NPS Form 10-900-b 0MB Wo. 1024-0018 (Jan. 1987) United States Department of the Interior National Park Service National Register of Historic Places Multiple Property Documentation Form This form is for use in documenting multiple property groups relating to one or several historic contexts. See instructions in Guidelines for Completing National Register Forms (National Register Bulletin 16). Complete each item by marking "x" in the appropriate box or by entering the requested information. For additional space use continuation sheets (Form 10-900-a). Type all entries. A. Name of Multiple Property Listing Androscoggin River Drainage Prehistoric Sites_____________________ B. Associated Historic Contexts ~~ Early and Middle Archaic Susquehanna Tradition Ceramic Period Early Contact Period C. Geographical Data The Androscoggin River Drainage Prehistoric Sites multiple property document encompasses those prehistoric sites located See continuation sheet D. Certification As the designated authority under the National Historic Preservation Act of 1966, as amended, I hereby certify that this documentation form meets the National Register documentation standards and sets forth requirements for the listing of related properties consistent with the National Register criteria. This submission meets the procedural and professional requirements set forth [oJ36 CFR Part 60 and the Secretary of the Interior's Standards for Planning and,Evaluation. Signature of certifying official Maine Historic Preservation ssion State or Federal agency and bureau I, hereby, certify that this multiple property documentation form has been approved by the National Register as a basis for evaluating related properties for listing in the National Register. Signature/jf the Keeper of the National Register Date NP8 Form 10-900* OMBAppmnlNo. 10240018 (we) United States Department of the Interior National Park Service Section number The local bedrock geology includes predominant pelite and interbedded pelite and sandstone of the Carrabassett and Seboomook formations, respectively. The precipitous drop at Rumford Falls lies along the boundary of the intrusive Littleton formation which is a muscovite-biotite granite and tonalite combination. Other bedrock attributable to the Hildreth formation and the Perry Mountain formation lies nearby the project area. These latter formations consist of interbedded pelite, sandstone,a nd limestone (and/or dolostone) and interbedded pelite and sandstone, respectively (Osbert et al 1985). NP8 Form 104004 0MB Approvtd No. 10240018 United States Department of the Interior National Park Service National Register of Historic Places Continuation Sheet Section number c Page 3 Surficial deposits in the river valley include predominant Holocene alluvium, that is, sediment deposited in the past 10,000 years after the late Pleistocene glaciation. However, late glacial sediments are specifically present in the Logan Brook area where glacial lake sediments include some combination of silt, clay, and sand. Other limited deposits of ice contact glaciofluvial deposits, including sand, gravel, and silt, are present on the north side of the project area near Rumford Center. Glacial outwash deposits are present in the Split Brook area to the northwest of Rumford Center. The local area beyond the river valley is clearly dominated by late Pleistocene glacial till which covers nearly all areas above the modern floodplain (Thompson and Borns 1984). This area was free of glacial ice by ca. 13,000- 12,000 B.P. The late marine invasion that covered a large portion of Maine during this general period did not reach the Rumford area since it only extended to the area around Jay in the Androscoggin River drainage. The general climate in the Rumford area is typically cold during the long winters and mild in the summer; the northern climatic division for Maine encompasses the project area. The average annual temperature is 39° F; the January and July averages are 10° and 64° F, respectively. The average annual precipitation is 92.7 cm (36.5 in) and snowfall averages 259 cm (102 in) each year. Frost-free days average 111 in the northern region. Local biotic communities exist near the boundary of the Transition Hardwoods-White Pine-Hemlock and Northern Hardwoods-Hemlock-White Pine vegetation zones, while the Spruce-Fir-Northern Hardwoods zone lies nearby in higher elevations to the north and west. The Transition Hardwoods zone fosters a dominant combination of beech, yellow birch, white birch, aspen, red maple, and sugar maple, with white pine and hemlock predominant among the conifers. Beech, yellow birch, sugar maple, and red maple dominate in the less diverse Northern Hardwoods-Hemlock-White Pine zone, with lesser amounts of hemlock and white pine present, as the name implies. Game species in both zones would include a variety of large mammals, such as white-tailed deer, moose, woodland caribou, and black bear, and a variety of smaller species. The Spruce-Fir-Northern Hardwoods zone is characterized by a still more reduced number of species, typically including predominant spruce and balsam fir, with lesser amounts of the hardwoods enumerated above. Typical game species would include those mentioned above, but the more northerly species (e.g., moose and caribou) would have been favored (Westveld et al 1956). The evolutionary development of local and regional biota was undoubtedly of some importance to human populations during the Holocene epoch. Conditions have varied from tundra and spruce-fir parkland soon after deglaciation in the late Pleistocene to about 9500 B.P. (7500 B.C.), to mixed NP8 Form 10-800* OMB Approve Mo. 1024-0018 United States Department of the Interior National Park Service National Register of Historic Places Continuation Sheet Section number c Rage 4 hardwood-conifer forests during postglacial climatic optimum, ca. 7500 B.P. (5500 B. C.) to 4500 or 4000 B.P. (2500-2000 B. C.). Near-modern conditions were established thereafter, with an increase in conifers from 2000 B.P., as cooler conditions prevailed (Bradstreet and Davis 1975; Davis el al 1980). Faunal communities have also unquestionably changed during the Holocene, such as the impediment of the annual salmon spawning run by man-made dams downstream from Rumford Falls, which has occurred in the very recent past. Of note, seasonal concentrations of Atlantic Salmon and other Anadromous fish species once reached Rumford Falls which was the limit of their annual spawning run up the Androscoggin River. Gulf Island Area Topography within the Gulf Island area ranges from low elevations of 63 m (206.6 ft) a.m.s.l. on the river in the Deer Rips head pond and from 80 m (262.4 ft) a.m.s.l. on the river in the Gulf Island head pond up to elevation limits of 83 m (270 ft) a.m.s.l. Local topography includes Sand Hill at 127 m (416 ft) a.m.s.l. and Clark Mountain at 221 m (725 ft) a.m.s.l. directly to the west of the area and Merril Hill at 215 m (705 ft) a.m.s.l. near the northeastern boundary of the area. Much higher ground exists along the southern flank of the Appalachian Mountains on Singepole Mountain at 430 m (1,370 ft) a.m.s.l. which lies 45 km northwest of the southern portion of the project area. The local bedrock geology is of Devonian and Silurian age in the immediate area. Bedrock of the Sangerville formation and Patch Mountain members exists throughout the length of the area. These are of Silurian age and include interbedded pelite and limestone and/or dolostone. An intrusive formation of Devonian age is present in the central portion of the area. This formation is composed of muscovite and biotite-rich granite (Osberg et al. 1985). Surficial deposits throughout the immediate project area include Holocene stream alluvium in the form of floodplains and stream terraces. Underlying much of this recent deposition in the southern and northern portions of the project area are fine-grained glacio-marine deposits of sand and silt with some clay and minor amounts of gravel. These sediments were deposited during the late glacial marine submergence of the area, and are largely glacial sediments which accumulated on this one-time ocean floor. In the central portion of the area a thin till drift is present. It is a heterogeneous mixture of sand, silt, clay, and cobbles directly deposited by glacial ice (Thompson and Borns 1984). This area was clear of late Pleistocene continental ice between 14,000 B.P. (12,000 B.C.) and 13,000 B.P. NP8 Form 10-900* 0MB Apprwul No. 10244018 United States Department of the Interior National Park Service National Register of Historic Places Continuation Sheet Section number c. Page 5 (11,000 B.C.)» The late Pleistocene marine invasion, which covered much of Maine immediately thereafter, reached this locale. The northern end of the Gulf Island area lies within 5 km (8 mi) of the northern extent of the marine invasion (Stuiver and Borns 1975). Local biotic communities in the study area fall within the Transition Hardwoods - White Pine - Hemlock vegetation zone. The Transition Hardwoods zone fosters a dominant combination of beech, yellow birch, white birch, aspen, red maple, and sugar maple, with white pine and hemlock predominant among the conifers. E. Statement of Historic Contexts Discuss each historic context listed in Section B. The Early and Middle Archaic context begins on this page. The Susquehanna, Ceramic and Early Contact contexts begin on pages E14, E35 and E64 respectively. In each context, an Evaluation section which specifies minimum criteria for site significance, is placed 2-3 pages from the end. EARLY AND MIDDLE ARCHAIC CONTEXT Nomination Version, May 1991 Introduction The Early and Middle Archaic Context includes the time from roughly 10,000 B.P. to 6000 B.P. The respective Early and Middle Archaic Periods are arbitrarily divided at 8000 B.P. in most chronological schemes applicable to the Northeast.