

I \

\ \ ,, ••,.. ,, ,•••. , , t.. • \ , '.•, .. . , , . •'.- moist tundra , " . , . • , ••••, "' , '. - "'

, disturbance vegetation "' ,, , ••• "' , , , , , .... , , • Unnamed Cove , , , - , - • N •• ,.-• '. A "' ,

0 30 e , meters "'

FIGURE 45: Map ofXCB-123 (adapted from US BIA 1991:106-108). INVESTIGATIONS AT NEWLY RECORDED ARCHAEOLOGICAL SITES

XCB-079

In 1995, while surveying between Outer Marker Road and XCB-005, we found a few artifacts in the inter-tidal zone (net sinkers and chipped basalt lunate knives). The site is located on the south side of the channel that drains west from Outer Marker road, and about 300 meters from XCB-005.

~- XCB-080

This site was found while surveying the myriad ofchannels south and west of Grant Point. On a south-facing 3 meter bluff we found a single 5x5 meter depression and an area of"site" vegetation about 30 x 7 meters in extent. Inthe water below the bluff were a large number offlakes, retouched flakes, and bifaces. There is no active erosion.

XCB-081

This site is on a high terrace at the far western end of Kinzerof Lagoon. The site consists of47 house and cache depressions in a tight cluster (Figure 46). Some mussel midden was found in ground squirrel excavations. No artifacts were seen in the intertidal zone or along the bluff edge indicating that little erosion had occurred at this site.

177 XCB-081 • i - ,,- •• Marsh • •• • • I,. •• • ., .•.• -' • , e -e • -- • •• -- - , & • • • ~& , • ~ ~ • & ~ - ~N

-- 0 30 ~ I i meters contours = 2m

FIGURE 46: Map ofXCB-081.

.,.. w__------XCB-082

Located during the Kinzarof Lagoon survey of 1995, this site is located approximately 100 meters east ofXCB-021. The site has three house depressions along the edge ofthe bluff (lOx6, 5x3, and

6x6). There are two faint Ixl meter depressions adjacent to the 6x6 meter depression. The depressions are all somewhat disturbed by coastal but few cultural items were found (Figure 47).

There is an organic band with charcoal flecks that extends for over 100 meters along this erosion cut.

Clam shell midden was seen in two sections.

XCB-083

Located during the KinzarofLagoon survey of 1995, this site is located a few hundred meters west of the 1st Kinzarof Creek at the base ofa small hill and near a small pond. Three nuc1ues-satellite houses and a number ofsmaller depressions are located on a sandy but stable surface (Figure 48). A shovel test in the northern-most house reveled little stratigraphy but a dense midden composed primarily ofurchin.

179 Figure 47: not yet drafted.

180 XCB-083 • •

...... - ......

I 1 • 1 o.

\ [ dry pond basin j \

.' 1 .' . \ .'

o' o 30 e-- meters contours = 1m .~ . -....~..• , •

• 1 • , , • • • , •

FIGURE 48: Map ofXCB-083. -, XCB-084

Located during the Kinzarof Lagoon survey of 1995, this site is located approximately 30 meters

west ofthe 2nd Kinzarof Creek. The site consists of a single 3x3 meter depression in a broad area of

disturbance vegetation (Figure 49). There is an erosion surface along the beach from with flakes,

artifacts, and exposed mussel midden. Inthe erosion cut are a number ofliving surfaces extending - down to 1.5 meters. A chipped basalt lancolate end with facial polish was found here. The creek next to the site, although less than a meter wide, has a sizable red salmon run.

XCB-085

XCB-085 is located on the west side ofPaul Hansen Lake. This site consists ofa single sod-walled

historic cabin. No further investigations were done. - XCB-086

In 1995, while surveying between Paul Hansen Lake and the Joshua Green River, along the high

terrace edge that forms the west edge ofthe Joshua Green River Basin, a site with a single house

depression was found. The depression measures 12x8 meters with the short edge along the bluff. The

site has not been eroded or otherwise disturbed in any way. A single .5x.5 meter test was excavated

in the house floor. Less than .10 meters below surfaces an organically stained probable house floor

was found. Below the house floor was .25m of stained and mottled sandy silts. Charcoal flecks were

found throughout. No artifacts were found. -

182 -- XCB-084 N o 30 A ~.-wM i meters contours = 1m

- . .' - _., _.' - .' - -' Kinzarof Lagoon

FIGURE 49: Map ofXCB-084.

.ii4kU4#l XCB-087

1bis site was found on a survey ofthe east shore ofMoffet Lagoon. Four ofFive depressions were

found in a large area of disturbance vegetation. The site is between XCB-028 and a small marsh NW

ofXCB-028. A 70m erosion surface showed dense midden ofmussel, clam, urchin, caribou, sea lion,

otter, harbor seal, and many birds. 1bis site will be mapped and investigated further in 1997.

XCB-088

1bis site is east and across the 500 meter marsh from XCB-087 on the east shore ofMoffet Lagoon..

There are 5-6 houses and a few cache pits along the bluff edge. Few flakes or other artifacts were

found on an extensive erosion surface. The site was not mapped but will be further investigated in

1997. - XCB-089

While flying over Moffet Springs in 1995, this site was found at the head of Moffet Creek. We - identified two house depressions at the springs. These appeared to be shallow but clear and surrounded by disturbance vegetation. We will visit this site in 1997.

XCB-09l and XCB-092

Both ofthese sites were found seen during an aerial survey ofSwanson Lagoon on the northeast side - ofUnimak Island. Both have from 5-10 large house depression that are not ofthe nucleus-satellite variety.

184 XCB-093: Russell Creek Blowout Site

The Russell Creek Blowout Site was found by Jim Jordan on the north side ofRussell Creek approximately two miles from Cold Bay. The site is deep within an eroding dune complex that has also been used as a sand quarry. A scatter offlakes and a single stemmed projectile reminiscent ofthe early Aleutian Tradition were found on the dune surface. A thin charcoal layer was found at the base ofthe dune. While there are a number ofpaleosols in this sequence, none have any charcoal except the lowest, where it is quite dense and concentrated. Ifthe surface artifacts do indeed come from the charcoallense, this is the earliest site yet recorded on the lower end ofthe Alaska Peninsula dating to approximately 4000 BC (calibrated, see Table 4). 1997 research at this site will attempt to find in situ artifacts.

XCB-094

This site is located on the peninsula separating Middle and Big Lagoons on the north end of

Morzhovoi Bay. The site is situated on a complex of old beach ridges that is now approximately eight meters above the modem shoreline and nearly 100 meters inland. The site consists ofthree large house depressions and a number of small depressions that may be cache pits (Figure 50). The site faces south and has close access to both Middle and Big Lagoons and the large tide flat between them

Because ofthe sites proximity to our base camp, four test pits were excavated. Test 1 (lx1 meter) was placed in the center ofthe floor ofhouse 1. This unit revealed a humic layer over a layer of probably roof fall over a charcoal stained house floor and hearth. A number ofgriddle stones and fire-cracked rocks were found. Artificats from the house floor consisted offlakes. Many ofthe materials, unlike the rest ofthe region, were not basalt. These include obsidian and yellow chert. The

185 house floor was situated on clean dune sand. There was no organic preservation within the center of

the house. Since no whale bone was found, the house probably had a wood and sod superstructure

Test two (Ix1 meter) was done in the house 1 berm because we found small fragments ofmussel I~ shell in a ground squirrel burrow. Three distinct shell midden layers were found with fill ofsilty soil

and crushed shell between them (Figure 51). Dense quantities ofshell, mammal, bird, and fish were

found. All ofthese reflect a subsistence strategy based on the immediate vicinity. This also implies

that the salmon run in Middle Lagoon has been in place for some time.

Test three (.5 x .5 m) was done at the edge ofthe house 1 floor to see ifdeeper, intact floor deposits

might be present. Two deep, super-imposed floors were found separated by a thin layer ofsilt and - sand. Some shell midden was found in the lowest floor.

Test four (Ixl m) was excavated in the floor ofhouse two. While having a stratigraphy much like

that ofhouse 1, the house 2 floor was covered with burned timbers that clearly indicate the house was

destroyed. Some flakes from this floor have pot-lid fractures. The floor was covered in charcoal.

Lithics from these excavation units are predominately flakes from bifacial reduction. One small,

obsidian projectile tip was found in Test 3, no other stone artifacts were found. Bone artifacts from - Unit two include a awls and a caribou antler wedge.

Two radiocarbon dates were run on samples collected from this house, one from the floor ofhouse 1

and one from the house 1 berm midden. These dates place the site occupation between AD 1200 and

AD1350 (Table 4). This is one ofthe few sites that fall within the Big Lagoon phase and the best

186 investigated making it a very important early village site. All ofthe materials excavated from this site are currently under investigation.

lbis site is on lands owned by the Isanotski Corporation. There is no evidence ofrecreational excavation and the landform is not subject to erosion.

187 old lake outlet

old pond •• XCB-094

old lagoon • -- • .,eo • o e:. • - ~ i~~ • meters A contours = 1m [J Excavation Unit N - FIGURE 50: Map ofXCB-094. House Depression Floor

0.00 0.00 0.50 1.00 Beach grass, humus and roots.

Dark sUty sand. Part of rooffall. 0.25 Dark brown day. 760+/-40 - Charcoal stained house floor.

Clean dune sand.

0.50

House Depression Berm

0.00 °r·oo;;:,o~~:-~r---:3?:~~~~IiIl~~1 Sphagnum moss, roots.

Humus and roots.

Mussel midden (complete valves) with some clam, fire-cracked rock, 025 charcoal, dense fish bone.

Sand with scattered shell.

0.50 Mussel Midden (all crushed), also ~=-_------,- limpets, chitons, bamacles. Sea mammal, fish, and bird. Mixture of dune sand and scattered midden. Possible older house floor 1.00 present. ~, ~--I------Mussel and clam midden, many whole valves.

1.25 Clean dune sand.

1.50 ......

FIGURE 51: Stratigraphic profile oftest excavations done at XCB-094. XCB-095

This site is located on the east side ofthe peninsula separating Big and Middle Lagoons. Located on a high bluff, it looks out over a huge inter-tidal area at low tide and an area filled with seals and otter at high tide. We have no data to detennine the age ofthis site. The artifacts were found resting on gravels that were ofthe late ice-age, but they could have been anywhere in the dunes before the dunes were eroded away.

The site consists of 12 stone artifacts scattered across a large eroding dune field. These include one dart tip and 11 basalt flakes that resulted from the making of a stone tools. XCB-095 was probably used as a hunting camp or was a day use area for peoples living in XCB-096 or XCB-094.

There is no evidence that any portion ofthis site is intact. The site is on Isanotski Corporation lands.

There is no evidence ofmodern human activities at this location.

XCB-096

This site is located on the peninsula separating Middle and Big Lagoons on the north end of

Morzhovoi Bay. The site is on a high dune facing Big Lagoon and overlooking the large tide flat between Middle and Big Lagoons.

The site consists oftwo large house depressions with attached side rooms and a scatter of cache pits

(Figure 52). These are the kinds ofhouses we generally associate with the later prehistoric and historic Aleut ofthe region. Because ofthe location ofthe site and the style ofthe houses, we expect that this site dates to after AD 1550, in the Morzhovoi Phase.

190 1bree small test excavations reveal a thin house floor and a short occupation (Figure 53). The house floor and external midden are situated directly on sterile dune sand. Subsistence remains are dominated by species found in the tide flat below the site, especially urchins and mussels, but also include quantities ofsalmon.

The site is on lands owned by the Isanotski Corporation. 1bis site is on a stable, non-eroding dune and there is no evidence ofrecreational excavation.

191 XeS-Og6

- • - • - •

D Excavation Unit

meters contours = 2m Big Lagoon

- FIGURE 52: Map ofXCB-096. House Floor Test 00 ~~m:--0.50 0.000'1082800 Sod and humus.

Sterile dune sand.

0.25 Charcoal-based house floor.

Sterile dune sand. ~, 0.50 L......

External Cache Pit Test 0.00 0.50 0.00 Sod and humus.

Sterile dune sand. Brown sandy silt. Not cultural. 0.25 Sterile dune sand, some organics.

Dark, charcoal-based organic stain.

0.50 Midden with mussel, clam, fish, and caribou.

Sterile dune sand.

House Berm Test 0.00 0.50 0.00 Sod and humus.

Sterile dune sand.

Brown sandy silt. Not cultural. 0.25 Sterile dune sand, some organics. Dark, charcoal-based organic stain with fire-cracked rock, flakes, griddle stones. Sterile dune sand, some organics. Charcoal-based organic surface with 0.50 some shell, bone, and flakes. Sterile dune sand.

FIGURE 53: Stratigraphic profiles oftest excavations done at XCB-096.

------_...... _------_._------XCB-097

This site is located on the east side ofthe north-south channel that separates the two large areas of - Middle Lagoon. The channel is an excellent location to net salmon and this small village site was - probably placed here because ofthe salmon run.

The site consists of a number of small depressions that were either summer tents or large storage - facilities (Figure 54). This site is unusual because ofthe dispersed organization ofthe depressions. A single basalt flake was recovered from the beach in front ofthe site.

The site is on lands owned by the Isanotski Corporation. There is some active erosion occurring at

this site. There is no evidence ofrecreational digging.

XCB-098

This site is located on the east side ofthe north-south channel that separates the two large areas of - Middle Lagoon. The site has one probable house with attached side rooms indicating that it is ofthe late prehistoric - early historic Aleut style (Figure 55). This site is probably located here to take

advantage ofthe salmon run in the channel ofMiddle Lagoon. We have no further information on

this site. This site probably dates to the Morzhovoi Phase of occupation based on the form ofthe

house.

This site is on lands conveyed to the Isanotski Corporation. There is some active erosion at this

location but no evidence ofrecreational digging.

194 -- XCB-097 o 30 ~ ! I meters contours =1m • • • • • • • • •

• ' .••

Middle Lagoon

FIGURE 54: Map ofXCB-097. XeS-Og8 •

(!) ~ •

CI)8: - • - •

MIDDLE LAGOON

o 30 ~ Ii I meters contours = 2m ~N .-

,- FIGURE 55. Map ofXCB-098. -

- XCB-099

TIlis site is located on the west shore ofBig Lagoon and is situated on a ridge that separates Big

Lagoon from a small lake. Since there is currently no navigable water in this area of Big Lagoon, the sea-level must have been higher when this site was occupied.

The site consists oftwo large house depressions with unusually large, attached side rooms (Figure

56). These are the kinds ofhouses we generally associate with the later prehistoric and historic Aleut ofthe region. One ofthe houses has been partially destroyed by coastal erosion but few artifacts were found in the eroded area. -

A test (.5 x .5m) in one ofthe houses revealed a thick house floor (Figure 57). There are some midden deposits visible in the erosion bank and found in the test unit. Since only a few stone tools or flakes were found below the erosion surface, this site probably dates to the early historic period, the later part ofthe Morzhovoi Phase. A single c14 date of conf1fffiS this observation (Table 4).

TIlis site is on Isanotski Corporation lands. Itis in danger offurther erosion. There is no evidence of recreational excavation.

197 XCB-099

•

- • - ,1.• •• Big Lagoon e·••••

marsh

~ 0 30 ~ I - meters :t contours = 2m

FIGURE 56. Map ofXCB-099. -

House Floor Test o.ooO.lm'oo~~ 0.50 Sod and humus.

Typical roof fall, dense with organics and charcoal

025 Light Charcoal stain. ~, Charcoal-based house floor with shell and poorly preserved fish bone. Compacted silty soil with charcoal and flakes. Grey ash. Medium brown sandy loam. 0.50 ~------... FIGURE 57: Stratigraphic profile oftest excavations done at XCB-099.

~{' - XCB-lOO 'This site is a lithic scatter on the tip ofthe large dune formation that forms the outer mouth ofMiddle

Lagoon. Ina number of areas the dunes have been eroded to reveal a gravel and silt glacial period

..... surface. Inthis area a number of stone tools and flakes from the manufacture of stone tools were found on the surface. No other cultural remains were found. The tools may represent a number of

different periods ofuse for this region.

It is quite probable that this area was used many times as a temporary camp, a hunting look out for

sea mammals in Morzhovoi Bay, or for other special purpose activities. At present we have no

possible means for dating this site as it is completely destroyed from the erosion ofthe dune fields.

'This site is on lands conveyed to the Isanotski Corporation. Since there is no apparent in situ deposit,

there is no possibly offuture damage to this location through natural or cultural processes.

XCB-lOI

This is a village site on a high dune east ofthe mouth ofLittle Lagoon at the head ofMorzhovoi Bay.

'This site is different in that although it is a big house with attached rooms as we have seen elsewhere,

the rooms are of odd shapes (Figure 58). Further, these sites usually date to the very recent past while

this site is nearly 2000 years old (Table 4).

A single test revealed three thin, charcoal-based house floors separated by clean dune sand indicating - that this house was only used periodically (Figure 59). We have no other information about this village.

200 XCB-101 N~

~ .• • •

o 30 ~...._~~I meters contours =2m

FIGURE 58: Map ofXCB-lO1. -

- House Floor Test 0.00°·00 0.50 Sod and humus.

- Dune sand.

Charcoal-based house floor. 0.25 Dune sand. Charcoal-based house floor.

Dune sand.

Charcoal-based house floor. 0.50

--- Clay and silt loam. Not clear if it is sterile. no charcoal, some pebbles.

0.75

FIGURE 59: Stratigraphic profile oftest excavations done at XCB-IOl.

- XCB -102 (Big Lagoon Cabin No. 1)

TIlls site is located at the northeast corner ofBig Lagoon. The site consists ofa sod-walled cabin, a historic cabin depression, and numerous artifacts ofthe 1920s to 1950s including bottles and metal.

XCB-I03: Dark Side ofthe Lagoon

TIlls is a large village site spread along a 30 meter bluff edge on the northeast shore ofBig Lagoon.

The site has 56 depression ranging from 1.0 to 60 square meters (Figure 60). The houses on the east end ofthe site are in moss and tundra that becomes grass towards the center ofthe site and then grass mixed with cow parsnip and more traditional "site" vegetation on the west end.

A single 1.0 x .60 meter test revealed .80 meters ofbedded house floors, all covered with red ochre.

Dense quantities ofbasalt flakes and stemmed projectiles were found. Dozens oflarge basalt flakes, retouched artifacts, and bifaces were found on the beach in front ofthe bluff. There is no active disturbance or erosion but ample evidence that erosion occurred at this site some time in the past. A

single AMS date places this site occupation around 600 BC (Table 4). ~I

203 1 1 1 1 1 1 1

• • •

•• • .•" . •• marsh •

meters XCB-103 contours = 2m

FIGURE 60: Map ofXCB-103, Dark Side ofthe Lagoon. XCB-l04

This is a village site on the east shore ofthe upper section ofMiddle Lagoon; The village is located on a low hill overlooking Middle Lagoon. The site consists of a number ofsmall houses in a loose cluster (Figure 61) and dates to approximately AD 750, in the Middle ofthe Izembek Phase (Table

5). The house size and village organization are similar to villages dating in the same time period elsewhere onthe lower Alaska Peninsula.

The site was probably positioned to take advantage ofthe Middle Lagoon salmon run. The many small depressions at this site are probably cache pits used to store salmon while a few are clearly houses although it is difficult to determine ifthey were winter houses or summer tents. A single test excavation revealed two house floor separated by what may be fill from a roof fall (Figure 62).

XCB-l05: Adamagan

This is a large village site that was found during survey on the west side ofBig Lagoon. The site is on a number oflow hills that form the north edge of a marsh that extends from the northwest comer of Big Lagoon to Morzhovoi Lake. During a briefreconnaissance ofthe site 400 depressions were counted, at least five ofwhich were nucleus-satellite houses. This site will be mapped and tested in

1997.

205 XCB-104

-• marsh \, .. \ . ' ,

\ _. , , \, .. , ~ Middle Lagoon , , .... .- , , , : , •

I I _e· r I , I , •• , • ,, ,, ,I ,J • marsh , I

I I - I, \, , '" , , A , , N '" '" , contours = 2m ~_iiiiiii~~''~'3Y __ .. __ .. __ .. __ .. __ .. __ .. __ .. __ .. __ .. __ . meters .-- .. --.

FIGURE 61: Map ofXCB-104. House Floor Test 0.000.00 ~RO.50 ~~~ 7TI Sodandhumua Brown sandy loam, rich in organics and roots.

Gret sandy silt. May be a tephra.

25 0. IJ·.· ••• ••• ••· ••••···•• •• •••••••••••••••••••• I Medium brown sandy silt.

Charcoal-based house floor. 0.50 Mixed sand and gravel, charcoal, flakes, some red ochre. Charcoal-based house floor, crusted and compacted.

Glacial surface with unsorted sand and gravel.

0.75

FIGURE 62: Stratigraphic profile oftest excavations done at XCB-I04. XCB-106, Big Lagoon Cabin #2 and XCB-l07, Big Lagoon Cabin #3

These two cabins are on the south and north points ofa small cove on the northwest comer of Big

Lagoon. Both are sod-walled. No surface artifacts were seen. Neither house was mapped due to time

constraints.

XCB-I08

This is a small camp that was probably associated with salmon fishing. The site consists on three

small cache pits on a point extending from the west shore ofMiddle Lagoon (Figure 63). There are a

number ofbasalt knives and other tools on the beach that were probably used for processing salmon.

Any area oflush vegetation indicates the total area that was used by the people living here. We have

no dates or other information on this site although the elevation ofthe site above the lagoon indicates

that it dates to the last 1000 years.

XCB-109

This is a small site on the upper end ofMiddle Lagoon that probably served as a camp or small

village (Figure 64). Notched stones or net sinkers in the inter-tidal zone attest to this site's use for

salmon fishing. No further investigations were done.

208 - xeS-10B

~( \ N \

J J grassland

Middle Lagoon

artifact concentration on the beach.

rocky ~ .. ~, point .".

terrace edge <2m above beach. Middle Lagoon ~

, J

I J

J J o 30

grassland J ~ _-~I I ... , meters I contours =1m ~,

FIGURE 63: Map ofXCB-108. .I

I • I, XCB-109 •, , I

I - I

I I

I Middle Lagoon I

\ \

\ , ., , , , , • , , , - ... , \

I • -e I I I ;f , , , , ,, , , ,, Middle Lagoon ,, , I , I

I I meters J

I contours =2m I

FIGURE 64: Map ofXCB-I09.

- XCB-110

This site is a large village on the south shore ofthe upper portion ofMiddle Lagoon. The site consists of55 house and cache depressions scattered along the 6 meter bluff edge (Figure 65). There is a low marsh that separates the bluff from upper Middle Lagoon. A spring leaves the bluff in the middle ofthe site with a small channel extending through the marsh. The surface topography ofthe site is hummocky with scattered patches of "site" vegetation.

A number ofnotched stones or net sinkers were found along the shore and on the site verifying that this location was probably used for salmon fishing. A single test unit revealed numerous bedded house floors extending to glacial gravel approximately 1.0 meters below surface. The house floors that are identified by dark-stained soil, dense charcoal, and red ochre fragments and stains (Figure

66).

This is one ofthe earliest villages inthe region with dates older than 1700 BC (Table 4). This is either one ofthe largest Moffet Phase villages in the region or the smallest ofthe Kinzarof Phase villages as the date ofthe transition is unknown. The houses appear both clumped at the west end

(like the Moffet Phase) and spread along the bluff edge on the east end (like the Kinzarof Phase).

211 •• XCB-110 -.. marsh • • ..... - • ..

Middle Lagoon ••• 1 40 meters ~I---- •• • •• ~•.. • marsh • . c.·• •• ..••• •, ..el···.-.•. _ • •

o 30 _.~.!iil5-iiiiiiii~~~ . .. l::J!I!II- , meters • contours =2m FIGURE 65: Map ofXCB-llO. House Floor Test

0.000.00 0.50 Sod and roots, grasses.

Humus

0.25 Highly organic silty loam. Possible room fall.

Charcoal-based house floor. Brown silty loam. Charcoal-based house floor. Charcoal-based house floor. 0.50 Brown to yellow-brown compacted sand and gravel. Dense charcoal. Charcoal-based house floor.

Brown to yellow-brown compacted sand and gravel. Dense charcoal. Thin charcoal bands and staining.

0.75 Charcoal-based house floor. Compacted sand and gravel. Probably glacial. Griddle stone.

FIGURE 66: Stratigraphic profile oftest excavations done at XCB-II0.

------_...... _---...... _------~----~- XCB-1l1 andXCB-1l2

During a tour ofMorzhovoi Bay we stopped at a large stream entering the southwest part ofthe bay

from the southwest. Two massive ridges that may be Holocene end moraines block the valley on - either side ofthe creek. There is a site on both sides. The site on the north, XCB-111, consists of three approximately 4x5m depressions and 12 smaller depressions. XCB-112 on the south side ofthe

creek consists of a 12x6 meter house with 6 satellites, a 12x6 meter depression with no satellites, a

3x3 meter depression and 3 1x1m depressions. These sites were not mapped or investigated indetail.

XCB-113

On the west side ofthe complex ofchannels forming grant point, a small village site was found

above a small lake and next to Applegate Cove. The site consists of 17 depressions in a small cluster

(Figure 67). A number of flakes and artifacts were found on the beach. This site will be further

investigated in 1997.

XCB-114

A number oflithic scatters, mostly intertidal, were found along the shores ofthe small islets that

make up the Cove Island group in Applegate Cove west of Grant Point. XCB-114 is located on the

island south ofCove Island (connected at low tide) on a north-facing point. The site consists of an

intertidal lithic scatter. No cultural remains were found on the bluff above.

214 XCB-113

o 30 ~----- ._~ meters ------

contours =2m

• • dry tundra • • •• • • • • •, •

FIGURE 67: Map of XCB-l13.

'jt XCB-115

This site is located on a south-facing bluff overlooking Cold Bay. The site is exposed in the side-wall

of a road cut that leads to Swan Lake west ofthe town ofCold Bay. There are no surface indications

and the vegetation is inconspicuous. Approximately 1.25 meters below surface a charcoal crusted

and stained floor was found with red ochre, a scatter ofbasalt flakes, and a few artifacts. A single

AMS date on this site places it at the beginning ofthe Early Izembek Phase (Table 4).

XCB-116

A number oflithic scatters, mostly intertidal, were found along the shores ofthe small islets that

make up the Cove Island group in Applegate Cove west of Grant Point. XCB-116 is located on the

island south ofCove Island (connected at low tide) on an east-facing point. The site consists of an

intertidal lithic scatter with a number oflarge artifacts made ofbasalt. No cultural remains were

found on the bluff above.

XCB-117

A number oflithic scatters, mostly intertidal, were found along the shores ofthe small islets that

make up the Cove Island group in Applegate Cove west of Grant Point. XCB-117 is located on the

south side of a small island north ofCove Island. The site consists of two lxl meters depressions

and a few flakes in the intertidal zone. A soil probe placed in one ofthe depressions recovered flecks

ofcharcoal .35m below surface.

216

____~ " __" w " -- ,------'------...... ------XCB-1l8

A number oflithic scatters, mostly intertidal, were found along the shores ofthe small islets that make up the Cove Island group in Applegate Cove west ofGrant Point. The site is located on a northwest facing beach on a very small and uncharted islet northwest of Cove Island. The site consists of a number ofbasalt flakes and artifacts in the intertidal zone. The scatter extends over a

20x5 meter area. There were no indications ofcultural material on the island above the site.

XCB-1l9

On the last day ofinvestigations on the Bering Sea shore near Morzhovoi Lake a small crew found a village site with 25 depressions including at least two nucleus-satellite houses. The site is situated in the dunes between the Bering Sea and the northeast comer ofthe lake. This site will be mapped in

1997.

XCB-122

This is a site ofseveral large, oval, house depressions at the back of the abandoned beach ridges that form the tip ofCape Glazenap. This site was discovered in 1988 by Brian Hoffman while the BIA crew was working in that area. The site had never been formally documented. We will map and visit this site in 1997.

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