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Pdf/83/8/2397/3443198/I0016-7606-83-8-2397.Pdf by Guest on 02 October 2021 2398 GREELEY and HYDE RONALD GREELEY Space Science Division, Ames Research Center, National Aeronautics and Space Administration, Mqffel Field, California 94035 JACK H. HYDE U.S. Geological Survey and Tacoma Community College, Tacoma, Washington 98465 Lava Tubes of the Cave Basalt, Mount St Helens, Washington ABSTRACT tumuli of the Cave Basalt collapsed, probably as a result of withdrawal of supporting lava The Cave Basalt, a high-alumina pahoehoe during drainage of the lava tubes. Raised-rim flow containing numerous lava tubes, originated craters found in many parts of the flow are at the southeast flank of Mount St. Helens, associated with lava tubes and were probably southwestern Washington, and flowed down a formed by collapse of hollow tumuli. stream valley incised in older pyroclastic flow deposits. In situ charcoal samples from two INTRODUCTION localities within lava tubes yield C14 dates of Abundant volcanic structures seen on high- 1,860 + 250 years B.P. and 1,925 + 95 years resolution pictures of the Moon and Mars, and B.P. Detailed survey of 9,125 m of lava tubes, the returned Apollo lunar samples showing correlated with surface geologic mapping, basaltic composition for mare surfaces have yields several geomorphic relations of basalt prompted interest in volcanic landforms as flows. Most of the lava tubes apparently formed analogs to lunar and planetary surface features. between shear planes in laminar lava flow, al- Volcanic geomorphology has been little studied though some tube sections show evidence that recently, particularly in relation to basalt flow the tube roof formed by accretion of spattered surface features. The existence of lunar lava lava in turbulent flow. Partial collapse of tube tubes and channels has previously been pro- interiors reveals: (1) The wall separating the posed (Kuiper and others, 1966; Oberbeck and tube interior from the preflow country rock others, 1969; Greeley, 1971a, 1971d). The ap- may be thinner than 25 cm. (2) Lava flows can plication of analogs to planetary structures re- erode the surface over which they flow. (3) quires a thorough understanding of the ter- Collapse of the tube interior can occur im- restrial counterpart. As part of an investigation mediately after the tube has been drained of molten lava and before the walls cool com- pletely. (4) Lava tubes may represent the thickest part of the lava flow, occupying topographic lows (stream channels). (5) Tubes can be modified extensively through accretion and erosion by later lava flows. Many surface features of basalt flows are directly related to lava tubes. Pressure within the closed lava-tube system caused by out- gassing and hydrostatic pressure and overflow of lava from ruptured roof sections (or from channel overflow prior to roof formation) result in formation of a topographic high along many sections of the lava-tube axis. If roof rupture does not occur, tumuli may develop in weak areas of the roof, forming positive features Figure 1. Location map; study area outlines area (may be solid or hollow) 40 to 50 m in diameter covered in Figure 2. Straight-line distance from Port- and several meters high. Most of the hollow land to study area is about 70 km. Geological Society of America Bulletin, v. 83, p. 2397-2418, 30 figs., August 1972 2397 Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/83/8/2397/3443198/i0016-7606-83-8-2397.pdf by guest on 02 October 2021 2398 GREELEY AND HYDE of terrestrial lava tubes and channels, the tubes The first published account of the tubes is an of the Cave Basalt (named here) at Mount St. article in Mazama (1903). Forsyth (1910) Helens in southwest Washington (Fig. 1) were described a lava tube (Ole's Cave) and at- studied in detail. Their excellent preservation tributed its discovery in 1895 to an early makes these tubes particularly well suited for settler, Ole Peterson. However, the other study because they show features that are less major lava tubes remained undiscovered until well exposed in lava tubes of other areas. Unlike the 1950s. Halliday (1963a, 1963b) presented a many basalt flows containing lava tubes, the detailed description of the known tubes, and margins of the Cave Basalt are fairly well de- Pryde (1968) discussed the tubes in a popular fined, and certain relations of the tubes to the article. The only geological descriptions of the configuration of the flow and surface features tubes are by Greeley and Hyde (1970) and can be determined. Hyde and Greeley (1971). Eruptive History and Previous Work Method of Study Although Mount St. Helens has not erupted Prior to field work, photogeologic maps were during this century, it has been active within made of the flow showing the locations of lava- historic time (for a review of historic eruptions tube entrances, surface features, and apparent see Jillson, 1917a; Erdmann and Warren, 1938; flow contacts. In the field, contacts were Holmes, 1955; Folsom, 1970). Published eye- checked and corrected, and additional surface witness accounts indicate that the volcano was features were noted. Following methods de- intermittently active between the mid-1830s scribed elsewhere (Greeley, 1971c), the lava and the mid-1850s. Volcanic ash was erupted in tubes were surveyed in detail (Table 1), and November 1842 and fell as far as 105 km to the where possible, surface features were related to southeast, and lava may have been erupted on the tubes. Rock samples for analysis were the south side of the volcano in 1844. An selected from surface exposures and from within eruption of pumice in about 1800 and an the tube (Fig. 2). eruption of lava on the northwest flank of the volcano sometime between 1800 and the 1830s AREAL GEOLOGY (Lawrence, 1938, 1939, 1941) evidently were The oldest rocks in the map area (Fig. 2) not observed by early explorers or settlers. consist of a series of altered Tertiary volcanic Recent geologic studies (Mullineaux, 1964; and volcanic-clastic rocks that have been in- Hyde, 1970; Hopson, 1971) indicate that the truded by small bodies of andesite, rhyodacite present may simply be the most recent porphyry, and hypabyssal rocks. These rocks quiescent interval between recurring episodes have been studied only in the vicinity of Mer- of volcanic activity. The last few hundred rill Lake (Hyde, 1970) where most of the rocks years have witnessed frequent violent volcan- are tuff-breccia, sandstone, and mudstone, each ism accompanied by hot pyroclastic flows, composed predominantly of rocks and minerals lahars, pumice eruptions, and lava flows. of volcanic origin. Tuff-breccia is predominant. Previous geologic studies of the Cave Basalt Minerals in both matrix and fragments are have been limited to brief observations made by mostly altered to chlorite, carbonate minerals, Verhoogen (1937) and by earlier workers who and clay. Although the ages of the rocks are noted tree wells and lava tubes in the pahoehoe unknown, correlation with similar rocks in basalt (Gibbs, 1854; Elliott, 1897; Diller, 1899; other parts of the Cascade Range suggests that Jillson, 1917b, 1921; Williams, 1922). Erdmann the rocks studied here are late Oligocene and Warren (1938) examined several dam sites (Hopson, 1971, personal commun.). Marble in the vicinity of the volcano and drew at- Mountain, about 10 km southeast of Mount tention to possible volcanic hazards. Lawrence St. Helens, consists mostly of nearly uniform (1938, 1939, 1941, 1954) and Carithers (1946) olivine basalt flows. The basalt flows typically described recent pyroclastic deposits on the are 1 to 3 m thick and consist of layers of north side of the volcano. Mullineaux and clinkery scoria alternating with light-gray to Crandell (1962), Mullineaux (1964), Hyde dark-gray basalt. The basalt is massive to platy (1970), and Hopson (1971) have discussed var- and dense to porphyritic with large laths of ious geologic aspects of the volcanic deposits. plagioclase and crystals of olivine. One sample The lava tubes in the Cave Basalt were ap- was selected for chemical analysis (sample 6, parently unrecognized by earlier observers. Table 2); it is distinguished from other basalts Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/83/8/2397/3443198/i0016-7606-83-8-2397.pdf by guest on 02 October 2021 GEOLOGICAL MAP OF SWIFT CREEK AREA MOUNT ST. HELENS. WASHINGTON R. Greeley and J. Hyde, 1971 EXPLANATION |::::::'ri";:*l Undivided surficial deposits; alluvium, lahars, pyroclastic flows, E&w?.ja and glacial drift. Quaternary ''Q\'/\ Undivided Mount St. Helens lavas; pahoehoe, aa, and block basalts, andesites and dacites. MN Qcb j Cave Basalt; olivine basalt, primarily pahoehoe, some aa. 21%° Quaternary (?) Marble Mountain Basalt; olivine basalt and andesite. Tertiary TV I Volcanic and volcanic-clastic deposits, with some intrusive rocks. 1958 ^_^ Contact, dashed where covered, dotted where approximate or uncertain. O Sample locations. 122° 22' 36" W K Dip and strike of beds. 46° 09' 45" N R-«.R.5E Lava tube Tumuli 0 1 2 3 I . 1 1 , Miles 0 1 2 30 4 I.I 1 1 I Kilometers Base from USGS Cougar and R.4E R.5E 122° 07' 13" W Mt. St. Helens 15' quadrangle and 46° 02' 32" N U.S. Forest Service maps. Figure 2. Geological map of the study area. GREELEY AND HYDE, FIGURE 2 Geological Society of America Bulletin, v. 83, no. 8 Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/83/8/2397/3443198/i0016-7606-83-8-2397.pdf by guest on 02 October 2021 LAVA TUBES OF THE CAVE BASALT, MT. ST. HELENS, WASH. 2399 TABLE 1. LOCATION AND PHYSICAL CHARACTERISTICS OF LAVA TUBES IN THE CAVE BASALT Maximum Elevation Length* Name Location width Average slope (ft) figr (m) (m) Ape Cave8 NEHSWWEH sec. 8, T. 8 N., R. 5 E.
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