State of Alaska > Natural Resources > Parks and Outdoor Recreation > History and Archaeology
J. David McMahan
Location and Physiography
Sitka is located on the west coast of Baranof Island, one of the largest of the numerous islands that comprise the Alexander Archipelago of southeastern Alaska. Baranof Island extends some 105 miles between Peril Strait to the north and Christian Sound to the south. It is bordered on the east by Chatham Straight and on the west by the Pacific Ocean. Although Sitka is located on the outer coast, the community is sheltered from the direct impact of storms by Kruzof Island and several smaller islands to the north and west (Figure 2). These islands form the north and west sides of Sitka Sound.
Physiographically, Baranof Island is within the Chilkat-Baranof Mountains Section of the Pacific Border Ranges Province (Wahrhaftig 1965:42). This province consists of several mountain ranges along the Pacific Coast, along with an adjacent coastal shelf. The Chilkat-Baranof Mountains Section, a highland of diversified topography, has been subdivided into four subsections: the Alsek Ranges, Glacier Bay, Chichagof Highland, and Baranof Mountains. Sitka is located in the Baranof Mountains subsection, a rugged asymmetric chain 3,000-5,300 feet in altitude, having a steep eastern slope and a more gentle southwest slope deeply indented by fiords (Wahrhaftig 1965:42). Drainage in this subsection is via short, swift streams that flow directly to the ocean. Indian River, which flows into Sitka Sound between Crescent and Jamestown Bays, drains a watershed of about 12.6 square miles (SNHP 1998:101). This small river, which originates in the mountains of central Baranof Island, is the largest freshwater stream in the community of Sitka. Cirque glaciers and small icefields are located on mountains higher than 4,500 feet on Baranof Island. Permafrost is nonexistent.
Castle Hill, strategically overlooking Sitka Sound, has long been a defining landmark of the local landscape. This majestic 60-foot-high promontory is a rocky headland typical of the erosional landforms which characterize coastal southeast Alaska. Formed by differential weathering of geologic strata by wave action, it was once cut off from the mainland by the highest tides. Due to filling and parking lot construction around the base of the hill in the 1960s, and the construction of a towering bridge to Japonski Island around 1970, the hill has lost much of its dramatic appearance. However, it remains a popular overlook for viewing Sitka Sound and the town of Sitka (Figure 3).
Geology and Soils
Geological survey and mapping of northern Baranof Island in the early 1960s has provided baseline data on the type, age, and stratigraphy of rock formations in the vicinity of Sitka (Berg and Hinckley 1963; Loney, et. al. 1964). Such mapping is useful to archaeologists attempting to identify source materials available for tool manufacture by pre-contact inhabitants of the area. Geologic deposits in the region are believed, based on correlations with adjacent areas, to range in age from Paleozoic to Mesozoic (Berg and Hinckley 1963:01). The strata are tightly folded, intricately faulted, and regionally metamorphosed. Bedded gneiss and schist predominate along the shore of Peril Strait. Dark-green and dark-gray amphibole-rich rocks, interlayered with metachert and subordinate marble, form a northwest-trending belt about a mile wide along the southwest coast of Catherine Island, Dead Tree Island, and part of the southwest shore of Portage Arm (ibid:3-5). A geologic complex termed the Nakwasina Group, comprised primarily of metachert, volcanic rocks, and greenstone, outcrops along a portion of the western shore of northern Baranof Island (ibid:6-9). Another geologic complex, termed the Kelp Bay Group, is widespread on northern Baranof Island, forming the shoreline from north of Rodman Bay to Kasnyku Bay and from Louise Cove to north of the mouth of St. John Baptist Bay (ibid:10). This group is mostly comprised of fine-grained thin- to medium-bedded rocks that include fissile quartzose greenschist and phyllite, graywacke, slate and sheared conglomerate, calcareous and quartzose slate with scattered lenses of metachert and volcanic rock, and granular moderately platy siliceous greenschist interbedded with jasper or slate and argillite lenses (ibid). Mesozoic age outcrops in the immediate vicinity of Sitka, probably including Castle Hill, have been termed the Sitka Group by Berg and Hinckley (1963:12-14). The Sitka group consists of a thick sequence of slate, graywacke, and conglomerate that crops out from Old Sitka (6 miles north of Sitka) southeastward to Silver Bay and makes up many of the smaller islands near Sitka. Principal rock types of this group are "thin- to medium-bedded interstratified graywacke and argillite and slaty argillite" (ibid:13). Conspicuous outcrops from Old Sitka to Sitka are comprised of beds of massive graywacke, conglomerate, and breccia as much as 50 feet thick. Overlying the Sitka Group on the south half of Kruzof Island are post-glacial basaltic and andesitic lava and pyroclastic debris from Mount Edgecumbe (ibid:14-15).
Overlying the bedrock on northern Baranof Island are unconsolidated deposits of alluvium, glacial debris, and volcanic ash. In Sitka, the Indian River delta and much of Sitka National Historical Park is comprised of alluvium that has been reworked by marine processes (SNHP 1998:100). Regional uplift has occurred over the last 9,000 years due to isostatic rebound, tectonic forces, and compression of crustal plates (ibid:100-101). This, coupled with local volcanic activity or earthquakes, has resulted in the uplift of the Indian River delta along with beaches, flood plains, and abandoned channels (Chaney, Betts, and Longenbaugh 1995). Land in the Sitka area is now rising at a rate of approximately 0.12 inches (0.3 cm) per year (SNHP 1998:101).
Soil development in southeast Alaska has been influenced by climate, topography, parent material, drainage, organisms, and time. They are typically classified as spodosols. Soils around Sitka have been classified by Rieger et al. (1979:152-154) as "typic cryohumods, loamy, hilly to steep humic cryorthods, very gravelly, hilly to steep." This soil association is found on steep hills in areas that are largely covered by volcanic ash from Mt. Edgecumbe (ibid). The ash is many feet thick in lower areas, where it overlies glacial till, but is thinner on higher slopes due to erosion. During the 1995 testing program on top of Castle Hill, stratified soils believed to be of volcanic origin were identified below cultural deposits. Soils on and around Castle Hill consist largely of organic-enriched cultural deposits. It appears that reworked cultural soils were moved from the slopes to the top of the hill during construction of the agricultural research building in 1898. In some areas, these overlie primary cultural deposits and preserved volcanic soils. Considerable variation occurs across the top of the hill, however, where cultural deposits rest directly on the high points of undulating bedrock in some locations. On the natural terrace near the southeast base of the hill, where intensive archaeological investigation occurred, highly organic cultural deposits were underlain directly by sterile gravels. These probably date from the end of the Pleistocene (i.e., around 8,000 to 10,000 years ago), when sea levels ranged up to 15 meters higher along the Pacific Northwest coast than at present (Clague et al. 1982; Swanston 1967).
Baranof Island is within a Western hemlock Sitka spruce (Picea sitchensis Tsuga heterophylla) forest ecosystem (Viereck and Little 1972:detached map; Viereck and Dyrness 1980; Viereck, et al. 1982). This is the coastal temperate, closed-canopy rainforest that is typical of southeast Alaska. Understory components include: blueberry/huckleberry (Vaccinium spp.) thickets, devils club (Oplopanax horridum), skunk cabbage (Symplocarppus foetidus), dwarf dogwood (Cornus canadensis), watermelon berry (Streptopus amplexifolius), and ferns. Disturbed areas support a dense growth of alder (Alnus spp.) and wild celery (Heracleum lenatum). A more complete list of understory plants is presented in Table 1. Due to extensive clearing and logging in the 19th and 20th centuries, few areas of old growth forest are preserved around Sitka. Some of the largest trees in the area are found in the northeast corner of Sitka National Historical Park, where scattered stumps provide evidence of only selective logging (SNHP 1998:103). Old growth characteristics in this area include multiple canopy layers, trees of varying diameters, dead standing trees, and woody debris (ibid). Because this area was once used as an artillery target range by the U.S. military, loggers may have avoided extensive timber harvest due to the potential for sawmill damage by the shrapnel said to be imbedded in the trees (Joe Ashby, personal communication 1997). Descriptions of the original old growth forest are provided in early 19th century descriptions by visitors to Sitka, such as the account which resulted from naturalist Baron von Kittlitzs 1827 visit:
Table 2.1. Common understory plants of Alaskan hemlock-spruce forests.
The present second growth forests around Sitka are the product of extensive logging throughout the 19th and 20th centuries. Evenby 1827, Kittlitz (1987:132) noted that the best trees had been "felled long ago for building purposes." Following the founding of New Archangel, Baranov attempted to burn the surrounding forests which provided ambush locations for the Tlingit, but his efforts were largely unsuccessful due to the dampness (Litke 1987:45). Extensive timber harvest for buildings, ships, firewood, and charcoal continued throughout the Russian occupancy of Sitka. Rakestraw (1981:4), in writing a history of the U.S. Forest Service in Alaska, noted that yellow-cedar ( Chamaecypari nootkatensis) was depleted around Sitka, but that impacts to Alaska forests in general were insignificant. The most significant impacts to old growth forests around Sitka occurred with the development of technology which allowed widespread clear-cutting, the development of logging into a major regional industry, and the construction of a large sawmill and pulp mill at Sitka during the 1950s.
Important terrestrial mammals of the Coastal Western HemlockSitka Spruce forest community include masked shrew, dusky shrew, little brown bat, red squirrel, northern flying squirrel, deer mouse, red-backed vole, long-tailed vole, porcupine, gray wolf, black bear, brown bear, pine marten, ermine, wolverine, lynx, Sitka black-tailed deer, and mountain goat (Selkregg 1976:128). Important species of the freshwater community include water shrew, beaver, northern bog lemming, tundra vole, muskrat, mink, and river otter (Selkregg 1976:138). Major marine mammal species in Sitka Sound include harbor seal, sea otter, sea lion, and several species of whale (Selkregg 1976:134, Figure 130). A more complete list of marine species in the southeast Alaska region is presented in Table 2. Birds associated with southeast Alaska coastal forests include goshawk, sharp-shinned hawk, bald eagle, blue grouse, great horned owl, rufous hummingbird, hairy woodpecker, downy woodpecker, western flycatcher, Stellers jay, common raven, chestnut-backed chickadee, winter wren, varied thrush, hermit thrush, golden-crowned kinglet, ruby-crowned kinglet, Townsends warbler, pine grosbeak, and pine siskin (Selkregg 1976:128). Several high density areas for waterfowl occur within Sitka Sound (Selkregg 1976:134, Figure 130). The numerous waterfowl species are included in Table 2. Saltwater and anadromous fish of the region include walleye pollock, Pacific cod, sablefish, Pacific pomfret, Pacific herring, albacore, sockeye (red) salmon, coho (silver) salmon, chinook (king) salmon, chum (dog) salmon, pink (humpback) salmon, steelhead trout, black rockfish, Pacific ocean perch, eulachon, sculpins, halibut and other flatfishes, and salmon shark (Selkregg 1976:136). Freshwater fish (excluding the anadromous fish reported above) include cutthroat trout, rainbow/steelhead trout, dolly varden char, sculpins, and northern pike (Selkregg 1976:138). Locally, pink and chum salmon spawn in the intertidal and lower floodplain portions of Indian River from mid-July through September, while coho salmon, steelhead trout, and dolly varden char migrate upstream (SNHP 1998:104).
It was the abundance of fur-bearing mammals, particularly the large sea otter populations, which prompted Russian exploration and settlement along the North Pacific coast. Shortly after the founding of New Archangel, Langsdorff (1993:57-61) described some of the more important land mammals, sea mammals, birds, and marine resources of the region:
Table 2.2. Marine species of the southeast Alaska region.
The naturalist von Kittlitz (1987:132-148), who visited Sitka in 1827, also described the birds and fish of the region in some detail. By that time, he reports that the economically important sea otter was already disappearing due to harvesting for trade (ibid:145).
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