Open File Report 81-07, The low temperature geothermal ... - WA - DNR
STATE OF WASHINGTON DEPARTMENT OF N A T U R A L RESOURCES D I V I S I O N OF GEOLOGY AND EARTH RESOURCES OLYMPIA, WASHINGTON 98504
T H E LOW TEMPERATURE GEOTHERMAL RESOURCE OF T H E YAKIMA REGION - A PRELIMINARY by John H . Biggane
Open-File Report 81-7
September 1981
REPORT
Table of Contents L i s t of Figures
iii
L i s t of Tables
v
Introduction
1
Location and Topography
1
Stratigraphy of the Yakima Region
1
Grande Ronde Formation Vantage Member of the Ellensburg Formation Wanapum Formation
2 3 3
Frenchman Springs Member
3
Squaw Creek Member of the Ellensburg Formation . . .
4
Roza Member
4
Priest Rapids Member
4
Mabton Member of the Ellensburg Formation
5
Saddle Mountains Formation
5
Umatilla Member
5
"Huntzinger" Valley Flow (Asotin Member?)
5
Selah Member of the Ellensburg Formation
6
Pomona Member
6
Rattlesnake Ridge Member of the Ellensburg Formation
6
Elephant Mountain Member
6
Upper Ellensburg Formation and Quaternary Sediments.
7
Previous Geophysical Investigations in the Yakima Region .
8
Table of Contents ( c o n t . ) Previous Geothermal Research in t h e Yakima Region. . . . .
9
Temperature Data
9
Calculation of Geothermal Gradients i n the Yakima Region
10
Geothermal Gradients i n the Yakima Region
12
Accuracy of the Geothermal Gradients Obtained by the Regression Analysis
12
Projected Land Surface Temperatures and Slope Aspect
14
Chemical Geothermometers
17
Summary
22
References
23
Appendices Appendix A:
Symbols Used on Figures 2 through 8 and 13 through 26
Appendix B:
Well Locations and Bottom Hole Temperatures from Wells in t h e Yakima Region
Appendix C:
Well Data Groups Used in t h e Bottom Hole Temperature Regression Analysis
ILLUSTRATIONS Page Figure
1.
Generalized stratigraphic section
2a
2.
Stratigraphic correlation line N o . 1
2b
3.
Stratigraphic correlation line N o . 2
2c
4.
Stratigraphic correlation line N o . 3
2d
5.
Stratigraphic correlation line N o . 4
2e
6.
Stratigraphic correlation line N o . 5
2f
7.
Stratigraphic correlation line N o . 6
2g
8. Stratigraphic correlation line N o . 7
2h
9.
Typical natural gamma response of the Umatilla and Squaw Creek Members
4a
10. Spring and well location map 11. Temperature logs of the DNR Black Rock Well No 12.
"Step-like" distortion of a temperature log
In pocket 1
10a 10b
13. Temperature versus depth for group 1
12a
14. Temperature versus depth for group 2
12b
15. Temperature versus depth for group 3
12c
16. Temperature versus depth for group 4
12d
17. Temperature versus depth for group 5
12e
18. Temperature versus depth for group 6
12f
19. Temperature versus depth for group 7
12g
20.
Temperature versus depth for group 8
12h
21. Temperature versus depth for group 9
12i
22.
Temperature versus depth for group 10
12j
23. Temperature versus depth for group 11
12k
ILLUSTRATIONS— Continued Page Figure
24.
Temperature versus depth for group 12
12L
25.
Temperature versus depth for group 13
12m
26.
Temperature versus depth for group 14
12n
27.
Well data group location map
In pocket
27a. M a p showing locations of w e l l data groups with respect to the locations of springs and wells
In pocket «
28.
Temperature logs, line N o . 1
12o
29.
Temperature logs, line N o . 2
12p
30.
Temperature logs, line N o . 3
12q
31.
Temperature logs, line N o . 6
32.
Temperature logs, line N o . 7
12s
33.
Slope aspect versus normalized surface temperature
14a
.
12r
L i s t of Tables Table
Page
1
Geothermal G r a d i e n t s , Land Surface Temperatures, and Depths to the 20°C Isotherm
13
2
Measured and Predicted "Aquifer" Temperatures
15
3
Mean E l e v a t i o n , Slope Aspect, and Normalized Land S u r f a c e Temperatures f o r Well Data Groups 1 - 1 3
18
4
Chemical Data f o r Springs in Yakima County, Washington
19
5
Chemical Data f o r Wells in Yakima County, Washington
20
Introduction The low temperature geothermal resource of t h e Yakima region i s c u r r e n t l y at t h e i n i t i a l s t a g e of i t s development. utilize
Several domestic heat
pump
systems
the warm groundwater f o r space h e a t i n g , and l a r g e r i n s t a l l a t i o n s have
been c o n s i d e r e d .
This report provides a preliminary summary of t h e geothermal
resource f o r p o r t i o n s of t h e Yakima r e g i o n .
Location and Topography The Yakima r e g i o n l i e s in the western portion of t h e Columbia Plateau south-central
Washington.
The
region's
major
topographic
f e a t u r e s are a s e r i e s of s o u t h e a s t - t r e n d i n g a n t i c l i n a l valleys.
in
and s t r u c t u r a l
ridges
and
synclinal
The Yakima River serves as t h e r e g i o n ' s major drainage.
S t r a t i g r a p h y of t h e Yakima Region The lava flows interbedded
the
sediments
region's near-surface underlying
of
the
of
Columbia the
River
Basalt
and
(CRBG)
stratigraphic
section.
The
nature
of
units
the
the
rocks
b a s a l t i c l a v a s i s u n c e r t a i n , but they are probably r e l a t e d t o
o t h e r s , 1980).
are
exposed
in
the
future.
Alluvial
Formation throughout much of t h e lowlands 1976, 1977a, 1977b;
to
the
west
Oil and gas e x p l o r a t i o n boreholes are p r e s e n t l y
being d r i l l e d in Yakima County and should provide information geologic
and
Ellensburg Formation comprise t h e bulk of the
o l d e r volcanic rocks (Ohanapecosh Formation) t h a t (Bentley
Group
on
the
deeper
sediments o v e r l i e the Ellensburg
of
the
Yakima
region
(Campbell,
Swanson and o t h e r s , 1979a).
The t o t a l t h i c k n e s s of t h e Columbia River Basalts i s unknown but probably exceeds 1,000m in t h e Yakima 1980).
region
(Bentley,
1977;
Bentley
and
others,
All t h r e e formations of the Yakima Basalt Subgroup (CRBG)--the Grande
Ronde, Wanapum,
and
Saddle
Mountains
Formations—are
found
in
surface
exposures (Swanson and o t h e r s , 1979a). Individual b a s a l t flows u s u a l l y contain two major and
the
underlying
entablature,
c h a r a c t e r i s t i c s (Swanson, 1967; columns
are
typical
of
the
which
are
zones.
apart
Diery and McKee, 1969). colonnade,
the
colonnade
by d i f f e r i n g j o i n t Straight,
vertical
while t h i n n e r , i n c l i n e d , or curved
columnar j o i n t s a r e found in the e n t a b l a t u r e . both
set
zones,
Horizontal j o i n t s a r e found
in
A basal breccia i s o f t e n observed beneath t h e colonnade, and a
v e s i c u l a r zone o f t e n occurs at t h e flow t o p . An g e n e r a l i z e d s t r a t i g r a p h i c s e c t i o n i s shown in stratigraphic
correlation
lines
are
explained in Appendix A.)
are
shown
in
(Symbols used in Figures 2
through
geophysical
logs.
Neutron-neutron
Figures 2 through 8, but i t should be noted t h a t natural
gamma, gamma-gamma, and correlations.
Subsurface
These c o r r e l a t i o n l i n e s were c o n s t r u c t e d by
i n t e r p r e t i n g both d r i l l e r s ' and borehole logs
1.
f o r t h e lower Yakima, Black Rock, and Moxee
Valleys are shown in Figures 2 through 8. 8
Figure
neutron-gamma
logs
were
also
utilized
for
these
Formation t h i c k n e s s e s reported in l a t e r s e c t i o n s of t h i s
report
a r e apparent t h i c k n e s s e s , since dip c o r r e c t i o n s have not been made. An overview of t h e r e g i o n ' s geologic u n i t s i s
given
below.
Interested
r e a d e r s are r e f e r r e d t o Swanson (1967), Schmincke (1967a and 1967b), Diery and McKee
(1969),
Bentley (1977), Campbell (1976, 1977a, and 1977b), Swanson and
o t h e r s (1979a), and Bentley and o t h e r s (1980) f o r more
detailed
information.
Grande Ronde Formation The Grande
Ronde
Formation
has
been
informally
divided
into
four
m a g n e t o s t r a t i g r a p h i c u n i t s of which t h r e e (N x , R 2 , and N2) have been mapped in t h e region (Swanson and o t h e r s , 1979a).
The t o t a l thickness of t h i s formation
COLUMBIA RIVER BASALT GROUP
ELLENSBURG FORMATION
ELEPHANT
QUATERNARY AND UPPER ELLENSBURG SEDIMENTS
MOUNTAIN MEMBER
POMONA
RATTLESNAKE RIDGE MEMBER
SELAH MEMBER
MEMBER
UMATILLA
MABT0N MEMBER
MEMBER
PRIEST RAPIDS
OUINCY
MEMBER
DIATOMITE?
ROZA MEMBER
SQUAW CREEK MEMBER
FRENCHMAN VANTAGE SPRINGS MEMBER MEMBER
GRANDE RONDE FORMATION
FIGURE 1 GENERALIZED STRATIGRAPHIC SECTION
13118-,
12N/20f-36PI
I IN/21£·1161.1
I IH/21f•lfil'I
I IN/21E·22G2
IIH/21£·361CI
1-
w w LL
llltl
91li -
'. I
11111
IN
12i
121 ·
-61
l.
11111 -
·Ill
I
- ·till
·61
--
; }ll8
- · 12i
·1 - -11111
•
1111
-
~ s r r ~ .... l11~-~-»9~c-rn · s,&tJ
NN
NN
s29 I
'3-r - ~ f " t - l n a NN
~..32l..CliiflS7~----11T-~ru::mrrszSEr;r.ut- -791
NN
FIGURE FIGURE 22 STRATIGRAPHIC STRATIGRAPHIC CORRELATION CORRELATION LINE LINE ##11
NN
··1 ts)
0-
13111
12N/28E-27NI
12N/211E-3,N2
llN/21lE-IIU11
I IN/21lE-,'IIU
(/)
er.:
131!111
1---
w
w w u._
li! :E
(/)
er.:
w ~ :c
3WI
241
ZAI
188
llll
121
121
61
61
-•
•
-61
-61
--
--
-121
-I
NN
NN
FIGURE FIGURE 33 STRATIGRAPHtC STRATIGRAPHIC CORRELATION CORRELATION LINF. LINE #2 #2
NN
FIGURE 4 STRATIGRAPHIC CORRELATION LINE
#3
FIGURE 5 STRATIGRAPHIC CORRELATION LINE #4
FIGURE 6 STRATIGRAPHIC CORRELATION LINE #5
FIGURE 7 STRATIGRAPHIC CORRELATION LINE #6
FIGURE 8 STRATIGRAPHIC CORRELATION LINE #7
in
the
Yakima region probably does not exceed 1,000m and may vary by as much
as 400m because of an i r r e g u l a r p r e - b a s a l t 1980).
Individual
topography
(Bentley
and
others,
flows average 20 t o 30m in thickness (Bentley and o t h e r s ,
1980).
Vantage Member of t h e Ellensburg Formation The Vantage Member of t h e Ellensburg Formation l i e s Ronde
and
Wanapum
Basalt
Formations
throughout
between
most
the
Grande
of t h e r e g i o n .
The
reported t h i c k n e s s of t h i s member ranges from 0 t o 30m (Diery and McKee, 1969; Bentley, 1977;
Bentley
and
volcaniclastic
sandstones,
others,
1980).
siltstones,
This
member
claystones,
conglomerate and d i a t o m i t e (Diery and McKee, 1969;
is
composed
of
and minor q u a n t i t i e s of
Bentley and o t h e r s , 1980).
None of t h e w e l l s f o r which s t r a t i g r a p h i c s e c t i o n s a r e
given
in
this
report
have p e n e t r a t e d t h e Vantage Member.
Wanapum Formation In t h e Yakima Region, t h e Wanapum Basalt Formation i s composed members:
of
three
t h e Frenchman Springs, t h e Roza, and t h e P r i e s t Rapids Members.
Frenchman Springs Member The Frenchman widespread
Wanapum
Springs Member,
(Bentley and o t h e r s , 1980).
Member, is
the
thickest
composed
of
up
(over to
been
tentatively
and
most
s i x flows a t Union Gap
None of t h e wells f o r which s t r a t i g r a p h i c s e c t i o n s
are given in t h i s r e p o r t have completely penetrated t h i s lave
150 m)
recognized
in
thickness ranges from 80 t o over 150m.
several
wells
member. where
Six
flows
t h e i r combined
Several t h i n (up t o 8 m t h i c k in well
11N/21E-22G2) d i s c o n t i n u o u s sedimentary i n t e r b e d s l i e between the flows of the Frenchman Springs B a s a l t Member.
Squaw Creek Member of t h e Ellensburg Formation The Squaw Creek Member of
the
Ellensburg
Formation
between
the
Frenchman Springs and t h e Roza Members throughout much of t h e study a r e a .
The
t h i c k n e s s of t h i s member ranges from 0 t o nearly 11 m. as
a
This member can be used
s t r a t i g r a p h i c marker due t o i t s high natural gamma response.
response i s shown in Figure 9. varies
lies
from
McKee, 1969;
The
composition
of
the
Squaw
A typical
Creek
Member
a d i a t o m i t e or j a s p e r o i d t o sandstone or conglomerate (Diery and Bentley and o t h e r s , 1980).
Roza Member The Roza Member occurs as a thickness
of
this
member
subsurface c o r r e l a t i o n l i n e s .
single
ranges
from
flow under
in
the
Yakima
region.
The
30m t o almost 45 m along the
A t h i n (0 t o 10m) i n t e r b e d (Quincy
Diatomite?)
s e p a r a t e s t h e Roza Member from t h e o v e r l y i n g b a s a l t flow.
P r i e s t Rapids Member Two b a s a l t flows of t h e subsurface
of
the
Priest
Rapids
Member
normally
occur
the
r e g i o n , with t h e upper flow t h i c k n e s s ranging from 10m to
almost 60m and t h e lower flow t h i c k n e s s ranging from 45m t o
almost
t h i n (up t o 5 m) i n t e r b e d occurs r a r e l y between t h e s e two f l o w s . was
in
60m.
Only one flow
found t o occur in several wells in the Black Rock and Moxee Valleys.
t h i c k n e s s of t h i s f l o w ranges from more than 20m t o 42m at
A
these
The
locations.
The upper s u r f a c e of t h e P r i e s t Rapids Basalt Member i s o f t e n deeply weathered (Bentley and o t h e r s ,
1980).
FIGURE 9 TYPICAL NATURAL GAMMA RESPONSE OF THE UMATILLA AND SQUAW CREEK MEMBERS
Mabton Member of t h e Ellensburg Formation The Mabton Member of the Ellensburg Formation o v e r l i e s the P r i e s t Member
throughout
much
of
v a r i e s from 0 m t o over 25m.
the
Yakima r e g i o n .
The thickness of t h e member
The Mabton Member i s composed
d e p o s i t s and a i r f a l l t u f f (Bentley and o t h e r s ,
Rapids
of
volcaniclastic
1980).
Saddle Mountains Formation Four members of t h e Saddle Mountains Formation are found region.
These
flows
Mountain Members.
in
the
Yakima
include t h e Umatilla, Huntzinger, Pomona, and Elephant
Interbedded
between
these
flows
are
sediments
of
the
Ellensburg Formation t h a t may reach t h i c k n e s s e s g r e a t e r than 100m.
Umatilla Member The Umatilla Member c o n s i s t s of a s i n g l e b a s a l t that
ranges
from
30m t o
poorly
developed
serves
as
a
a
thickness
Valley.
The
colonnade
columns 1 m t o 2 m in diameter and is o v e r l a i n by a
glassy e n t a b l a t u r e and flow t o p Member
with
60m in t h e s u b s u r f a c e of t h e Black Rock and Moxee
Valleys and from 60m t o over 80m in t h e lower Yakima contains
flow
breccia
stratigraphic
response (Crosby and o t h e r s , 1972).
(Schmincke,
1967b).
The
Umatilla
marker because of i t s high n a t u r a l gamma A t y p i c a l response i s shown in Figure
9.
"Huntzinger" Valley Flow (Asotin Member?) The Huntzinger Valley flow (Asotin Member?)
occurs as a " v a l l e y f i l l i n g "
b a s a l t flow s o u t h e a s t of Selah in the Moxee and Black Rock 1977;
Campbell,
1977a).
This
flow
Valleys
(Bentley,
has not been i d e n t i f i e d in any of the
s t r a t i g r a p h i c s e c t i o n s t h a t were prepared f o r t h i s
report.
Selah Member of t h e Ellensburg Formation The Selah Member, an i n t e r b e d Members, 1967a).
is
lying
between
the
Umatilla
and
Pomona
composed of v o l c a n i c l a s t i c d e p o s i t s and v i t r i c t u f f s (Schmincke,
The t h i c k n e s s of t h i s member ranges from l e s s than 10m t o over 15m in
t h e s u b s u r f a c e of t h e Black Rock and Moxee Valleys and from 0m t o
almost
25 m
in t h e lower Yakima Valley.
Pomona Member The Pomona Member, a s i n g l e b a s a l t f l o w , ranges in than
40m t o
over
thickness
80m in t h e subsurface of t h e lower Yakima Valley.
s u b s u r f a c e of t h e Black Rock Valley, t h e Pomona Member was found 30m t h i c k
from
and in several l o c a t i o n s was absent a l t o g e t h e r .
to
less In the
be
The Pomona Member
in t h e s u b s u r f a c e of t h e Moxee Valley was found t o be 45 m t o 55m t h i c k . upper
surface
of
the
Pomona
Member
only
The
i s o f t e n broken i n t o blocks of highly
oxidized s c o r i a (Schmincke, 1967b).
R a t t l e s n a k e Ridge Member of t h e Ellensburg Formation The R a t t l e s n a k e Ridge Member, an i n t e r b e d l y i n g between Elephant
Mountain
Members,
member
ranges
from
Pomona
and
i s composed p r i m a r i l y of s i l t s t o n e and c l a y s t o n e
with interbedded conglomerate (Bentley and o t h e r s , 1980). this
the
The
thickness
of
40m t o over 100m in t h e subsurface of t h e r e g i o n .
Bentley and o t h e r s (1980) r e p o r t t h i c k n e s s e s of up t o 200m f o r t h i s member
in
t h e Toppenish b a s i n .
Elephant Mountain Member The Elephant Mountain Member u s u a l l y occurs as one region
with
a
second
flow,
the
Ward
flow
in
the
Yakima
Gap, being found at Snipes Mountain
(Campbell, 1977b) and at Ward Gap (Schmincke, 1967a). flow
ranges
The thickness
of
this
from 8m t o over 15 m in t h e subsurface of t h e lower Yakima Valley
and i s absent in most of t h e w e l l s s t u d i e d in t h e Black Rock Valley.
In
the
subsurface of t h e Moxee Valley, t h e t h i c k n e s s ranges from 0 m t o j u s t over 10m. A t h i c k (48 m) s e c t i o n occurs in well 12N/20E-16D1, but i t i s uncertain whether the e n t i r e s e c t i o n i s Elephant Mountain B a s a l t .
Upper Ellensburg Formation and Quaternary Sediments Overlying t h e Elephant Mountain Basalt Member a r e Ellensburg and Quaternary
sediments.
younger
The t h i c k n e s s of t h e s e sediments range from 0 t o over
170m along the c o r r e l a t i o n l i n e s t h a t were prepared f o r t h i s r e p o r t , and i t i s expected t h a t g r e a t e r t h i c k n e s s e s would be found towards lower
Yakima
Valley.
The
Ellensburg
sediments
the
center
of
the
c o n s i s t of v o l c a n i c l a s t i c
d e p o s i t s with i n t e r b e d d e d conglomerates and sandstones, whereas t h e Quaternary sediments c o n s i s t of s i l t , sand, g r a v e l , and loess d e p o s i t s 1977a, and 1977b;
(Campbell,
1976,
Bentley and o t h e r s , 1980).
In regions where t h e Elephant Mountain and/or Pomona Basalt
Members
are
a b s e n t , t h e Selah and R a t t l e s n a k e Ridge Members are d i f f i c u l t t o s e p a r a t e from the
upper
Ellensburg
R a t t l e s n a k e Ridge Ellensburg
sediments.
Members
sediments
have
Where t h i s s i t u a t i o n occurs, t h e Selah and not
been
differentiated
from
the
upper
on t h e c o r r e l a t i o n l i n e s t h a t a r e shown in t h i s
report.
Previous Geophysical I n v e s t i g a t i o n s in t h e Yakima Region Gravity and aeromagnetic s t u d i e s have been conducted in the Yakirna region by Robbins and o t h e r s (1975), Konicek (1975), and Swanson and o t h e r s The
known
seismic
history
of
the
(1979c).
region i s summarized by Myers and Price
(1979). Analysis of g r a v i t y data suggests t h a t t h e b a s a l t s
(CRBG)
extend
to
a
depth of 2m t o 4 km in the Yakima and Toppenish Valleys and t o a depth of about l km
in
the
Ahtanum
Valley
(Robbins
and
others,
C i r c u l a r g r a v i t y lows were observed j u s t west of Zillah
and
Konicek, 1975).
cities
of
Yakima
and
were i n t e r p r e t e d as p o s s i b l y r e s u l t i n g from buried volcanic cones
or d e p o s i t s of rock having a lower others,
the
1975;
1975).
A
density
than
the
basalts
(Robbins
and
l a r g e g r a v i t y high, centered j u s t south of Union Gap, was
a t t r i b u t e d t o a t h i n l a y e r of sediments (Robbins and o t h e r s , 1975). The aeromagnetic study showed low i n t e n s i t y , over
the
valleys
and
small
amplitude
anomalies
anomalies of g r e a t e r i n t e n s i t y and amplitude over the
r i d g e s (Swanson and o t h e r s , 1979c).
Magnetic s t u d i e s
may
prove
useful
for
mapping t h e younger v a l l e y - f i l l i n g Yakima Basalts (Swanson and o t h e r s , 1979c). Magnetotelluric
studies
hold promise f o r e x p l o r a t i o n work below the level of
the b a s a l t s , but u n f o r t u n a t e l y none have been published f o r t h i s region. H i s t o r i c a l earthquake e p i c e n t e r s with hypocenters. than
10 km deep
c i t i e s of earthquake
Yakima
to
or
greater
tend t o be concentrated along a north-south l i n e between t h e and
epicenters
Ellensburg with
(Myers
hypocenters
and less
Price, than
t r e n d i n g , through
the
lower
Yakima
Valley
1979). 10ckm deep
concentrated along t h e same north-south l i n e and along line
equal
a
tend
t o be
northwest-southeast
(Myers
Magnitudes of 4 or l e s s have been r e p o r t e d f o r t h e s e shallow earthquakes (Myers and P r i c e , 1979).
Historical
and P r i c e , 1979). and
deep-seated
Previous Geothermal Research in t h e Yakima Region Geothermal r e s e a r c h in t h e Yakima region began with (1901).
In
this
report,
Smith,
a
report
noted the warm t e m p e r a t u r e s
by
Smith
(approximately
22°C) of the ground water flowing from a r t e s i a n wells in the Moxee Valley
and
c a l c u l a t e d geothermal g r a d i e n t s of 50 t o 73°C/km f o r t h e r e g i o n . Foxworthy (1962) reported an average geothermal g r a d i e n t of 40.5°C/km
in
water wells g r e a t e r than 15m deep in t h e Ahtanum Valley and suggested t h a t t h e rock type had l i t t l e e f f e c t on t h e g r a d i e n t . Blackwell (1980) reported geothermal g r a d i e n t s of 26 t o 37°C/km and
heat
flow values of 57 t o 64 mWm2- from water wells in the r e g i o n . Schuster (1980) noted t h a t goeothermal g r a d i e n t s of 50 consnonly
measured
to
70°C/km
were
in water w e l l s of t h e region and t h a t several very shallow
w e l l s produced warm w a t e r s .
Depth t o 20°C in water w e l l s of t h e Yakima region
were reported t o range from 9 m t o 471 m ( S c h u s t e r , 1980).
Temperature Data Subsurface temperature data in t h e Yakima region has the
Geological
Engineering
been
collected
Section of Washington S t a t e University (WSU), by
t h e Department of Geological Sciences of Southern Methodist University by
the
Washington
by
(SMU),
S t a t e Department of Natural Resources (DNR), by the U . S .
Geological Survey (USGS), and by the Oregon
Institute
of
Technology
(OIT).
Some 200 bottomhole temperatures and depths f o r wells in t h e Yakima region are given in Appendix B.
The
Well l o c a t i o n s a r e shown in Figure 10.
The accuracy of t h e temperature data v a r i e s with t h e
collecting
temperature
have an accuracy of
data
collected
by
SMU and
approximately ±0.2°C (Blackwell, 1980). c o l l e c t e d by the USGS and OIT i s unknown.
the
DNR
agency.
The accuracy of t h e temperature
data
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DIVIDE
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6,E- S . M. U.
TEMPERATURE - - - - TEMPERATURE and CHEMICAL
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The temperature probes u t i l i z e d by WSU since 1974 were r e c a l i b r a t e d in water
bath as p a r t of t h i s p r o j e c t .
because of t h e use of a nonstandard temperature
P r i o r c a l i b r a t i o n s were only approximate thermometer.
Previously
published
WSU
data have been c o r r e c t e d t o r e f l e c t t h e c a l i b r a t i o n changes.
The
change in c a l i b r a t i o n averaged l e s s than -1.0°C. temperature
a
probes
is
approximately ±0.4°C.
approximately
±0.2°C,
The
precision
and
the
of
field
the
accuracy
WSU is
The temperature probes used by WSU p r i o r t o 1974 a r e no
longer a v a i l a b l e , and t h e i r accuracy i s t h e r e f o r e u n c e r t a i n . The DNR Black Rock well #1 was logged on s u c c e s s i v e temperature
probe "A" and with t h e SMU probe VPR 1.
days
with
the
WSU
The temperature logs are
p l o t t e d in Figure 11 and are in c l o s e agreement, even though the WSU probe was t h e f o u r t h tool t o be run in the hole t h a t day.
C a l c u l a t i o n of Geothermal Gradients in t h e Yakima Region Determination of geothermal g r a d i e n t s in water w e l l s of the Yakima region is complicated by i n t r a - a q u i f e r borehole flow.
The net r e s u l t of t h e borehole
flow i s a d i s t o r t e d thermal g r a d i e n t , o f t e n assuming a the
recorded
temperature
distribution
step-like
form,
with
being u n r e p r e s e n t a t i v e of t h e actual
geothermal g r a d i e n t (see Figure 12). Three o p t i o n s were a v a i l a b l e t o past i n v e s t i g a t o r s in t h e i r determine
a c c u r a t e geothermal g r a d i e n t s in t h e s e water w e l l s .
most common method, i s based on recorded bottom hole
=
BHT
-
LST
to
The f i r s t , and
temperatures
assumed land s u r f a c e temperatures (LST), as shown in equation
Geothermal Gradient
attempts
(1).
(1)
(BHT)
and
10o
....... ..,J._
....... ..,J. ......
........
W$U .....
... ..
Yl'tl ....... 9111/80 _ _ _ _ _ _ _ _ $MU .......
___ 9112J8() __ - - ____ --15.2't
~ ~
_ _ _ _ _ _ _
_
15.23°c
/
21(),.----------
-25.2•c
330----------------------1-4
16
20 TEMPERATURE ("c)
FIGURE 11 TEMPERATURE LOGS OF THE ONR DNR BLACK ROCK WELL +#11
FIGURE 12 'STEP-LIKE' DISTORTION OF A TEMPERATURE LOG
For shallow w e l l s , i t i s very important t h a t an a c c u r a t e LST be t h i s method.
used
in
The e r r o r involved v a r i e s according t o equation (2) and is l a r g e
f o r even small e r r o r s in t h e LST.
This method was a p p l i e d in t h e Yakima region with because
accurate
LST
are
not
available.
The
very
limited
geothermal
success
gradients
of
neighboring w e l l s c a l c u l a t e d in such a manner o f t e n d i f f e r e d by more than
100
percent. A second method i s based on s e l e c t i n g p o r t i o n s of gradient
the
recorded
thermal
t h a t appear u n d i s t o r t e d and then c a l c u l a t i n g t h e geothermal g r a d i e n t
over t h a t i n t e r v a l .
This method i s time-consuming and does not allow a
check
on whether t h e s e l e c t e d i n t e r v a l i s a c t u a l l y u n a f f e c t e d by borehole flow. The t h i r d option a v a i l a b l e t o t h e i n v e s t i g a t o r i s t o d i s r e g a r d
the
data
altogether. A new approach t o t h e problem was developed f o r t h i s r e p o r t .
This method
involves a simple l e a s t squares l i n e a r r e g r e s s i o n a n a l y s i s of t h e BHT's group
of
wells.
a s p e c t and a n g l e .
of
a
Well data groups were based on proximity and s i m i l a r slope An a d d i t i o n a l well data group was s e l e c t e d f o r well
depths
g r e a t e r than 650m. The BHT l i n e a r r e g r e s s i o n a n a l y s i s has several advantages over t h e g r a d i e n t d e t e r m i n a t i o n methods. quality
data
can
be
other
Uphole flow does not a f f e c t t h e BHT, and poor
discriminated
by i t s "lack of f i t " t o the r e s t of t h e
data.
Downhole flow can a f f e c t t h e BHT, but in many cases t h e deepest portion
of t h e well appears t o be i s o l a t e d from t h e f l o w . temperature
A very
rapid
increase
of
i s recorded in t h e bottom of t h e w e l l s t h a t a r e i s o l a t e d from the
downhole flow ( s e e Figure 12).
Wells in which downhole flow does
BHT are discussed in a l a t e r s e c t i o n of t h i s
affect
the
Figures
13
report.
Geothermal Gradients in t h e Yakima Region Plots of BHT v s . depth f o r t h e well data groups a r e shown in through A.)
26.
The
(Symbols used in Figures 13 through 26 a r e explained in Appendix
results
summarized
in
of
the
Table 1.
least
squares
temperatures
range
range from 142 m t o 344m.
regression
analysis
are
Geothermal g r a d i e n t s f o r t h e shallow ( l e s s than 650m
deep) well data groups range from surface
linear
from
25.1°C/km
to
10°C t o 14°C.
52.2°C/km.
Projected
land
Depths t o t h e 20°C isotherm
The areal d i s t r i b u t i o n of t h e geothermal
gradients,
p r o j e c t e d land s u r f a c e t e m p e r a t u r e s , and depths t o the 20°C isotherm are shown in Figure 27. The m a j o r i t y of w e l l s t h a t were included in the deep ( g r e a t e r deep)
well d a t a group are l o c a t e d o u t s i d e of Yakima County.
that these
deep
relationship
wells
between
are
separated
BHT and
depth
by
large
an
excellent
The l e a s t squares
r e g r e s s i o n a n a l y s i s of t h e deep well data group y i e l d e d a geothermal of
29.9°C/km,
650 m
Despite the f a c t
distances,
e x i s t s (Figure 26).
than
gradient
a p r o j e c t e d land s u r f a c e temperature of 24.3°C, and a depth t o
t h e 100°C isotherm of 2,532m.
A l i s t i n g of t h e wells t h a t
were
included
in
t h e i n d i v i d u a l well d a t a groups i s given in Appendix C.
Accuracy of t h e Geothermal Gradients Obtained by the Regression Analysis Temperature logs (Figures 28 through 32) of wells in well data groups
4,
FIGURE 13
-
TEMPERATURE VS. DEPTH FOR GROUP 1
FIGURE 14
-
TEMPERATURE VS. DEPTH FOR GROUP 2
FIGURE 15
-
TEMPERATURE VS. DEPTH FOR GROUP 3
FIGURE 16
-
TEMPERATURE VS. DEPTH FOR GROUP 4
FIGURE 17
-
TEMPERATURE VS. DEPTH FOR GROUP 5
FIGURE
18
-
TEMPERATURE VS. DEPTH FOR GROUP 6
FIGURE 19
-
TEMPERATURE VS. DEPTH FOR GROUP 7
FIGURE 20
-
TEMPERATURE VS. DEPTH FOR GROUP 8
FIGURE 21
-
TEMPERATURE VS. DEPTH FOR GROUP 9
FIGURE 22
-
TEMPERATURE VS. DEPTH FOR GROUP 10
FIGURE 23
-
TEMPERATURE VS. DEPTH FOR GROUP 11
FIGURE 24
-
TEMPERATURE VS. DEPTH FOR GROUP 12
FIGURE 25
-
TEMPERATURE
VS. DEPTH FOR GROUP 13
FIGURE 26
-
TEMPERATURE VS. DEPTH FOR GROUP 14
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Gro up #
1 1.3+2 9.8°C /km T . 15N.
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1 7 1 m .,.... .,.....
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- -
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10 .0+45 .8°C / km 219m
1 / - - - ,-- --------Jr-- - -~.....::::-.......J,r - - - - -- I...!......- -1---....:_ / ,,, , 1 2 .o + 4 6 . 9° c 1 ':,m,.....-:-r---:,~-+-..;;..;::----=,- - - +- - - -- - --r----/ / / / T . 11 N
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Group #
13.0+ 40.0° C / km \
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175m
14.0+ 36.o 0 c t km
, ---
16 7 m
\
.... .......... \ I ', ......... \ I ', ' \ I ' ' -- - -I l---i--------+- -- - - - - - - - + - - - - - - -- + - - - - ---=-=--~1---- - - - - + -- - -- - - - ; - - - -- - - - - l - - - -- - ---1 I
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GRA NDVIEW
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I
PROSSER
,
..... ..... .....
T.8 N.
R. 16E .
R. 17E.
R.18E .
R.19E.
Sca le - 1 : 25 0 ,000 USGS Base Map
R.2 0 E.
R.22E .
R.21 E .
Map Legend E
R. 23E .
R .24E .
R.25E .
W e ll Data Group Numbe r °C = Land Surface Temp erature+Geothermal Gradient Dep th to the 20°c Isotherm
FIGURE 27
WELL DATA GROUP LOCATIO N MAP
QE1 75 •
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T H E LOW TEMPERATURE GEOTHERMAL RESOURCE OF T H E YAKIMA REGION - A PRELIMINARY by John H . Biggane
Open-File Report 81-7
September 1981
REPORT
Table of Contents L i s t of Figures
iii
L i s t of Tables
v
Introduction
1
Location and Topography
1
Stratigraphy of the Yakima Region
1
Grande Ronde Formation Vantage Member of the Ellensburg Formation Wanapum Formation
2 3 3
Frenchman Springs Member
3
Squaw Creek Member of the Ellensburg Formation . . .
4
Roza Member
4
Priest Rapids Member
4
Mabton Member of the Ellensburg Formation
5
Saddle Mountains Formation
5
Umatilla Member
5
"Huntzinger" Valley Flow (Asotin Member?)
5
Selah Member of the Ellensburg Formation
6
Pomona Member
6
Rattlesnake Ridge Member of the Ellensburg Formation
6
Elephant Mountain Member
6
Upper Ellensburg Formation and Quaternary Sediments.
7
Previous Geophysical Investigations in the Yakima Region .
8
Table of Contents ( c o n t . ) Previous Geothermal Research in t h e Yakima Region. . . . .
9
Temperature Data
9
Calculation of Geothermal Gradients i n the Yakima Region
10
Geothermal Gradients i n the Yakima Region
12
Accuracy of the Geothermal Gradients Obtained by the Regression Analysis
12
Projected Land Surface Temperatures and Slope Aspect
14
Chemical Geothermometers
17
Summary
22
References
23
Appendices Appendix A:
Symbols Used on Figures 2 through 8 and 13 through 26
Appendix B:
Well Locations and Bottom Hole Temperatures from Wells in t h e Yakima Region
Appendix C:
Well Data Groups Used in t h e Bottom Hole Temperature Regression Analysis
ILLUSTRATIONS Page Figure
1.
Generalized stratigraphic section
2a
2.
Stratigraphic correlation line N o . 1
2b
3.
Stratigraphic correlation line N o . 2
2c
4.
Stratigraphic correlation line N o . 3
2d
5.
Stratigraphic correlation line N o . 4
2e
6.
Stratigraphic correlation line N o . 5
2f
7.
Stratigraphic correlation line N o . 6
2g
8. Stratigraphic correlation line N o . 7
2h
9.
Typical natural gamma response of the Umatilla and Squaw Creek Members
4a
10. Spring and well location map 11. Temperature logs of the DNR Black Rock Well No 12.
"Step-like" distortion of a temperature log
In pocket 1
10a 10b
13. Temperature versus depth for group 1
12a
14. Temperature versus depth for group 2
12b
15. Temperature versus depth for group 3
12c
16. Temperature versus depth for group 4
12d
17. Temperature versus depth for group 5
12e
18. Temperature versus depth for group 6
12f
19. Temperature versus depth for group 7
12g
20.
Temperature versus depth for group 8
12h
21. Temperature versus depth for group 9
12i
22.
Temperature versus depth for group 10
12j
23. Temperature versus depth for group 11
12k
ILLUSTRATIONS— Continued Page Figure
24.
Temperature versus depth for group 12
12L
25.
Temperature versus depth for group 13
12m
26.
Temperature versus depth for group 14
12n
27.
Well data group location map
In pocket
27a. M a p showing locations of w e l l data groups with respect to the locations of springs and wells
In pocket «
28.
Temperature logs, line N o . 1
12o
29.
Temperature logs, line N o . 2
12p
30.
Temperature logs, line N o . 3
12q
31.
Temperature logs, line N o . 6
32.
Temperature logs, line N o . 7
12s
33.
Slope aspect versus normalized surface temperature
14a
.
12r
L i s t of Tables Table
Page
1
Geothermal G r a d i e n t s , Land Surface Temperatures, and Depths to the 20°C Isotherm
13
2
Measured and Predicted "Aquifer" Temperatures
15
3
Mean E l e v a t i o n , Slope Aspect, and Normalized Land S u r f a c e Temperatures f o r Well Data Groups 1 - 1 3
18
4
Chemical Data f o r Springs in Yakima County, Washington
19
5
Chemical Data f o r Wells in Yakima County, Washington
20
Introduction The low temperature geothermal resource of t h e Yakima region i s c u r r e n t l y at t h e i n i t i a l s t a g e of i t s development. utilize
Several domestic heat
pump
systems
the warm groundwater f o r space h e a t i n g , and l a r g e r i n s t a l l a t i o n s have
been c o n s i d e r e d .
This report provides a preliminary summary of t h e geothermal
resource f o r p o r t i o n s of t h e Yakima r e g i o n .
Location and Topography The Yakima r e g i o n l i e s in the western portion of t h e Columbia Plateau south-central
Washington.
The
region's
major
topographic
f e a t u r e s are a s e r i e s of s o u t h e a s t - t r e n d i n g a n t i c l i n a l valleys.
in
and s t r u c t u r a l
ridges
and
synclinal
The Yakima River serves as t h e r e g i o n ' s major drainage.
S t r a t i g r a p h y of t h e Yakima Region The lava flows interbedded
the
sediments
region's near-surface underlying
of
the
of
Columbia the
River
Basalt
and
(CRBG)
stratigraphic
section.
The
nature
of
units
the
the
rocks
b a s a l t i c l a v a s i s u n c e r t a i n , but they are probably r e l a t e d t o
o t h e r s , 1980).
are
exposed
in
the
future.
Alluvial
Formation throughout much of t h e lowlands 1976, 1977a, 1977b;
to
the
west
Oil and gas e x p l o r a t i o n boreholes are p r e s e n t l y
being d r i l l e d in Yakima County and should provide information geologic
and
Ellensburg Formation comprise t h e bulk of the
o l d e r volcanic rocks (Ohanapecosh Formation) t h a t (Bentley
Group
on
the
deeper
sediments o v e r l i e the Ellensburg
of
the
Yakima
region
(Campbell,
Swanson and o t h e r s , 1979a).
The t o t a l t h i c k n e s s of t h e Columbia River Basalts i s unknown but probably exceeds 1,000m in t h e Yakima 1980).
region
(Bentley,
1977;
Bentley
and
others,
All t h r e e formations of the Yakima Basalt Subgroup (CRBG)--the Grande
Ronde, Wanapum,
and
Saddle
Mountains
Formations—are
found
in
surface
exposures (Swanson and o t h e r s , 1979a). Individual b a s a l t flows u s u a l l y contain two major and
the
underlying
entablature,
c h a r a c t e r i s t i c s (Swanson, 1967; columns
are
typical
of
the
which
are
zones.
apart
Diery and McKee, 1969). colonnade,
the
colonnade
by d i f f e r i n g j o i n t Straight,
vertical
while t h i n n e r , i n c l i n e d , or curved
columnar j o i n t s a r e found in the e n t a b l a t u r e . both
set
zones,
Horizontal j o i n t s a r e found
in
A basal breccia i s o f t e n observed beneath t h e colonnade, and a
v e s i c u l a r zone o f t e n occurs at t h e flow t o p . An g e n e r a l i z e d s t r a t i g r a p h i c s e c t i o n i s shown in stratigraphic
correlation
lines
are
explained in Appendix A.)
are
shown
in
(Symbols used in Figures 2
through
geophysical
logs.
Neutron-neutron
Figures 2 through 8, but i t should be noted t h a t natural
gamma, gamma-gamma, and correlations.
Subsurface
These c o r r e l a t i o n l i n e s were c o n s t r u c t e d by
i n t e r p r e t i n g both d r i l l e r s ' and borehole logs
1.
f o r t h e lower Yakima, Black Rock, and Moxee
Valleys are shown in Figures 2 through 8. 8
Figure
neutron-gamma
logs
were
also
utilized
for
these
Formation t h i c k n e s s e s reported in l a t e r s e c t i o n s of t h i s
report
a r e apparent t h i c k n e s s e s , since dip c o r r e c t i o n s have not been made. An overview of t h e r e g i o n ' s geologic u n i t s i s
given
below.
Interested
r e a d e r s are r e f e r r e d t o Swanson (1967), Schmincke (1967a and 1967b), Diery and McKee
(1969),
Bentley (1977), Campbell (1976, 1977a, and 1977b), Swanson and
o t h e r s (1979a), and Bentley and o t h e r s (1980) f o r more
detailed
information.
Grande Ronde Formation The Grande
Ronde
Formation
has
been
informally
divided
into
four
m a g n e t o s t r a t i g r a p h i c u n i t s of which t h r e e (N x , R 2 , and N2) have been mapped in t h e region (Swanson and o t h e r s , 1979a).
The t o t a l thickness of t h i s formation
COLUMBIA RIVER BASALT GROUP
ELLENSBURG FORMATION
ELEPHANT
QUATERNARY AND UPPER ELLENSBURG SEDIMENTS
MOUNTAIN MEMBER
POMONA
RATTLESNAKE RIDGE MEMBER
SELAH MEMBER
MEMBER
UMATILLA
MABT0N MEMBER
MEMBER
PRIEST RAPIDS
OUINCY
MEMBER
DIATOMITE?
ROZA MEMBER
SQUAW CREEK MEMBER
FRENCHMAN VANTAGE SPRINGS MEMBER MEMBER
GRANDE RONDE FORMATION
FIGURE 1 GENERALIZED STRATIGRAPHIC SECTION
13118-,
12N/20f-36PI
I IN/21£·1161.1
I IH/21f•lfil'I
I IN/21E·22G2
IIH/21£·361CI
1-
w w LL
llltl
91li -
'. I
11111
IN
12i
121 ·
-61
l.
11111 -
·Ill
I
- ·till
·61
--
; }ll8
- · 12i
·1 - -11111
•
1111
-
~ s r r ~ .... l11~-~-»9~c-rn · s,&tJ
NN
NN
s29 I
'3-r - ~ f " t - l n a NN
~..32l..CliiflS7~----11T-~ru::mrrszSEr;r.ut- -791
NN
FIGURE FIGURE 22 STRATIGRAPHIC STRATIGRAPHIC CORRELATION CORRELATION LINE LINE ##11
NN
··1 ts)
0-
13111
12N/28E-27NI
12N/211E-3,N2
llN/21lE-IIU11
I IN/21lE-,'IIU
(/)
er.:
131!111
1---
w
w w u._
li! :E
(/)
er.:
w ~ :c
3WI
241
ZAI
188
llll
121
121
61
61
-•
•
-61
-61
--
--
-121
-I
NN
NN
FIGURE FIGURE 33 STRATIGRAPHtC STRATIGRAPHIC CORRELATION CORRELATION LINF. LINE #2 #2
NN
FIGURE 4 STRATIGRAPHIC CORRELATION LINE
#3
FIGURE 5 STRATIGRAPHIC CORRELATION LINE #4
FIGURE 6 STRATIGRAPHIC CORRELATION LINE #5
FIGURE 7 STRATIGRAPHIC CORRELATION LINE #6
FIGURE 8 STRATIGRAPHIC CORRELATION LINE #7
in
the
Yakima region probably does not exceed 1,000m and may vary by as much
as 400m because of an i r r e g u l a r p r e - b a s a l t 1980).
Individual
topography
(Bentley
and
others,
flows average 20 t o 30m in thickness (Bentley and o t h e r s ,
1980).
Vantage Member of t h e Ellensburg Formation The Vantage Member of t h e Ellensburg Formation l i e s Ronde
and
Wanapum
Basalt
Formations
throughout
between
most
the
Grande
of t h e r e g i o n .
The
reported t h i c k n e s s of t h i s member ranges from 0 t o 30m (Diery and McKee, 1969; Bentley, 1977;
Bentley
and
volcaniclastic
sandstones,
others,
1980).
siltstones,
This
member
claystones,
conglomerate and d i a t o m i t e (Diery and McKee, 1969;
is
composed
of
and minor q u a n t i t i e s of
Bentley and o t h e r s , 1980).
None of t h e w e l l s f o r which s t r a t i g r a p h i c s e c t i o n s a r e
given
in
this
report
have p e n e t r a t e d t h e Vantage Member.
Wanapum Formation In t h e Yakima Region, t h e Wanapum Basalt Formation i s composed members:
of
three
t h e Frenchman Springs, t h e Roza, and t h e P r i e s t Rapids Members.
Frenchman Springs Member The Frenchman widespread
Wanapum
Springs Member,
(Bentley and o t h e r s , 1980).
Member, is
the
thickest
composed
of
up
(over to
been
tentatively
and
most
s i x flows a t Union Gap
None of t h e wells f o r which s t r a t i g r a p h i c s e c t i o n s
are given in t h i s r e p o r t have completely penetrated t h i s lave
150 m)
recognized
in
thickness ranges from 80 t o over 150m.
several
wells
member. where
Six
flows
t h e i r combined
Several t h i n (up t o 8 m t h i c k in well
11N/21E-22G2) d i s c o n t i n u o u s sedimentary i n t e r b e d s l i e between the flows of the Frenchman Springs B a s a l t Member.
Squaw Creek Member of t h e Ellensburg Formation The Squaw Creek Member of
the
Ellensburg
Formation
between
the
Frenchman Springs and t h e Roza Members throughout much of t h e study a r e a .
The
t h i c k n e s s of t h i s member ranges from 0 t o nearly 11 m. as
a
This member can be used
s t r a t i g r a p h i c marker due t o i t s high natural gamma response.
response i s shown in Figure 9. varies
lies
from
McKee, 1969;
The
composition
of
the
Squaw
A typical
Creek
Member
a d i a t o m i t e or j a s p e r o i d t o sandstone or conglomerate (Diery and Bentley and o t h e r s , 1980).
Roza Member The Roza Member occurs as a thickness
of
this
member
subsurface c o r r e l a t i o n l i n e s .
single
ranges
from
flow under
in
the
Yakima
region.
The
30m t o almost 45 m along the
A t h i n (0 t o 10m) i n t e r b e d (Quincy
Diatomite?)
s e p a r a t e s t h e Roza Member from t h e o v e r l y i n g b a s a l t flow.
P r i e s t Rapids Member Two b a s a l t flows of t h e subsurface
of
the
Priest
Rapids
Member
normally
occur
the
r e g i o n , with t h e upper flow t h i c k n e s s ranging from 10m to
almost 60m and t h e lower flow t h i c k n e s s ranging from 45m t o
almost
t h i n (up t o 5 m) i n t e r b e d occurs r a r e l y between t h e s e two f l o w s . was
in
60m.
Only one flow
found t o occur in several wells in the Black Rock and Moxee Valleys.
t h i c k n e s s of t h i s f l o w ranges from more than 20m t o 42m at
A
these
The
locations.
The upper s u r f a c e of t h e P r i e s t Rapids Basalt Member i s o f t e n deeply weathered (Bentley and o t h e r s ,
1980).
FIGURE 9 TYPICAL NATURAL GAMMA RESPONSE OF THE UMATILLA AND SQUAW CREEK MEMBERS
Mabton Member of t h e Ellensburg Formation The Mabton Member of the Ellensburg Formation o v e r l i e s the P r i e s t Member
throughout
much
of
v a r i e s from 0 m t o over 25m.
the
Yakima r e g i o n .
The thickness of t h e member
The Mabton Member i s composed
d e p o s i t s and a i r f a l l t u f f (Bentley and o t h e r s ,
Rapids
of
volcaniclastic
1980).
Saddle Mountains Formation Four members of t h e Saddle Mountains Formation are found region.
These
flows
Mountain Members.
in
the
Yakima
include t h e Umatilla, Huntzinger, Pomona, and Elephant
Interbedded
between
these
flows
are
sediments
of
the
Ellensburg Formation t h a t may reach t h i c k n e s s e s g r e a t e r than 100m.
Umatilla Member The Umatilla Member c o n s i s t s of a s i n g l e b a s a l t that
ranges
from
30m t o
poorly
developed
serves
as
a
a
thickness
Valley.
The
colonnade
columns 1 m t o 2 m in diameter and is o v e r l a i n by a
glassy e n t a b l a t u r e and flow t o p Member
with
60m in t h e s u b s u r f a c e of t h e Black Rock and Moxee
Valleys and from 60m t o over 80m in t h e lower Yakima contains
flow
breccia
stratigraphic
response (Crosby and o t h e r s , 1972).
(Schmincke,
1967b).
The
Umatilla
marker because of i t s high n a t u r a l gamma A t y p i c a l response i s shown in Figure
9.
"Huntzinger" Valley Flow (Asotin Member?) The Huntzinger Valley flow (Asotin Member?)
occurs as a " v a l l e y f i l l i n g "
b a s a l t flow s o u t h e a s t of Selah in the Moxee and Black Rock 1977;
Campbell,
1977a).
This
flow
Valleys
(Bentley,
has not been i d e n t i f i e d in any of the
s t r a t i g r a p h i c s e c t i o n s t h a t were prepared f o r t h i s
report.
Selah Member of t h e Ellensburg Formation The Selah Member, an i n t e r b e d Members, 1967a).
is
lying
between
the
Umatilla
and
Pomona
composed of v o l c a n i c l a s t i c d e p o s i t s and v i t r i c t u f f s (Schmincke,
The t h i c k n e s s of t h i s member ranges from l e s s than 10m t o over 15m in
t h e s u b s u r f a c e of t h e Black Rock and Moxee Valleys and from 0m t o
almost
25 m
in t h e lower Yakima Valley.
Pomona Member The Pomona Member, a s i n g l e b a s a l t f l o w , ranges in than
40m t o
over
thickness
80m in t h e subsurface of t h e lower Yakima Valley.
s u b s u r f a c e of t h e Black Rock Valley, t h e Pomona Member was found 30m t h i c k
from
and in several l o c a t i o n s was absent a l t o g e t h e r .
to
less In the
be
The Pomona Member
in t h e s u b s u r f a c e of t h e Moxee Valley was found t o be 45 m t o 55m t h i c k . upper
surface
of
the
Pomona
Member
only
The
i s o f t e n broken i n t o blocks of highly
oxidized s c o r i a (Schmincke, 1967b).
R a t t l e s n a k e Ridge Member of t h e Ellensburg Formation The R a t t l e s n a k e Ridge Member, an i n t e r b e d l y i n g between Elephant
Mountain
Members,
member
ranges
from
Pomona
and
i s composed p r i m a r i l y of s i l t s t o n e and c l a y s t o n e
with interbedded conglomerate (Bentley and o t h e r s , 1980). this
the
The
thickness
of
40m t o over 100m in t h e subsurface of t h e r e g i o n .
Bentley and o t h e r s (1980) r e p o r t t h i c k n e s s e s of up t o 200m f o r t h i s member
in
t h e Toppenish b a s i n .
Elephant Mountain Member The Elephant Mountain Member u s u a l l y occurs as one region
with
a
second
flow,
the
Ward
flow
in
the
Yakima
Gap, being found at Snipes Mountain
(Campbell, 1977b) and at Ward Gap (Schmincke, 1967a). flow
ranges
The thickness
of
this
from 8m t o over 15 m in t h e subsurface of t h e lower Yakima Valley
and i s absent in most of t h e w e l l s s t u d i e d in t h e Black Rock Valley.
In
the
subsurface of t h e Moxee Valley, t h e t h i c k n e s s ranges from 0 m t o j u s t over 10m. A t h i c k (48 m) s e c t i o n occurs in well 12N/20E-16D1, but i t i s uncertain whether the e n t i r e s e c t i o n i s Elephant Mountain B a s a l t .
Upper Ellensburg Formation and Quaternary Sediments Overlying t h e Elephant Mountain Basalt Member a r e Ellensburg and Quaternary
sediments.
younger
The t h i c k n e s s of t h e s e sediments range from 0 t o over
170m along the c o r r e l a t i o n l i n e s t h a t were prepared f o r t h i s r e p o r t , and i t i s expected t h a t g r e a t e r t h i c k n e s s e s would be found towards lower
Yakima
Valley.
The
Ellensburg
sediments
the
center
of
the
c o n s i s t of v o l c a n i c l a s t i c
d e p o s i t s with i n t e r b e d d e d conglomerates and sandstones, whereas t h e Quaternary sediments c o n s i s t of s i l t , sand, g r a v e l , and loess d e p o s i t s 1977a, and 1977b;
(Campbell,
1976,
Bentley and o t h e r s , 1980).
In regions where t h e Elephant Mountain and/or Pomona Basalt
Members
are
a b s e n t , t h e Selah and R a t t l e s n a k e Ridge Members are d i f f i c u l t t o s e p a r a t e from the
upper
Ellensburg
R a t t l e s n a k e Ridge Ellensburg
sediments.
Members
sediments
have
Where t h i s s i t u a t i o n occurs, t h e Selah and not
been
differentiated
from
the
upper
on t h e c o r r e l a t i o n l i n e s t h a t a r e shown in t h i s
report.
Previous Geophysical I n v e s t i g a t i o n s in t h e Yakima Region Gravity and aeromagnetic s t u d i e s have been conducted in the Yakirna region by Robbins and o t h e r s (1975), Konicek (1975), and Swanson and o t h e r s The
known
seismic
history
of
the
(1979c).
region i s summarized by Myers and Price
(1979). Analysis of g r a v i t y data suggests t h a t t h e b a s a l t s
(CRBG)
extend
to
a
depth of 2m t o 4 km in the Yakima and Toppenish Valleys and t o a depth of about l km
in
the
Ahtanum
Valley
(Robbins
and
others,
C i r c u l a r g r a v i t y lows were observed j u s t west of Zillah
and
Konicek, 1975).
cities
of
Yakima
and
were i n t e r p r e t e d as p o s s i b l y r e s u l t i n g from buried volcanic cones
or d e p o s i t s of rock having a lower others,
the
1975;
1975).
A
density
than
the
basalts
(Robbins
and
l a r g e g r a v i t y high, centered j u s t south of Union Gap, was
a t t r i b u t e d t o a t h i n l a y e r of sediments (Robbins and o t h e r s , 1975). The aeromagnetic study showed low i n t e n s i t y , over
the
valleys
and
small
amplitude
anomalies
anomalies of g r e a t e r i n t e n s i t y and amplitude over the
r i d g e s (Swanson and o t h e r s , 1979c).
Magnetic s t u d i e s
may
prove
useful
for
mapping t h e younger v a l l e y - f i l l i n g Yakima Basalts (Swanson and o t h e r s , 1979c). Magnetotelluric
studies
hold promise f o r e x p l o r a t i o n work below the level of
the b a s a l t s , but u n f o r t u n a t e l y none have been published f o r t h i s region. H i s t o r i c a l earthquake e p i c e n t e r s with hypocenters. than
10 km deep
c i t i e s of earthquake
Yakima
to
or
greater
tend t o be concentrated along a north-south l i n e between t h e and
epicenters
Ellensburg with
(Myers
hypocenters
and less
Price, than
t r e n d i n g , through
the
lower
Yakima
Valley
1979). 10ckm deep
concentrated along t h e same north-south l i n e and along line
equal
a
tend
t o be
northwest-southeast
(Myers
Magnitudes of 4 or l e s s have been r e p o r t e d f o r t h e s e shallow earthquakes (Myers and P r i c e , 1979).
Historical
and P r i c e , 1979). and
deep-seated
Previous Geothermal Research in t h e Yakima Region Geothermal r e s e a r c h in t h e Yakima region began with (1901).
In
this
report,
Smith,
a
report
noted the warm t e m p e r a t u r e s
by
Smith
(approximately
22°C) of the ground water flowing from a r t e s i a n wells in the Moxee Valley
and
c a l c u l a t e d geothermal g r a d i e n t s of 50 t o 73°C/km f o r t h e r e g i o n . Foxworthy (1962) reported an average geothermal g r a d i e n t of 40.5°C/km
in
water wells g r e a t e r than 15m deep in t h e Ahtanum Valley and suggested t h a t t h e rock type had l i t t l e e f f e c t on t h e g r a d i e n t . Blackwell (1980) reported geothermal g r a d i e n t s of 26 t o 37°C/km and
heat
flow values of 57 t o 64 mWm2- from water wells in the r e g i o n . Schuster (1980) noted t h a t goeothermal g r a d i e n t s of 50 consnonly
measured
to
70°C/km
were
in water w e l l s of t h e region and t h a t several very shallow
w e l l s produced warm w a t e r s .
Depth t o 20°C in water w e l l s of t h e Yakima region
were reported t o range from 9 m t o 471 m ( S c h u s t e r , 1980).
Temperature Data Subsurface temperature data in t h e Yakima region has the
Geological
Engineering
been
collected
Section of Washington S t a t e University (WSU), by
t h e Department of Geological Sciences of Southern Methodist University by
the
Washington
by
(SMU),
S t a t e Department of Natural Resources (DNR), by the U . S .
Geological Survey (USGS), and by the Oregon
Institute
of
Technology
(OIT).
Some 200 bottomhole temperatures and depths f o r wells in t h e Yakima region are given in Appendix B.
The
Well l o c a t i o n s a r e shown in Figure 10.
The accuracy of t h e temperature data v a r i e s with t h e
collecting
temperature
have an accuracy of
data
collected
by
SMU and
approximately ±0.2°C (Blackwell, 1980). c o l l e c t e d by the USGS and OIT i s unknown.
the
DNR
agency.
The accuracy of t h e temperature
data
,.
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OPEN FILE REPORT OF 81-7
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() - · · · GEOPHYSICAL --::3'() SPRING - - - - TEMPERATURE and CHEMICA L DATA
+ + + , + + +
TOPOGRAPHIC
DIVIDE
+++
FIGURE 10 - SPRING AND WELL LOCATION MAP -
6,E- S . M. U.
TEMPERATURE - - - - TEMPERATURE and CHEMICAL
OE- u. S.G .S. STRATIGRAPH IC GORRE LA T \0N 'LINE_
SCALE - I : 250,000
USGS BASE MAP I 2°SHEET)
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athe,
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WA. DEPT af WATER RESOURCES CHEMICA
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-==-• DATA I Vao De obuc
QE175 A3
The temperature probes u t i l i z e d by WSU since 1974 were r e c a l i b r a t e d in water
bath as p a r t of t h i s p r o j e c t .
because of t h e use of a nonstandard temperature
P r i o r c a l i b r a t i o n s were only approximate thermometer.
Previously
published
WSU
data have been c o r r e c t e d t o r e f l e c t t h e c a l i b r a t i o n changes.
The
change in c a l i b r a t i o n averaged l e s s than -1.0°C. temperature
a
probes
is
approximately ±0.4°C.
approximately
±0.2°C,
The
precision
and
the
of
field
the
accuracy
WSU is
The temperature probes used by WSU p r i o r t o 1974 a r e no
longer a v a i l a b l e , and t h e i r accuracy i s t h e r e f o r e u n c e r t a i n . The DNR Black Rock well #1 was logged on s u c c e s s i v e temperature
probe "A" and with t h e SMU probe VPR 1.
days
with
the
WSU
The temperature logs are
p l o t t e d in Figure 11 and are in c l o s e agreement, even though the WSU probe was t h e f o u r t h tool t o be run in the hole t h a t day.
C a l c u l a t i o n of Geothermal Gradients in t h e Yakima Region Determination of geothermal g r a d i e n t s in water w e l l s of the Yakima region is complicated by i n t r a - a q u i f e r borehole flow.
The net r e s u l t of t h e borehole
flow i s a d i s t o r t e d thermal g r a d i e n t , o f t e n assuming a the
recorded
temperature
distribution
step-like
form,
with
being u n r e p r e s e n t a t i v e of t h e actual
geothermal g r a d i e n t (see Figure 12). Three o p t i o n s were a v a i l a b l e t o past i n v e s t i g a t o r s in t h e i r determine
a c c u r a t e geothermal g r a d i e n t s in t h e s e water w e l l s .
most common method, i s based on recorded bottom hole
=
BHT
-
LST
to
The f i r s t , and
temperatures
assumed land s u r f a c e temperatures (LST), as shown in equation
Geothermal Gradient
attempts
(1).
(1)
(BHT)
and
10o
....... ..,J._
....... ..,J. ......
........
W$U .....
... ..
Yl'tl ....... 9111/80 _ _ _ _ _ _ _ _ $MU .......
___ 9112J8() __ - - ____ --15.2't
~ ~
_ _ _ _ _ _ _
_
15.23°c
/
21(),.----------
-25.2•c
330----------------------1-4
16
20 TEMPERATURE ("c)
FIGURE 11 TEMPERATURE LOGS OF THE ONR DNR BLACK ROCK WELL +#11
FIGURE 12 'STEP-LIKE' DISTORTION OF A TEMPERATURE LOG
For shallow w e l l s , i t i s very important t h a t an a c c u r a t e LST be t h i s method.
used
in
The e r r o r involved v a r i e s according t o equation (2) and is l a r g e
f o r even small e r r o r s in t h e LST.
This method was a p p l i e d in t h e Yakima region with because
accurate
LST
are
not
available.
The
very
limited
geothermal
success
gradients
of
neighboring w e l l s c a l c u l a t e d in such a manner o f t e n d i f f e r e d by more than
100
percent. A second method i s based on s e l e c t i n g p o r t i o n s of gradient
the
recorded
thermal
t h a t appear u n d i s t o r t e d and then c a l c u l a t i n g t h e geothermal g r a d i e n t
over t h a t i n t e r v a l .
This method i s time-consuming and does not allow a
check
on whether t h e s e l e c t e d i n t e r v a l i s a c t u a l l y u n a f f e c t e d by borehole flow. The t h i r d option a v a i l a b l e t o t h e i n v e s t i g a t o r i s t o d i s r e g a r d
the
data
altogether. A new approach t o t h e problem was developed f o r t h i s r e p o r t .
This method
involves a simple l e a s t squares l i n e a r r e g r e s s i o n a n a l y s i s of t h e BHT's group
of
wells.
a s p e c t and a n g l e .
of
a
Well data groups were based on proximity and s i m i l a r slope An a d d i t i o n a l well data group was s e l e c t e d f o r well
depths
g r e a t e r than 650m. The BHT l i n e a r r e g r e s s i o n a n a l y s i s has several advantages over t h e g r a d i e n t d e t e r m i n a t i o n methods. quality
data
can
be
other
Uphole flow does not a f f e c t t h e BHT, and poor
discriminated
by i t s "lack of f i t " t o the r e s t of t h e
data.
Downhole flow can a f f e c t t h e BHT, but in many cases t h e deepest portion
of t h e well appears t o be i s o l a t e d from t h e f l o w . temperature
A very
rapid
increase
of
i s recorded in t h e bottom of t h e w e l l s t h a t a r e i s o l a t e d from the
downhole flow ( s e e Figure 12).
Wells in which downhole flow does
BHT are discussed in a l a t e r s e c t i o n of t h i s
affect
the
Figures
13
report.
Geothermal Gradients in t h e Yakima Region Plots of BHT v s . depth f o r t h e well data groups a r e shown in through A.)
26.
The
(Symbols used in Figures 13 through 26 a r e explained in Appendix
results
summarized
in
of
the
Table 1.
least
squares
temperatures
range
range from 142 m t o 344m.
regression
analysis
are
Geothermal g r a d i e n t s f o r t h e shallow ( l e s s than 650m
deep) well data groups range from surface
linear
from
25.1°C/km
to
10°C t o 14°C.
52.2°C/km.
Projected
land
Depths t o t h e 20°C isotherm
The areal d i s t r i b u t i o n of t h e geothermal
gradients,
p r o j e c t e d land s u r f a c e t e m p e r a t u r e s , and depths t o the 20°C isotherm are shown in Figure 27. The m a j o r i t y of w e l l s t h a t were included in the deep ( g r e a t e r deep)
well d a t a group are l o c a t e d o u t s i d e of Yakima County.
that these
deep
relationship
wells
between
are
separated
BHT and
depth
by
large
an
excellent
The l e a s t squares
r e g r e s s i o n a n a l y s i s of t h e deep well data group y i e l d e d a geothermal of
29.9°C/km,
650 m
Despite the f a c t
distances,
e x i s t s (Figure 26).
than
gradient
a p r o j e c t e d land s u r f a c e temperature of 24.3°C, and a depth t o
t h e 100°C isotherm of 2,532m.
A l i s t i n g of t h e wells t h a t
were
included
in
t h e i n d i v i d u a l well d a t a groups i s given in Appendix C.
Accuracy of t h e Geothermal Gradients Obtained by the Regression Analysis Temperature logs (Figures 28 through 32) of wells in well data groups
4,
FIGURE 13
-
TEMPERATURE VS. DEPTH FOR GROUP 1
FIGURE 14
-
TEMPERATURE VS. DEPTH FOR GROUP 2
FIGURE 15
-
TEMPERATURE VS. DEPTH FOR GROUP 3
FIGURE 16
-
TEMPERATURE VS. DEPTH FOR GROUP 4
FIGURE 17
-
TEMPERATURE VS. DEPTH FOR GROUP 5
FIGURE
18
-
TEMPERATURE VS. DEPTH FOR GROUP 6
FIGURE 19
-
TEMPERATURE VS. DEPTH FOR GROUP 7
FIGURE 20
-
TEMPERATURE VS. DEPTH FOR GROUP 8
FIGURE 21
-
TEMPERATURE VS. DEPTH FOR GROUP 9
FIGURE 22
-
TEMPERATURE VS. DEPTH FOR GROUP 10
FIGURE 23
-
TEMPERATURE VS. DEPTH FOR GROUP 11
FIGURE 24
-
TEMPERATURE VS. DEPTH FOR GROUP 12
FIGURE 25
-
TEMPERATURE
VS. DEPTH FOR GROUP 13
FIGURE 26
-
TEMPERATURE VS. DEPTH FOR GROUP 14
\
,
.' A.)~•fH.· I "
OPEN FILE REPORT OF 8 1-7
13
Gro up #
1 1.3+2 9.8°C /km T . 15N.
,--\
\
\
·--.___ - , ,
I I
I
T .14 N.
............
I
292m
,_ --- ..... --- --- -l
...........
12
Gr oup #
---- -,
,,
11.4+ 2s . 1°C / km
1 - ,_
' ·1
-- --- -- 343m
\
......
--
/
, __ YAKIMA
T . 13N.
\\ G ro up #
\
9\
(
.I .
\
\ 11.4 + 43.4 °C tk m \, 19 9m\ / \ /
---1
- I
-
T.12 N
-
-
-
--___ ___
-
• G r o VP #
_
8
, .. 10\
o·
~ 2.9 + 40 .5 C /k m \ \ 176m I
\
/
I
......
Gro up #
'
_ ......... ---
/
/
., .....
\ "
/
,. .
\
,.,,,,.
,,
,, ,,.
191 m
- - - --
---7 I
- ----------
,,-
o / 11. 4+45 . 1 C/km/
·--
,-- - ---- - --: \
Group #
I
1 7 1 m .,.... .,.....
,, ~G ro up #
('
4
- -
-
-- --
-
11
I
10 .0+45 .8°C / km 219m
1 / - - - ,-- --------Jr-- - -~.....::::-.......J,r - - - - -- I...!......- -1---....:_ / ,,, , 1 2 .o + 4 6 . 9° c 1 ':,m,.....-:-r---:,~-+-..;;..;::----=,- - - +- - - -- - --r----/ / / / T . 11 N
/
Group #
2
/
.,,, ' 14 .0+3 3.7 ° Ctkm
//
179m
/ ,, - - -
.... ..... ......
........
....... ,,.,,. T. 10 N
...,, ...,, ~roup ,- _..,,
--~
--- --. --
\_ Group #
5\ \
Group #
13.0+ 40.0° C / km \
I, ...... ,.....,.....,.....
/
' .....
175m
14.0+ 36.o 0 c t km
, ---
16 7 m
\
.... .......... \ I ', ......... \ I ', ' \ I ' ' -- - -I l---i--------+- -- - - - - - - - + - - - - - - -- + - - - - ---=-=--~1---- - - - - + -- - -- - - - ; - - - -- - - - - l - - - -- - ---1 I
__ ,
T OPPEN ISH
I
---
I
' , ....
..... ' ..... ..... ..... ..... ....
I
1\
'
--- ---
.....
SU NN YS IDE
\
2 12 m
... .... ,
I
\
1 1 . 8 + 3 8 .7 OC I k m\
I.
6
...,, '\ #
---+-- - - - -- -+----------1
.....
G ro up #
',
' ' ,_
\
\ .,.....
., I
.... ....
.,
..... ... .,
.
,.....
I
Gro up #
I I
3
..... 12.5 + 3 4.1 ° C / km '
-,I
.,.........
,..... ,.....
T .9 N
...... ......
......
7' ,
220 m
-- -
...........
, ________ ......... .,.,,. --
GRA NDVIEW
I
12.6+ s2.2° C / k m1
..... .....
-
142m
..... .....
I
PROSSER
,
..... ..... .....
T.8 N.
R. 16E .
R. 17E.
R.18E .
R.19E.
Sca le - 1 : 25 0 ,000 USGS Base Map
R.2 0 E.
R.22E .
R.21 E .
Map Legend E
R. 23E .
R .24E .
R.25E .
W e ll Data Group Numbe r °C = Land Surface Temp erature+Geothermal Gradient Dep th to the 20°c Isotherm
FIGURE 27
WELL DATA GROUP LOCATIO N MAP
QE1 75 •
•
A3
06
81 - 7 copy 2
WASHINGTON DEPARTMENT OF NATURAL RESOURCES DIVISION OF GEOLOGY AND EARTH RESOURCES
OPEN FILE REPORT OF II- 7 \ )
"\ '"
\
I
I
/
')
'\ --------~----~--,- ---- -
/
--
-
.
FIGURE 27A MAP SHOWING LOCATIONS OF WELL DATA GROUPS WITH RESPECT TO THE LOCATIONS OF SPRINGS AND WELLS 6 34[ - -·- - ----- - --------=.::::..::..._~--------;------------ .---------,---- ------1----------,------- ----.--------,-------~,-------, - --------, I
I J,Ri
I
C)
3F
04 J
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... + + + ... .,.
[ Tl6 N ,
.
'•
24 N
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+
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..... : .. ,
... + ...... +
.... 19E
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Ct
8
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6
29 H
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...
0
+ ... + ...... .,. ' ............
c:;7
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.......
1 - - - - - - - - 4- - - - - - --,L·;:•.!•~•:...·:_____ _ -l~_J~..:32:::....___- ,I_ _____ __ i•+-- - - - -- - ~ - -- - - - - --t----..C:.. "l33~P ~ --+- - - - - - - -~ --------+- -- - - - - -~ - - - - - - -.1-- - - - - -- j--- - - - - - --t- - -- - - -i
I"\
~
+;.. ...
C)2K 13C
(I:
)
230
....... .,
""'-~"""'
++
T 15 N (._
.,.,_
, +•
\ ......
24 H
\
•••
Group 13 11.3+29.8°C/km 292m
0
I
22 L 8 22P
0
C)
: ~-
l ~J.. ,
._-'':, 3
w
.,. .,. .... ·•.
I
114+25.I C/km ,., • 6 7 ~·.; • • . 13K 343m l i-,......._ . + +• '1 Q 19K ~ N 13H "::_1,
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I
Tl4N,_~
B~l 0 P
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£:, 29M
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