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Seventy-five genera and 288 species of lichens are reported from the North Cascades Range, Washington. Twenty of these represent new records for Washington. The list includes all literature reports as well as recent collections. The Cascade Range, extending from southern British Columbia to southern Oregon, can be subdivided into a number of ecological provinces on the basis of geology, soils, topography, and vegetation. The northernmost of these provinces, the western and eastern North Cascades provinces (Douglas, 1972), constitute the North Cascades Range. In Washington this area extends from the International Boundary (49'00' N Lat.) to Stevens Pass (47030' N Lat.) (Fig. 1), encompassing approximately 18,000 km2. The higher peaks of the North Cascades Range generally reach elevations of 2150-2450 m, although the volcanic peaks of Mt. Baker and Glacier Peak (3284 and 3209 m, respectively) tower above the main Range. This rugged, relatively inaccessible region includes within it the North Cascades National Park, Glacier Peak and Pasayten Wilderness Areas, Ross Lake and Lake Chelan National Recreation Areas, Mt. Baker and Okanogan National Forests, and portions of the Wenatchee and Snoqualmie National Forests. The climate of the North Cascades Range varies considerably from west to east. The prevailing westerlies from the Pacific Ocean create a maritime climate on the western slopes, while a more continental climate exists on the eastern slopes. Annual precipitation ranges from 180 to 280 cm on the west side of the range to as little as 35 cm on the east side. The climate, along with the physiography of the region, creates a mosaic of vegetation types that change markedly, both with distance (west to east) and elevation. Montane forests in the western North Cascades are dominated by Tsuga heterophylla, T. mertensiana, Pseudotsuga menziesii, Thuja plicata, and Abies amabilis while in the eastern North Cascades forest dominants include Pinus ponderosa, P. contorta, Pseudotsuga menziesii, Abies lasiocarpa, and Picea engelmannii. In the subalpine zone (sensu Douglas, 1971, 1972) of the western North Cascades, Abies amabilisTsuga mertensiana tree clumps are interspersed throughout heath (mainly Phyllodoce empetriformis and Cassiope mertensiana) dominated meadows. Similar subalpine vege1 Dr. I. M. Brodo kindly permitted use of his unpublished collections from Mt. Baker, Washington. The following taxonomists identified or verified difficult taxa: C. D. Bird, G. E. Howard, M. Ostafichuk, J. W. Thomson, W. A. Weber, and P. Y. Wong. Gloria G. Douglas assisted with manuscript preparation. 2Department of Botany, University of Alberta, Edmonton, Alberta, Canada. Present Address: British Columbia Provincial Museum, Victoria, British Columbia, Canada. This content downloaded from 207.46.13.187 on Sun, 15 May 2016 06:09:41 UTC All use subject to http://about.jstor.org/terms 1974] DOUGLAS: LICHENS OF NORTH CASCADES RANGE 583 OMYT' I , B-CMONUMENT 104 OMYHO I . ..... ..( ARN LD PK-x S CHURCHAMTNx WINCHESTER WASH HORSESHOE MTN x TNxCOPPER 0 HORSESHOE MTN X MTN'XMAPLE FALLS N ' x MTN-; BEAGLRIER UTH i 1 Cr cSNOWSHOE MTN-x SILVER -MTN.\ C' FIR CAMPGROUND BEAVER OAJOE GROUSE fxMTBAKE TABLE MTNXh SUMMIT -1 WINDY MILL MTNx -A RIDGE$ t CHOWDER RIDGE . PKI CHOPAKA x 13 MARMOTSKDYLINE " X HAYSTACK MTN. MTN. RIDGE DIVIDE % "HAYSTACK MTNL' / . f HATCOM CO Ru8Y C SLATE PKSCHREIBERS ELEPHANT BUTTE x MC ROCKLEOD MT MTN E SOURDOUGH MT MCLEOD MT MIDDLE p .MEADO 'GOAT PKTIFFANY MTNX MAZAMA TIFFANY MTN-x SNOO~sv oHAMILTON

Since the middle of the eighteenth century the climate of northern Europe has undergone a change. Several series of temperature recprds from different places show the same trend towards a more maritime climate (Angstrom, 1939; Manley, 1946; Ahlmann, 1949a). Winter temperatures have risen and the difference between summer and winter extremes has been reduced. This effect is clearly seen in Manley's account of the secular variation in running means of temperature for different months in Lancashire, where the January and December values alone show a definite rise. The rise in temperature has been more pronounced at higher lati? tudes. Thus whilst the rise in mean annual temperature between about 1870 and 1940 has been only a fraction of a degree centigrade in Britain (Manley, 1946), mean annual temperatures have increased by nearly one degree in Stockholm (Ahlmann, 1949a) and by nearly two degrees in northern Finland (Keranen, 1944). The rise in winter temperatures shows an even more pronounced trend with lati? tude, the increment amounting to four or five degrees in west Greenland and Spitsbergen (see Rubinstein, 1946; Hesselberg and Birkeland, 1940-4). The greater circulation of warm air into these northern latitudes has been accompanied by the anticipated increase in precipitation. During this same period there has been a general decrease in precipitation and a slight lowering of mean annual temperature over large land masses in lower latitudes (Lysgaard, 1948, 1949). These changes have left their mark on the great natural registers of climate, namely the mountain glaciers, the polar ice and the inland seas. Glaciers advance or recede in response to the difference between their rate of accumulation from snow? fall and their rate of melting in the warmer part of the year. Their size depends, therefore, both upon annual temperature and on precipitation integrated over a very long period. It is well known that a number of glaciers in northern Europe reached their maximum extent some 200 years ago and have since receded at a rate which has tended to increase in recent years (see Ahlmann, 1949b). Photographs of glaciers (e.g. Ahlmann, 1949a) taken from the same place at a time lapse of several decades show how dramatically this shrinkage has taken place. Since precipitation in these regions has, if anything, increased, the glacial recession must be entirely due to the longer and warmer melting season. The temperature of the Arctic Sea has risen, probably as a result of increasing atmospheric circulation causing an intensification of the North Atlantic drift (Smed

A LARGE portion of eastern WVashington is occupied by the dark-colored soils of the Palouse and closely related series. These soils belong to the chernozem group. The development of the chernozems is a mass effect of a certain natural combination of definite climatic conditions, grass vegetation, and topographical configuration of the general landscape. The great geographical unit known as the northern horizontal zone of chernozems, famous for its fertile and productive black soils, is a broad belt throughout which such a combination of physiographic conditions remains relatively uniform. This belt does not stretch entirely across the continents, being interrupted in various places by the mountainous regions and the coastal regions strongly affected by the influence of a marine climate, in neither of which normal chernozems can be developed. It may be assumed that in the western United States chernozem soils would occupy most of W;ashington and Oregon but for the Cascade Range. The Cascades, standing as a barrier across the path of the prevailing westerly winds from the Pacific Ocean, create on their western slopes and foothills an independent, exceedingly humid west-coast natural province and cast a dry climatic shadow over the part of Washington and Oregon east of the mountains. The exceedingly high humidity of the humid province, which stretches from British Columbia into the northern part of California, coupled with a luxuriant forest vegetation composed mainly of evergreens, creates an environment that has caused the development of a group of soils fundamentally and strikingly different from the chernozems. On the other hand, a meridional belt of arid semidesert reaching far northward extends through the entire region covered by the dry climatic shadow east of the Cascades. This is a northward peninsulalike protrusion of another great horizontal zone, south of the chernozem zone. If the Cascade Range and the coastal mountains did not exist, this zone would hardly extend as far north as the northern boundary of Utah and Nevada and would reach the coast only in the southernmost part of California. This region is occupied by the very light gray, grayish-brown, or brown soils similar to those of Ritzville, Wheeler, and many other series, which form another great group of light-gray and brown soils of the semidesert "serozems" and " burozems. " This geographical distribution of the principal soil groups of Wtash

development on our moorland fringes. One such area, which has recently been investigated, and where public and private investment might result in increased food production, is the Land's End Peninsula of Cornwall. Here, over an area of about 55,000 acres west of a line joining Penzance and St. Ives, is some of the finest early vegetable and flower land in the country, some very good dairying land, and moorland which is as bleak and depressing as any in Britain. In many parts of highland Britain, between the regularly culti? vated land of the valleys and the rough grazings of the upper slopes, there are narrow belts of enclosed rough grazings which have been cultivated from time to time whenever market prices made the effort worthwhile. But here in the western tip of Cornwall, a casual observer is struck by the great number of enclosed rough grazings and by the irregular manner in which they are found amongst improved pastures. The dyke-like stone "hedges" represent a great deal of time and effort, and one inevitably asks if this land was not put to better use in the past. Yet these uplands which are windswept and damp, almost completely lacking in trees, and scattered with declining, depressed settlements do not appear conducive to agriculture, in contrast to the lower slopes and coastal pockets. Many visitors therefore are apt to consider existing dissimilarities in agricultural values as inevitable and due to basic physical differences. Early in 1952 the Research Group of the Agricultural Land Service of the Ministry of Agriculture and Fisheries began a general investigation into the possibilities of developing this virtual wasteland. A preliminary study of physical conditions in the peninsula was essential to avoid wasted effort, should basic influences, such as soil and climate, preclude agricultural development. If however these did not prove to be insuperable obstacles, it would be reasonable to ask why certain areas were lying idle whilst neighbouring fields were being intensively stocked with dairy herds, or producing valuable crops of early vegetables and flowers. An answer, it was thought, might be found in the long history of the district. The Land's End Peninsula is essentially a granite mass rising from the sea, with small areas of old Palaeozoic rocks and a little alluvium on its southeastern fringe around the town of Penzance. Its maritime climate notably lacks extremes of any kind. Annual and diurnal temperature ranges are slight

Background Climate variability modifies both oceanic and terrestrial surface CO2 flux. Using observed/assimilated data sets, earlier studies have shown that tropical oceanic climate variability has strong impacts on the land surface temperature and soil moisture, and that there is a negative correlation between the oceanic and terrestrial CO2 fluxes. However, these data sets only cover less than the most recent 20 years and are insufficient for identifying decadal and longer periodic variabilities. To investigate possible impacts of interannual to interdecadal climate variability on CO2 flux exchange, the last 125 years of an earth system model (ESM) control run are examined. Results Global integration of the terrestrial CO2 flux anomaly shows variation much greater in amplitude and longer in periodic timescale than the oceanic flux. The terrestrial CO2 flux anomaly correlates negatively with the oceanic flux in some periods, but positively in others, as the periodic timescale is different between the two variables. To determine the spatial pattern of the variability, a series of composite analyses are performed. The results show that the oceanic CO2 flux variability peaks when the eastern tropical Pacific has a large sea surface temperature anomaly (SSTA). By contrast, the terrestrial CO2 flux variability peaks when the SSTA appears in the central tropical Pacific. The former pattern of variability resembles the ENSO-mode and the latter the ENSO-modoki1. Conclusions Our results imply that the oceanic and terrestrial CO2 flux anomalies may correlate either positively or negatively depending on the relative phase of these two modes in the tropical Pacific.