FAGHt
HRNU BULLKT1N, RN1), OIUCMOn, THUILSDAY, AVflUflT 10, 10UO.
t
P
I
CROSBY REPORT
TELLS HISTORY
OF EARLY AGES
(Contlnuod from pngo 1.)
to tholr Imported flulillty, thcso
lavas illd not, na n rulo. extend far
from tho vonls, which wcro chlolly
confined to tho great fissure, tho
characteristic, also, ot subordinate
and branch flBsures. Prom this
poriod dato tho most, at least, ot
tho old, orodod rhyollto volcanoes
mid plugs scattered ovor tho plateau
for 50 to 100 miles caBt ot tho Cas
cades and protruding as stcptocs
through tUo subsequent great flows
ot basalt. Tho mora important only
ot thcso stcptocs havo been named
nnd mapped, Including: Newberry
Crntor (Paulina Mountains), Pino
Mountain, Powell Butte, Horse.
Hdgc, Smith's Rock, Gray's Unite,
Haystack llutto, Hampton Butte,
Glass Buttos, Wngontlro mountain,
Horso Mountain, Junlpor Mountain,
Coyote Hills, etc.
lrcf Deposits Formed.
Although tho relatively ncld nnd
sluggish lavas ot this period did
not spread far from the vents, nnd
contributed but little, and that little
very locally nnd irregularly, to tho
upbuilding ot tho general surfucc ot
tho plateau, they have, neverthe
less, by virtue of tholr hardness nnd
durability, played an Important role
as dralnago controls, or natural
dams retarding and regulating tho
discharge ot rivers. In tact, It
would bo difficult to And a more
striking or pertinent illustration
than is presented In the old stock
or mass ot rhyollto to which wo owe
Ilonham Falls, tho most Important
and most beautiful cascade ot this
shooting river, a natural dam si to,
and aboro it a natural reservoir
Bite as wall.
The scdlmonts of tnis period, con
sisting of alternate beds of ash, lapll
11 and lava, aro known to geologists
ns tho Clarno formation of tho John
Day valley and attain here a thick
ness of about 400 feet.
Following tho Clarno formation,
in Mloceuo or mid-Tertiary time, vol
canism still prevailed, but tho lavas
were, predominantly, of moro basic
type basaltic rather than andlsltlc
or rhyolltlc. Tho eruptions wcro,
for a long tlmo of a highly exploslvo
character, yielding In what Is now
tho John Day valley and, presumably
also, in tho region traversed by the
Deschutes river, a vast thickness,
possibly soverat thousand feet, ot
stratified anh or tuff, constituting tho
John Day scries. This was followed,
still in tho Miocene poriod, by gi
gantic flssuro eruptions of basalt
tho many successive thick flows ag
gregating 2000 to. possibly, 4000
feet in thickness. This Is the great
Columbia lava formation, which, nat
urally, attains Its maximum develop
ment in tho valley of the Columbia,
and is, presumably comparatively
thinwhero It mantles tho crest ot
cono time tho great vnlloyn of tho
Columbia on tho north nnd tho Snnko
on tho south woro filled to overflow
ing and to n depth nt their lower cuds
of fully 4000 feet.
Somo conception of tho length of
tho poologlc periods Is nftorded by
tho prodigious amount ot erosion re
quired to reopen tho lnva-floodod
cnnyouB nnd thou, nttor they had
been filled by tho Mnscall and Hat-
tlesnako formations, to opon thorn
ngnln nnd to tholr present profound
depths.
flinders Played Piirt.
Tho principal eplsodo ot tho earlier
Quaternary or Plolstocono tlmo was
tor this region, ns tor tho greater
part of tho continent, tho culmination
ot glnclatlon. Thoro is llttlo or no
evidence of general, glnclatlon or of
nn Ico sheet covering tho uppor part
even of tho Deschutes valley. The
valley glaciers, remnants of which
now linger on tho slopes and In tho
craters of tho higher Cascado volcan
oes, Including tho Sisters nnd llrokcn
Top, appear never to havo extendod
tar down tho eastern slopo of tho
range. It Is truo that a largo pro
portion ot tho lakes and lakelets dot
ting tho lower enstcrn slopo ot tho
ran go down to about nn elevation ot
4400, nnd to still lowor levels farth
er north, nro duo to mornlnnt dams.
To this class belong Odell nnd Cres
cent lakes and many minor oxnm
ples. Characteristically, they occu
py, deep nnd narrow vnlloyn on tho
rock walls of which tho lateral nnd
tormlnul moraines nro roadlly traced
to heights. In somo caso ot 1000 feet
or moro above tho present water lev
el. .Many of tho lakelets, also, oc
cupy glacial cirques or rock-rlinmed
basins directly duo to tho eroslvo ac
tion of tho valley glaclors. Equally
conclusive evidence of former glac
lal extension is afforded by the dls
trlbution or tho bowlder clay or
ground moraine. As this would bo
tho case but for tho heavy mantle of
post-glacial pumico dust and lapllll
covering tho ontlro region and ob
scuring tho drift and other surface
formations. Moro convincing, under
tho circumstances, Is tho testimony
of tho washed or modified drift, sand
nnd gravel, especially ns regards Its
topographic liifluonco. A particular
ly clear examplo is afforded by tho
Twin lakes, southeast of Crane prair
ie, and 10 miles cast of tho Cascado
crest. Tho only satisfactory expla
nation of tho deep depressions occu
pied by theso lakelets Is the subse
quent melting of masses of ico bur
icdln modified drift. From these
witnesses wo learn that tho Cascado
glacier or Ico cap extended at least
this far to tho eastward.
On tho cast sldo of the Deschutes
valley wo find evldenco that New
berry crater was occupied by Ico and
that from it a glacier ndvanced sev
eral miles down tho valley of Paulina
creek and to lesser distances down
other radiating valleys.
Heat Predominated.
We must conclude, then, that gln
clatlon has not played an important
Just nbovo
tho stream
northward,
rhyollto on
tho Blue mountains. Tho numerous rolo In tho development of tho Dos
dikes of basalt cutting through tho chutes valley, not even ot this most
underlying formations mark in part
the channols through which tho lava
lias come up from the Interior ot tho
earth.
Following this great outpouring
of lava, tho most extenslvo In geo
logic history, and almost completely
filling tho broad and deep valleys
of tho Columbia and Snake rivers, in
lata Miocene tlmo, further explosive
eruptions spreading over tho lava
plateau of Central Oregon hundreds
'of feet ot ash, now consolidated to
tuff and constituting the Mnscall
formation.
elevuted section ot it It further
proof were wanted It would bo found
in a consideration of tho cones ot
cinder nnd lapllll dotting tho faco
ot tho country nnd dating from tho
earliest Quaternary tlmo down to tho
human period and almost to tho pres
ent. Thut somo of tho cones ante
date tho period ot maximum glacial
development Is practically certain,
but so far us noted they havo not
suffered appreciable or at least not
Important, glacial erosion; and yet
it would bo difficult to find a for
mation moro susceptible to rapid cro-
Unconformably above tho Mascall . slon. In this field tho two antagon
ibods was doposlted in I'lioceno or.lstic agencies, volcanlsm and glacla
lato Tertiary tlmo, 100 feet, moro or. Hon, or flro and frost, havo been ac
less of water-worn gravel and ovor-(tlvo for an Indefinitely long poriod,
lying rhyollto tuff and lava. This tho volcano building up nnd tho glu
ts tho Rattlesnake series ot Morrlam Icier wearing down tho faco of tho
nnd of its occurrence In the Benham .land. But to tho present tho forces
falls district there can bo llttlo. of flro havo greatly predominated
doubt.
Great Valley Filled.
Whether tho stupendous eruptions
over those of frost; though it ap
pears not imposslblo that with tho
gradual extinction of tho volcanic
ot tho Cascado volvanoes result In! energy, now so plainly In progress,
any part of tho district In lava, cin- tho glacier may yet bo in tho ascend
dors or ashes (dust and lapllll) do- ant, at loast this might bo antic!
pends upon tho distance from tho patod but for tho obvious fact that
vont. Cinders pile up around tho glaciatlon is also on the wane,
vent lu stoop cones. Tho ashes aroj Tho chiot Incidents or phases o(
spread over areas proportional to tho expiring volcanlsm embraco tho
tholr flnonoss and to the force and formation of tho widespread and
shift ot tho wind, but attain notablo thick mantlo of pumiceus lapllll or
thickness only within modorato dls- comminuted pumico, which, liko a
tances, possibly Bcores, but not hun-j snowfall, covers tho face ot tho coun
dreds, ot miles from tho vent. Tho try, and tho building of tho latest and
In ! still uucroded basaltic flows
lava or molten rock, if Issuing
sufficient volume, us in the great fls
suro oruptions, may, howover espe
cially it the topography or surface
and
cones, tho series ending, for tho tlmo
bolni;, with Lava butto and the flow
spreading from Its base. This flow
gradiont be favorable spread ovor, turned tho Deschutes river ovor tho
truly vast uroas, oven many thou
sands of square miles,
Tho throw of tho great Cascade
fault being up to tho west and down
to tho cast, tho normal movoment of
tho oxtruded lava lias been, to a
largo extent, upstream, or, moro ox
actly, into a closed basin, accumu
lating liko water in a reservoir and
attaining its maximum thickness or
depth In tho lowest parts of the origi
nal valleys, It was thus that in Mlo-
rhyollto rldgo, thus inaugurating
Benham falls and permitting tho silt
ing up of tho broad, shallow basin
above tho falls, which bocame there
by an Idoal reservoir floor. Con
temporaneously, too, with tho de
clining volcanlsm and glaclatlou has
been tho final canyon cutting accom
plished by tho Deschutes and its
principal tributaries north of Ben
ham falls and, especially, north of
Bond.
OKscmin'iVH okolooy of thi:
11KNIIAM F.Iil.S 1UKT1UCT
Tho llhyollto Dike
This nppeurH to ho, on tho wholo(
tho best geological designation ot
tho hold rock rldgo standing athwart
tho Deschutes valley In tho latltudo
ot lleuhnm Fulls, nnd to which the
river owes this jnost Impressive ot
all Its chutes, Tho rldgo raugoH
from 100 to possibly 200 foot lu
elovntton nbovo tho river; varies
lu width, roughly, from one-fourth
to throe-fourths ot n mllo; nud has
boon traced approximately two
miles, from tho vicinity ot tho wost
sldo rond to tho point- 2,000 foot
east ot tho head ot tho falls whoro
tho rhyollto Is seen to pnss under
tho Lnvn llutto flow ot basalt. So
far. It Is, In its relation to tho val
ley, a great natural dam, extending
from a point on tho wostern slopo
well nbovo any contemplated How
lino across moro than half tho prob
able breadth ot tho valtoy below
that line.
Tho river first encounters Iho
rhyollto near tho westorn end of
tho rldgo; nud, promptly turning to
tho eastward, closoly follows Its
southern or upstream border to tho
margin of tho now lava. I lore,
tho abandoned bridge,
turns abruptly to tho
flowing between tho
tho loft nnd tho now
lava on tho right for halt a mllo
to tho apox of tho marked re
entrant nnglo ot tho rldgo, where
Its crest descends to tho river lovol
nnd tho river escapes ncross tho
rldgo, which Is bouudod on tho
north by n tone ot basalt tuff rep
resenting, no doubt, tho old Colum
bia basalt. ,
Tho rhyollto Is throughout a mas-
slvo and wonderfully homogeneous,
hard, compact and resistant Igneous
formation, which may, probably,
best bo regarded as tho plug or
neck ot nn anclotit volcano which
has long since been removed by
erosion. Plnlnly enough, tho rhyo
llto is older than both tho nower
and tho older basalt flows by which
it Is environed nnd nbovo which It
rises as a genuine stoptoo. Con
cerning tho courso and extent ot
tho rhyollto beyond tho cast end ot
tho rldgo, or tho lino whoro It dis
appears beneath tho Lava Butto flow
ot basalt wo can only conjecture;
but tho probabilities will bo dls
cussd in a later section.
The Columbia basalt Is tho great
lava formation of tho Columbia
plateau, covering continuously and
to n vast thickness many thousands
and scores of thousands ot square
miles. From tho open fissures and
craters ot tho Cascades tho highly
fluid molten rock was poured out
flow after flow, filling tho broad
valley ot tho Columbia and cover
ing to lessor depths all but tho
higher parts ot tho broad summit
ot tho Bluo Mountains, layers of
volcanic dust and lapllll alternat
ing to somo oxtent with tho mas
slvo shcots ot columnar basalt.
Although formed back In Mlocono
time, tho Columbia basalt . shown,
outsldo of tho canyons, whore it has
felt tho powerful eroslvo action of
tho rapid streams, but llttlo evl
denco of erosion. Whero not cover
ed by soil it Is still hard and black
and exhibits tho gently undulating
or wavy nurfaco of tho original flow,
as woll as tho prismatic Jointing
and prcssuro ridges. In fact, It ap
pears prohablo that whoro soli Is
present It has boon derived chlofly
from volcanic dust and lapllll, and
not from tho solid lava.
Vt'vnt Hide IhiNiilt Newer
In tho Benham Falls district, or,
moro gonornlly, south of Bond,
abovo which tho rlvor and tho Cas
cado rango aro slightly dlvorgont
northward, tho basalt of tho op
posite slopes ot tho valley, tho east
slopo and tho wost slopo, is moro or
loss distinctly contrasted, especially
as regards indications of ago. Tho
basalt of tho west slopo has, of
courso, boon derived from tho Cas
cado rango; whilo that of tho east
slopo may most reasonably bo ro
ferred to the gigantic Newberry
Crater and Its subsidiary vonts with
in a radius of ton to fifteen miles,
which havo, no doubt, boon moro
roccntly actlvo than tho neighbor
ing soctlon of tho Cascado, rungo.
At nny rate, tho west slopo basalt
Is, at all points south of Jlond, do
cldedly moro weathored and older-
looking than that ot tho cast slopo.
Owing to tho moro weathored
and decomposed aspect ot tho west
sldo basalt, its outcrops aro fowor
and loss bold. And slnco it In tho
older flow wo may assumo that it
oxtendH eastward somewhat in
definitely, or without regard to tho
wostern limits ot tho newer oast
sldo flow. In other words, It ap
pears probable thut tho eastern
overlaps tho western flow to somo
oxtent. And It lu a natural .sug
gestion that ovidonco of such over
lap may bo affordod by Homo of tho
boring pt tho Ilonham Falls area.
Tho now boring (1) ut Minor's
Cabin or Damslto "A" Is ot special
interest lu this connection, slnco it
shows, from tho surface down, hard,
sound basalt for tho first 05 foot
(eastern and newer flow) followed
by brown to red, oxldltod nud
wonthorod hnsoU (wostern nnd older
flow), A similar, lu fact nu almost
Identical, record In afforded by Bor
ing No, 5 ot tho original Minor's
Cabin Horlos, nud, again, by tho
boring of tho BronkH-Scnulun Lum
ber Company (8), on tho east hIiIu
road, u llttlo moro than two miles
south-HOUthcaHt ot Minor's Cabin,
Here, also, tho drill, after passing
through ovor 00 toot of tho hard
and comparatively fresh hatialt ot
tho eastern flow pouotratod the oxi
dized and rotten basalt of tho wost
ern flow, and eudod lu It ut a depth
ot 100 fot.
llhyollto Itlilgo Volcnnlu Node
Wo nro, thus, Justinod lu conclud
ing that the old, decayed western
flow of basalt probably extends nt
lonst this tar to tho eastward; nnd
this Is far enough to Insure Its un
derlying practically tho ontlro area
ot tho proposed reservoir, save
whero It may hnvo boon removed
by tho rlvor In tho development of
Its channel. But for this possible
exception, wo might, then, nssumo
for tho reservoir n continuous sub
floor of tho older and, probably,
moro Impervious basalt.
Whether tho flood ot basalt from
olthor sldo over submerged tho
transverse rhyollto rldgo, Is vory
doubtful. On tho west side ot tho
rlvor, north ot Benham Falls rhyo
llto tuff Is seen to ho capped with
basalt. But tho rhyollto ot tho Ben
ham Falls rldgo, with Its vortical
flow structure, must bo rognrdod ns
a truo volcanic neck. Tho basalt
falls fur short ot covering It now;
nnd slnco the sharp rldgo of rhyo
llto must havo lost elevation by
erosion much moro rapidly than
tho broad plain of basalt, wo can
only coucludo that tho floods ot
basalt surged nround tho rhyollto
relief but did not ovortop It.
Iiivn Tunnel
No feature ot tho basalt Is ot
greater scientific Interest or prac
tical liuportnnco than tho lava tun
nel. This exists where after tho
main part ot a flow has cooled and
solidified, cracking of tho crust al
lows tho still molten residuum to
cscnpo, and tho tunnel, or a vacant
spaco of somo form, naturally ro
suits. Whethor or not water or
soma other constituent ot tho basalt
tending to promote Its liquidity,
determines tho location or forma
tion ot a tunnel Is nn unsolved
problem; but to tho writer It ap
pears moro prohablo that tho princi
pal factors aro differential cooling,
gradient and velocity.
Tho Incandescent lava Is cooled
and stiffened by contact with tho
cool earth below and tho cool air
abovo. Botwcon tho two crusts
thus determined It flown most rapid
ly In tho lines ot highest gradient
(most rapid descent). Whom tho
gradiont Is low and tho movoment
sluggish, as on upland areas, tho
lava first solidifies through tho on
tlro thickness of tho flow; nud tho
moro fluid, rapidly moving portions
aro confined moro nnd moro to the
vnlloyn or topographic lines of
steepest descent. Tho hottest, most
fluid and most rapidly flowing lava
will bo that freshest from tho crntor
or flssuro nnd tho subterranean
sources, and when tho Intter finally
tall, tho lava within tho tunnol
drains away and leaven tho tunnol
ompty.
Luvn Tunnel Important
Tho normal topographic relations
of tho lava tunnol nro of special
practical Importanco In connection
with this study bocuuso of Its
tendency to follow tho axis ot tho
vulloy as It oxlntod at tho tlmo of
tho eruption and tho outpouring ot
tho lava, and also bocausa thoro
exists In tho Doschutcn valley abovo
Ilonham Falls, and thoro In tho pro
posed reservoir area, a magnlllcent
examplo of tho lava tunnol.
Tho ontranco to thtr tunnol Is on
tho oast sldo of tho vulloy, about
ono and ono-halt mlloB southeast ot
tho main road at a point ono mllo
south ot Lava Butjo; and probably
In Soctlon 35 of Tp. 10 8., II. 11 K.
For tho discovery of tho tunnol and
for accosH to its Interior wo aro
Indebted to a local fall ot tho roof,
duo, porhapn, to tho passago of
oarthquako vibrations.
Tho gonoral courso of tho tunnel
is northwest-southeast; but it Is far
from straight, winding much us a
surfnea stroam of wator might in
traversing tho samo territory.' It
is said to havo boon travorsod for
a mllo southeasterly from tho on
tranco; and In company with As
sistant Englnoor Irving B, Crosby
I travorsed It to a point nearly ono"
and a fourth miles northwostorly
from tho ontranco,
Kroslon Blight.
Tho tmnsvorso dimensions of tho
tunnel aro fairly uniform say 20
to 30 foot wldo nnd 15 to 25 foot
high, disregarding oxtromon;, nnd
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T
Its nbsonco. Tho lluor Is sensibly
level, trnvo whoro encumbered by
sand washed lu through cracks lu thu
roof or by rare falls of rock Tho
tunnel, however, Is not luvul; but
It bus n surprisingly uniform north
wostorly gradient, agreeing, approxi
mately, with the general slope ot
tho ground nbovo It, Toward Iho
Inner or northwestern ifntl ot tho
tunnel, tho said derived lu part,
nt least, from thu roof, becomes
moro and moro abundant, ami final
ly reaches tho root and closes Iho
tunnel, without, however, appreci
able contraction of Itn bore. As tho
sand gnlim lu depth It npponrs to
gain, also, lu moisture, tho ap
pearance being, at tho last, that
tho tunnel Is Hearing tho water
table. Klthor this supposition Is
ot tho tunnol.
Ono dlfllculty In deriving thu main
part or nny largo part, of tho tun
nel, sand through tho roof Is Iho
truo or tho damp snud conserves
with great tenacity tho drip water
general tightness of tho tunnel, tho
floor nud lateral walls being almost
nlmolutely tight, and tho roof ditto,
so far as could bo neon by cnudia
light. Tho sand Is of very uniform
character, entirely free from clay
clearly of volcanic origin, nnd Iden
tical In chnrnclor with largo vol
umes ot sand which Iho drill han
shown lo underlie tho Benham Falls
reservoir area. To account for Its
nbundnut prcsonco In tho lowor part
ot tho tuunul wo need only assumo
a local collapso of tho tunol roof.
Tho tunnel In much newer than tho
basalt ot tho western slopo nnd
contemporaneous with that ot tho
eastern slope, but older than tho
gorge which tho river has cut In
tho newer and older basalts, nnd
older still than tho volcanic and
organic scdlmonts deposited In this
gorge and over tho general floor
of Iho Bcnhnm Falls basin and tho
prospective reservoir.
Tunnel's Cotirno Nought
Wo aro, naturally, specially con
cerned to discover, If posslblo, Ilia
probable courso or thu lava tunnel
bononth tho reservoir area nud Its
relation to tho burled gorge of tho
Deschutes river, Tho snfost as
sumption In Hint, an previously Indi
cated, thu tunnel follows tho steep
est nnd deepest lino of flow of tho
east side basalt. This would bring
It to and Into tho undent gorge of
tho Deschutes river nt or nbovo tho
point whero Iho Deschutes or that
tlmo cut through tho rhyollto ridge.
That tho statin pressure nud tho
high liquidity ot tho column of lava
would maintain the discharge to tho
point of exhaustion, nud finally leave
the tunnol empty, Is most probable;
for the loan of heat sustained by
Iho lava lu Its passago through the
tuunul would ho Inconsiderable; nnd
lava suftlcleiilly fluid lo enter tho
tunnel would bo likely to complete
tho passage. This Is (ho conserva
tive view nnd certainly accords with
the present stnto of the tunnol,
especially with Itn rogulnr form and
smooth walls. It Is a perfect con
duit, of ample bore and well forti
fied against loss of bent; but be
coming, an It slowly cooln, nu Ideal
channel of n subterranean river.
It does not appear, however, to
hnvo been occupied, even temporar
ily, by a stream of water, nt least
not In tho part now accessible, for
wo detected not tho slightest trace
or Indication of stream erosion, or
deposition; oven tho sand with
which the tunnel Is finally clogged
hnvlng moro tho appearance of hav
ing boon deposited by drip wator
than by running water.
Tho tunnel Is not only nn Im
portant contemporaneous structural
feature of tho great east sldo flow
ot basalt; but It In probably through
out, nud not ntono whoro tho root
has fallen, n comparatively shallow
feature; for this sheet of basalt has
not been covered, along Iho proh
ablo lino ot tho tunnel, by nny later
formation, save, perhaps, tho flood
plain deposit (silt, etc.) of tho
(Continued on Pago 7.)
f9W9999S9339J39J!fJ3
BUCKHECHT
iHOES
tho root rangos from 20 to 40 toot
In thickness. Tho walls aro sur
prisingly smooth, oxcopt for tho
minor drip forms ot lava; nnd tho
characteristic columnar Jointing or
basaltic structuro is conspicuous by
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