Hawaii text and bibliography
The Huelmo/Mascardi Cold Reversal (HMCR) is the name given to a cooling event in South America
between 11,400 and 10,200 14C years BP. This cooling began about 550 years before the Younger Dryas
cooling in the Northern Hemisphere, and both periods ended at about the same time
http://en.wikipedia.org/wiki/Huelmo/Mascardi_Cold_Reversal
The Illinoian Stage is the name used by Quaternary geologists in North America to designate the period
of geologic time of ~300,000—130,000 years ago, a period of ~0.17 million years during the middle
Pleistocene when sediments comprising the Illinoian Glacial Lobe were deposited. It precedes the
Sangamonian stage and follows the Pre-Illinoian Stage in North America. The Illinoian Stage is defined as
the period of geologic time during which the glacial tills and outwash, which comprise the bulk of the
Glasford Formation, accumulated to create the Illinoian Glacial Lobe
http://en.wikipedia.org/wiki/Illinoian_(stage)
The Wisconsin Glacial Episode was the most recent major advance of continental glaciers in the North
American Laurentide ice sheet.[1] This glaciation is made of three glacial maxima (sometimes incorrectly
called ice ages) separated by interglacial warm periods (such as the present). These glacial maxima are
called, from oldest to youngest, Tahoe, Tenaya and Tioga. The Tahoe reached its maximum extent
perhaps about 70,000 years ago. Little is known about the Tenaya. The Tioga was the least severe and
last of the Wisconsin Episode. Termed the Late Wisconsin, this last of the Wisconsin glaciation began
about 30,000 years ago, reached its greatest advance 21,000 years ago, and ended about 10,000 years
ago. At the height of glaciation the Bering land bridge permitted migration of mammals, including
humans, to North America from Siberia
http://en.wikipedia.org/wiki/Wisconsin_glaciation
See also

8.2 kiloyear event

Blytt-Sernander

Deluge (prehistoric)

Holocene calendar
– used to date geological, archaeological, dendrochronological and historical events from the approximate
beginning of the Holocene Epoch


Holocene extinction
Holocene Impact Working Group
Holocene Impact Working Group
The Holocene Impact Working Group is a group of scientists from Australia, France, Ireland, Russia and the
USA who hypothesize that meteorite impacts on Earth are more common than previously supposed....


Homogenocene
Neolithic Subpluvial

Older Peron

Piora Oscillation

10th millennium BC

Last Glacial Maximum



1 E11 s
Cenozoic Era
Prehistory
http://www.absoluteastronomy.com/topics/Holocene
A lack of extant erosion shows that Mount Cleveland is likely a Holocene volcano.
A lack of extant erosion shows that Mount Cleveland is likely a Holocene volcano.
http://en.wikipedia.org/wiki/Mount_Cleveland_(Alaska)
Mauna Loa has probably been erupting for at least 700,000 years and may have emerged above sea
level about 400,000 years ago, although the oldest-known dated rocks are not older than
200,000 years.[4
http://en.wikipedia.org/wiki/Mauna_loa
mt shasta
There are many buried glacial scars on the mountain which were originally created in recent
glacial periods ("ice ages") of the present Wisconsinian glaciation. Most have since been filled-in
with andesite lava, pyroclastic flows, and talus from lava domes. Shastina, by comparison, has a
fully intact summit crater indicating that Shastina developed after the last ice age.
About 593,000 years ago andesitic lavas erupted in what is now Mount Shasta's western flank
near McBride Spring. Over time an ancestral Shasta stratovolcano was built to large but
unknown height; sometime between 300,000 to 360,000 years ago the entire north side of the
volcano collapsed, creating an enormous landslide or debris avalanche, 6.5 cubic miles (27
km3)[11] in volume. The slide flowed northwestward into Shasta Valley where the Shasta River
now cuts through the 28 miles (45 km) long flow.
What remains of the oldest of Shasta's four cones is exposed at Sargents Ridge on the south side
of the mountain. Lavas from the Sargents Ridge vent cover the Everitt Hill shield at Shasta's
southern foot. The last lavas to erupt from the vent were hornblende-pyroxene andesites with a
hornblende dacite dome at its summit. Glacial erosion has since modified its shape.
The next cone to form is exposed south of Shasta's current summit and is called Misery Hill. It
was formed 15,000 to 20,000 years ago from pyroxene andesite flows and has since been
intruded by a hornblende dacite dome.
Nearby Black Butte from Weed, California
Since then the Shastina cone has been built by mostly pyroxene andesite lava flows. Some 9,500
years ago, these flows reached about 6.8 miles (10.9 km) south and 3 miles (4.8 km) north of the
area now occupied by nearby Black Butte (see image at right). The last eruptions formed
Shastina's present summit about a hundred years later. But before that, Shastina, along with the
then forming Black Butte dacite plug dome complex to the west, created numerous pyroclastic
flows that covered 43 square miles (110 km2), including large parts of what is now Mount
Shasta, California and Weed, California. Diller Canyon (400 feet (120 m) deep and 0.25 miles
(400 m) wide) is an avalanche chute that was probably carved into Shastina's western face by
these flows.
Mount Shasta from Mount Shasta City, CA. Taken July 2, 2009
The last to form, and the highest cone, the Hotlum Cone, formed about 8,000 years ago. It is
named after the Hotlum glacier on its northern face; its longest lava flow, the 500 feet (150 m)
thick Military Pass flow, extends 5.5 miles (8.9 km) down its northwest face. Since the creation
of the Hotlum Cone, a dacite dome intruded the cone and now forms the summit. The rock at the
600 feet (180 m) wide summit crater has been extensively hydrothermally altered by sulfurous
hot springs and fumaroles there (only a few examples still remain).
In the last 8,000 years, the Hotlum Cone has erupted at least eight or nine times. About 200 years
ago the last significant Shasta eruption came from this cone and created a pyroclastic flow, a hot
lahar (mudflow), and three cold lahars, which streamed 7.5 miles (12.1 km) down Shasta's east
flank via Ash Creek. A separate hot lahar went 12 miles (19 km) down Mud Creek. This eruption
was observed by the explorer La Pérouse, from his ship off the California coast, in 1786.[3]
http://en.wikipedia.org/wiki/Mount_Shasta
The height above ground where surface friction has a negligible effect on wind speed is called
the "gradient height" and the wind speed above this height is assumed to be a constant called the
"gradient wind speed".[7][12][13] For example, typical values for the predicted gradient height are
457 m for large cities, 366 m for suburbs, 274 m for open terrain, and 213 m for open sea.[14]
Although the power law exponent approximation is convenient, it has no theoretical basis.[15]
When the temperature profile is adiabatic, the wind speed should vary logarithmically with
height,[16] Measurements over open terrain in 1961 showed good agreement with the logarithmic
fit up to 100 m or so (within the surface layer), with near constant average wind speed up
through 1000 m.[
http://en.wikipedia.org/wiki/Planetary_boundary_layer
Pele's greatest rival was Poliahu, goddess of snow-capped mountains
http://www.coffeetimes.com/pele.htm
'ohelo berries can be used as metaphor overthrowing tradition/s.