Lyman Glacier in 1988-Bill Long
Lynch Glacier in 1990 From Pea Soup lake-Bill Long
Late
Pleistocene and Holocene Chronology of Cirque Moraines,
North Cascade Range, Washington
William
Long, Cashmere WA
Lyman Glacier in 1988-Bill Long |
Lynch Glacier in 1990 From Pea Soup lake-Bill Long |
| Introduction Field Observation Conclusions Acknowledgements Table 1 Home Page |
ACKNOWLEDGEMENTS:
Thanks to Kathleen for sharing Bill’s photo collection and old reports with me in preparing this paper. Thanks also to Stephen Porter who acted as Bill Long’s mentor on many occasions. Most of all I am thankful to have been able to spend time in the field with Bill and share in his joy and knowledge.
SUMMARY
An examination of 48 cirque and valley head moraines between Mount Stuart and Bonanza Peak, North Cascade Range was made to identify the chronology of moraine emplacement. Nine moraines are mantled by Glacier Peak Tephra(11,250 BP) and represent a Late Wisconsin advance. Mazama Ash (7180 BP) mantles 25 moraines indicating a Late Wisconsin or Early Holocene advance. Fifteen moraines lack either tephra or ash, have immature vegetation and are neoglacial in age. Several alpine basins were largely ice free when Glacier Peak Tephra was deposited. Soil development on moraines mantled only by Mazama Ash was substantial in all five locations where soil profiles were completed. Both factors indicate a Late Wisconsin advance instead of an Early Holocene advance for North Cascade cirque glaciers that advanced.
This study discusses an investigation of 48 cirque and valley head
moraines along the crest and eastern slope of the North Cascades between
chronology of cirque moraine formation during the Holocene epoch.
Dendrochronology, tephrochronology and relative position were used in
assigning age of emplacement for each moraine.
The objective in examining such a large sample of moraines was to put in
perspective the relative timing and magnitude of glacier advances since the peak
of the late Wisconsin glaciation.
The interval of mild climate that followed the Wisconsin is the
Hypsithermal. In the Pacific
Northwest examination of pollen records have provided an age of approximately
10,000-5200 years for this period (Kearney and Luckman, 1983; Heusser, 1985;
Barnosky et al., 1987). The North
Cascade Range experienced extensive deglaciation during the Hypsithermal which
was followed by a period of glacier rebirth and expansion, the Neoglacial
(Porter and Denton, 1967). The
Neoglacial has exhibited two distinct period of glacial advance.
Pollen records indicate the early Neoglacial extended from 5000 to 2500
BP, and the youngest corresponding to the Little Ice Age of the last several
hundred years (Denton and Karlen, 1973: Miller, 1969; Heikkinen, 1984).
In this study tephrochronology, soil profiles, and dendrochronology are
used to determine or at least bracket the age of cirque moraine formation.
Each geographic area is examined in turn to provide a spatial sense of
the glacier variations. Previous
studies have examined a few cirques in lesser detail.
Regional mapping of Holocene glacier behavior requires a combination of
both types of glacier mapping studies.
Beds of volcanic tephra resulting from eruption of volcanoes in the
Cascade Range provide two important time horizons in the North Cascades,
Mazama Ash (MA) which is 7180BP and Glacier Peak Tephra (GPT)
approximately 11,250 BP (Mehringer et al., 1977).
In the North Cascades the GPT consists largely of
pumic and lapilli. Most of
the GPT fell eastward of the summit reaching the northern and western edge of
the study areas. The Icicle Creek drainage at the southern edge of the study
area is south of the GPT zone. GPT
has two widespread member, layers B and G (Mehringer et al., 1977; Porter,
1978). Both layers based on
radiocarbon dating are approximately 11,250 BP in age.
Ash layer O was produced by eruptions at Mount Mazama.
This layer has oxidized in
the study area to an orange brown layer that is seen throughout
the study are.
This layer is comparatively thick and continuous in regions where soil
development has occurred.
Icicle
Creek Drainage
No GPT is found in the Icicle Creek Drainage because it is south of the
GPT limit at Chiwakum Mountain (Figure 1-3; Table 1).
Colchuck Lake at 1700m occupies the floor of a large cirque carved in the
north flank of the Stuart Range. Early
in the 20th century the level of the lake was artificially raised for water
storage. In the fall at lake Drawdown
a terminal moraine is exposed that bisects the lake at its narrow northern end.
A bouldery left lateral moraine grades into the terminal moraine.
On the lateral moraine the MA is present beneath a white sandy ash
thought to be the 450 year old Mt. St. Helens Wn tephra (Mullineaux, 1974).
The upper Enchantment Lakes basin is at 2310-2350m and only 2km southeast
of Colchuck Lake. At the south edge
of these lakes is the rapidly disappearing Snow Creek Glacier (Pelto, 1993).
Just beyond a fresh moraine (Brynhild) and
400m from Snow Creek Glacier is a weathered moraine, the Brisingamen.
On and behind the Brisingamen both MA and Mt St.Helens Wn are found
(Waitt et al., 1982). Mainly
because the Brisingamen moraine underlies MA and is far upvalley of the late
Wisconsin Rat Creek Moraine, Waitt et al(1982) concluded that it probably is
early Holocene in age. However, as
only a minimum limiting age is available for the Brisingamen, it could also
represent a late Wisconsin advance.
Other pre-Mazama moraines in the Icicle Creek Drainage impound Eightmile
lake, Lake Sylvester, Lake Margaret, Turquoise Lake, Chain Lakes, and one lies
on the threshold of the Square-Wolverine Lake Cirque.
Thus, Icicle Creek experienced a widespread late glacial (substantially
after Rat Creek) or early Holocene advance.
Because of the lack of GPT, the timing in this basin cannot be determined
more accurately using tephra. No
evidence of radiocarbon datable material was seen in any of the moraines.
This is not surprising given the certainly barren bedrock and talus
environment that would have existed during the late glacial-early Holocene
period. A series of soil
stratigraphic sections were exposed on the Lake Margaret moraine.
Soil development between glacial material and MA is substantial ranging
from 10-30cm. This suggest moraine
emplacement long before MA deposition.
The Brynhild Moraine in front of Snow Creek Glacier is a conspicuous
unvegetated moraine belt named the Brynhild.
Brynhild bisects one of the Enchantment Lake’s at 2350m.
This moraine is almost barren of lichen and is devoid of tephra, ash and
soil. The above suggests that this
moraine is no more than a century old, and this is corroborated by observations
of Snow Creek Glacier in contact with the moraine (Rusk, 1924). There are also conspicuous fresh moraines located just
beyond the edges of Colchuck Glacier, and all three glaciers on the north side
of Mt. Stuart. The lack of lichen
and vegetation on these four moraines indicate that the Little Ice Age advance
was the most extensive of the Neoglacial period in Icicle Creek valley.
Chiwakum
Mountains
A well developed right lateral moraine of the Chiwakum Creek Glacier
comparable in age to the late Wisconsin Rat Creek moraine lies 90m above the
west end of Chiwakum Lake. The type
moraine of the latest Wisconsin glacial episode is the Larch Lake Moraine 8km
upvalley from the terminal moraine of Rat Creek age, at the head of the Chiwakum
Creek Valley (Long, 1989). The
Larch Lake Moraine is a multiple terminal moraine that reaches an altitude of
1735m that is mantled by GPT. A GPT
layer underlies a thick silty ash layer in a surface locality behind the
innermost Larch Lake Moraine.
A stratigraphic cross section was obtained in the wet meadow inside the
Larch Lake Moraine. The base of the
section in in dark gray lacustrine silt, the deposit of a small lake formerly
dammed by the moraine. The silt is
overlain by 30cm of tephra consisting of yellowish brown and brown pumice
lapilli up to 0.8cm in diameter(GPT). The
GPT is covered by 43cm of dark gray sand and gravel and 30cm of black sandy
organic sediment. Above the sand is
70cm of strong orange to yellow-brown silty ash (MA) capped by about 30cm of
fine loamy sand laced with roots. The
unusual thickness of the volcanic ash layer is most likely due to fluvial
reworking and concentration of the ashes.
Because the Larch Lake Moraine lies behind the Rat Creek Moraine of Late
Wisconsin age and has GPT on and behind it, the moraine was built sometime
before 11,250 BP.
In the cirque that holds Grace Lake is a well defined end moraine that
reaches 1860m. MA was found at the east end of the left lateral moraine, but
no GPT is present. A
MA mantled moraine also dams Lake Brigham at 1780m.
As described by Merrill (1966), a moraine impounding Cup lake at 1965m
lies in the highest cirque in the Chiwakum Valley.
The Cup Lake Moraine is exceedingly fresh and is devoid of soil and
vegetation. MA is absent on the
moraine but is present on the steep slope immediately beyond it, indicating a
Neoglacial emplacement probably during the LIA.
A small cirque with a small amount of glacier ice is located above Upper
Grace Lake (2105m). Approximately
125m beyond the existing ice are two moraines.
Both moraines lack MA and are Neoglacial in age.
The slope of the outer moraine is stable and has considerable alpine
vegetation suggesting an early Neoglacial advance (5000-2500 BP).
The slope of the inner moraine is unstable and unvegetated indicating a
LIA advance.
In Chiwakum Valley evidence for a late glacial advance after 13,000 BP
(Rat Creek age) and before 11,250 BP is exhibited in the Larch Lake Moraine.
Two additional moraines of pre-Mazama age either early Holocene or late
glacial also exist at Grace Lake and Lake Brigham. Two of the three existing Neoglacial cirque moraines date
from the LIA, indicating that the LIA was the most extensive ice advance of the
Neoglacial in Chiwakum Valley.
Stevens
Pass
A Rat Creek age moraine occupies Stevens Pass at 1240m on the Cascade
Crest at the head of Nason Creek (Porter, 1978).
No GPT has been found on the surface of the moraine.
GPT is seen about 10km downvalley suggesting that the upper valley was
still ice covered at the time of the Glacier Peak eruption.
A moraine overlain by MA lies near the head of Smith Brook at 1225m, 6km
north of Stevens Pass. These two
moraines occupy similar positions in upper valley reaches, have similar
morphology and weathering characteristics and lie at almost identical altitudes;
hence, the moraines are regarded as correlative in age, late glacial.
Surprise Lake is impounded behind a bouldery, completely intact, MA
covered terminal moraine. Two
recessional moraines covered with MA descend to the lake from a prominent right
lateral moraine. This lateral
moraines is more than 2km long. Along
Glacier Lake the lateral moraine is double crested, and between the crest is a
small narrow lake. Three bouldery
moraines or protalus ramparts lie on the floor of the Surprise Creek valley-head
cirque well above Surprise Lake. The
outer two moraines underlie the MA, the inner one is ash free and Neoglacial in
age.
Snow Creek is a tributary to Rainy Creek which flows northward into the
Little Wenatchee River. Abundant
GPToccurs in Snowy Creek valley to about 1090m but none was found in the upper
2.7km of the valley, suggesting that the upper valley was still ice covered at
the time of the Glacier Peak eruption. The
well formed Snowy Creek cirque on the west side of Nason Ridge has a moraine at
the cirque threshold mantled with MA. The
Crescent Creek Cirque on the east side of Nason Ridge has a late glacial moraine
that underlies GPT.
Mount
Daniel
Glacier crowned Mount Daniels lies on the Cascade Crest 21km south of
Stevens Pass. On the east side of Mount Daniel the former Hyas Creek
Glacier reached an altitude of 1675m terminating west of Peggy’s Pond.
The terminal moraine is covered by MA.
Several soil profiles were completed on this moraine.
Each profile showed substantial organic rich soil horizons from 7-25cm in
thickness between the late glacial material and MA.
The area has been ice free since MA and soil development suggests
considerable time between moraine emplacement and MA deposition.
A well defined lateral moraine 10m high descends to the closed terminal
moraine behind which are two recessional moraines emanating from the lateral
moraine. Behind each moraine is a
small pond. The moraines have a
well developed soil and a thick turf. Each
of these moraines is overlain by MA.
At 1690m a 3m high recessional moraine lacking volcanic ash, bears a 10cm
cover of soil and immature alpine vegetation.
The oldest tree cored on this moraine was a 6m alpine fir, that began
growing more than 110 years ago, suggesting moraine formation during the LIA.
The innermost moraine is 100m upvalley of the LIA maximum moraine and 0.5km down-valley from the
existing Hyas Creek (Ice Worm) Glacier. The
moraine is very fresh and devoid of soil. During
the last 20 years the first alpine fir seedlings have taken hold.
This moraine is less than a century old.
The moraine of the maximum Neoglacial advance of Lynch Glacier on the
north side of Mount Daniel. lies
against Dip Top Peak. This terminal
moraine descends 100m both to the east and west out of the Pea Soup Lake Basin
(1900m), indicating that the former
Lynch Glacier drained down both sides of the Cascade Crest.
This moraine is fresh lacking any soil or alpine vegetation.
This moraine was still ice cored as late as 1984 and is from the LIA.
Beyond this moraine MA is found in the cut bank of several drainage
channels. Thus, the LIA advance was
the largest of the Neoglacial for Lynch Glacier.
Lynch Glacier receded out of Pea Soup Lake Basin in 1983. From air photo mapping Lynch Glacier had shrunk from 0.8km2
in 1955 to 0.5km2 in 1992 (Pelto, 1993). Daniels
Glacier has a distinctive LIA lateral moraine and a MA mantled moraine in the
cirque basin immediately below the current glacier.
On Mt. Daniels the maximum Neoglacial advance on all three glaciers
occurred during the LIA.
Entiat
and Chelan Mountains
With the exception of the headward 3km of the Entiat River Valley, GPT
was found throughout the Entiat drainage basin, indicating that the Chelan and
Entiat Mountains were largely deglaciated by 11,250 BP.
GPT is traceable upvalley to a well defined moraine between 1615m and
1675m. GPT and MA were not found on the surface of the
moraine, but is found immediately beyond the moraine, indicating a Neoglacial
age emplacement. This outer moraine
has good soil development and well established alpine vegetation.
Just upvalley is an exceedingly bouldery LIA moraine belt lacking soil
and overlaps the upvalley end of the older moraine at 1675m.
Pumice can be traced to upper Ice Lake Cirque.
Within the cirque thick pumice deposits are found behind a
fresh boulder moraine, and GPT is found within the moraine which overlies
GPT and MA. This moraine lacks
soils and lichen development and is from the LIA.
The Choral Lake cirque at 2195m is 10km east of the Upper Ice Lake
cirque. The Choral Lake cirque also
must have been ice free from GPT to the Neoglacial, since the rubbly moraine
impounding the lake overlies MA and contains abundant GPT.
Chronologic relations between the final late glacial advance of alpine
glaciers and the GPT are see in the west-facing Carne Mountain cirque (Beget,
1984). On the Carne Mountain cirque threshold at 1875m is a large
terminal moraine up to 5m high. The
moraine contains blocks of gneiss from Carne Mountain and is buried under GPT.
This basin remained ice free after the Glacier Peak eruption.
Cow Creek Meadow at 1555m occupies the flat floor of a cirque carved in
the north side of Rampart Mountain. The
meadow is fronted by a moraine that
lies 600m north of the cirque headwall. Like
the Carne Mountain cirque, Cow Creek Meadow and its moraine are buried by GPT
and date to a late Wisconsin advance.
A well defined bouldery protalus rampart lies at 1950m on the north side
of Milham Pass at the head of Emerald Park Creek.
The deposit underlies GPT, again indicating that most cirques in the
Chelan Mountains have been ice free for more than the last 11,250 years.
The Entiat River provides
evidence that the LIA advance was the most extensive of the Neoglacial and the
most extensive since the GPT in Ice Lake and Choral Lake cirques.
In the Entiat Cirque the Neoglacial advance was slightly more extensive.
Glacier Peak.
Pear Lake at 1465m is dammed by a bouldery moraine and drains subsurface
through the moraine. GPT was not
found on or behind the moraine or at Top Lake 1km east of Pear Lake.
This suggests that this area was ice-covered at the time of the Glacier
Peak eruption. MA is abundantly
exposed throughout the Top Lake and Pear Lake area, indicating glacier
disappearance by this time with no Neoglacial rejuvenation.
Lyman
Lake and Dome Glacier Area
Lyman Glacier is the source of Railroad Creek a major tributary to Lake Chelan. The absence of GPT from the upper 9km of the Railroad Creek Valley suggest that it was still ice covered at 11,250 BP (Porter, 1978). Lyman Glacier ends at 1830m. One prominent moraine belts records the Holocene activity of this glacier. The outermost moraine has extensive alpine vegetation, larch and subalpine fir on it. The moraine overlies MA indicating that it represents the most extensive advance of the last 7000 years. This moraine is then likely a result of a Neoglacial advance. The outermost moraine merges with the in several
Upper
Upper Chiwawa Basin at 1450m is at the head of the Chiwawa River 2km east
of the Cascade Crest. On the north
side of the basin, two well defied lateral moraines 15 to 20m high descend to
the basin floor. One moraine was
built by a glacier on the south side of Chiwawa Mountain, and the other by a
glacier on the east side of Fortress Mountain.
The moraines are densely vegetated and mantled by GPT.
Like the outermost moraine in the Entiat Glacier cirque, the upper
Chiwawa Basin moraines have good soil development. GPT was not found behind the moraine suggesting that the
upper 2km of the valley was ice covered at the time of the Glacier Peak eruption.
The Pear Lake cirque lies on the Cascade Crest 24km south of l locations
and is even overrun in the center of the basin by a younger fresh moraine.
This moraine dates from the LIA, has little vegetation and soil developed
on it. Photographs by C.E. Rusk
(1924) in 1906 show the glacier is still partially in contact with the LIA
moraine. The oldest tree on the LIA
moraine, determined from coring is 90 years old, suggesting a mid to late 19th
century moraine stabilization. Soil
profiles were completed 45m beyond the Lyman Glacier Neoglacial moraine on a
small ridge. The base of the soil
profile was a glacial till at a depth of 90cm,
the nest 20cm was fine grained sand followed by 12-15cm of organic rich soil. Then
MA ranging from 5-10cm in thickness. Above
the MA is 20cm of organic rich topsoil. The
thickness of pre MA soil development suggests a considerable time span from
deglaciation to MA deposition, which suggests no early Holocene ice cover was as
extensive as Neoglacial advances. The
Neoglacial advance of Lyman Glacier was slightly more extensive than the
LIA advance.
Dome Peak on the Cascade Crest 22km north of Glacier Peak has yielded a
detailed Neoglacial record. No
early Holocene advances were identified by Miller (1969).
Miller (1969) examined the Holocene deposits in four valleys radiating
from this massif and in two of these found MA on the valley floors immediately
beyond moraines dated to the 16th century from dendrochronology.
In three of the four valleys the most extensive advance was during the
LIA. No evidence of earlier
Neoglacial advance was recognized
in front of LeConte Glacier or Dome Glacier.
However, several overrun trees found in front of South Cascade Glacier,
but well behind the LIA moraines, dated to 4700-4900 BP (Miller, 1969).
A moraine beyond Chickamin Glacier was dated to the 13th century using
dendrochronology of the oldest sub-alpine fir.
However, this date is based on the a 600 year old sub-alpine fir.
This age is beyond the expected life span of sub-alpine fir in this area
and is suitable only as a minimum age and is more likely an earlier Neoglacial
advance. This is the only potential
evidence for a more extensive early Neoglacial advance than LIA advance around
Dome Peak. As on Mt. Ranier
reexamination of 13th or 14th century moraines appear to be from the early
Neoglacial (Burbank, 1981).
Sawtooth
R
Sawtooth Ridge marks the boundary between the Chelan and Methow drainages
and the crest lies generally above 2200m and culminates in several summits 2450m
or higher. For 20km Sawtooth Ridge
was almost entirely a nunatak above the Cordilleran Ice Sheet (Waitt, 1972).
This is indicated by bedrock whalebacks aligned SSE and erratic boulders
in the vicinity of 1890m in the Libby Creek Valley (Waitt, 1972).
The headwaters of Libby Creek are defined by alpine cirques, Libby Lake
at 2322m is the fourth highest lake in the Cascade Range.
It is small, deep, circular
and dammed by a broad moraine
mantled by MA. A MA mantled moraine
also impounds Upper Eagle Lake at 2167m 3km south of Libby Lake. No evidence of Neoglacial activity in seen on Sawtooth Ridge.
North
Fork Skykomish River
The south facing Columbia Glacier cirque lies 13km west of the Cascade
Crest. Below the current glacier
extending most of the way to Blanca Lake are two left lateral moraines.
The inner moraine is very bouldery and bears only scattered alpine
flowers. The outer moraines
supports a continuous alpine heather turf, with 3-5m high alpine firs. Both moraines date from the LIA.
The LIA terminal moraine is preserved on the west side of the basin.
Soil profiles on a small knob 20m beyond this moraine reveal an
uninterrupted soil development (50cm thick) above the MA layer.
Below the MA is 10-15cm of sandy organic soil, and then 60cm of glacial
till on bedrock. The outwash plain
beyond the LIA moraines is cut by several streams.
The soil profile is well exposed in the stream banks.
Thick organic rich soils lie both below and above the laterally
continuous MA layer across an area of 0.2km2.
Moraines at Silver Lake and Portal Peak also have MA immediately beyond
the moraines, indicating no late Wisconsin or early Holocene advance in the
basin.
In the North Cascade Range between Mount Stuart and Bonanza Peak abundant
weathered cirque moraines are found that underlie the 7100 BP MA.
On 8 moraines the 11,250 BP is found in addition to MA.
MA is found alone mantling 25 moraines.
These 25 moraines were emplaced prior to 7100 BP.
There are 14 moraines that date to the Neoglacial period, 11 of these
during the LIA. This indicates that
in the North Cascades the LIA was generally the most extensive Neoglacial
advance. On Lyman Glacier, Entiat
Glacier and Hyas Creek Glacier LIA moraines and early Neoglacial moraines are
somewhat overlapping, demonstrating the similar extent of early Neoglacial and
LIA advances.
No GPT was found along the 70km stretch of the Pacific Crest Trail from
Stevens Pass north to White Pass. This
implies that the North Cascade Crest was still ice covered at 11,250 BP.
The pre-Mazama cirque moraines near and along the Cascade Crest are
devoid if GPT indicating that these moraines postdate GPT.
Further east of the Cascade Crest in the Chiwakum, Entiat and Chelan
Mountains numerous cirque moraines and cirque floors are mantled with pumice
indicating that these
cirques were ice free at the time of the eruptions.
At least one valley head cirque has a moraine underlying GPT.
These relationships imply that pre-Mazama cirque moraines were built just
before, during and after the Glacier Peak eruption.
The question that remains is when were the 25 MA mantled moraines
emplaced? Three
lines of evidence have been compiled in this study to
address this question.
1. Ten cirques and high
alpine valleys were ice fee from the time of GPT deposition to MA deposition
(Upper Ice Lake, Choral lake, Cow Creek Meadow, Milham Pass, Crescent Lake,
Saska Peak, Larch Lake, Carne Mountain, Upper Chiwawa Valley and North Fork
Entiat Valley). This is strong
evidence that Wisconsin alpine glacier retreat was largely completed by 11,250
BP, and that no substantial period of glacier formation and growth occurred
prior to MA deposition.
2. Soil profiles from four locations
on or adjacent to four moraines mantled by MA indicate considerable thicknesses
7 to 30cm of organic rich soil developed between the late Wisconsin and
MA deposition. This suggests
that no advance had occurred within the 2000-3000 years between GPT and MA
deposition.
3. Observation of terminus behavior on 47 glaciers
and mass balance annually on 8 North Cascade glaciers indicates a close
similarity in behavior amongst glaciers throughout the range to significant
climate change (Pelto, 1993 and 1996). All
47 North Cascade glaciers examined annually are currently retreating. The cross correlation coefficients for annual mass balance
between the eight glaciers always exceeds 0.87 (Pelto, 1996).
This argues against substantial local advances in the North Cascades.
The conclusion drawn from this data is that the early Holocene or late
Wisconsin emplacements represent a minor readvance of existing late Wisconsin
glaciers, not a later early Holocene period of glacier growth.
Table
1. Data on the age of cirque
moraines. See Figure 1 and 2 for
location. Tephra GPT=Glacier Peak
Tephra, MA=Mazama Ash. LW=Late
Wisconsin, LIA=Little Ice Age, NEO=Neoglacial, EH=Early Holocene
Map
Cirque Basin Moraine
Cirque Distance
Tephra Age
No.
Altitude Aspect
to Crest
(km)
Icicle Creek
Drainage
11.
Enchantment Lakes 2315
NE
40 E MA on, behind
EHLW
12.
Colchuck Lake 1700
N
37 E
MA on
EHLW
13.
Lake Ann
1875
NW
28 E
MA on
EHLW
14.
Lake Sylvester 1905
W
14 E
MA on
EHLW
15.
Turquoise Lake 1665
E 5
E MA on
EHLW
16.
Lake Margaret 1645
NW
13 E
MA on
EHLW
17.
Chain Lakes 1705
NW
8 E
MA on
EHLW
18.
Square Lake
1555
E
1 E MA on
EHLW
19.
Little Eight Mile 1340
E
35 E
MA on
EHLW
20.
Colchuck Glacier 1900
N
37 E
LIA
21.
Snow Creek Glacier 2350
NE
40 E
LIA
Chiwakum Mountains
25.
Larch Lake
1768
N
12 E GPT
on, behind LW
26.
Lake Grace
1860
NW
13 E
MA on
EHLW
27.
Lake Brigham 1775
NE
15 E
MA on
EHLW
28.
Upper Grace Lake 2135
N
14 E
MA in front
LIA
29.
Lake Charles
1915
NE
15 E
MA in front
LIA
30.
Cup Lake
1965 NE
11 E
MA in front
LIA
Nason Creek Drainage
35.
Crescent Lake 1705
E
10 E
GPT on
LW
37.
Lake Valhalla
1470
SE
0
MA on, behind EHLW
38.
Lake Susan Jane 1400
N
0
MA on, behind EHLW
39.
Surprise Lake
1570
N
0
MA on, behind EHLW
Mount Daniel
40.
Peggy's Pond
1675
SE
2
E
MA on, behind EHLW
41.
Hyas Creek Glacier 1720
E
2 E
LIA
42.
Daniel Glacier 1495
NE
1 E
MA in front
NEO
43.
Lynch Glacier 1890
N
0
MA in front
LIA
Chelan and Entiat
Mountains
45.
Entiat Glacier 1615
E
13 E
GPT in front
LW
46.
North Fork Entiat 1980
NE
28 E
GPT on
LW
47.
Cow Cr. Meadow 1540
N
30 E
GPT on
LW
48.
Milham Pass
1950
N
22 E GPT on
LW
49.
Saska Peak
2135
NW
23 E
MA on
EHLW
50.
Choral Lake
2195
NE
27 E
GPT under LIA
51.
Entiat Glacier
1660
E
13 E
MA in front NEO
52.
Upper Ice Lake 2195
NE
12 E
GPT under LIA
53.
Carne Mountain 1875
NW
14 E GPT on, behind
LW
Railroad Creek
Drainage
56.
Lyman Glacier 1815
N
4 E
MA in front
NEO
57.
Isella Glacier 2000
S
7 E
MA in front
LIA
58.
Martin Peak 2040
E
13 E
MA in front
LIA
Upper Wenatchee
River
34.
Snowy Creek 1400
NW
8 E
MA on
EHLW
54.
Upper Chiwawa 1450
E
5 E
GPT on
LW
55.
Pear Lake
1465
E
0
MA on, behind EHLW
Sawtooth Ridge
59.
Upper Eagle Lake 2165
E
45 E
MA on
EHLW
60.
Libby Lake
2320
E
46 E
MA on
EHLW
61.
Star Lake
2185
E
40 E
EHLW
62.
Horseshoe Basin 2135
E
41 E
MA on
EHLW
North Fork Skykomish
63.
Columbia Glacier 1280
SW
13 W MA
in front LIA
64.
Silver Lake 1300
E
19 W MA
in front
EHLW
65.
Portal Peak
1735
NE
5 W MA
in front EHLW
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Dendrochronological evidence of variations of Coleman Glacier,
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Denton, G.H., 1967. Chronology of
Neoglaciation in the North
American Cordillera. Amer.
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FIGURE
CAPTIONS
Figure
1. Index map of North
Cascades. Black areas indicate
glaciers. Moraine locations
indicated by dot and numeral (see Table 1).
Figure
2. Index map of North Cascades. Black
areas indicate glaciers. Moraine
locations indicated by dot and numeral (see Table 1).
Figure
3. Localities
where airfall deposits of tephra erupted from Glacier Peak Volcano have been
found.
Figure
4. Map or Mount Daniel glacier system showing positions
of glacier margins between latest Pleistocene and 1990.
Figure
5. Little Ice Age moraines
at Lyman Glacier.
