PY-CEI-NRR-0478, Rev 0 to Deep Well Injection at Calhio Wells & Leroy,Oh Earthquake of 860131
| ML20211G509 | |
| Person / Time | |
|---|---|
| Site: | Perry  |
| Issue date: | 06/10/1986 |
| From: | Acree S, Talwani P CLEVELAND ELECTRIC ILLUMINATING CO. |
| To: | |
| Shared Package | |
| ML20211G508 | List: |
| References | |
| PY-CEI-NRR-0478, PY-CEI-NRR-478, NUDOCS 8606190463 | |
| Download: ML20211G509 (200) | |
Text
{{#Wiki_filter:_- __ _-_ ATTACHMENT I PY-CEI/NRR-0478L Re. O ll' , June 10. 1986 l L 4 4 Deep Well Injection at the Calhio Wells
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and j The Leroy, Ohio Earthquake of January 31, 1986
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9 Pradeep Talwani and Steve Acree l 1 I.j
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^ 1. INTRODUCTION
.i m, On January 31, 1986 at 11:46 a.m. (Eastern Standard Time) a ( ] magnitude 5.0 earthquake occurred near Leroy in northeastern 8 Ohio. The epicenter was located about 17 km (11 miles) south of 5 the Perry Nuclear Power Plant at Perry. Ohio. In common with s similar moderate earthquakes in the northeastern United States, this event was shallow (about 5 km deep) and not associated with 3. d any surface manifestation. It occurred in an area with no known il g seismogenic feature and thus its cause was not understood and i could only be speculated upon. There are two deep injection j l wells located about 11 km (7 miles) north of the epicenter. The a observation that a large volume of fluids had be'en pumped into j these wells in the last twelve years, and the knowledge that in a few cases such operations in other locations have in some cases j , triggered small to moderate earthquakes, led to the speculation s that this fluid injection may have triggered the January 31, 1986 ll ] '4 event - the Leroy earthquake. j In this report a variety of data are examined in order to
)
7: address this possible association. The Leroy earthquake, its A l aftershocks and the historical seismicity in the area are described in Section 2. Data pertaining to the two deep wells and fluid injection operations are given in Section 3. and those ,(
; regarding solution mining in the area are given in Section 4. In
.t I order to assess the characteristics of the observed seismicity at
.Leroy vis a vis well induced seismicity, a review of the latter is presented in Section Recent instrumentally recorded earth-(
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s 2 h () quakes in tectonic settings similar to that of the Leroy earthquake are described in Section 6. In the final section the i various data presented are analyzed to assess the validity of the s speculation that the observed seismicity at Leroy, Ohio was induced by the injection of fluids in the two deep wells. Some
$ of the concerns expressed by Professor Ahmad in his testimony before the Subcommittee on Energy and the Environment. Committee 3
1
! on Interior and Insular Affairs. U.S. touse of Representatives on
(
$ April 8, 1986, are addressed in Appendix I.
)1, i
; Our conclusion is that although it is possible for the Leroy earthquake to have been induced, it is highly unlikely that it was. The event appears to be a normal, typical tectonic earth-l
, ;, quake which occurs regularly, albeit infrequently in northeastern s-(s United States.
ii.
- 2. THE LEROY EARTHQUAKE, AFTERSEOCES AND HISTORICAL SEISMICITY l
1 IN THE ARIA i i. 1 The Main Shock l} On January 31, 1988 at 11:46 a.m. (EST), a body-wave magni-tude 5.0 earthquake, with a maximum Modified Mercalli intensity VI, shook northeastern Ohio. Preliminary location of this event by the National Earthquake Information Service (NEIS) based on teleseismic data and the standard Jeffreys-Bullen earth model. , placed the epicenter at 41.649'N and 81.105*W (41* 38.56'N, 81* l 06.18'W). Using a U.S. seismic model, this event was relocated about 6 km to the west at 41.650*N and 81.162*W (41* 39.00'N and 6
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t '. : 3 1 _, 81* 09.43'W) with an epicentral accuracy of i4 km (2.5 miles) at l ( the 904 confidence level (Borcherdt, 1986). The best solution l , was obtained when the depth was constrained at 5 km (3.1 miles) - the best estimate for the hypocentral depth. (The latter epicentral location was also found to lie within the cluster of aftershocks and the region of maximum intensity.), ___ l I q f 2 Aftershock Studies i At least seven teams of seismologists deployed portable I seismographs in the epicentral area to record possible after-shocks of the Leroy earthqake. (Please see Weston Geophysical j data for details.) The U.S. Geological Survey deployed a ten-station array of broad band digital instruments, the General Earthquake Observation Systems or GEOS (Borcherdt, 1986). These a ', complemented several smoke-paper recorders deployed'by other r groups. Through April 15, 1986, 13 aftershocks with coda wave i magnitudes between -0.1 and 2.5 had been located. Preliminary j locations of six aftershocks recorded on the GEOS instruments between 2/1/86 and 2/10/86, using a layered seismic velocity model are given in Table 1. The aftershock epicenters are . t i tightly clustered and lie in a 1 km square (0.4 mile 2) (Figure 1
& 2). These six and an additional seven events (to 4/15) were f
also located by Weston Geophysical (Figure 3 and Table 2). The l locations of the six' events common to the two data sets are in general agreement, with the Weston epicenters located on average O()
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35- -' 35-1 11- 10- 9- 8- 7- 5-i ,e (From Borcherdt,1986) ]1 ? 1I l-Figure U.S.G.S. epicentral location of aftershocks (y 2. (2/1-2/10/86) detail. C,j r -7 i-*-- - * - - - * " - - '
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Table 1 i U.S.G.S. LOCATION OF AFTERSHOCKS. J f .{ l Aftershocks: - 1 YR MO DA ORIGIN LAT N LON W DEFIH RMS ERH ERZ GAP 71 i 86 2 322 48.57 41 38.76 81 9.50 5.12 0.01 1.16 0.78 150 l 86- 2- 3 1947 19.65 41 38.92 81 9.43 5.81 0.03 0.88 0.76 116 86- 2- 5 634 2.40 41 38. % 81 9.68 4.05 0.02 0.88 1.31 134 ( 86- 2- 6 1836 22.26 41 38.68 81 9.33 6.06 0.03 0.82 0.80 121 U- 86- 2- 7 1520 20.19 41 38.97 81 9.42 4.66 0.03 0.92 5.21 115 86- 2-10 20 6 13.59 41 39.07 81 9.31 3,38 0.04 0.81 6.31 115 !i{. - I
,] (From Borcherdt,1988) 3 Table 2 1
I COORDINATES OF MAIN SHOCK AND AFTERSHOCKS. c;; YA MC3Y HRMIS EC LA7. L 3N 3. DEPTH MB MC l
- ) I 15360131 164642.3 41.650h 81.162W 5- 6 4.9J.90.00.0 1 15860201 135,41.3 41.545h 81.153W 4.3 1.5
- 15360202 032246.9 41.645h S1.159h 4.3 0.9
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15360203 19471).6 41.649h 31.153W 5.3 , 2.3 15360205 063402.3 41.64Sh al.155W 3. 7 0.1 15360206 183622.4 4 1 . 6 4 5f. 31.160W 5. 5 2.5
! 19360207 15I010.3 41. 6 51t. 81.154W 3. 7 1.1 j 15360210 200613.5 41.652N 81.157W 4.7 0.3
=; 19963223 032148.5 41.653h St.152W 5. 4 0.1 if 15363224 165506.5 41.649h 31.163h 3.2 0.1 l2' u n':2 '!:!t!!:!!!"
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4 - lli' 15363324 134241.3 41.639h 81.156W i:? 4.7 l:1 1.4 ^} w 15363410 065805.7 41.647h 81.159W 4.7 -3.1 O (From Weston Geophysical)
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i j . b 3 4 MAINSHOCK and AFTERSHOCKS UP TO APRIL 15,1986 l 6
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!' Figure 3. Weston Geophysical location of main shock and aftershocks to 4/15/86.
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) about 0.5 km to the northwest of those by U.S.G.S. With.the exception of a N g 1.4 event on March 24, 1986, the remaining !
J twelve epicenters lie in a tight cluster about 0.5 km (0.3 mile) i l to the east of the location of the mainshock. The depths of all I the events lie between 3 and 6 km (1.9 - 3.7 miles) (Table 2). ' Since the location of the mainshock was based on distant sta-i 1 tions, it is very likely that it too was located in the narrow j a cluster defined by the twelve aftershocks. The lack of an 3 obvious elongation in the aftershock pattern (if the March 24 j event is not included) makes it difficult to infer the orienta-I
;} tion of the fault plane. If the March 24 event is included, an y
i apparent north-south trend emerges. l 4 j g The March 12. 1986 Microcarthquake I At the progress meeting with the NRC and the utility on
. April 30, 1986, Dr. Wesson of the U.S. Geological Survey brought to our attention the occurrence of a miniscule event on March 12, lj 1986 that had been recorded on the GEOS station at site 4 (GSO2) ?.;
(Fig. 4). This coda magnitude -0.3 (LeBlanc, personal communica- ] tion) event with a total duration of about 4 seconds was also ll 11 recorded on some stations deployed by Weston Geophysical Co. and
- s by Woodward Clyde Consultants (WCC). Using their preliminary N' arrival times the event was located by U.S.G.S. at 41' 43.63'N.
; 81* 10.24'W, with a depth of about 2 km (1.2 miles) (Table 3) -
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The event was located by using a 7-layer seismic velocity model
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1 10 Table 3 LOCATIONS OF THE MARCH 12. 1986 MICR0 EARTHQUAKE Origin Lat. Long. Depth 03:12:18.55 41*N 81*N K a_ Gap RMS Remarks 26.59 43.63' 10.24' 2.01 216 .06 USGS prelim. location 7-layer model. Prelim, arrival times for WCC stations. 26.64 43.83' 10.13' 1.73 .05 WCC solution, revised picks and 3-layer model. 26.64 44.00' 10.29' 1.76 176 .05 Used revised picks 3-layer model and data for Weston stations. 26.52 43.85' 10.40' 1.97 175 .09 Used revised picks 06- 7-layer model and i data for Weston stations.*
- For comparison.
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1/22/83 DEPTHS 11/19/83 A PROH CALHlO X 0.0+ WELLS A WELL Revised , ,,,, - Avv locat. ion 3/12/86 g, A cs02
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y,o. o o s.0+ p USGS (Prellm.) . *g,0 MAGN 110 DES A CON a -1.0* A CAL A HLH AT 3M O 0.0+ g O 1.0+ A CFD A WC08 2.0+ 40' - A NCO2 - 3.0+ A GS03 A ERJ A BUR 4.0+ 2 KM 5.0+ i . . A FARM
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I 10' (Modifled from Wesson. Pers. Comm. 19 f16 i Figure 5. Preliminary U.S.G.S. and revised Weston location of 3/12/86 event and location of the 1983 earthquakes.
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'(Table 4). Using revised picks for the arrival times for the WCC 04 .:
stations and a 3-layer velocity model (the same as the one used by Weston Geophysical) the location of the event moved about 200 m (655 ft) to the northeast. Incorporation of data from Weston stations moved it about 380 m (1245 ft) to the northwest. Thus our preferred location 41' 44.0'N, 81* 10.29'W and depth 1.76 km (1.09 miles) is about 2.5 km (1.6 miles) SSW of the deep wells, and about 10 km (6.2 miles) north of the epicenters of the Leroy sequence. The implications of this event vis a vis a possible association with fluids injected in the deep wells is discussed in Section 7. The 1983 Microcarthauakes Two microcarthquakes occurred within 10 km (6.2 miles) of the two deep Calhlo wells in January and November 1983. These events have been studied by Dr. LeBlanc of Weston Geophysical, who provided the following information. The January 22, 1983 earthquake was recorded on regional stations - the nearest being at John Carrol University. It was also recorded on stations of the Anna. Ohio network and by stations in Western Ontario. Canada. The Earth Physics Branch (EPB), Canada assigned it a Nutt11 magnitude (MN) 3 . 3 wh e r e'a s the National Earthquake Information Service (NEIS) assigned it a body wave magnitude (m,bLg) 2.7. The epicentral location of the event obtained by Dr. LeBlanc based on these data is 41' 45.9'N, 81* 06.6'W with an uncertainty of a few kilometers. The best depth estimates place the event between 2 and 4 km (1.2 and 2.5 miles). A smaller
13 Table 4 i THREE LAYER VELOCITY MODEL. Depth to Top P Velocity Vp/Vs of Layer (km/s) (km) 0.0 - 4.25 2.0 6.5 1.73 35.0 8.1 I Weston Geophysical. Depth Thickness P Velocity S Velocity vp/Ya *
- Description *
(km) (km) (lun/s) (km/s) Layered Crust 0.0 0.05 1.80 0.60 3.00 Glacial till 0.05 0.45 3.00 1.60 1.88 Devonian shale 0.50 0.50 (20 2.36 1.78 Silurian dolomite 4 1.00 0.75 4.5'O 2.53 1.78 Ordovician limestone and dolomite I 1.75 0.35 4.75 2.67 -1.78 Cambrian sandstone and dolomite 2.10 17.90 6.15 3.68 1.67 Precambrian granite i 20.00 25.00 6.70 3.87 1.73 Lower crust 40.00 99.00 8.15 4.65 1.75 Mantle l Cleveland Electric Bluminating Co. (1982) (From Borcherdt, 1986)
*
- In locations given in Table 3 a Vp/Vs ratio of 1.73 was used for all the layers.
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14 Cp V.) event occurred on November 19', 1983 and was assigned a magnitude 2.5 by EPB and was not assigned a magnitude by NEIS. Based on similarities in the wave trains of the two events at some Canadian stations Dr. LeBlanc argued that both events had the same epicentral location (within our ability to locate them). This location is shown on Figure 5, and the possible implication of these events vis a vis their being induced by fluid injection is addressed in Section 7. Historical Seismicity The historical seismicity in the region and in a 80 km (50
. mile) radius centered at the Leroy epicenter and of Ohio are shown in Figures 6. 7 and 8. These maps are discussed by
( Weston Geo, and are presented here to make the observation that felt earthquakes had occurred here in historical times. The largest previous event in the 80 km (50 alle) radius was the magnitude 4.7 event on March 9, 1943. Composite Fault Plane Solutions Composite fault plane solutions using events in the cluster yielded strike slip solutions (See Weston Geophysical's data ), with either right-lateral strike slip motion on a steep NNE striking fault or left-lateral strike slip motion on a steep fault oriented to the northwest. In view of available gravity and aeromagnetic data discussed by Weston Geophysical, the NNE trending nodal plane is the more likely fault plane. l
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' [m).' DEPARTMENT OF THE INTERIOR
'Q* UMffEO STATE 5 Gt0 LOGICAL $URYtY
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l . . . . . ._ ). . . . . . - Figure 8. SEI5MICITY MAP OF THE STATE OF OHIO r l {N , Sr l
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i 18 n 3. REGIONAL DEEP MELL FLUID INJECTION i Three high pressure fluid injection wells currently operate within Lake County, Ohio. Two wells owned by the Calhio Chemi-cals division of the Stauffer Chemical Company (Calhio al and #2) have been in operation since 1974 and mid 1981, respectively. These wells, spaced at approximately 800 m (2600 ft) apart, are located about 11 km (7 miles) north of the epicentral area. The fluids injected through these wells consist of a dilute aqueous brine containing waste products from the manufacture of agricul-tural fungicides. A cumulative total of 1.17 x 106 ,3 (310.2 million gallons) of fluid has been injected at depths below =1670 m (5480 ft) (Nealon, 1982; Ohio EPA, 1985) and pressures to = 112 bars (1830 psi) (top hole) at rates to 326 liters / min (86 gal / min). Of this total, 1.02 x 106 ,3 (268.2 million gallons) have been injected in Calhlo #1 (Figure 9 and 10) (Table 5) and 1.59 x 10 5 ,3 (41.9 million gallons) have been injected through Calhio #2 (Figures 11 and 12) (Table 6). 3 Approximately 3069 m I (0.8 million gallons) of a salt water brine have been injected through a single well located near Painesville, Ohio owned by Environmental Brine Services, Inc. at top hole pressures to 55 l bars (800 psi) since initiation of injection in October 1985 (Ohio Dept. Nat. Res., 1986). In all three wells fluids were injected into the Mt. Simon Formation, a friable fine to coarse grained dolomitic Cambrian sandstone, which overlies Precambrian granitic basement (Nealon. 1982). In Calhio *2, the Mt. Simon was logged as approximately 6
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) Table 5 VOLUMES OF FLUIDS AND INJECTION PRESSURES FOR CALHIO CHEMICALS WELL *1.
Calhio Injection Well
- 1 Total Cumulative Injection l Start S too Gallons Gallons Pressure McDaYear MoDa Injected Injected Man. Min. Ave.
03191975 0331 697333. 3630743. 700. 3. 555. 04011975 0434 2158682. 5739425. 1000. O. 875. 01011976 0131 2435051. 22742513. 1430. O. 1415. 02011976 0229 1105083. 23847606. 1455. O. 1440. 02011976 0331 2034653. 25532264 1270. O. 1130. 04011976 0430 2622620. 17554384. 1340. O. 1230. 05011976 0531 246964. 27801349. 1225. 3. 1220. 07011976 0731 3003889. 33333973. 1410. O. 1330. 08011976 0831 1679345. 35058313. 1425. O. 1230. 05011976 0930 1930055. 37048373. 1370. O. 1300. 1C 0119 76 1031 2854348. 39903721. 1425. O. 1350. l 11011976 1130 2634417. 42598139. 1450. 3. 1375. 12011976 1231 1938593. 44576731. 1230. O. 1230.
-l 01011977 0131 2660877. 47237603. 1430. 3. 1430.
l 02011977 0228 2673412. 49911020. 1525. O. 1530.
. 02011977 0331 2560253. 52471273. 1525. O. 1440.
04011977 0430
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2350339. 54621612. 1500. O. 14J0.
,_/
05011977 0531 1891692. 56713304 1330. O. 1130. 06011977 0630 2134498. 53897302. 1355. O. 1350. 07011977 0731 1798450. 60696252. 1210. O. 1230. , 0E 0115 77 0 831 1596976. 62293223. 1270. O. 1255. 09011977 0930 2006380. 64299603. 1260. O. 1250. 10011977 1031 2319269. 66618377. 1255. 3. 1250. 11011977 1130 1930569. 63549446. 1220.e 0. 1250. 12011577 1231 2298476. 70647922. 1240. O. 1220. 01011978 0 131 18452St. 72693203. 1230. O. 1240. 02011578 0228 1955072. 74643275. 1240. 0.- 1220. 03011978 0331 2832535. 77430310. 1460. 3. 1430. 04011978 0430 2949999. 30430803. 1480. O. 1440.. 05011978 0531 3314135. 83744943. 1500. O. 1470. 36011978 0630 2094065. 85839003. 1500. O. 1350. 07011978 0731 1236726. 87125734. 1290. O. 1230. 08011978 0 831 3648315. 90774049. 1295. O. 1230. 05011978 0930 1944327. 92718376. 13 20. O. 13J0. 1C 0119 78 1031 2247499. 94966375. 1420. O. 1340. 11011978 1130 263S632. S7605007. 1470. O. 1370. 12011978 1231 3016456. 100621463. 1440. O. 1400. 01011979 0131 1367075. 101938529. 1420. O. 1430. 02011979 0 22d 2701315. 104690453. 1430. O. 1330. 03011979 0331 2829000. 107519451. 14 20. O. 14J0. 04011979 0430 2S16038. 11C335489. 1460. O. 1420. 05011979 0531 2861572. 113197061. O. () 06011979 0530 07011979 0 731 2351740. 3103232. 1155493C1. 113652033. 1450. 1420. 1440. O. O. 1420. 1430. 1430. 08011579 0831 2735412. 121437445. 1440. O. 1410. 01011979 0930 3134716. 124622161. 1440. O. 1420. 1C011979 1031 3173303. 127795464 1430. O. 1410. 12011979 1231 3406783. 124268336. 1560. 3. 1510.
~ .
22 ! Calhio Inj ec tion Well e 1 0" Total Cumulative Injection Start S top Gallons Gallons Pressure Mo3aYe ar M o0a Inject 2d 2njacted Max. Min. Ave. 01011980 013f 3353000. 137631336. 1560. O. 1520. 02011980 0229 2771584. 139402920. 1510. O. 1330. 02011980 0 331 3253619. 142656539. 1520. O. 1430. 04011980 0430 3534030. 146240563. 1560. O. 1520. 05011980 0531 3127521. 147363190. 1520. O. 1420. 06011980 0630 3136545. 1525.04725. 1550. O. 1450. 07011980 0731 3258443. 155763173. 1560. O. 1520. 08011980 0831 2776363. 153539541. 1550. O. 1530. 05011980 0930 2877980. 161417621. 1460. O. 1420. 1C 1019 80 1031 2919511. 164337232. 1500. O. 1450. 11011990 1130 2625173. 166953205. 1440. O. 1340. 12011980 1231 3517327. 170431132. 1430. 3. 1440. I 01011891 0131 2457250. 172948322. 1430. O. 1350. 02011181 0223 3250175. 176138559. 14 20. 980. 1430. 03011181 0331 35?9074. 179797532. 1520. 1223. 1410. l 04011981 0430 3428650. 183226282. 1495. 1420. 1450. 05011581 0531 1600319. 184826901. 1530. 1120. 1370.
, 06011981 0630 75046 5. 185577366. 1430. 390. 1230.
07011131 0731 2355992. 187943353. 1560. 1040. 1340. O E 0119 81 0 831 1869980. 187447346. 1550. 800. 1430. 05011981 0930 1058205. 139535551. 1320. 1053. 1230. () 11011991 1130 12011991 1231 1674386. 932543. 192922365. 193825796. 1430. 1310. 1000. 1150. 1350. 1020. 01011982 0131 3056153. 196632746. 1470. 1140. 1230. 02011982 0228 3157200. 200049946. 1560. 1270. 1430. 03011982 0331 1934574 210954620. 1430. 1070. 1330. 34011982 0430 1121864 201076484. 1330. 1043. 1330. 06011982 0630 634482. 201710966. 1140. 340. 930. 07011982 0731 231422. 201942363. 1020. 780. 840. 11011982 1130 755343. 202637731. 1110. 680. 840. 12011982 1231 3073793. 205771524 1310. 1010. 1230. 01311983 0131 2744922. 20S516446. 1330. 1300. 1320.
! 02011983 0223 3119054. 211635503. 1440. 1120. 1370.
02011983 0331 3238646 215024346. 14 60. 1120. 1330. 8 04011983 0430 3335133. 213330276. . 1510. 1223. 1470. l 01011583 0531 1334399. 211635375. 1510. 1020. 1230. 06011983 0630 62613. 213637993. 1030. 933. 970. 07011983 0731 451944. 220134937. 1250. 920. 930. OE 3119 83 0 331 1159455. 221254392. 1250. 903. 1050. 01011993 0130 748463. 222132352. 1350. 910. 1230. 10011933 1031 2254463. 224357315. 1440. 903. 1220. 11011983 1130 1530796. 225943111. 1510. 1010. 1230. 12011933 1231 2333184 228291295. 15 10. 1020. 1350. 01311984 0 131 2252359. 230544154 1470. 1110. 1430. 02011984 0229 2675326. 233219180. 1620. 1240. 1450. 03011984 0331 2635053. 235855021. 1610. 1160. 1450. 04011984 0430 2752377. 233637409. 1610. 1320. f540. ~ l 05311934 0531 2376413. 243933821. 1550. 1240. 1230. S e *
,ewr--y,p--,-- --
,9--.---- ,r,- --y-e v -
,.m,c. ,
, . . . - & , . a.- .
. - .< ~ ~ . . .
23 Calhio Injection Well e 1 Tota'l Cumulative Injection Start Stop Gallon s Gallons Pressure McDaYe ar M oDa Injected Injected M ax. Min. Ave. 06011984 0630 1338978. 242372799. 1520. 1000. 1100. 07011984 0731 0. 242372799. 930. 960. 970. 08011984 0831 0. 242372799. 950. O. 530. , 09011985 0 930 3. 2423'72799. O. O. O. l 10011994 1031 824985. 243197784. 1300. 950. 1030. 11011984 1130 1634477. 244832261. 1420. 940. 1225. 12011984 1231 2665795. 247498056. 1460. 1260. 1430. 01011985 0131 2631156. 250179212. 1465. 1260. 1430. 02011985 0223 2437963. 252617175. 1530. 1300. 1470. 03011985 0331 2348933. 254966105. 1!00. 1190. 1425. 04011985 0430 2576547. 257542652. 1510. 1300. 1470. 05011995 0531 2230432. 259823084. 1500. 1240. 1410. I 06011985 0630 2568510. 262391594. 1450. 1203. 1400. 07011985 0731 2053425. 264445019. 1420. 1160. 1330. O E 0119 95 0 831 955207. 265430226. 1440. 1020. 1250. 09011985 0930 3. 265430226. 1040. 340. 990. 10011985 1031 16633 5. 265556561. 1090. 380. 950. l 11011985 1130 2046986. 267613547. 1300. 1100. 920. 12011985 1231 661501. 263275148. 1310. 920. 1050. (From Weston Geophysical). e I l O
. - ~ _ , -
Q- -- - Q 500 o CALHIO #2 - 3000 8 o O O O o ~ o 400 , x
~
x . 2500
~ S
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ct y 300 _ 2000 o- *
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- 1500
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. =
=
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i, l. 0 , , , ,, ,l T 3 1 . ll o 1975 1977 1979 1981 1983 1985 1987 (Modified from Weston Geophysical) Figure 11. Volume of fluids injected per month and cumulatively at Calhio #2.
25 d'.', g 20co , , , , ,
,. * ~*
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I e 500 . _ 1 o i e i e i ~ 1975 1977 1979 1981 1983 1985 1987
.... INJECTION WELL
- 2 From Weston Geophysical Figure 12. Injection pressures utilized at Calhio #2.
J O
- g - -- --- -e , - . , - - - , - - - , - , ,w,---
k _ () Table 6 VOLUMES OF FLUIDS AND INJECTION PRESSURES FOR CALHIO CHEMICALS WELL #2. Calhao 2njec tion Well
- 2 Total C ue 91 a t iv e Injection Start 5 too Gallon s Gallons Pressure Me3aYear MoDa 2njected injected M an. Min. Ave.
O!011181 0531 12:1124 1235284 1430. 1050. 1230. 04011181 0 630, 1333384.- 2556163. 1410. 1093. 1340. 07311131 0 731 324317. 2810,185. 1400. 960. 1030. 08311131 0 831 168241. 3534417. 1550. 12!O. 1430. 01011181 0 933 1160575. 541411'. 1560. 1053. 1430. 11011191 1130 1211686. 8137641. 156C. 1040. 1440. 12311181 1231 204638). 13154033. 162C. 1160. 15J0. 01311182 0131 67536. 1J221366. 1220. 160. 1150. 03011132 0 331 1221573. 11443436. 1623. 1413. 1550. 07011182 0731 731632. 12235J68. 1220. 760. 830. ' 38011182 0431 628177. 12833245. 1130. 953. 1030. 10311182 1J31 345331. 132285t4 124C. 760. 830. 11011142 1130 816644 14125221. 1130. 703. 840. 12011132 1 231 633971. 14759207. 1410. 380. 1030. 01311193 0 131 5 3 C 3 51. 13310053. 1400. 183. 930. 32011183 0224 68272. 15278333. 920. 360. 130. e 03011183 0331 13376. 15391406. 1240. 900. 950. 04011183 0430 214702. 15606103. 1390. 1300. 130. j 05011183 0 331 1859744. 17465352. 1610. 183. 1230.
'u J4 01113 3 0 63J 1763216. 11227141. 1600. 1323. 1330.
07011183 0731 457473.- 19636613. 1260. 303. 950. 08011183 0831 3. 19634613. 160. 880. 130. 01011183 0930 1918153. 21634771. 1550. 893. 1320. IC 011183 1331 617417. 23332138. 159C. 960. 1150. 1101118 3 113J 1139565. 24441753. 1590. 143. 1130. 12011183 1231 336783. 24713533. 1610. 180. 1130. 01011984 0 131 138363. 24916313. 1250. 16J. 1050. 02011184 0221 67366. 230644!1. 1340. 970. 1C30. 02011184 0 331 315503. 25415151. 1210. 173. 930. 04011134 0433 249782. 23739742. 1430. 1050. 1130. 32011184 0531 533333. 262177!3. 1380. 1320. 1233. 06 011g a4 0 63J 1639171. 27136921. 157C. 123J. 1430. 07011134 0 731 2210717. 30117633. 1550. 1340. 1520. I 28011184 0331 1939323, 3384972J. 1560. 1283. 1!10. 01011185 013J 2137683. 36037603. 1590. 1280. 1530.
' 1C011184 1031 1562783. 37633183. 155C. 1100. 1430.
11011194 1 130 1466413. 39067073. 1530. 1123. 1430. 12011184 1231 13701. 31150774 1330. 1041. 1130. 01011135 0131 J. 39150774 1060. 1340. 1030. 02011135 0224 3. 31130774 106C. 1033. 1035. 02011185 0331 1114353. 4:265632. 1500. 1340. 13J0. 04011165 0431 1022J83. 412187I3. 1620. 1113. 1450. O!011115 0531 273353. 41561773. 1430. 1310. 11 50. Ge 011155 0 634 3. 4156177J. 1020. 1003. 1010. 07011195 0731 3. 41161773. 1000. 160. 175. 08 J11185 0 831 179314 41741524 1315. 943. 1030. 01011185 0130 3. 41741584 99C. 123. 950. 1CJ11195 1J31 J. 41741584 910. 440. 870. 11011135 113 J 111*.86. 41133373. 12504 123. 8J0. 12311135 1131 J. 41132371. 113. 363. 8 10. (From Weston Goephyelcell O( 4
^-
wh_
27 45 m (148 ft) thick (Resources Services, 1980). The Mt. Simon Formation is overlain by the Shady dolomite, a sandy, medium to coarse grained dolomite, and the Rome Formation, a sandy, fine to medium grained dolomite with thicknesses of a 58 m (189 ft) and = 26 m (86 ft), respectively. About twenty-four meters (80 ft) of
~
the Conasauga Formation, consisting of fine grained sandstones and limestones with interbedded shales , cap the Rome Formation. Above the Conasauga lies the 31 m (102 ft) thick Maynardville dolomite. consisting of alternating sandstones and dolomites. Highly fractured zones were encountered while drilling the Maynardville in Calhlo #2 The Copper Ridge dolomite caps the Maynardville. Permeability and porosity measurements'were obtained from 57 o samples taken from = 19 m (62 ft) of cored Maynardville dolomite in Calhio 82 (Table 7) . The average permeability was 2.1 mDar-cies and the average porosity was 2.12. These values may be too low as recrystallized calcium chloride from the drilling mud was found to contaminate many of the samples. The maximum permea-bility obtained was 54.4 m0arcies with a porosity of 2.9% I (Resources Servi c es ,198 0 ) . The average permeability and porosity l l values reported f or the Maynardville dolomite and the Mt. Simon
- ?
l Formation from Calhio 81 were 4.2 mDarcies. 8% and 5.5 mDarcles. l l 8.5% respectively (Ohio EPA, 1985). Nealon (1982) reported per-meabilities of 3 to 6 aDarcies for the Mt. Simon Formation at the Calhio well sites as determined f rom drill stem tests. I i The specific gravity and total dissolved solids (TDS) of l I i _ ~ - - .. . . . _ _ _ _ . _ ._ _ - . _ _ _ _ _ _ _ _ _ . . . . _ _ _ _ , . , . , _
= - - - _ . . . _- _- .- -
g __ _ _ . . _ . 28 _ ( :q Table 7
.V PERMEABILITY AND POROSITY DATA OBTAINED PROM CORED SECTION OF MAYNARDVILLE DOLOMITE (CALHIO #2).
otetw ggy, ,y3 ny PERMCABILITY ...... MatuoAacts POROSITY oro=. gI AvtAAG( ANa50 % N W MMU* PERCtWT uo Tayvg 25 50 PS 10 20 30 5480.0-81.2 .1 12.3 .9 o 5482.0-83.1 1.9 13.4 .9 x n 5483.1 84.0 ( .1-) 7.4 .1 o
-5484.1-85.1 .2 2.3 1.2 no 5485.7-86.7 .2 10.2 1.6 ho 5487.9-88.6 .: 9.6 3.2 pon 5488.8-89.6 1.4 12.1 .5 x o lI 5490.1-90.8 ( .1 - )l 19.3 4 3 5490.8-91.7 3 9.2 2.6 no 5491.8-92.5 8,1 98.5 2.0 axx on 5492.9-94.0 .1 3.8 1.3 no 5494.0-94.9 6 49.7 2.7 no 5495.3-96.1 .1 24.4 2.4 w 5496.1-96.9 .2 4.0 2.0 %
$496.9-97.7 .5 6.3 4.1 ,co 5497.8-98.8 .1 55.4 1.0 3 5498.9-99.8 .3 2.8 2.0 oo 5499.9 .6 .2 15.9 2.2 ao 5501.4 -1.9 ( .1-) 8.8 1.8 no 5502.0 -2.5 54.6 80.7 2.9 mmmommmom non A $503.0 -3.5 6.0 72.5 1.5 ax 5503.7 -4.9 2.8 39.3 1. 7 k V' 5505.0 -5.6 5505.9 -7.1
.2
.1 24.6 57.4 2.7 I 1.2 po 3o 5507.3 -7.7 .1 30.9 3.7 m 5508.0 -8.6 .1 11.3 2.2 w 5509.5-10.0 .1 58.5 1.6 ao 5510.1-11.1 ( .1-) 24.7 1.4 m 5511.3-11.7 ( .1-) 3.5 3.5 m 5512.5-13.7 12. 6t 20.3 .9 ____ _ _ _ .
5513.3-14.3 3.] 88.5 2.9 xx w 5514.6-15.1 ( .1-) 11.3 .5 a 5515.1-15.6 .1 8.4 4 o l 5516.0-16.5 ( .1-) 4.2 9 b 5516.8-17.8 ( .1-) .0 4 m 5518.0-18.5 ( .1-) .0 .8 s
$519.1-19.9 2.0 77.5 1.9 e ao 5520.1-20.9 .1 59.8 2.4 ao 5520.9-21.7 .2 17.6 1.7 no 5521.8-23.0 3.6 46.9 2.6 a no
$523.7-24.7 8.11 1.9 .5 axx o 5524.8-25.7 .6 11.0 4.4 woo 5526.3-26.8 1.2 44.7 3.6 x oco 5526.8-27.8 4 4.1 3.7 m 5527.8-28.6 .1 18.2 .8' s
$529.6-30.3 ( .1-) . 3.1 .9 3 5530.5-31.0 .1 5.7 3.6 mn 3531.0-31.4 ( .1-) 2.3 4.8 :m) 5531.8-32.8 4 8.5 3.5 son 5532.8-33.7 .5 4.5 3.7 aoo 5533.9-35.1 1.0 48.6 3.4 mo 5535.4-36.0 .3 .0 4.9 mco 5536.6-37.3 1.2 4.1 4.4 m wo
$537.4-38.4 .1 .0 2.7 bn 5538.4-39.5 .3 1.6 2.5 bo 5540.2-51.4 ( .1-) 11.2 2.7 no 5541.7-42.1 .1 34.4 .8, P 4
Q(% (From Resources Services,1980) l
~
l 29 formation fluid from the Maynardville in Calhio #2 was 1.213 with 319,699 ag/ liter and a pH of 5.7. Fluid obtained from the M't. Simon had a specific gravity of 1.158, a pH of 5.3. and a TDS of
- I 224,896 ag/ liter (Ohio EPA, 1985). Nealon (1982) reported a i
+
specific gravity of 1.218 for formation fluid from the Mt. sinon formation. It is noted that the specific gravities reported for the resident brines are considerably greater than the specific gravity of the fluids injected through the Calhio wells (1.025) (Nealon, 1982). In sita pore pressures. measured in Calhio #1 were 170 bars (2472 psi) la the Maynardville dolomite and 187 bars (2716 psi) within the Mt. Simon at depths of 1867 m -(5468 ft) and 1807 m (5928 ft), respectively (Ohio EPA, 1985). Calhio well #1 reaches a total depth of 1851 m (6072 ft) below ground cc - level with injection intervals in the Maynardville dolomite (1670
- 1716 m) (5480 - 5360 ft) and the Mt. Simon Formation (1807 -
1847 m) (5928 - 6060 ft) (Nealon, 1982). Calhio well #2 reaches a depth of a 1862 m (6110 ft) below ground level with injection intervals in the Maynardville dolomite (1869 - 1716 m) (5475 - 5630 ft), the Rome Formation (1743 - 1765 m) (5720 - 5790 ft), and the Mt. Simon Formation (1813 - 1858 m) (5948 - 6096 ft) l (Nealon, 1982). The well operated by Environmental Brine injects salt water in the interval between approximately 1779 and 1806 m (5838 - 5926 ft) (Ohio Dept. Nat. Res., 1986). All injection intervals were hydraulically fractured. l Instantaneous shut in pressures (ISIP) (top hole, after stimula-tion) obtained within the Maynardville dolomite and Mt. Simon (:) - l - l l
30 Formation were 152 bars and 159 bars in Calhio well #1 (Resources p( r' . Services. 1986) and 139 bars and 165 bars in Calhio well 82, respectively (Resources Services, 1980). The ISIP measured at the Environmental Brine well site was 114 bars within the injec-tion interval (Ohio Dept. Nat. Res., 1985). Under the conditions of a controlled scientific experiment ISIP is directly related to the minimum horizontal stress (Shmin) at the test depth. ISIP measured under the prevailing conditions can only be used as an indication of the possible maximum value of S hain'
- 4. REGIONAL SOLUTION MINING Solution mining of salt deposits has. taken place in north-eastern Ohio since the late 1880's. Dunrud and Nevins (1981) list two active and five abandoned operations within approximately
( 100 km (62 miles) of the epicentral area (Figure 13) (Table 8) including a Painesville. Ohio mine listed as possibly abandoned around 1977. With the exception of the questioned Painesville mine, the sites listed as active are greater than 75 km (47 miles) from the epicentral area. l
- 5. RIGH PRESSURE INJECTION INDUCED SEISMICITY Most cases of fluid injection are not associated with any seismicity. However, in the last decade the high pressure injec-tion of fluids into the earth has been associated with the onset or increase in seismicity at a few sites worldwide. The favored explanation of the mechanism by which these earthquakes are i triggered (Martin. 1975: Lockner et al., 1982) is the effective
(:)
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9
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y 7
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Table 8 DATA PERTAINING TO SOLUTION MINING OF EVAPORITE DEPOSITS IN OHIO 'l l t n.a . :---i a u-. - ... .-. .a i n . . .n. a i .. r,,u.i . 1,,. .e -.i s.. i.e i s.wa. m a s.u Cy
.:4..8 s.-i.-
s., ss B ag.i t i.e S 3 s. 8 . f-. 88 t.4 by
- . --a - n. . .a . .e.
. . f. .-.
,- . .a
. . . .u.-.
.. .. e a- - s - s.ua ..
. .a- .e..is.. ... .u 8000 M
l m a~.e-ea- ases ,. ees - - y s.e 1 .-_ - un . ni . - - . , 6 $9771 - 84 & et:1. l.4.--===== 8988 = $93F1 570 - I 1 85
-^
._ Sw s- Bett = 89919 8 30 b -
83 C3.w.I C.y.h .--. MS b === - - ---
.e.t.e .193,: sa
.B n.
. -; w . i9n >= s. - - - -
1 i (thodified from Dunrad and lievine,1981) i i f 4
s .u:u <.w- .~.>- .v- -.....e :: - - $, 33
~
I stress theory of Terzaghi as applied by Hubbert and Rubey (1959). O In this model, injection increases the pore pressure along exist- [ ing fractures reducing the frictional strength through. reduction y of the effective normal stress. If the shear stress along the fracture is greater than the sum of the frictional resistance and the cohesive strength then slip occurs. An extension to this model involving the transformation of high strength barriers into high stress asperities through aseismic creep ultimately leading
- to failure has been invoked to explain certain observed features b
of injection induced seismicity near oil fields (Pennington and Davis, 1985; Davis, 1985: Pennington et al., 1986). Aseismic creep is postulated to occur in regions of relatively higher pore pressure leading to the formation of high stress asperities in locked regions of relatively lower pore pressure. This model has been particularly useful in explaining features associated with fluid injection to enhance petroleum recovery where fluid extraction occurs simultaneously. A direct correlation between fluid injection and the trigger-ing of. earthquakes was first identified by Evans (1966). This relationship was based on empirical evidence of the temporal l correlation between waste injection at the U.S. Army's Rocky Mountain Arsenal near Denver, Colorado and earthquake activity surrounding the site. In controlled experiments at Rangely 011 Field, Colorado (Raleigh at al., 1976), and near Matsushiro. Japan (Ohtake, 1974), investigators confirmed the suspected link
, between deep well injection and seismic activity. Seismic acti-
] l
, . - . - - . - , . - - - - , - - . , . . - - - - - - - - . . ~ . . - - . - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
34
- - vity has been induced by high pressure fluid injection associated %J' with secondary recovery techniques for petroleum production (e.g., Teng et al., 1973; Rogers and Malkiel, 1979; Harding, 1981; Davis, 1985), solution mining of evaporite deposits (Fletcher and Sykes, 1977; Wong et al.. 1985), and with such projects as fluid stimulation for the hot dry rock geothermal system at Fenton Hill, New Mexico (Pearson, 1981; House and McFarland, 1985). The largest reported events associated with deep well injection and petroleum production are M m 5.5 (Denver) and M = 5.0 (Cogdell Oil Field). The only documented cases of induced seismicity associated with solution mining occurred at Dale. NY (Pletcher and Sykes, 1977) and in southeastern Utah (Wong et al., 1985). In both instances the largest earthquakes
(} had magnitudes around 1.0. A magnitude 2.7 earthquake (2/73) near Dale. NY was determined by Fletcher and Sykes (1977) to be of tectonic origin. Many instances of injection induced seis-micity have been investigated. Pertinent details of the better documented cases are presented in Table 9 and are described l below. R'ocky Mountain Arsenal Routine injection of waste fluids at the Rocky Mountain Arsenal well near Denvar, Colorado began on March 8, 1962. Fluids were injected into Precambrian crystalline basement at a depth of 3671 m (-12.044 ft) with a maximum top hole pressure of 72 bars (1050 psi) (Evans, 1966) and average monthly bottom hole I
, pressures ranging to = 415 bars (6020 psi)(Figure 14). Initial
~
--,.--..--.--.s .-,- - - - - - ,- - y.. - - - - - - - , - , , n . - - , -
- . . - . - - - . - -m
~
. 35 f-y s Table 9 DATA PERTINENT TO INJECTION RELATED SEISMICITY. NOTE Injection pressures are cited either as top hole pressure (THP) or bottom hole pressure (BHP). Other pertinent pressure related data (e.g., pore pressures (initial - Po; otherwise Pp). hydrofrac data (al, a2, a3), the reported ratio of bottom hole pressure to lithostatic pressure (BHP /LP), etc) are recorded under Other Pressure History. Hydrological parameters reported for each site include transmis-sivity (T), storativity (S), permeability (k), and coefficient of diffusivity (a). The volume of fluid injected (gross and net) is reported in cubic meters. Distances are given in kilometers and injection rates in liters /
-l min.
Time delays are the time legs between injection phases (increases, decreases, etc) and changes in seismicity patterns. Dimensions of the epicentral area defined by the spatial extent of the earthquakes are given in kilometers. The range of earthquake magnitudes (where applicable) and the maximum magnitude event are described under EQ magnitudes. Fault plane solutions (where available) are described. B-values calculated for the periods of study are given under b-values. References References for each item appear in brackets (e.g., [1)) and refer to the reference list accompanying the table. In those cases described by a single reference this reference is reported with the case heading and i s not repeated. Unit Conversions Units in the table are generally those of the SI system. Conversion factors to English units are listed below. 1 bar a 14.504 psi 1 1/ min u 0.264 gallons / min 1 km = 3280 ft = 0 62 miles 1 m 3 = 264 gallons ( 1 m= 3.28 ft O o m- - - ~ - v ow-- my y,v e ,-,4--,o- -, - - - , - - - - - ,----p,v---w- v-+c,-,w-, # --
(
' ~
.. -j m ?
v
-) (g) ..
j { J
?
5 i a vell eenver (socky Mt. areemell Noteeshire. Japaa [12) Dele, NY [3] lajectlea Nes TNP 72 bare [2] TEP 320 bare ' Freneures men avg meathly SEP = 14-30 bare Well Sit man TNP 42-74 bare 418 bara {T) P 2ae bare f73 Other eve 830 bare l7) 3 separate lajectlene Nigh preneurs Isas et melt egl Pressere Level in mell felt et 0 50 14-23 34-20 bare Calculated Polly (e e.8) NIstery 0.074 t/ min eithin I et 812 a = 133 bare der efter shutdown I?] f42 bare TEPl. NydrelegIcel e=T/S-1.Os a 30 0ce f, 2 g, ,,,,,, , , ,,,,3 , ,,,,8 c,2 j , Properttee T.S free [8] e = 0.5-4s80,g,c,,m /s ha eDercy reage Velene of 3 plaid 8.2 m 10 m [20] 2043 m Pumped e Depth of well 3.878 km l7) 8.8 km 0.43 km ta Os 3/82-9/63 478 1/mtm . Rejecties 10/s3-8/84 0 l/ela [7] 220 to 200-300 t/ ale 2-3 a avg. rate at Denver potes 9/64-4/65 178 1/ ale 4/45-2/64 307 t/olm Oletence from Close to well well to EQs (elcre eg. met) [7] 2-4 km Nest 5 2 km
*fle/73 - 11/73)
Ts e celay 7 wks from etert of Injectsen. s.3-4.s dare 2 km - oO days (esset) getween Injec- 30 days (evg. daring lajecties). 0 2-4 km 2 km e 2 days (lejec. helt) mn & EOs f71 3.5-7.3 km 0.3-1.1 km Depth Estent 4.5-5.8 km {f) of Eos Eplcentral 80 km u 3 km (NGO*w eS.S km a4 km Length a 2.3 km jgg e surroundina wollt 171 elear C-L feelt. EQ Nagm8tudes Nea. S.O. S.23-S.S. S.1 Nas. 2.8 -1.3 sN 5 0.8 f4/47. 8/47. II/471 f71 Fault Plane Strike ally {f) Strike ellp. buried Threat faulting (mas EQ) Solution NS5'N sorellel to C.L. fault b-valuee 0.00-0.90 during lajecties 3.5-2.1 (before, deflag, 1.5-1.S f71 after integtlant ( Besarks ml00 felt EQs (20) Suarse of alcro EQs. Setestetty a 3 event /me prior 1000s toe osall to feel. e2SO events during to Sajection. Smeras after injectlen perled. lajectica lup to 80 evente/ EQ emnet Py 32 bare above Setsmicity lacrossed fel- day). 3/4/73 to 33/31/73 e lattial. 18] lewing injections. 800 evente. EQs lie along sepped fault. N 2.7 EQ (2/73) EQs occurred so seerby believed to be tectente. fault.
'f
~ ~
N 4 v ~ q) well pengely all Field. C0 Sleepy uallow Gil Fjeld. Lee Angelse Seela Oil Fielde Nehreeks fig] Injertion TMP = e3 here I41 Tur Se bara (temalag Group) Pressures Tur 22 pel lueeges 35 Group) (4/82-S/04) (Nestese) [18) Po e 170 here. al.s2.e3 Other SS2 427 384 hero {I3l . Preneure Nos. Pp itse?)e290 here. ulatory Some wolle reopend rapidly to changes in other melle. ayerategical k e I muercy 1831 2.9 Dercles (seegen SS) Properties lueberaSS)3 T ls-30 80 eDercy-ce gleg volume of Through 8/~0 fluid Totales.7 a ge I I m Total e 2. Sale 8 3 Pumped metm2.3 a le e l4.9) Net e -4.9s10 8 a Depth lajectles at 3050-1530 m and of well a 2 he (4] 1850-8870 a [87l 314 1524 m ta Injecties e 37.680 t/ala se of 1964 Rotes (90 melle) ISI castence free Close to welle llal close to well [17.1s] c I -m 3 km Well to EQs Time Delay EQs stepped I day-few see. Fleedlag begem 1984. Between lajec- felleming Injectica Nemiterlag boges 2/73. iloa a EOS d'er'***- f831 Depth Essent 2 km leeer welle) Nest c4 km (Isj 2-Is km of EOs 3-S kne f$w of wellet 1831 (most > S kol Epicentral width =3ke. lengthee km l331 Area EQ Nagettedes $ worse of alcre EQs. Nea. N=2.9 l37) Nea. Ne 3.2 Nos. 4-3.3 f831 f3/79-3/80) ft/71-12/73) Poult Plane Strike ellp 133) Reverse. mermal l37.38] 3451gue ally Solutlea b-values 0.88-0.96 ll3) menerke Suerms. 133] le EQs 83/79-3/80) {l?l 47 EOs 80.9 5 N5 3.2) 30/89-S/74 > 3400 EQs recorded 2/8/73-32/31/73. EQs perellel to espped a 250 evente (4/82-4/84) [38] le all fielde in Seels. surface fault. EQ easet pressure e257 here Background selenicity le high.
=_. , -- - -
'e l j t 1
$h 38
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=.,
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- P m%
= e +
- Me w % We se h MGm Gm a # wm WG m
BMS *M ew w % SS Mw SS Me em a
- I
- 6 mm GS *= De O 99 s S Am 9 e WS+
> SW 99 4 m 39 9 e4 GM A Om m 9 hm WO S Se e s ee dw am S A GW es e a g h %
- e kh a m& & *M m W mW M' e e e km B h > *O e - D e U >M G O V OS E9 QW m
h O. M kW e e T w e e S me e e 9 >S S w am Me e a S e9 %m & > e e am PW Sm > > > hm b 6 e e9 % e > E 6W Um > m%'
= > > e e
- OMM
= e %m *m e see OW e M eb M 9 s tG m b m p ** % MP SW G ww em M h %
= e A = m m SWM GR Sm AOw > m e m me w QE et M s m e e g 9 m Se W 3S M We GE m e -
= m e e A e 3 == = epe a e 3 ee e SMm G e e B e Sa g h e s b N O 9 e N b e G sow e9 9 a
h e em
- S e e b> G= 3 Em m www e
S U e a e e e e e h e M S T e ue WO hG e e m 3 m Se m e we h S M emO m a w e Se a e e e a W M h a m S e e h h h em m a UG, es W w 5 &O e e
- w 3 sh mh e 9 m e Sw See S S W = 3 m us hee Se Sge d e se e e Ac e e ww = h m t e eew h a se& w3 es wm eSa wM ue E m e e e m MS Ate T$ m SS & MW em Swa & m e Sm D G
, 9 5h whe kh em s th 5 m m e m em eh th O ee 4 e 3 mb Ohm 3h Whb Se me S3 kew ee me m he a m 4
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l Well Cathie Welle et and 82 Envireneestal .rsee Serv. te.e e.e.t.. .hi. to e coa.t.. .hi. ii.i .R e f erences
....ct... .... ., . ,,2 h.r. .... ,.,. .. h.r.. >- a i <ia'=>
Presseres (83.21) Aug. daily pressure I*
, ',*** I I ',0 8,d gyge, (i,99}
- 4. CIhhe et al. (1.T3) eydrefrec. Santanteneses Nydrafrac. Smetentassous shut * *# '*E II
.ther la pressures 182 here 18.7.-
shut In pressuree 384 here (8179- .. Ear lag et of. (1 7.) I i Pressere 171. al. 35 here ( I... al I* E'*IF 88 *I* II'88I utatory 33 here (l...-378.I.a), 7-81 47 al. 5 here .. Releh and .redehoeft (5..I) f1 33-1 5. el II4.1SI ***** II *I
'.'. ."ble Department S of Natural .eesucces (I...)
sydrelegscal k = eDercy reage 3. - ' Fe- P8 #c 88 teacy (I. 5) tropertses *'8 (sel 32. .btake 13 74) (l.'s of a.orcy la fractures) 13. .alel.h of sl. (1 1.)
... .....rc.. .....co.
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- ;;I;;**' c. h.. .... .= i- - i i i <>=i
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ta 8
.Injecties 2 5. 24.. er 32. 5/ ale. [13] Aug. I.23 m /meath ates i
.setence
.eii t.
. efees = is h.
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.etween cath 8e 2 e 4 yre. m 3 me.
tien . E.laiec-o Depth Estent Nela check S*. km of E.e Aftersheche 3-. ha 4 Eplcentrol Tight cluster , Area EQ Negattedes Meta check a 5.. Aftershocke II31 - . . t' s N 5 2 S
- yeelt Plane .trike etty Soletion h-walmes a ..S - ...
i
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l I t b i
40 pore pressures at this depth were estimated to be around 269 bars (m 3900 psi) (Healy et al., 1968). Hsieh and Bredehoeft (1981) calculated that a 32 bar (m 460 psi) increase in pore pressure was required to trigger seismicity. Approximately 6.2 x 10 5 ,3 (m 164 million gallons) of fluid were injected at average rates to 478 liters / min (126 gal / min) before the well ceased operation in February, 1966 (van Poollen and Hoover. 1970). Seismicity began approximately seven weeks following the l start of injection and was correlated with injection volume at an average time lag of ten days (Figure 15). High quality hypocen-I ters (January-February, 196,6) were located at depths of 4.5 to l 5.5 km (2.8 - 3.4 miles) within an epicentral area approximately 10 km long by 3 km wide (6.2 x 1.9 miles) surrounding the well and striking N60 W (Figure 16). Focal mechanism solutions indi-cated right lateral strike slip faulting on a northwest oriented plane. Approximately 100 events were felt and thousands too small to be felt were recorded (van Poollen and Hoover, 1970). B-values. a measure of the magnitude distribution of an earthquake sequence, ranged from 0.80 to 0.90 (Healy et al., 1968). The larger the absolute value of a b-value the greater the ratio of small magnitude events to larger ones. The largest events of magnitudes 5.0, 5.3, and 5.1 occurred in 1967 (4/10, 8/9, and 11/26, respectively). An epicentral area similar to that outlined by the events of January-February, 1966 (Figure 16) was defined by the aftershocks of the 8/9/67 event and the 4/10/67 event (Healy et al., 1968).
1 l
\
41 ' 3 2 : . ; . ; . y 4so - l Si.
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so g' f, : 't 2=- g >:
?, %,s
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to
==
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- 370 2
Y
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am _ i , .
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!, l-**' g $ ].
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h 330 - 0,'#e,
- f*
=
U s 320 -) ' ' ' '
- O assa i 4343 i itse i 1945 4 1964 I ses7 I 1945 (From Healy et al.,1968) t Figure 14. Average monthly bottom hole pressures at Rocky Mt.
Arsenal well and comparison with seismicity. O -
42 so' c, eo EARTHQUAKE FREQUENCY a l C 70 - l
$ 60 -
4 50 - l I C 40 O s8 x, CONTAMINATED WASTE INJECTED 7, (n z 7 a:_ 4% [ --
]6 t;If l5 NTyh-d g$-?-l
--gi;t-mw Tws
*4 cm ;
- a. ~'
!G 3 - -y,-g-w#qbDi!%-
TW84N W t
/Gw W 82 w=nsm.AL.W..i:: u. .x-rbC J m 4M46N 3
i4G%swm T;M-No r/ u/D -E "Y, h J
$$ $h?h$$ll5 M M M M
/NJECTED l5 J S N J J S N J M M J S N J V .i J S N A
N A A Y V E P O A A A V E O A A A U E A AlA U E Of
.R L V N R Y L P V N R Y .L IP .
N RI Y L P V! 1962 1963 1964 19G5 l l (From Evans,1966) l l t Figure 15. Correlation between seismic activity and volume of injected fluid at the Rocky Mt. Arsenal well. l l
.. l lO i
1 e
43 N/ l N s
+
.s s .. . .
.p s - -
.s- . s. i 7 .4 R.M. A .
R0CKY M
)
MCUNTAIN ARSENAt. l , l . Earthqueke Epicenter
- 4em Ave.
DENVER ^ Afters of 10 April 1947 earthquehe A O Y Aftwenocas of 9 August 1947 earthquake [ N e p ,,,,, i,, g ,,,, g,, O* I O tnm 4 - 26 Nov.
<l 10 April ,
kM. A. Welt e ROCKY I MOUNTAIN A R S E N J, t.
' L
. sin a,e.
~
- - . OENVER
/ (From Healy et al.,1968)
Figure 16. Epicentral area surrounding the Rocky Mt. Arsenal during January-February 1966.
44 Matsushiro. Japan One of the few experiments in earthquake control occurred at , l Matsushiro, Japan. In 1970, 2883 m 3 (0.78 million gallons) of water were injected at a depth of 1800 m (5905 ft) near the Matsushiro fault zone using top hole pressures of 14 to 50 bars (203 - 725 pal) and rates of 120 to 300 liters / min (32 - 79 gal / min). Permeabilities along the fault were estimated to range from 10 to 100 mDarcles (Ohtake, 1974) During the two month duration of the experiment. several hundred events were triggered within 4 km (2.5 miles) of the well. at depths ranging from approximately 1.5 km to 7.5 km (0.93 , , 4.7 miles). Seismicity increased following injection with a delay of 5 to 9 days at distances of 2 to 4 km (1.2 - 2.5 miles). Activity was significantly greater during the injection than either before or after as seen in the center panel of Figure 17. B-values ranged from 1.9 - 2.1 before, during. and after the injections. The maximum magnitude for the sequence of earthquakes was 2.8. Strike slip focal mechanism solutions were I obtained (Ohtake, 1974). Fenton Hill. New Mexico Several hundred microearthquakes of magnitudes -4 to -2 occurred within 0.4 km (0.25 alles) of a 3050 m (10,000 ft) borehole during the injection of 460.000 liters (121,520 gal) of fluid in a 5.5 hour hydraulic stimulation at the hot dry rock geothermal site. These shear failure events were located up to O' p
--,,w-,---,v --n -
- - - , . , . - - - - , - - - - , . - - q,, , --
- _ ~ . . . _ ._ _
4$ v.
. * * ** .. N
, yy.$
.
- A * *,
g%wN. "* (. ,o'. . ."V su
- v. ** w 1km g
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- user
] . .
7
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.4. .ed .
. . . . , w.n .n.
1-2 3
..e
{gg (b) 12/01/69 - 01/25/70 - 03/10/70 - 01/24/70 03/09/70 03/31/70 (From Ohtake,1974) l i Figure 17. Map view (top) and vertical cross sections (bottom) showing locations of events triggered by deep well injection at Matsushiro, Japan. The hypocenters in the depth sections are projected to the vertical plane through points AB.
. 46
() 30 m (98 ft) away from the expanding hydraulic fracture (Pearson, 1981) (Figure 18).
; House and McFarland (1985) describe the results of another hydraulic fracturing experiment at the Fenton Hill site. Water 3
(7600 m . 2.0 million gallons) injected at a depth of 3400 m (11,150 ft) at a rate of approximately 1.6 m / 3 min (423 gal / min) triggered 850 seismic events iu the vicinity of the well. 4 SEISMICITY CORRELATED WITH PETROLEUM OPERATIONS l The association of seismicity with fluid injection for secon-dary petroleum recovery has been established, but few cases are well documented. Shurbet (1969) alludes to an increase in sels-micity associated with petroleum production and water flooding projects in the Persian Basin near Kermit. Texas. Milne (1970) studied the a 5.1 Snipe Lake. Alberta. Canada, earthquake b of March 8, 1970, and noted the event occurred in an area where prior seismicity had not been reported. Within 80 km (50 miles) of the epicenter were located 646 oil or gas wells. Injection had been employed at 56 wells beginning six years earlier. The net result of which was a reservoir pressure somewhat below the virgin reservoir pressure. In a later raview of induced seismi-city Milne and Berry (1976) described the event as appearing "to be the only known Canadian example of an earthquake probably l induced by water injection into a producing field". Insufficient i- details were given of the seismicity or well locations. pumping history etc. to adequately establish the contention that j 1 l l L 1
- a. +, -
s . .= , . . -- 4 47 k/ T dr
- a. b.
- - , ,oo . ,
m.,
..- -- um une "i . :..-- -
/ .
. \_ . .. -
-si '
q
'If: ""E f'
*p' s
*' ser our O i N.- - .,
\ .* ,k* -
*. f s 'S s . /
\
..q..
/
\ .
,/
x y -
.:g- /
\ / -
/
s nm uma mi ., j .
\ /
s - o.m - . N / m.us s . i s_____' me as. no -. (From Pearson,1981) Figure 18. Microseismic events located near hydraulic fracturing site at Fenton Hill. NM and projected to (a) a hori-
. zontal plane. (b) a vertical plane perpendicular to the hydraulic fracture plane. and (c) a vertical f_
s plane parallel to the hydraulic fracture plane with elapsed times since initiation of injection. e
- - - - - - - ,v --,,v g-e- ---e -
48 this event was injection related. However, several indisputable cases of induced seismicity have been associated with water flooding projects. Rangely O!! Field, Colorado The most famous and best documented case of injection in-duced seismicity related to petroleum production occurred in the Rangely 011 Field. Investigators were able to control the frequency of seismic activity through variations in the reservoir fluid pressure. Secondary water flooding within the Rangely 011 Field began in late 1957 at a depth of approximately 2 km (6700 ft). Through June, 1970, 9.7 x 10 7 3 m (25,690 million gallons) of water were injected at a top hole pressure of approximately 83 bars (= 1200 () psi) representing a net increase of 2.3 x 10 6 ,3 (596 million gallons) (Munson, 1970; Olbbs et al., 1973) after petroleum withdrawal (Figure 19). Water was being injected at an average rate of 17,660 liters / min (4666 gal / min) as of 1964 (Munson, 1970). Pressures in the reservoir had risen above the virgin reservoir pressure of 170 bars (m 2470 psi) by 1962 and were as (
-high as 290 bars (m 4200 psi) by 1967. Hydraulic fracture data obtained at = 2 km (m 6700 ft) yielded stress values of S Haax
(=#g) = 552 bars, a 2 (vertical) = 427 bars, and S hmin I"#3) = 314 bars (s 8000, 6200, 4550 psi, respectively). Using these stres-ses, Raleigh et al. (1976) calculated a critical pore pressure of 257 bars (m 3730 psi) for the triggering of earthquakes. Seismicity was first located at Rangely 011 Field upon O i 9 e - -- , - - - , . . _ . . - , - . , , . _ , . . , - , - , _ , . - , , _ ~
i 49 . O s-l P, j i (3 - f.k 8 k s
-:so p
2
.s '
g 1 . ~ s 9
- -.o g r .
a
- c. -
-n
_o O -- aa t.o f
..u f 9
.u
?
e..
. m t f
- c. =
?
.2,,,
(From Munson,1970) 200 5000 t I L _ 1 i ISO
~ { 'acco g_.
- _-- _____ _____. . _ _____ _____ ________a ;
I b i !:
!. l a
iar _ q soo. g-l ! i i L ! - E L q $
~
E
"[ ,- l P i . ~1 '"' 3 il_u -
i
- u w D . d i~- f ., l
* . . . . . . . . . . . . c... . :w. . . . . ... . ..i l... ......:
i n,. iero i ieri i.,. i
.: .r.; ,;.
.: wo.,.:.2.,, %,I=i,,,
no.a rio,e - rio,a I
.. u i. .. -. ! .in a ....!. ,,,.o... 'v (From Raleigh et al.,1976)
Figure 19. Seismicity correlated with injection volume and pressures at Rangely 011 Field, CO. Stippled bars in the bottom figure indicate events located within 1 km of the injection wells. - -
50
~
installation of the Uinta Basin Observatory in 1962. Instrumen- j tal records were not available prior to this time (Raleigh et al., 1976). Between October, 1969, and November, 1970, over 900 earthquakes were accurately located within the Rangely field, 367 l of which occurred within 1 km (0.6 miles) of the bottom of the injection wells. Seismicity appeared to be correlated with in-jection volume and pressures. The earthquakes tended to occur as swarms, sometimes followed by main shock - aftershock sequences' (Figure 19). Hypocenters clustered in two groups, one located at
-depths of 2 to 2.5 km (1.2 -
1.6 miles) (near the wells and I within the injection zone) and the second group clustered at depths between 3 and 5 km (1.9 - 3.7 miles). Seismicity was concentrated along a vertical zone approximately I km wide by 4 O km long (0.6 x 2.5 miles), and parallel to a mapped fault (Figure 20). Focal mechanism solutions indicated predominantly right lateral strike slip faulting on northeast trending planes plunging 10* - 20* to the southwest. B-values ranged from 0.81 to 0.96 during the study period. The maximum magnitude recorded at Rangely 011 Field was 3.1 (Raleigh et al., 1976). Sleepy Hollow 011 Field. Nebraska Water injection at bottom hole pressures to approximately 172 bars (m 2495 psi) within the Lansing Group (1050 to 1170 m)- (3440 - 3840 ft) and 142 bars (2055 psi) with the Sleepy Hollow sandstone (1150 - 1170 m) (3770 - 3840 ft) resulted in the trig-gering of earthquakes within the Sleepy Hollow 011 Field. The O . a
* - _ + - - ---*_ v - -n- or--wa --we i---- -9, r---y--,w-- -ws w---- y- r -,
,_ _ -- .w- . -
51
,\
As 40 72 40 F f.' '.40 7.2 40 72 *j 40 7 2
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- : : 2 a!
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*3 Oct 1969 Oct 1970
*:3.
[. N0v 1970 . Jul 1971*3, i.* Aug 1971. Oct 1971*.
-4018 4030 t 40 38 40301 de 3 0 4033"*
4~ 4e 7 2 4072 ' l,,40 7 2 40 7.2 40 7.2
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. N0v 1971 Aug 1972 . '. Sep 1972 . May 1973 .; L Jun 1973 May1974.l 40 s e 40 3 s : 40 s e 40 a e f 40 3 e 40 e I
/ \' X (km) X (km) X (km) 0 l 2 3 4 0 1 2 3 4 0 1 3 3 4 injec t:0ns inject:0n injection wells wells h l' wells
' ~ ~~~'""" ~ ~ " " ~
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,. Oct 1969 . Oct 1970 . N0v 1970 Jul 1971 . Aug 1971 Oct 1971 e
injection , injection ' Inject:0n wells wells wells
- n l
- f. .. . . .. . .. . , psa.;.+... gg..........
N Y' s.~'.rign'0e. g .o~. 9.... ,w.4,.z.. 4 * *
,, N0v 1971 Aug 1972 , Sep 1972 . Ma y 1973 , Jun 1973 Mey 1974 (From Raleigh et al., .1976)
O. Ij s Figure 20. Rangely seismicity as a function of time. (a) Bottom hole pressure contours are in bars. (b) Vertical sections trend N-S.
.-Q,
52 . earthquakes were located near the well and most were shallower than 2 km (1.2 miles). Sixteen events were located between March, 1979, and March, 1980. The maximum magnitude recorded was 2.9 (Rothe and Lui, 1983). An additional 250 events were recceded within the active field between April, 1982, and June, 1984 (Steeples, 1985) (Figure 21 and 22) at a time when top hole pressures ranged to mS6 bars (810 psi). Los Angeles Basin. California Fourteen oil fields operate within the Los Angeles Basin where water flooding began in 1954. Total fluid injection as of 1970 was 2.5 x 108 ,3 (67,300 million garlons) with a net injec-tion of -6.9 x 10 6 ,3 (-1810 million gallons) at depths of approximately 910 to 1520 m (2990 - 4990 ft). Earthquakes with depths ranging to 16 km (9.9 alles) with the majority deeper than 5 km (3.1 alles) were located predomi-nantly along the Newport-Inglewood fault. Activity appears to be correlated with injection volume from nearby wells (Figure 23). Approximately 50 events with magnitudes (M ) ranging to 3.2 occurred in the basin between February 6, 1971, and December 31, 1971. A single event focal mechanism solution indicated predomi- l nantly oblique slip motion (Teng et al., 1973). Cordell Oil Field. Texas Water flooding between 1952 and 1982 resulted in yearly net injections between -1.6 x 10 6 ,3 and 4.0 x 106 ,3 (-420 to 1050 million gallons) with top-hole pressures to approximately 220 t O
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n LF T h -in A N J J A 5 0 tt 0lJ F N A N J J A 5 0 N 0lJ F M A N J 1982 1983 19e4 (From Steeples,1985) i l l I' l l l l_ Figure 21. Average monthly seismicity and pressures for the f Lansing Group and Reagan sandstone within the Sleepy i Hollow 011 Field, NE. r 1D 1
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=
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0 i e i l l JA N FEB .YAR AFRIL MAY JU.NE JULY AUG SEPT OCT NOV OEC q a e a < u s s , , , ,
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- Figure 23. Correlation of seismic activity with net fluid 1
l injection at the Inglewood Oil Field, CA.
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56 r", . bars (3190 psi). Injection has taken place at depths of approxi-mately 2071 m (6796 ft) (Harding et al.. 1978; Davis, 1985). Over 50 earthquakes have been attributed to the Cogdell field since 1977 (Figure 24). Accurate locations for the period (May, 1979 - March, 1980) indicate seismicity was shallow (0.1 - 6.5 km) (.0.6 - 4.0 miles) with 90% of the events at depths less than 3 km (1.9 miles) (Davis, 1985). The maximum magnitude event attributed to Cogdell was a b 4.7 (Harding, 1981) (Mg=4.75 - 5.0 (Harding et'al., 1978). Permian Basin. Texas Seismicity has been associated with several fields in the Central Basin Platform of the Permian Basin. Texas (Figure 25) where water flooding continues with top hole pressures in excess of 138 bars (2000 psi). Over 400 earthquakes with magnitudes ranging from -0.3 to 3.9, many occurring in swarms, were cata-logued by Rogers and Malkiel (1979) for the period December, 1975, through July, 1 9 7 ,7 . Depths generally ranged from 0 to approximately 5 km (3.1 miles), but few locations were of a j quality better than C. B-values calculated for the period were 1.04 - 1.28. Focal mechanism solutions obtained from Keystone field data indicated predominantly normal faulting (Orr and Keller, 1981; Rogers and Malkiel. 1979). SOLUTION MINING OF EVAPORITE DEPOSITS Dunrud and Nevins (1981) cataloged 107 producing and aban-
, doned solution mining projects in the United States. Documented D
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0 -10 l 52 54 56 58 60 62 64 66 68 70 72 74 76 78 80 82 ' YEAR (From Davis,1985) I Figure 24. Comparison of seismicity at Cogdell Oil Field with the net volume of injected fluids and the ratio of the bottom hole pressure (BHP) to the lithostatic pressure (LP). O
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l ,,, nor g [] ir d$ ,,, (From Ro9ers and Malklel,1979) Figure 25. Locations of earthquakes associated with oil ( production within the Central Basin Platform of the
/'N Permian Basin. Texas.
b .
n l l l 59 histories of induced seismicity surrounding these projects are O-,- rare. In one of the few documented cases of seismicity corre-lated with solution mining Wong et al. (1985) reported shallow (<2 km, 1.2 miles) seismicity (M ' generally < 1) at a potash mine in southeastern Utah. Solution mining has taken place in New York and Ohio since the late 1800's. Both these states have experienced low level seismicity in historical time. Accurate correlation of seis-micity with solution mining in such areas is not possible without accurate earthquake locations and injection histories. Informa-tion of a sufficient quality is not generally available. In a detailed study Fletcher and Sykes (1977) were able to correlate seismic activity with mining at a site in western New York. Attica - Dale. Western New York Salt mining with top hole pressures to 120 bars (1740 psi) and injection rates two to three times those utilized at the Rocky Mountain Arsenal has been spatially and temporally l associated with microseismic activity in the Attica - Dale area i of western New York. Six injection wells were employed with
- l. depths of approximately 430 m (1410 ft). The well operating at the time of the study conducted by Fletcher and Sykes (1977) was l
located approximately 50 m (164 ft) from the trace of the l Clarendon - Linden fault. Seismicity occurred in swarms with up to 80 events per day. l More than 800 microcarthquakes (magnitudes ranging from -1.1 to o 0.8) were located close to the operating wells between August 4 l e I I I
60 ( and November 11, 1971 (Figurd 26). B-values ranged from 1.1 - 1.5. The largest event of the sequence occurred 0.6 km below the bottom of the injection well. The low level of background activity (less than one event per month) prior to high pressure injection. the dramatic increase in activity following injection, the spa-tial association of seismicity with the injection, and the rapid cessation of activity upon decrease in injection pressure below 52 - 55 bars (750 - 800 psi) strongly suggest this activity was injection induced. i An earthquake of magnitude 2.7 which occurred about 7 km l west of brine field in 1973 was determined to be unrelated to the. injection by Fletcher and Sykes (1977). A predominantly thrust faulting focal mechanism solution was obtained indicating motion along a plane parallel to the Clarendon - Linden fault. SUNNARY Summarizing, seismic activity has been triggered by a variety of fluid injection projects (Table 9). The correlation between earthquakes and injection can only be established through the spatial and temporal association of accurately located events with known injection histories. Of the cases for which adequate information exists, several similarities are apparent. Earth-quakes are generally located near the injection well and often along nearby faults. Swarms with large numbers of low magnitude events are common. A'ccordingly, b-values are around 1.0 and sometimes greater than 1.0, often higher than those obtained for (~) - i _p , _ _ _ - _ _ . _ - . . . , _ .__ _ _ _ . , _ _ _ _ . . . _ _ . _ _ _ _ . , .
e1 O' o P#*"r=*==c Y Oct 5-H on : a g *o or nwcu. s a - w 3 ,,,, : g l3o _ ,, m
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- O IS 20 25 30 3 0 0 20 23 30 4 NQV IS71 DEC, JAN tS72 l
(From Fletcher and Sykes,1977) Figure 26. Seismicity correlated with injection pressures during solution mining near Dale. NY. ( O O
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l-62 tectonic sequences in the region (as noted by Gupta and Rastogi, 1976) for tectonic and induced sequences in India. Documented cases of injection induced seismicity exist, but in many in-stances insufficient information is available to establish a valid correlation, particularly in tectonically active regions. The injection at the Calhio Chemicals site is siellar to sites where seismicity has been correlated with injections in several ways. The volume of fluids injected is within the range reported at other sites as are the observed formation permeabili-ties (mDarcy range). Injection pressures are greater than at many other sites and injection rates are comparable. Considering the distance involved, the time delay between injection and the Leroy earthquakes is theoretically possible. However, in comparing the seismicity observed at Leroy with activity associated with injection several important differences are noteable. The distance between the injection point and the initial hypocenters is much greater than reported in any other instance. The time delay between the start of injection and the onset of seismicity, though plausible, is much longer than in any other case. The activity at Leroy was tightly clustered in both i l time and space. Injection induced seismicity is characteristi-cally more diffuse temporally and spatially with many more small i magnitude events than occurred at Leroy. Accordingly, the b-value obtained for the Leroy sequence (= 0.5 - 0.8) is much lower than values characteristic of induced seismicity. Though t' the physical parameters related to the Calhio injections are O - I
h 63
.-s similar to those in cases of injection related seismicity, the seismicity patterns observed at Leroy are quite different from
, such activity.
- 6. REGIONAL TECTONIC EARTHQUAEES Several earthquakes with magnitudes greater than 4.0 have occurred in the eastern United States and adjacent Canadian provinces since the mid 1960's. These earthquake sequences of tectonic origin (Figure 27) (Table 10) are quite similar in several respects.
Such earthquakes are temporally and spatially diffuse. How-I ever, the historical record often contains reference to similar events. Hypocenters calculated for the.se events are generally deeper than 5 km. Associated aftershocks are usually few in number and often tightly clustered. Only in three instances were more than 25 aftershocks recorded. Accordingly, b-values asso-clated with these sequences are predominantly less than or equal to 1.0. These characteristics contrast sharply with the similar-ities observed in instances of injection induced seismicity pre-viously described, particularly in the small numbers of observed shocks with relatively greater numbers of larger magnitude events. Temporal and spatial patterns of seismicity associated with the Leroy, Ohio sequence are quite similar to other tectonic sequences. Only 13 tightly clustered aftershocks were recorded (through 4/15/86) with an epicentral area of al km 2 (m0.4 miles 2) and a depth range of 3 to 6 km (m 1.9 - 3.7 miles) (main shock = l
- , -- - . - . . . - ,,---v. -e
9 - % o o o . 1 Cunningham, V A 2 Dixfield, ME 15 g
- 3 La ncaster, P A - 5 13
4 Caza, NH 12 5 Bath, ME , , ,2 , ! 6 Mir amic hi, N.B. ' e 5 7 Goodnow, NY e'I 7 4 8 Sharpsburg, KY
# 14 c
! t
'II 9 St. Dona t, Quebec ,)
10 North Gower, Ontario E 3 Leroy. ON * + 40*N 11 Ardsley, NY l 70ew ,
- 12. Quebec-ME border 16 h 13 Maniwa ki, Quebec 9 e e 14 Attica, NY 15 St-Fidele, Quebec ,,
16 5. C entral lilinois ; I# 17 Laf ayette, G A M A GNITUD E l 18 Knoxville, TN _.j ' i e 4.0 - 4.4.
> e 4.5 - 4.9' :
[L l , 9 5.0 - 5.4-P G 5.5 - 8.s
+ 30* N t
; 89* W ;
I Figure 27. Locations of eastern U.S. tectonic earthquakes with M2 4.0 which has occurred since the mid 1960's. ;
m m. V)- -
) - - -
f) u Table 10. DATA PERTINENT TO RECENT EASTERN U.~S. EARTHQUAKE SEQUENCES OF TECTONIC ORIGIN EQ Attica. Ny Date 1/8/06 EQ Attice. My Date 9/12/af EQ 5. Central Illisele Date 13/0/80 Lec. 42.s*N TS.2*N 0.7. 13:24 Lee. 42.9* 18.2* 0.7. 19:00 Esc. 37.98+N 84.40*N 0.T. 17:03 Nageltedels) e bed.8 l35] NNI, VI Negalludele) a b*4*4 WI Magallude(s) a b=5.5 t3St NN!* NNI, Vil [33) Focal It be (13] Depth 2-3 km [IS) 2-3 he lle] 22 km [37) fRevlelah wavest fRg M g u itegl 28 km f341 Faultleg Beverse a rt. lateral en NME poweree a rt. lateret sa NNE Neverse (P-este EN) piene (P-eele ENE) piene lP-este ENE) -{34] strike tit strike dit strike dit let model 120* S0*S 320* S0*S Nel*N 47'E tiel glel 2nd essel: 02o* 10*a 030+ 10*E MI5*a es*N Rapture teerth Equivalent Redlue Setemic Moment 2.3 a 10 22 dyme-de 188) 1.5 a 10 22 dyme-ce 1881 9.7 a 19 33 g,,,,,, g39g u, 1.3 s 10 22 dyne-ce (35] a.0 m 19 33 dyse-ce l3Sl Strees Drop Felt Area I.484.000 ka t fl31 Foresheese Aftershocke Depth Reage Number Deretten D-walues 3.0 (20) 1.0 (20j Mas. Misterle Vill 18929) vill 18929) Earthquake . Geelegy Several km of gently dipplag Severet he of gently dipplag Silurlan and Deventen med!- 388mtlen and Devealen medleen-seatery rocke evertle Gren- tery rocke everlie Grenville wille basement. beoement.
~~ - .=mems h
.[
4 e I F.9 Quebec-Neine Aerder Date S/95/73 gg geesellte. TN l43 pote 11/30/73 gg Nealuekt. Quebec Date 7/12/75 Loc. 45.40*N TI.02*w 0.T. 01:09 Lec. 35.80* N 03.9e* w 0.7. 07:48 Lec. 48.48*N 18.28*W 0.7. nacaltedelel a g=e.e. 5.0 NNI, V. VI negaltedelel a,L,=4.s NNI, vt Negnitude(s) a b 4.2 MMB, IV , 139.s71 Focal liepth a km tearface neve) [171 3 km 17 4 2 km (Reyleigh waves and aftershocket f201 Faultlag normel a strike elly (39) Dip elly Reveree/ threat Reverse & atrike ellp lit] (probably reverse) (P-este SSW) Reverse tell strike gig. Lirjk3, (jjt ist medal: N64*W GS* SW (20]
. 2nd medal N34*W - N120*W 28-40*N ,
Rupture IStS km (free eftershocke) Area = 0.8 he I Lt3gth ffrom eftershocket f201 Equivalent me km ifree eftershocks) End [u e Ave. dislocation - e em f201 Setemic Noment 8.2 a 10 22 dyme-ce 1.7 a 10 22 dyme-ca (Repleigh moves) C 1871 (201 Stress Drop al her Se bare felt Generally felt to 100 km Area 250.000 km 2 fell es.000 km 2 (Nea. 350 km SWA f201 Foreshocke None > N 3.5 I (a Nome (3 day before obeckt bL3 = 3.4) f201 . Aftershocke Nes. M =1.5 l391 Nypocentere clustered. Clustered la volume with I km 0 112 km. 5 2.5 km. dieseter. 1024 km -2 4 Ng<!
-0.esN g st.s (2el Depth Reage al-15 km Number 4 [4ll >30 (30 days) 14 (let et bre.)
Deretten No aftershocke free 4-8 days fellewlar sala shock. b-values 3.04 (grRl/AAI Selselc Source tenel f241 noe. Mistoric N= S.0 {24] Earthque,ke vil Geology Appelechless. Ng treading Valley and Ridge prowlace. Precambrien. Grenville Prowlace. belte of volceale med Nerlas cleotice and carbon- 1.1 b.y. eld erogeale belt. eedleestery roche (Deventen etes. Ceeples foldlag and and Ordivicles). [391 reverse faulting. i l l l l
'* . ~- .
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, EQ St.Demet. Quebec Date 2/18/78 EQ Seth. NE Date 4/18/79 EQ St Fidele. Quebec Date S/39/19 Lee. 4a.32 74.13 0.T. 14:48 Lee. 43.9e*N et.a0*N 0.T. 02:34 Lec. 47.st*N e9.90*w 0.T. 22:49 Negeltedels) a bLg***I ""I s v "*8"I'"d'I*I "htg**** ""I o V [23) NegmItudels) s NNI, V hLa*S.O recal 1 a i km (3 8 8 km Pa + Sa) 30 e 2 km (preferred-after-Depth (8-10 km eP + pP) (IS) 4 km {G) 8.7 km tS] shochel (IS] e-Il km leurrece unveel Faulting Reverse (P-este WSW) Reverse (P-este EN) Reveree/ thrust (IS] etrike UE etrike dA ddk UE let sedal N20*W 40*NE N-S 45'E 048* TS*SE (preferred) (ISI [23] (Rake *381*) 2nd nedels N20*w 30*SW N-S 45*u tal* 43* feeke=200*1 Rupture Length m3 km (malm + eftersbecks) aftershock stes=2.3-4.7 km IISI Equivalent Avg. dielecetten*lt ce gadius flSI Seismic Nomente.0 m le tt dyme-ce [19] 8.3-8.7 a 0.1 s 10 23 gj dyme-ce Strees Orop mSO bero (IS] s Felt e Felt ISO km from epicenter 2 Area 70.000 km l19) SS.000 ka t f231 f1SI Foreshacke AftersheChe Nes, a bLg*3.4 Nes. N*3.0 0.4 N g g-3.0 abLg Aftershocke de met {l0] [8] correlate alth model pienes or lie along ' a slagte plane. [15] Depth Range 7 km . 3-7 km 9.8 eI km Number 2 39 (ultble 90 days) Il Deretten 3 days e days b-values 1.04 (EPRl/RAI Salsalc .44 (New England) {$) 0.72 (klaterical + Source tonel f241 feetrumental E0s1 f31 Mas, uleteric N
- 5.0 {24] S.S e, 12/30/3s40 Earthquake OseTypee. NN u=7 (1925) [3sl Geelegy Reglen ulth many St. Laurence Rift (ege uncertela).
j- Precambrien. Grenville Paleesolc faults. Logan's Line (interred outure) Province. 1.5 b.y. eld separatee Precambrisa platfors l oregealc belt. (NW) free Paleeselc mappe structures (SE). Charlevels meteertte Impact crater. e
.a
O ty u - - a
)
EQ Sharpsburg. EV Date 7/27/e0 Lec. se.it N es.st*w 0.7. 18:52 30 Mirealcht. N. BrumeWick Date 1/e/e2 EQ Nirealcht. N. Brunswick Date I/II/e2 Lec. 47.00*u es.e*w 0.T. 12:33 Lec. 47.00 es.e 0.T. 23:41 nacattadels) e,-s.2 mul, u.saltedete) e,=e.7 Nul, y-vl Negattedetal e,=e.4 Nul, surest recal e km (NEls) lapth IS km {28] 72 3 km [40) 7 km {40) Faul:Ing 12 km (301 p-aale Ew fattershocks. surface neveel Reverse Reverse marske_ (12. etrike 112. strike 112. Ist medal N30*E 50*$E (preferred) leS* 50*w (fault plane) 332* 48'E (fault plaae) (rt. lateral e...) tiel (make = 120*) (seke = se*3 [40] 2nd nedet: Ne0*w vertical 332* 4e*E [40] Nepture Length = a km Length = 4.5 - e.5 km f.emeth Width = 4 km Midth = 4 km (40] Aftershock aree=30-50 he t Area = 18-28 ke I Equivalent 25-37 ca endlue Dislocation.2.0-3.4 en feve. dislocationi feel 5eleair Noment 4.1 a 10 23 dyne-ca 2.2 a 0.7 a 10 24 ,,,,,,, 00 Stress Drop 2.e-a bare [40] 35-70 bare Felt Area 470.000 ka t [23] 000.000 km 2 fl21 3e2.000 km 2 gggy Foresherke Aftershocke Nos. a bLg=2.2 Leag and comptes sequence. See Miraatcht. New 4 ovente N 2 4.8 Mas, o b= S.4 reasulck (1/e/st) This le the largest (18] b-value = 0.e [40] aftershock of the sequence. Depth Range 1-14 km (seet alt km) Number c 70 a00 eeente N 2 1.0 Duratten el me. (through e/30/et) b-valuee 0.es l20) 1.07 (reglemel) (24) 0.04 fNew Emelandt fel Nas. Nietoric This EQ (7/27/e0). This EQ (1/s/e2). Earthquake Geelegy Nypocenter in precambrian Appalachten erogenic belt. basement meer er within Deventen Plutone , sene of Grenville Front and in the test Continent Reglemal stress - Ew compreselen.
' Gravity Nigh and old rif t zone.
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v - e t
\m,/f EQ Oeza, NN Date 1/10/82 EQ Disfleld. NE Date S/29/03 EQ Osednew. NY Date 10/7/03 Lee. 43.es*N TI.So*u 0.7. 00:34 Lec. 44.50*N TO.el w 0.7. 05:43 Lec. 44.03 74.33 0.7. leale e,=e.a um3, v.l2?l Negaltede(s) e, = 4.4 V magnitadate) o ggg=S.2 unt, v1 i Narnitudelel MMS, Focal 7 -8. S. k m (aftershocks)
Depth 3-15 km (2.4.22) 3.8 e 3.4 [10] 82 km (local network) {38] Faulting Strike-ellP Reverse Faultles (P-este gu) Reverse (P-eels g-ul strike (1L 8tFlk' dlL elrike [OL 174* e0*w (preferred) TS N let nedsli 2o0* 333 44*E (Rake = -33*) [103 l30.33) 2nd medal 020* so E 195* 40*W 384* 38*S 19 eke = -343 1 1221 Rupture m2 ku long eftershock zone lS) Length m2 he ggelvelent 0.5-1.2 km (displacement =70-ISO cm) Redlue 1371 22 dyne-cm IO dyne-ce (bedy moveel Setemic Noment 3 a 10 0.5-1.3 g,10 hh (eceler No) [22) 2.S a 30 dyme-ca (surface moveel Strese Orop 210-700 bare l37) Felt Area 143.000 km 2 [27] Small 1101 m300.000 he t g3,y Foreshocke Nome AftersheChe -3.7 4 N ( 2.8 Nes. NC = 1.8 Largest 0 2.7-4.7 km depth Smelt enee 1-2 km from rupture eres and shellever. (S] Depth Range 0.3 - 9.7 km one 8 2.4 2 0.5 km (10] S.5-T.S km . Number 14 (3 week ourvey) 7 (23 days) al0S (S oks.) Duratica b-valuee 0.84 (New Englead) (9) 0.34 (New Englandl [9] 8.35 (let SS days) [3tl 0.92 (Adirondocke-EPRil 1291 a men. Historic S.S a 12/20/1940 Gesippee. NN b bLg = S.S (Messene. NY. S/5/1944) Earthquake S.4 N 32/24/1940 Oselppee. MM S.S e b Oselppee. NN lIll Illt 82/20/3,9,4,0y Geelegy Paleozoic Appelechten erogeny - Grenville basement esposed at geologically comptes Merrimack surface. Nemy fractures, meet Synclinertue. NE of epicenter le striking NE. Reglemal fault plane Winnipeseekee Pluten (Devonian selettees strike N er NW. Two emplacement). No mejor faulta la seleeft belte la Adirondacks esse-lamediate epicentral eree. lSl clated with Grenville featu.es. [32) e
3 -- N
.- 'm i '/
-}~ \.
I to North Gener. Osterte Date le/il/s3 sq Lancaster. PA sete 4/23/e4 gg commenthem. VA Sete 9/37/04 Lec. 45.10*N TS.fS*W 0.7. '44:30 Lec. 39.92*N 78.30*w 0.T. 20:38 Lee. 37.et*N .14.32*W O.7. 18:05 Negnitude(s) s hLs*8'I - ""I e Y u"8"tt*d*(*i "bLg"8'I ""I s V* WI (28) Negeltedels) N, = 4.9 NNI, V recal 32 km (aftershocks) Depth {38) 4.5 km (artershocks) [29] 8.2 e 3.7 km [7] Paultlag Thrust (Penale=IS4*), Reverse a rt, lat. en east .P sale SSE dipping piene (P-eele ENE) . {T) i strike dist strike. djit strike flat
; let nedal: STS- TS* 080* - et's (preferred) N25*w Ss*Ne i (seme-se ) 12el (meke-le* lett-let. ....;
2nd selet: 228 It* (preferred) lle* se*su sSe*w to Nw fpeke=41*l f381 fpeke.tes* rieht-reversel
. , Nepture Seel! [38). 3 he (esp view - NNE treed)
Length 4-5 km depth (29] . ! Equivalent Oleplacement=0.S re pedias f341 8I dyne-ce Selsele Nesent 2a 19 ile.3s1 %J Stress prep to here (static) o
. Felt t Area 80.000 ka t f381 m99.000 km 2 f2st 30.000 ka g9y I (4/19/84)
Foreshocks a bLg=3.0 ,[23.29) Nome iTI Aftershocks Nee. a bLg et, le well-recorded some [7] i fl.2sj l [38) . ! Depth Reage 4-8 ke l Number 3 (withlm I week) ble (le day servey) { Derettee b-walues 1.04 (reglemel) (24) 0.98 (reglemal) [24] 8.93 (Central VA Selsele
- Zees-RPRIl 1241 l Nes. Elsteric N = S.0 [24) Thle 84 (4/23/04)
Earthquake Nest largest N=4.3 (1889) VI 18/02 1882 fll VI 12/2s Isas (si Geelegy Grenellte Precambrien la Appelschiene ulth Neesselc Otteme-Seesechere Graben, pull-spert beelse. Overprintlog Age unkmemm (Peet- elong sees structural ljaa. Nottic i' ord!vician). Line (lemer Peteeselc outure) l trende EW. Jureselt dikes at a high eagle to Nottic Llas med Gettysburg Beale. l l
- g }
r -- . - g j - - ---. 7"3_ l W g Q:j EQ Lafayette. CA Dale 10/9/85 Ardeley. My Date 80/IS/85 EQ Lorey. OE Lec. 34.7C*N SS.28*W O.T. EQ Date 1/33/se 13:$4 Lec. 40.se*N 73.03*W 0.T. 10:07 Lec. 48.88* N 88.30' W O.7. 38:48 magnitudete) N 4.s n48, SW (33 Nagastudefel Ng 4.0 NNI, W Negnitude(s) a "8*8 b ""Io 'I Fecel Depth 3 km (leces met . eftersheChe) II.S (2s) {2ej 5-8 km routtseg strske este se us er tw trendsne strike-else tr-emie umal strske elle pleae. [2e] Ist model etrike ola. 11rthe (13. NNW steep (preferred) NNg-S$N eteep (left jeteret e.e.) and medal WNW-ESE l2a) eteep Rupture Length I km {28) Aftershoca area et km 2 squivalent Redlus L Seismic Noment Stress Drop N
>=
Felt Area 2 10.000 km 1331 m 940 km2 (Int. VI Foreshocks I (8 min. before mela) [28l 4ftershocke Nes. N=2.0 Naz. Ng=3.2 (30/23/s5) Tight cluster 8N > 0.5 -0.1 4 Aft $rebecke have euhotential N* < 2.5 l28) component of reverse metten. Ital Depth Reage 4.e-3.s km 3-6 km Neober Seeeral (30/9-20/20/84) 24 13 (thre 4/85/84) Derettaa b-values 0.98 treglemal) [24) m 0.5 - 0.8 Nea. Masterle Ne 5.0 (NY City. 8/11/30048 i Earthquake V (3/0/1943) , GeologF Tecenten h8thly deformed j , (ductile) and metenerphosed See report by Nesten .
- rocks (Membatten Prong). Geophysical.
Ceneree's Line (CL) (releesbic auture) ne.r epicenters but l faulting to at high eagle t o 0 8. . 1 4 i
72 L References 1
- 1. Armbruster and Seeber (1986)
- 3. Serstew et 48. (1988)
- 3. - Seehan 38 et. (1983) s 4. Be!!!agJr et at. (1978)
- 5. Brosa sad Ebel (1905)
- 8. Chiburle and Ahner (1980)
- 7. 06steen et at. (1984)
- 8. she! (1983)
- 9. thel (1984)
- 10. She! and McCaffrey (1984)
- 11. Ebel and Melver (1985)
- 13. EPRI (1988)
- 13. Garden et al. (1970)
- 14. Neeegeus (1983)
- 15. Resegese and Sata 111er (1980)
I it. Herreena (1974)
- 17. Norreena (1979)
- 18. Herreena et at. (1983)
- 19. Normer'et*st. (1979)
. 30. Nerner et at. (1978)
- 31. Neuk et al. (1983)
-33. Pull! et al. (1983)
- 33. Pu!!! et al. (1980)
- 34. Readent Aseectates (1985)
- 25. Scheraberger and Eeme!! (1984)
O_,/ - s St. Schechter et al. (1985)
- 37. Schneelager-Mitter et al. (1983)
- 38. Seeber et at. (1980s)
- 39. Seeber et al. (1984e)
- 30. Seeber et al. (1984b)
- 31. Seeber et at. (1988b)
- 33. Seeber et 48. (1984c)
- 33. Shand end' Leet (1985) 4 34. Stauder and Nutt!! (1970) i SS. Street (1974)
- 30. Street and Turcotte (1977) 37, Saares et al. (1984)
- 30. Watetres (1985)
? 39. tefailler
**s \*sailler(1975) et at., (1984)
[ 44, Y 1g and Aggeruel (1981)
- i. l F
(< - _
- t. l I'
73' (f 5 - 6 km) (3.1 - 3.7 alles). The b-value obtained for this sequence was approximately 0.6. Several significant earthquakes are recorded in the historical record for northeastern Ohio. The largest earthquake noted within 80 km (50 miles) of the epicen-tral area was a M = 4.7 event on March 9, 1943. There appear to be no significant differences between characteristics of the Leroy earthquake sequence and other. tectonic sequences studied in the eastern United States.
- 7. DISCUSSION AND CONCLUSIONS In the various sections above we have presented data from which we can assess the validity of the suggestion that the Leroy earthquake of January 31, 1986 was associated with the injection of fluids in the two deep wells. The various arguments for and against the association are taken in turn.
Factors favoring the Lerov earthquake being induced-by fluid injection
- a. Large volumes of fluids have been injected in the two deep wells. These volumes and the pumping rates are comparable with other wells where seismicity is known to have been asso-ciated with fluid injection (Table 9).
- b. The range of permeabilities in the rocks (alllidarcies) is comparable with other wells which have been associated with induced seismicity (Table 9).
- c. With these permeabilities. the time lags between'injec-tion of fluids and the onset of seismicity are consistent with
,7 -
1 l 74 ( available models. I
- d. There exists the possibility that small microcarthquakes l (with magnitudes less than 2.0) could have remained undetected.
I Factors against the Lerov earthauakes being induced by fluid injection
- a. There were very few earthquakes (< 15) compared to known ,
cases of induced earthquakes (100s to 1000s) (Figure 27).
- b. The Leroy earthquakes were associated with low b-values I
(0.5-0.8) (i.e. the relative ratio of the number of small earth-quakes to larger earthquakes), whereas for induced earthquakes the b-values are usually in the 0.8-1.1 range. l
- c. The Leroy sequence was relatively short compared to those near injection wells which can last for several months or years.
- d. There was an absence of intense seismicity in the vici-nity of the Calhio wells. A large number of earthquakes often persisting over long periods of time is a characteristic feature
, of documented cases of induced earthquakes.
I
- e. There was a lack of any known felt (magnitude 2 2.0) earthquakes in the corridor between the wells and the epicentral area of the Leroy earthquake. Although this does not preclude undetected microseismicity with lower magnitudes, it would be
.. highly unlikely to have a large number of very small earthquakes f and no felt event. . l O . l l i
75 INDUCED EARTHQUAKE SEQUENCES (2132) e l (1314) 2 In
' 1500 = a
/
7
/
/ . (DAYS) i E / /
1000 = I E / i Q
/ (596) l (821)
S [ j o (328)
& E 500 - m z e e h . (395) (90) lE $ (1155) g
/ / / -
e : / *
/ -
/ j5 d / / / d / 1 /
1.5 - 1.0 -0.5 1.0 0 0 0 (2-3) APPROXIMATE MAGNITUDE THRESHOLD Figure 27. A comparison of the number of events in documented cases of well injection induced seismicity with the Leroy sequence. Note the differences in the recording periocBin parentheses, and the detection threshold. 4
--- - - - - - - - - - - - - _ _ ~ - - - _. . - - - - ,,w-e - - - , ,, - , , - * -.-,n.- . - - , . . - - , - , ,, ,a, -,-- - - - - ,,
76 Pactors favorine Lerov earthauake being a tectonic event
,O a. By tectonic event we mean a " natural' earthquake that occurs in response to plate tectonic stresses - as opposed to having been induced by pressure transients from the wells super-imposed on the plate tectonic forces. The clustered pattern of seismicity of the main shock and the aftershocks is similar to other tectonic events.
- b. The small number of aftershocks (Figure 28) and low b-values is similar to other tectonic events in the area.
! c. The duration of the aftershock sequence is also similar to that for other tectonic-earthquakes.
- d. The magnitude of the main shock (5.0) is not anomalously l*
1arge and'is comparable to other earthquake sequences recorded in the region (Table 10).
- e. The Leroy earthquake occurred in a region of known historical seismicity including a magnitude 4.7 event in 1943.
Thus its occurrence was not surprising. l. Other Microcarthauakes
- a. The March 12, 1986 microcarthquake, described in Section 2 above, was associated with an energy release, roughly one hundred millionth (10-8) of that associated with the Leroy earthquake. It occurred close to the wells - in a distance range where other examples of induced earthquakes have occurred.
However, in over 90 days of recording with sensitive instruments, l no other comparable event has been detected in the vicinity of the wells, or between the wells and the epicentral area of the
I F i g u r e 2 8 i N n u *d o uNExo x, m t b h e e r 2 5 1 8 7 0 0 r o 0 5 0 5 0 0 e f ~ - - - - c o r a f 4 ( N d i e t . 8 :2 *.E 33 ?) n r g s 4 ( p h o 6 y *c53i ez 1 0
)
e c r k 4 i s .2
=*2I i d'$ g (8 o )
d o T s f 4 g
. ; 8*. - ** )s E a 1 n
t e ( C d c 4
*.$ I s T t 0 F o O m o )
a n N g i 5
* , )a ( I n c .
0 "L"mi- C i t e 5 ( E u a 3 d r e t M A 2 /l/!/} ",?2$_ U 0
)
A R
.s h G 5
( T q u N I 7 //!p / / l / / /- zSE~ 1 z *. 27 H a T k U 4 ( 2
)
Q e s D . s o** z1) U E A ( i n 4 ma3 5 2 K 4 ) 3 E e a 5 ( S t s . 2 / / 7 / / j / / $Ek z> 3 )5 E e 4 Q r n 3s
- I . = , 7
( U 1 ) E
.U 4 I N
. "i* : * , < 8 C
.S 1 3 E 4 S N 0
=se i y
_ o ( t 3 e 4 t 0 7 <"{_ 50 0
)
( h I D e 5 ' A aIog g 0 Y 0 3 S d ) i f f e r e n c e s 0 u -
4 78 (f. Leroy earthquake. Also, the Leroy cluster is at a depth range between about 3 and 6 km (1.9 and 3.7 miles) compared to about 1.76 km (1.09 alles) for this event. Thus it is not likely that this event is associated with the Leroy cluster. It is possible that it is a natural event or possibly associated with the Calhlo wells.
- b. The two 1983 earthquakes occurred within 5 km (3.1 alles) of the Calhio wells (Figure 5) and about 9 years after the initial injection of fluids. However, there is a fair amount of uncertainty about their depths. The nearest station used to locate them was at John Carrol University, nearly 50 km (31
. alles) away. The other stations were located at dist'ances of 100 I
km (62 miles) or greater. According to Dr. LeBlanc the best depth estimates (which yield the lowest travel time residuals) are between 2 and 4 km (1.2 and 2.5 alles). Given the epicentral proximity to the deep wells, and an elapse of nine years, and uncertainties in depth estimates it is not possible to rule out that these two events may have been induced by the injection of fluids. It is equally likely that these events were minor tectonic events the like of which have occurred in the past. However, in neither case do they appear to be spatially or temporally associated with the Leroy sequence. Conclusion After evaluating the various factors enumerated above we conclude that the possibility that the Leroy earthquakes were O
l 79 induced by well injection is highly unlikely, although it can not I O.. ^ be completely ruled-out. It is auch more likely that the Leroy sequence was a "run of the mill" tectonic earthquake and its ! l aftershocks. j j. LO O l l t e l 1 l O
. _ . . . .. a m x _ . . - - _ -
80 ^ (} BIBLIOGRAPHY Armbruster, J.G. and L. Seeber, The April 12, 1984 Martic C earthquake and the Lancaster Seismic Zone in eastern Pennsyl-vania, Preprint, 1985. Barstow, N.L., J.A. Carter, and A. Suteau-Henson, Focal depths of shallow local earthqukes from comparison of polarization + filtered data with. synthetics, Earthguske Notes, 57, No. 1, 18, 1986. Basham, P.W., D.H. Weichert, F.M. Anglin, and M.J. Berry, New probabilistic strong ground motion maps of Canada: A compila-i tion of EQ source zones, methods and results. Earth Physics 1 Branch, Energy Mines and Resources, Ottawa, Canada, Open File, i No. 82-33, 1982. Bollinger, G.A., C.J. Langer, and S.T. Harding. The eastern Tennessee earthquake sequence of October-through December, 1973. Bull. Sels. Soc. Am., 66, 525-547, 1976. Borcherdt, R.D., Preliminary report on aftershock sequence for
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-h- -v -
---n- n - . - --
,,-.,.n , - - , , v--.----,--, ,,,,--.,-,-.v-,- ..--....,._.n...n---..,. , .
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,,,m__,%,.w v.-s-,, ,,-_m,,,.-o .--,,--mw- - . - . , - , , , - - . - - _ , . _ - - - - . ._ - - - -
82 Harding. S.T., D. Carver, R.F. Henrisey, R.L. Dart, and C.J.
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I 1 C)
. - - - , . - - - . - , , . +..s --e-.-w - - - - _ - , - - , _ . . , , _ . . . . , - - , , - - - , , , - . , . - - , . _ - - _ - - - , , , . . - - - - , , - . - - - - - , - - - -
. .. ~ . - = . - . - .. - ,
83 i (- Lockner. D.A., P.G. Okubo, and J.H. stick-slip failures on a simulated fault by pore fluid injec-tion, Geophys. Res. Lat., 9, 801-804, 1982. Dieterich, Containment of Martin, J.C., The effect of fluid pressure on effective stresses
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--e,- v ~,-e-,c- -. r, . ---c,-r-------+--y,--w..~..~.+L-~-~. - - - . - - - . . - . . - - - . - - . . - - = = . - - - - ~ - * - - - - - - - - - - - - - -
84 Pennington, W.D., S.D. Davis, S.M. Carlson, J. DuPree, and T.E. [~'[ A-Ewing, The evolution of seismic barriers and asperities caused by the depressuring of fault planes in oil and gas fields of south Texas. Bull. Sels. Soc. Am.. in press, 1986. Phillips, D.E. and D.H. Oppenheimer, Induced seismicity in the Geysers Geothermal Area, California, J. Geophys. Res., 89, 1191-1207, 1984. Pulli, J.J., J.L. Nobelek, and J.B. Sauber, Source parameters of the January 19, 1982 Gaza, N.H., earthquake, Earthquake Notes, 54. No. 3, 28-29, 1983. Pulli, J.J., R.R. Stewart, J.C. Johnston, K.M. Tubman, and A. Michaels. Field investigation and fault plane solution of the Bath, Maine earthquake of April 18, 1979, Earthquake Notes,
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/~T' .
U
i < - - - l l 85, , Schlesinger-Miller, E.A., N.L. Barstow, and A.L. Kafka, (' Earthquake intensities and evaluation. Earthquake Notes, 53, No. 3, 34, 1982. Seeber, L., J.G. Armbruster and D. Coyle, A prolonged, but spatially concentrated earthquake sequence at the northern outskirts of New York City, Earthquake Notes, 57, No. 1, 18, 1986a. Seeber, L., J. Armbruster, and G. Suarez. The April 1984 Martic. Lancaster Co. earthquake, historic seismicity and tectonic setting in eastern Pennsylvania. Earthguske Notes, 55, No. 3, 12, 1984a. Seeber, L., J. Armbruster, N. Barstow, E. Schlesinger, unpublished data, 1986b. Seeber, L., E. Cranswick, J. Armbruster, and N. Barstow. The October 1983 Goodnow, N.Y. aftershock sequence; Regional seismicity and structural features int he Adirondacks, EOS Trans. Am. Geophys. Union,. 65, 239, 1984b. Seeber, L., E. Cranswick, N. Barstow, J. Armbruster, G. Suarez, K. Cales, and C. Aviles, Grenville structure and the Central 1 Adirondack Seismic Zone including the October 7, 1983 mainshock-aftershock sequence, Can. Geophys. Union Mtg., Halifax, Nova . Scotia, 1984c. Shand, J.B., and L.T. Long, Intensity of the Lafayette, Georgia, earthquake, Geol. Soc. Am. Abstracts with Programs, 17, 135, 1985. Shurbet. D.H., Increased seismicity in Texas, Texas J. Sci., 21, 37-41, 1969. Stauder, W. and 0.J. Nuttli, Seismic studies: South central Illinois earthquake of Nov. 9, 1968, Bull. Sels. Soc. Am., 60, 973-981, 1970. Steeples. D.W., Induced seismicity in the Sleepy Hollow 011 Field, Red Willow County, Nebraska, in National Earthquake Hazards Reduction Program, Summaries of Technical Reports Volume XX, U.S.G.S. Open File Report 85-464, 429-432, 1985. Street, R.L., Scaling northeastern United States / Southern Canadian earthquakes by their Lg waves, Bull. Sels. Soc. Am., 66, 1525-1538, 1978. Street. R.L. and E.T. Turcotte, A study of Northeastern North American spectral moments, magnitudes, and intensities, Bull. Sels. Soc. Am., 67, 599-614, 1977. O
- -. - - ~ > - . , , , - , - , , - - , --
cv , - . . - , - --r-- -,- - -._- - - -
86
. Suarez, G., L. Seeber, C. Aviles, and E. Schlesinger, The Goodnow, N.Y. earthquake: Results of a broad band teleseismic f~)'[
s m analysis, EOS Trans. Am. Geophys. Union, 65, 239, 1984. Teng, T.L., C.R. Real, and T.L. Henyey, Microcarthquakes and water flooding in Los Angeles, Bull. Sels. Soc. Am., 63, 859-875, 1973. van Poollen, H.K. and D.B. Hoover, Waste disposal and earthquakes at the Rocky Mountain Arsenal, Derby, Colorado, J. Petr. Tech., 22, 983-993, 1970. Wahstram, R., The North Gower, Ontario, earthquake of 11 October, 1983: Focal mechanism and aftershocks, Submitted to Earth-guake Notes, 1985. Wetailler, R.J., The Quebec-Maine border earthquake, 15 June 1973, Can. J. Earth. Sci., 12, 1917-1928, 1975. Wetailler, R.J., J. Adams, F.M. Anglin, H.S. Hasegawa, and A.E. Stevens, Aftershock sequences of the 1982 Miramichi, New Brunswick earthquakes, Bull. Sels. Soc. Am., 74, 621-653, 1984. j Wong, I.G., J.R. Humphrey, W. Silva. D.A. Gahr, and J. Huizingh, A case of microseismicity induced by solution mining, south-eastern Utah, Earthquake Notes, 56, No. 1, 18, 1985. O~ Yang, J.P. and Y.P. Aggarwal, Seismotectonics of northeastern U.S. and adjacent Canada, J. Geophys. Res., 86, 4981-4998, 1981.
=
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87 APPENDIX I. CONCERNS EEPRESSED BY PROFESSOR AIDIAD In his testimony on April 8, 1986 before the House Committee on Interior and Insular Affairs. Subcommittee on Energy and Environment, Dr. Mold U. Ahmad of the Ohio University expressed several concerns. Some of these pertained to the Leroy earthquake and the possible role of fluids injected in the two deep Calhio wells. In particular he suggested that his review of the historical seismicity data, injection history at Calhio wells suggested that the injection of fluids in the Calhio wells had induced the earthquakes in the Leroy sequence. The paragraphs below address the comments made in his written testimony. General Remarks
- 1. The status of seismicity in Dr. Ahmad's testimony was
( not up to date. The more recent data regarding number of events, locations, etc, have been incorporated in Section 2. and will also be available in the report by Weston Geophysical.
- 2. The information regarding the structural trends and Woollard's data is completely out of date and current data /
thinking do not support the concept of a mega-linear trend from ( New Madrid to the St. Lawrence rift zone in Canada (see Dr. Hinze's report for details). In his response to the concerns i i raised by OCRE, Dr. Pomeroy also cautioned against such " linesman-ship". I' l.
- 3. The Pittsburgh-Washington and the Tyrone-Mt. Union are i
two lineaments identified by analyses of Landsat images and po-O
88
- . s.
(} tential field data by Lavin et al. (1982). According to those-authors there was lateral movement of a block contained by these lineaments during the late Pre-cambrian to Lower Ordovician time (600-450 million years ago) and vertical displacements in Paleo-zoic times (to about 300 million years ago). Since then, there is no evidence of lateral or vertical movement on these features, i.e. there is no evidence that these are active faults as implied by Professor Ahmad. Hence his classification of these features as " Cleveland-Pittsburg (sic) Washington strike slip fault" and "Tyrone NT (sic) Union strike slip fault" are incorrect.
- 4. Next. Dr. Ahmad appeals to "hydroseismicity", a mecha-
, i nism according to which "... natural water flow can trigger earthquakes by increasing the fluid pore pressure in the rocks and lubricating an already stressed fault..." This is based on a news story in Science News by Stefi Weisburd - following a talk given by Costain et al. Dr. Ahmad in his oral testimony was critical of the U.S.G.S., NRC and the utility for not incorpo-rating "hydroseismicity".
We are thoroughly familiar with this idea. In fact, it is not new at.all. The idea of seismic activity triggered by changes in rainfall patterns is not new and has been explored in research concerned with other earthquake sequences, expecially in
- Japan. In its current form, Costain and Bollinger (1985) and Costain et al. (1986) offer it as a speculative model to explain all intraplate seismicity in the southeastern United States. It i
__,._n,,,-,.-n,
l I 89 s is one of about a dozen speculative models that have been sug-gested in the last five years or so. The use of this mod'el as a 1 general mechanism for seismicity on a regional basis and at I depths of 10-20 km is very speculative and full of scientific loopholes. It is by no means an accepted " theory" that can be applied-to explain the temporal and spatial pattern of seismicity observed at Leroy.
- 5. The study of earthquakes in the Denver area associated with the Rocky Mountain Arsenal was by Healy et al. (1968) whereas the seismicity in the vicinity of the Rangely 011 Field was by Raleigh et al. (1976) and not by "Healy and others, 1961" as stated by Professor Ahmad (see section 5 above). Also, the Baldwin Hills Reservoir is in California not Louisiana as stated
( by Professor Ahmad.
- 6. Describing the magnitude 3.8 earthquake in Louisiana in 1983, "... occurring about 2 alles south of Browning Ferris Industries injection well at Lake Charles. Louisiana". Dr. Ahmad y quotes his own unpublished presentation to assert that, "...the 1
injection well increased the pore pressure and lubricated an already stressed fault". No supporting data or evidence are l provided for this assertion. This earthquake has been studied by 1 i various workers in Louisiana and Texas and according to them it is not associated with the wells and appears to be similar to an earlier earthquake offshore (Pennington, Personal Comunication, 1986: Don Stevenson, State Seismologist, La., Personal Communica-(:) ~ -
.. ---,.,,,,.-nn. , - - - , - - , , - gg.-gy,. .n. , ~ , , --
-,---e,,,,_,_w-www,, - -
90 tion, 1986). That a b 4.8, offshore earthquake occurred on July ( 24, 1978 and it was suggested that events in the Gulf of Mexico occur along zones of weakness associated with Mesozoic rifting (Frohlich and Dumas, 1980; Frohlich, 1982). However, others ascribe them to flexuring because of the sediment load in the Gulf.
- 7. Dr. Ahmad's description of the induced earthquakes near Snyder. Texas was based on a thesis by Davis (1985) and the pre-print of a forthcoming paper in the Bulletin of Seismological Society of America by Pennington et al. (1986). We reviewed these and also an abstract of a talk by Pennington and Davis (1985) with respect to the impact on hypotheses concerning the cause of the Leroy, Ohio earthquake of 1/31/86. Their model for g induced seismicity relates to petroleum operations and is based on the premise that regions of high pore pressure undergo aseismic creep while regions of lower pore pressure (often associated with fluid withdrawal) cannot move aseismically and become high strength barriers. Continued aseismic creep leads to increased stress at the locked barriers resulting in the transformation of l
l these high strength barriers into high stress asperities. Stres-ses at these asperities continue to build until failure occurs seismically. This model represents a logical extension of the Mohr coulomb failure criteria (Jaeger and Cook, 1979) which is often invoked to explain seismic activity. Such a model is a good application of the laboratory results of Lockner et al. (1982) and the suggested cause of seismicity at the Geysers O t
, ,,. , - - - - , . . . - , - , . , - , - , - - , - - - _ , - , . . . , , , , , , , -----,,---------.---~w v.--------.,.,-.,-,--,_-.,-c--
91
/~'p geothermal field (Phillips and Oppenheimer. 1984). This model is .D particularly useful in explaining the spatial patterns of sels-nicity associated with fluid WITHDRAWAL and simultaneous injection. '
Using the best estimates of the pore pressure increases resulting from the Calhio injections it is unlikely that this model can be invoked to explain the spatial or temporal pattern of seismicity observed near Leroy, Ohio.
- 8. Assuming the injection pressure history at the well site, Dr. Ahmad calculated the excess pore pressure at an epicen-tral distance corresponding to the site of the Leroy earthquakes.
Assuming radial flow in a homogeneous layer he obtained an excess pore pressure of about 100-200 feet of head at the epicentral location or about 3-6 bars. This estimate is in agreement with that obtained by U.S.G.S. (Wesson. Personal Communication). If the flow is along a channel (as was modeled for Denver (Hsieh and ] Bredehoeft. 1981)), the excess pore pressure is likely to be greater within the channel and lesser outside it. However, there is no known evidence of such a channel near Leroy.
- 9. While concluding, Dr. Ahmad makes some sweeping state-ment that invites a comment. For example, "...We believe that large and destructive earthquakes will occur in the East..."
Yes, but the crucial question is where and with what return periods? There are several studies under way (e.g. by EPRI. LLNL. and others under NRC sponsorship) aimed at arriving at the O i
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92 l
-n answer to the above question. He also asserts that "...PNPP is surrounded by at least four known faults and two earthquakes of about magnitude 5 within a ten alle radius in the past four
.. years. The presence of high pressure deep injection wells have increased the possibility of future earthquakes in this area..." The existence of any one of these four faults has not been demonstrated either in Dr. Ahmad's testimony (or in the litera-ture). Only one magnitude 5.0 event i s known to have occurred in that area, and that was the Leroy 1/31/86 event. The association of seismicity with injection wells in Ohio is arguable at best and has not been demonstrated. Hence, the assertion that there is an increased possibility of future earthquakes because of injection is perhaps both wrong and misleading. f l l l O D
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- Attcchment 2 PY-CEI/NRR-0478 L Page 1 of 2 PRELIMINARY SYSTEM DESCRIPTION INJECTION WELL MONITORING NETWORK INTRODUCTION The earthquake of January 31, 1986, mangitude approximately 5.0, occurred a . '
little more than ten miles to the south of the Perry Nuclear Power Plant (PNPP) site. Throughout the regulatory review process concerning the cause of this earthquake, a possible relationship between the local inje'ction wells and the earthquake has been of considerable concern. In his review of data presented [ to the ACRS subcommittee on Extreme External Phenomena, Dr. Paul W. Pomeroy, i ACRS Consultant, has expressed his opinion that the "long-term seismic monitoring with high-quality, high-sensitivity instruments should be carried J out in the area (including the aftershock zone and the injection well area, as well as the vicinity of the plant)". (Pomeroy letter to Advisory Committee on Reactor Safety, US Nuclear Regulatory Commission, dated March 25, 1986). Although the 1/31/86 earthquake has been determined to be a natural event and , not induced seismicity due' to the injection well, CEI will implement a a monitoring program for detection of micro-seismic events. The seismic network described in this proposal is consistent w'.th Dr. Pomeroy's i opinion and utilizes state-of-the-art instrumentation to provide detailed monitoring around the local injection wells extending to the south to the epicentral area of the January 31, 1986 earthquakes as defined by the detailed aftershock monitoring conducted by Weston Geophysical. The overall concept includes seismometers located at 5 stations with signals telemetered by radio frequencies to a central recordi'ng location. Digital recording of any event will be triggered by computer when any seismic event is detected at one or more stations within the seismic network. The seismic data will be sampled at a , l rate of 250 samples per second, allowing for broad-band recording of l frequencies up to 100 Hz. l SEISM 0 METER LOCATIONS , The digital telemeter array will have a proposed configuration of 5 stations as shown in Figure 1. Four of the stations are located around the local injection wells and a fifth station is located to the south of the January 31, 1986 epicentral area. These five stations provide detailed monitoring of the PNPP-well corridor. Based on recording experience in the area it is anticipated that seismic events of magnitudes above background will be recorded and located by the proposed seismic network. The seismograph stations are located at the appropriate distance so that the difference in arrival times of the compressional "P" and shear "S" waves from an earthquake can be used for accurate determination of epicentral location and depth (hypocenter). To further enhance the detection capability of the seimic network, horizontal geophones are used at all locations, except at the station closest to the local well area, where a three component seismometer system is installed to provide full seismic wave analysis. Horizontal geophones record the higher amplitude S wave arrivals which allows the network logic to detect and trigger on low magnitude seismic events.
Attachment 2 PY-CEI/NRR-0478 L Page 2 of 2 To further enhance the detection capability of this seismic network, the seismometers ars installed below ground surface.to minimize noise, thereby improving the signal to noise ratio. Each remote transmitting site (see Figure 2) has from one to three geophone t motion sensors connected to low noise pre-amplifiers whose gain can be set consistent with local noise conditions and signal level to be recorded. An l anti-alias filter is-followed by a 16-bit (96db) analog-to-digital converter l which samales up to 250 samples per second. The digital data is then sent via wide-band radio transmitter to a central recording site. Wherever local conditions preclude line of site, repeater stations relay the signals past obstacles. Battery back-up at each site carries the system through most power outages. . RECORDING SITE ! At the recording site (see Figure 3), data processing is managed by a digital I computer system whcre radio signals are received and the digital data is sorted by channel. The data is immediately converted for display on visual recorders. In parallel with this operation, digital data is processed to determine l short-term averages and long-term averages for each channel. Whenever the quotient of these two averages reaches the operator-selected ratio for the specified channels (within the prescribed time) an event is declared, and the system automatically records the data digitally. At the conclusion of the recording period, the system returns to its monitoring mode and awaits another event. During this time, the operator may display the data on screen, pick arrival times, and make printouts. When another event arrives, operator control is suspended until data recording of the new event has been completed. The operator selects time windows with precision timing from a WWVB synchronized calendar clock. All data is archived on 9 track tape and simultaneously recorded as a quick-access file on removable, 5 megabyte disk media. In order to ensure that all seismic events are recorded, complete analog monitoring will also take place at a central recording site. The incoming digital signals will be converted to analog traces, with each of the seven channels recorded on a separate drum recorder. Once all the proper adjustments have been made to the seismic network, and a few months of recording has been completed, the need for total analog backup recording will be evaluated. D16/11 i _-..-- _.. . . - _ _ _ . . . - - _ _ _ . _ . _ _ . _ _ _ _ _ . _ _ _ . _ . _ . - _ _ _ _ _ - _ _ _ - _ _
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- I
'I I Deep Well Injection at the Calhio Wells and The Leroy, Ohio Earthquake of January 31, 1986 I
g ev Pradeep Talwani and Steve Acree I I I I II 1 i I I l I 'I
I
- 1. INTRODUCTION On January 31. 1986 at 11:46 a.m. (Eastern Standard Time) a magnitude 5.0 earthquake occurred near Leroy in northeastern Ohio. The epicenter was located about 17 km (11 miles) south of the Perry Nuclear Power P'. ant at a erry. Ohio. In common with similar moderate earthquakes in the northeastern United States, this event was shallow (about 5 km deep) and not associated with any surface manifestation. It occurred in an area with no known seismogenic feature and thus itn catise was not understood and could only be speculated upon. There are two deep injection wells located about 11 km (7 miles) north of the epicenter. The observation that a large volume of fluids had been pumped into these wells in the last twelve years, and the knowledge that in a few cases such operations in other locations have in some cases triggered small to moderate earthquakes, led to the speculation that this fluid injection uay have triggered the January 31, 1986 event -
the Leroy earthquake. In this report a variety of data are examined in order to address this possible association. The Iecoy earthquake, its aftershocks and the historical seismicity 44 the area are described in Section 2. Data pertainihg to the two deep wells and fluid injection operations are given in Section 3 and those regarding solution mining in the area are given in Section 4. In order to assess the characteristics of the observed seismicity at Leroy vis a vis well induced seismicity, a review of the latter is presented in Section 5. Recent instrumentally recorded earth-5 I
I 2 I quakes in tectonic settings similar to that of the Leroy earthquake are described in Section 6. In the final section the various data presented are analyzed to assess the validity of the speculation that the observed seismicity at Leroy, Ohio was induced by the injection of fluids in the two deep wells. Some of the concerns expressed by Professor Ahmad in his testimony before the Subcommittee on Energy and the Environment. Committee on Interior and Insular Affairs. U.S. House of Representatives on April 8, 1986, are addressed in Appendix I. Our conclusion is that although it is possible for the Leroy earthquake to have been induced, it is highly unlikely that it was. The event appears to be a normal, typical tectonic earth-quake which occurs regularly, albeit infrequently in northeastern United States.
- 2. THE LEROY EARTHQUAEE, AFTERSHOCES AND HISTORICAL SEISMICITY IN THE AREA Th_e Main Shock On January 31, 1988 at 11:46 a.m. (EST), a body-wave magni-I tude 5.0 earthquake, with a maximum Modified Mercalli intensity VI, shook northeastern Ohio. Preliminary location of this event by the National Earthquake Information Service (NEIS) based on teleseismic data and the standard Jeffreys-Bullen earth model, i placed the epicenter at 41.649'N and 81.105*W (41* 38.56'N, 81*
l l
= 06.18'W). Using a U.S. seismic model, this event was relocated l
about 6 km to the west at 41.650*N and 81.162*W (41* 39.00'N and lE . I
3 81* 09.43'W) with an epicentral accuracy of i4 km (2.5 miles) at the 904 confidence level (Borcherdt, 1986). The best solution was obtained when the depth was constrained at 5 km (3.1 miles) - the best estimate for the hypocentral depth. (The latter epicentral location was also found to lie within the cluster of aftershocks and the region of maximum intensity.) l
~
Aftershock Studies At least seven teams of seismologists deployed portable seismographs in the epicentral area to record possible after-shocks of the Leroy earthgake. (Please see Weston Geophysical data for details.) The U.S. Geological Survey deployed a ten-station array of broad band digital instruments, the General Earthquake Observation Systems or GEOS (Borcherdt. 1986). These complemented several smoke-paper recorders deployed by other groups. Through April 15, 1986, 13 aftershocks with coda wave magnitudes between -0.1 and 2.5 had been located. Preliminary g locations of six aftershocks recorded on the GEOS instruments between 2/1/86 and 2/10/86, using a layered seismic velocity model are given in Table 1. The aftershock epicenters are tightly clustered and lie in a 1 km square (0.4 mile 2) (Figure 1
& 2). These six and an additional seven events (to 4/15) were also located by Weston Geophysical (Figure 3 and Table 2). The locations of the six' events common to the two data sets are in general agreement, with the Weston epicenters located on average
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,l Figure 2. U.S.G.S. epicentral location of aftershocks E (2/1-2/10/86) detail.
I I
6 I Table 1 U.S.G.S. LOCATION OF AFTERSHOCKS. B Aftershocks: YR MO DA CRIGIN LAT N LON W DEFIH RMS ERH ERZ GAP 86 2 322 48.57 41 38.76 81 9.50 5.12 0.01 1.16 0.78 150 I 86 3 1947 19.65 86 5 634 2.40 41 41 38.92 38.96 81 81 9.43 9.68 5.81 4.05 0.03 0.02 0.88 0.88 0.76 116 1.31 134 l 86 6 1836 22.26 41 38.68 81 9.33 6.06 0.03 0.82 0.80 121 ,I 86 7 1520 20.19 86- 2-10 20 6 13.59 41 41 38.97 39.07 81 81 9.42 9.31 4.66 3.38 0.03 0.04 0.92 0.81 5.21 115 6.31 115 l (From Borcherdt,1986) l l I Table 2 I COORDINATES OF MAIN SHOCK AND AFTERSHOCKS. ig YR MC3Y HRM*S EC LAT. L 3N 3. 3EPTH MB MC (W 15360131 164642.3 41.650h 81.162W 5- 6 4.93.00.00.0 15360201 135.43.3 41.64Sh 81.153W 4.3
- 1.5 15360202 032246.9 41.645h S1.159h 4.3 0.9
- 41. 6 4 9 t. 81.153W 5.3 2.3 l5 15360233 194719.6 15360205 063402.3 41. 6 4 S h 31.155W 3.7 0.1 15360206 183622.4 41. 6 4 5 t. 51.160W 5. 5 2.5 15360207 151010.3 41. 6 51t. 81.154W 3. 7 1.1 8 15360210 200613.5 41.652N 81.157W 4.7 0.3 19963223 032946.5 41. 6 5 3h 61.152W 5.4 0.1 15363224 165506.5 41. 64 Sh St.163h 3.2 0.1 8 15363228 013134.2 15360308 204249.7 41.654h E1.163W
- 41. 6 4 6h 81.153W 3.9 3.1 3.1 3.1 15363324 134241.3 41.639h 81.156W 4.7 1.4
'I 15363410 065605.7 41.647h 81.153h 4.7 -0.1 (From Weston Geophysical)
April 1986 I
c 51.18W 81' 10' W 81* 0 9'W 81.14 W
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I Figure 3. Weston Geophysical location of main shock and aftershocks to 4/15/86. I I
[ about 0.5 km to the northwest of those by U.S.G.S. With the exception of aM 1.4 event on March 24, 1986, the remaining twelve epicenters lie in a tight cluster about 0.5 km (0.3 mile) to the east of the location of the mainshock. The depths of all the events lie between 3 and 6 km (1.9 - 3.7 miles) (Table 2). Since the location of the mainshock was based on distant sta-tions, it is very likely that it too was located in the narrow { cluster defined by the twelve aftershocks. The lack of an obvious elongation in the aftershock pattern (if the March 24, event is not included) makes it difficult to infer the orienta-tion of the fault plane. If the March 24 event is included, an apparent north-south trend emerges. The March 12. 1986 Microearthquake At the progress meeting with the NRC and the utility on April 30, 1986, Dr. Wesson of the U.S. Geological Survey brought to our attention the occurrence of a niniscule event on March 12, 1986 that had been recorded on the GEOS station at site 4 (GSO2) (Fig. 4). This coda magnitude -0.3 (LeBlanc, personal communica-I tion) event with a total duration of about 4 seconds was also recorded on some stations deployed by Weston Geophysical Co. and by Woodward Clyde Consultants (WCC). Using their preliminary arrival times the event was located by U.S.G.S. at 41' 43.63'N, 81* 10.24'W. with a depth of about 2 km (1.2 miles) (Table 3) - or about 3 km (1.9 alles) SSW of the two deep wells (Fig. 5). The event was located by using a 7-layer seismic velocity model I I
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10 I Table 3 LOCATIONS OF THE MARCH 12, 1986 MICR0 EARTHQUAKE Origin Long. Depth I Lat. 03:12:18.55 41*N 81*N K m_ Gap RMS Remarks 26.59 43.63' 10.24' 2.01 216 .06 USGS prelim. I location 7-layer model. Prelim. arrival times for WCC stations. 26.64 43.83' 10.13' 1,73 .05 WCC solution. revised picks and 3-layer model. I 26.64 44.00' 10.29' 1.76 176 .05 Used revised picks 3-layer model'and I data for Weston stations. 26.52 43.85' 10.40' 1.97 175 .09 Used revised picks 7-layer model and data for Weston stations.*
- For comparison.
I I I I I I I I
1/22/83 DEPTHS 11/19/83 A PROH CRMO - X 0.0+ WELLS
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- 2 KH 5.0+
A FARM I . . l . . 10' l (Modifled from Wessoti. Pers. Comm. 1986i Figure 5. Preliminary U.S.G.S. and revised Weston location of 3/12/86 event and location of the 1983 earthquakes.
I 12 (Table 4), Using revised picks for the arrival times for the WCC stations and a 3-layer velocity model (the same as the one used by Weston Geophysical) the location of the event moved about 200 m (655 ft) to the northeast. Incorporation of data from Weston stations moved it about 380 m (1245 ft) to the northwest. Thus our preferred location 41' 44.0'N, 81* 10.29'W and depth 1.76 km (1.09 miles) is about 2.5 km (1.6 miles) SSW of the deep wells, and about 10 km (6.2 miles) north of the epicenters of the Leroy sequence. The implications of this event vis a vis a possible association with fluids injected in the deep wells is discussed in Section 7. The 1983 Microearthquakes Two microearthquakes occurred within 10 km (6.2 miles) of the two deep Calhio wells in January and November 1983. These events have been studied by Dr. LeBlanc of Weston Geophysical, who provided the following information. The January 22, 1983 , earthquake was recorded on regional stations - the nearest being l at John Carrol University. It was also recorded on stations of I the Anna. Ohio network and by stations in Western Ontario. Canada. The Earth Physics Branch (EPB), Canada assigned it a !I Nuttli magnitude (MN) 3.3 whereas the National Earthquake Information Service (NEIS) assigned it a body wave magnitude (abLg) 2.7. The epicentral location of the event obtained by Dr. l LeBlanc based on these data is 41* 45.9'N, 81* 06.6'W with an l uncertainty of a few kilometers. The best depth estimates place
" A' smaller the event between 2 and 4 km (1.2 and 2.5 miles).
13 Table 4 THREE LAYER VELOCITY MODEL. I Depth to Top P Velocity Vp/Vs of Layer (km/s) (km) 0.0 4.25 2.0 6.5 1.73 35.0 8.1 Weston Geophysical. Depth Thickness P Velocity S Velocity Vp/Vs *
- Description *
(km) (bn) (hn/s) (km/s) Layered Crust I 0.0 0.05 1.80 0.60 3.00 Glacial till 0.05 0.45 3.00 1.60 1.88 Devonian shale 0.50 0.50 4.20 2.36 1.78 Silurian dolomite 1.00 0.75 4.5'O 2.53 1.78 Ordovician limestone and dolomite 1.75 0.35 4.75 2.67 1.78 Cambrian sandstone and dolomite 2.10 17.90 6.15 3.68 1.67 Precambrian granite 20.00 25.00 6.70 3.87 1.73 Lower crust 40.00 99.00 8.15 4.65 1.75 Mantle
" Cleveland Electric Illuminating Co. (1982)
(From Borcherdt, 1986) I ** In locations given in Table 3 a Vp/Vs ratio of 1.73 was used for all the layers.
L r ( 14 { event occurred on November 19, 1983 and was assigned a magnitude 2.5 by EPB and was not assigned a magnitude by NEIS. Based on similarities in the wave trains of the two events at some Canadian stations Dr. LeBlanc argued that both events had l the same epicentral location (within our ability to locate them). l This location is shown on Figure 5, and the possible implication of these events vis a vis their being induced by fluid injection is addressed in Section 7. Historical Seismicity The historical seismicity in the region and in a 80 km (50 mile) radius centered at the Leroy epicenter and of Ohio are shown in Figures 6, 7 and 8. These maps are discussed by Weston Geo, and are presented here to make the observation that felt earthquakes had occurred here in historical times. The largest previous event in the 80 km (50 alle) radius was the magnitude 4.7 event on March 9, 1943. Comoosite Fault Plane Solutions I j Composite fault plane solutions using events in the cluster yielded strike slip solutions (See Weston Geophysical's data ), with either right-lateral strike slip motion on a steep NNE striking fault or left-lateral strike slip motion on a steep fault oriented to the northwest. In view of available gravity and aeromagnetic data discussed by Weston Geophysical, the NNE trending nodal plane is the more likely fault plane. I ,
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17 I DEPARTMENT OF THE INTERIOR UNITED STATES GEOLOGICAL SURVEY S.
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1979 I
18
- 3. REGIONAL DEEP WELL FLUID INJECTION Three high pressure fluid injection wells currently operate within Lake County, Ohio. Two wells owned by the Calhio Chemi-cals division of the Stauffer Chemical Company (Calhio #1 and #2) have been in operation since 1974 and mid 1981, respectively.
These wells, spaced at approximately 800 m (2600 ft) apart, are located about 11 km (7 miles) north of the epicentral area. The fluids injected through these wells consist of a dilute aqueous brine containing waste products from the manufacture of agricul-tural fungicides. A cumulative total of 1.17 x 10 0 m3 (310.2 million gallons) of fluid has been injected at depths below zi670 m (5480 ft) (Nealon, 1982: Ohio EPA, 1985) and pressures to = 112 bars (1630 psi) (top hole) at rates to 326 liters / min (86 gal / min). Of this total, 1.02 x 10 6 ,3 (268.2 million gallons) have b'een injected in Calhio #1 (Figure 9 and 10) (Table 5) and 1.59 x 105 ,3 (41.9 million gallons) have been injected through 3 Calhio *2 (Figures 11 and 12) (Table 6). Approximately 3069 m (0.8 million gallons) of a salt water brine have been injected through a single well located near Painesville, Ohio owned by Environmental Brine Ser. vices, Inc. at top hole pressures to 55 bars (800 psi) since initiation of injection in October 1985 (Ohio Dept. Nat. Res., 1986). In all three wells fluids were injected into the Mt. Simon Formation, a friable fine to coarse grained dolomitic Cambrian sandstone, which overlies Precambrian granitic basement (Nealon, 1982). In Calhio *2, the Mt. Simon was logged as approximately I I -
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;.a LNJECTION WELL
- 1 (From Weston Geophysical)
I Figure 10. Injection pressures utilized at Calhio *1. I I I
Table 5 - VOLUMES OF FLUIDS AND INJECTION PRESSURES FOR CALHIO - CHEMICALS WELL #1. Calhio Injection Well # 1 l I Start McDaYear MoDa S top 7otal Gallon s Injected Cumulative Gallons Injected Max. Injection Pressure Min. Ase. l I 03191975 0331 04011975 0434 01011976 0131 2158682. 2435351. 637333. 3630743, 5739425. 22742518. 700. 103C. 1430. O. O. O. 565. S75. 1415.
+
2 02011976 0229 1105383. 23847606. 1455. O. 1440. - B 03011976 0331 2034653. 25932264 1270. O. 1130. 04011976 0430 2622620. 27554384 1340. O. 1230. - I 05011976 0531 246964. 27831948. 1225. 3. 1220. 07011976 0731 3003889. 33333973. 1410. O. 1330. - 08011976 0831 1679345. 35068313. 1425. O. 1230. 09011976 0930 1930055. 37048373. 1370. 3. 1330. ; I - 1C 0119 76 1031 11011976 1130 12011976 1231 2854348. 2634417. 1938593. 39933721. 42598138. 44576731. 1425. 1450. O. J. 1350. 1375. 1230. O. 1250. W
... 01011977 0131 2660877. 47237603. 1430. 3. 1430.
02011977 0228 2673412. 49911023. 1525. O. 1530. 03011977 0331 2560253. 52471273. 1525. O. 1440. ; 04011977 0430 2350339. 54821612. 1500. O. 14J0.
'I 05011977 0531 06011977 0630 1891592.
2134493. 56713304 53E37302. 1330. 1365. O. O. 1130. 1360. 07011977 0731 1798450. 60636252. 1310. O. 1230. ,
]
OE 011977 0 831 1596376. 62293229. 1270. O. 1265. 5 09011977 0930 2006380. 64239603. 1260. 3. 1250. __ 10011977 1031 2319263. 66618377. 1255. J. 1250. I 11011977 1130 12011977 1231 01011978 0131 1930569. 2238476. 18452S1. 63549446. 70647922. 72633203. 1220. 1240. 1230. O. O. O. 1250. 1220. 1240. M 1 I C2011978 0228 1955372. 74643275. 1240. O. 1220. 2832535. 03011978 0331 77430910. 1460. 3. 1430. 04011978 0430 2949993. 80430303. 1480. O. 1440. 3314135. 05011978 0531 83744943. 1500. O. 1470. I 06011978 0630 2034065. 85839009. 1500. 3. 1350. , 07011978 0731 1236726. 87125734. 1290. O. 1230. O E 0119 78 0 831 3648315. 90774049. 1295. O. 1230. 4 I 09011978 0930 1C 0119 7 8 1031 11011978 1130 1944327. 2247493. 2638632. 92718376. 94966375. 976050C7. 1320. 1420. 1470. O. O. O. 13J0. 1340. 1370.
=
s I 12011978 1231 3016456. 100621463. 1440. O. 1430. - 01011979 0131 1367375. 101938523. 142C. O. 14J0. -3 020119 79 0 22d 2701315. 104630453. 14 30. 3. 1330. - 03011979 0331 2829308. 107519451. 14 20. 3. 1430. 34011979 0430 2816038. 11C335483. 1460. 3. 1420. 05011979 0531 2861572. 113137061. 1460. O. 1420. $ 06011979 0630 2351743. 1155493C1. 1420. O. 14J0. 1 I 07011979 0731 O E 0119 7 9 0 3 31 39011979 0930 3103232. 2735412. 3134716. 113652033. 121437445. 124622161. 1440. 14 40. 1440. O. O. O. 14J0. 1410. 1420. ! l 1C011979 1031 3173303. 127735464 I 12011979 1231 3406783. 124268336. 1430. 1560. O. 3. 1410. 1510. 2
22 Calhio Inj ec ti on Well e i Total Cumulative Injection Start S top Gallons Pressure I Gallon s Mo 3af e ar M o0a Injectsd Inj ac te d Max. Min. Ave. 01011980 0131 3363000. 137631336. 1550. O. 1520. I 02011980 03011930 04011980 0229 0331 0430 2771584. 3253519. 3534333. 139402920. 142656539. 146240569. 1510. 1520. 1560. 3. O. O. 1330. 1430. 1520. I 05011980 0531' 06011980 0630 07011980 0731 3127521. 3136545. 3258443. 149363190. 152534725. 155753173. 1520. 1550. 1560. O. O. O. 1420. 1450. 1520. ! g 08011980 0831 2776363. 153539541. 1550. O. 1530. E oSo2 980 0 930 2877980. 1614t7621. 1460. O. 1420. l 1C 1019 80 1031 2919511. 164337232. 1500. O. 1450. i 11011990 1130 2625973. 166953205. 1440. O. 13'.0. I 12011980 1231 3517927. 170431132. 1490. 3. 1440. l 01011881 0131 2457250. 172948382. 1400. O. 1350. 1 02011981 0223 3250175. 176138559. 1420. 980. 1430. I 03011981 0331 04011981 0430 05011981 0531 3599074 3428550. 1630519. 173797532. 183226282. 1520. 1495. 184825901. 1530. 1223. 1420. 1120. 1410. 1450. 1370. 06011981 0530 75046 5. 185577366. 1430. 990. 1230. l 07011931 0 731 2355992. 187943353. 1560. 1040. 1340. O E 0119 81 0 8 31 1869980. 187447346. 1550. 800. 1430. 09011981 0930 1058205. 183535551. 1320. 1053. 1230. I 11011991 1130 12011991 1 231 31011982 0131 1674386. 902543. 3056953. 192922365. 193825796. 196832746. 1430. 1310. 1470. 1000. 1150. 1140. 1350. 1020. 1330. I 02011982 0228 03011982 0331 34011982 0430 3157200. 1934574. 1121864. 200049946. 201076484. 1550. 210954623. 1430. 1330. 1270. 1070. 1043. 1430. 1330. 1330. 06011982 0633 634482. 201710965. 1140. 340. 930. I 07011982 0731 11011982 1130 231422. 755343. 201942363. 202697731. 1020. 1110. 780. 680. 840. 840. 12011982 1231 3073793. 205771524 1310. 1010. 1230. I 01311983 0131 02011983 0228 03011983 0331 2744922. 3119054. 3338846. 20SS16446. 211635503. 215024346. 1330. 1440. 14 60. 1300. 1120. 1120. 1320. 1370. 1330. I 04011983'0430 05011983 0531 06011983 0630 3335933. 1334399. 62613. 212330276. .1510. 219635375. 219637993. 1510. 1030. 1223. 1020. 933. 1470. 1230. 970. 07011983 0731 451944 220194937. 1250. 930. I 920. OE 3119 83 0 331 1159455. 221354392. 1250. 903. 1050. 090119 3 3 0 93J 748463. 222132352. 1350. 910. 1230. 1 C 0119 3 3 10 31 2254463. 224357315. 1440. 903. 1220. I 11011983 1130 12011983 1231 01311984 0 131 1590796. 2333184 2252359. 225943111. 228291295. 233544154. 1510. 1510. 1470. 1010. 1320. 1110. 1330. 1350. 1430. I 02011984 03011984 04011964 0229 0331 0430 2675326. 2635053. 2752377. 233219980. 233855021. 233637403. 1620. 1610. 1610. 1240. 1160. 1320. 1450. 1430. 1540. 05311934 0531 2376413. 243933321. I 1550. 1240. 1330. I
I 23 Calhio Injection Well a 1 Tota'l Cumulative Injection I Gallons Pressure Start S top Gallon s MoDaYear M oDa Injected Injacted M ax. Min. Ave. 06011984 0630 1338978. 242372793. 1520. 1000. 1100. I 07011984 0731 08011984 0 831 09011985 0 930 0. 0. 0. 242372799. 242372799. 242372799. 930. 950. O. 960. O. O. 970. 530. 0._ 10311934 1031 824985. 243197784 1300. 950. 1030. I 11011984 1130 1634477. 244832261. 1420. 940. 1225. 12011984 1 231 2665795. 247498056. 1460. 1260. 1430. I 01011985 02011985 03011985 0131 0223 0331 2631156. 2437963. 2348133. 250179212. 252617175. 254956105. 1465. 1530. 1500. 1260. 1300. 1190. 1430. 1470. 1425. 04011985 0430 2576547. 257542652. 1510. 1300. 1410. 05011995 0531 2230432. 259823084. 1500. 1240. 1410. 06011985 0630 2568510. 262391594. 1450. 1200. 14J0. 07011985 0731 2053425. 264445019. 1420. 1160. 1330. 08011985 0831 955207. 265430226. 1440. 1020. 1250. I 09011985 0930 3. 265430226. 1040. 340. 930. 10011985 1031 156335. 265556561. 1030. 380. 950. 11011985 1130 2046986. 267613547. I 1300. 1100. 920. 12011985 1231 651501. 263275148. 1310. 920. 1050. (From Weston Geophysical). I I I I I I I I I
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.. . INJECTION WEL.L
- 2 From Weston Geophysical I
, I 5 Figure 12. Injection pressures utilized at Calhio *2. I I I
I 26 I Table 6 VOLUMES OF FLUIDS AND INJECTION PRESSURES FOR CALHIO CHEMICALS WELL #2. I Start Mc3aYear MoDa Stop Calhio Injec tion Well e 2 Total Gallon s Injected Curolative Gallons Injected Injection Pressure M an. Min. Ave. I 01011941 0531 12:1124 1235224 1430. 1050. 1330. 06011981 0530, 1333384. 2555163. 1410. 1093. 1340. 07311981 0731 324317. 2810J85. 1400. 960. 1030. 08311531 0831 95824). 3534417. 1550. 1253. 1430. 01011181 0133 1160575. 5434192. 1550. 1053. 1430.
- 11011991 1130 1331585. 8137541. 155C. 1040. 1440.
i 12311951 1231 204638). 1315403J. 1620. 1160. 15J0. 01311582 0131 57S35. 1J221365. 1220. 160. 1150.
- 02011992 0331 1221573. 11443436. 1620. 1410. 1550.
07011982 0731 711632. 12255368. 1220. 760. 830.
! Of 011182 0 431 628177. 12833245. 11J0. 950. 1030.
l 10311982 1331 345331. 13228524 124C. 76J. 850. l 11011982 1130 816544. 14125223. 1130. 703. 840. 12 J 119 82 1231 633971. 14759207. 1410. 380. 1030. lI 01011133 0131 02011983 0228 530351. 58272. 15310053. 15278333. 1400. 920. 383. 360. 930. 130. 02011983 0331 13375. 15311405. 1240. 900. 950. 04011983 0430 214702. 15606103. 1390. t000. 930. 05011983 0531 1859744 17455352. 1610. 183. 1230. 5 l 36011543 0 63J 07011943 0731 1753295. 457473.- 1922?l43. 19636513. 1600. 1250. 1323. 103. 1330. 950. ! 08011983 0831 3. 1963661'. 150. 980. 920. I 05011983 0930 1C 0119 83 1331 1101113 3 113J 12011983 1231 1918153. 637417. 1139565. 356783. 21634771. 23332138. 24441753. 24713533. 1590. 1!90. 1530. 1610. 893. 960. 143. 180. 1320. 1150. 1130. 1130. 01011984 0131 138363. 24916313. 1 50. 163. 1050. 02011984 0221 57566. 250544!1. 1340. 170. 1C30. 5 03011184 0331 04011534 0433 315503. 249782. 25415151. 257J9742. 1210. 1430. 173. 1050. 930. 1150. 05311984 0531 538333. 26217753. 1380. 1020. 1233. 040119 84 0 63J 1639171. 27936921. 157C. 1233. 1430. 01011984 0731 2210717. 30117523. 1550. 1340. 1520. t 08011984 0331 1939923. 33849723. 1560. 1280. 1510. 01011985 013J 2137683. 35037403. 1530. 1280. 15J0. 1C011984 1J31 1562780. 37630183. 155C. 1103. 1450. I 11011994 1130 12011994 1231 01011985 0131 02011135 0223 1456393. 33701. c. 3. 39057073. 31150774 39150774 31150774 1530. 1330. 1060. 104C. 1123. 1043. 1340. 1030. 1450. 1130. 1030. 1035. , 02011985 0331 1114353. 40255522. 1500. 1340. 13J0. l 04011135 0431 1022383. 41238723. 1620. 1110. 1450. 01011995 0531 273353. 41551773. 1430. 1310. 1150. 08 0115 35 0 63J 3. 4155177J. 1020. 1003. 1010. 01011195 0731 3. 41:51770. 1000. 160. 975. 08311935 0831 41741524 1315. .t 05011945 0130 1C 3119 9 5 13 31 179314. 3. 3. 41741524 41741584 1 10. 910. 943. 123. 340. 10J0. 950. 870. 110115 3 5 113 J 111*.35. 41533373. 1250. 123. 830.
, 1I011135 1231 3. 41932373. 913. 363. 8 30.
W (From Weston Geophysical) I I
27 45 m (148 ft) thick (Resources Services, 1980). The Mt. Simon Formation is overlain by the Shady dolomite, a sandy, medium to coarse grained dolomite, and the Rome Formation, a sandy, fine to medium grained dolomite with thicknesses of = 58 m (189 ft) and z 26 m (86 ft), respectively. About twenty-four meters (80 ft) of the Conasauga Formation, consisting of fine grained sandstones l and limestones with interbedded shales, cap the Rome Formation. Above the Conasauga lies the 31 m (102 ft) thick Maynardville dolomite, consisting of alternating sandstones and dolomites. Highly fractured zones were encountered while drilling the Maynardville in Calhio *2. The Copper Ridge dolomite caps the l Maynardville. Permeability and porosity measurements were obtained from 57 1 samples taken from = 19 m (62 ft) of cored Maynardville dolomite I in Calhio *2 (Table 7). The average permeability was 2.1 mDar-cies and the average porosity was 2.14. 'These values may be too l low as recrystallized calcium chloride from the drilling mud was found to contaminate many of the samples. The maximum permea-l bility obtained was 54.4 mDarcles with a porosity of 2.9% (Resources Services, 1980). The average permeabf.lity and porosity values reported for the Maynardville dolomite and the Mt. Simon Formation from Calhio #1 were 4.2 mDarcies, 84 and 5.5 mDarcles, 8.5% respectively (Ohio EPA, 1985). Nealon (1982) reported per-meabilities of 3 to 6 mDarcies for the Mt. Simon Formation at the I Calhio well sites as determined from drill stem tests. The specific gravity and total dissolved solids (TDS) of I I 9
f. 28 Table 7 I PERMEABILITY AND POROSITY DATA OBTAINED FROM CORED SECTION OF MAYNARDVILLE DOLOMITE (CALHIO #2). I H I P Ihy PCR% PERMEA81UTY suus POROSITY cm OCP1H ITY MILUDADCY$ gI Ab[ RAG [ Amsg % m uf MANUMt PERCINT wo Taopyg 25 50 75 to to 30 I 5480.0-81.2 5482.0-83.1 5483.1-84.0 5484.1-85.1 5485.7-86.7 ( .1-)
.1 1.9
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29 formation fluid from the Maynardville in Calhio #2 was 1.213 with 319,699 ag/ liter and a pH of 5.7. Fluid obtained from the Mt. Simon had a specific gravity of 1.158, a pH of 5.3, and a TDS of 224,896 mg/ liter (Ohio EPA, 1985). Nealon (1982) reported a I specific gravity of 1.218 for formation fluid from the Mt. Simon formation. It is noted that the specific gravities reported for the resident brines are considerably greater than the specific gravity of the fluids injected through the Calhio wells (1.025) (Nealon, 1982). In situ pore pressures measured in Calhio #1 were 170 bars (2472 psi) in the Maynardville dolomite and 187 bars (2716 psi) within the Mt. Simon at depths of 1667 m (5468 ft) and 1807 m (5928 ft), respectively (Ohio EPA, 1985). Calhio well #1 reac'hes a total depth of 1851 m (6072 ft) below ground level with injection intervals in the Maynardville dolomite (1670
- 1716 m) (5480 - 5360 ft) and the Mt. Simon Formation (1807 -
1847 m) (5928 - 6060 ft) (Nealon, 1982). Calhio well #2 reaches l a depth of a 1862 m (6110 ft) below ground level with injection intervals in the Maynardville dolomite (1669 - 1716 m) (5475 - 5630 ft), the Rome Formation (1743 - 1765 m) (5720 - 5790 ft), i and the Mt. Simon Formation (1813 - 1858 m) (5948 - 6096 ft) i (Nealon, 1982). The nell operated by Environmental Brine injects salt water in the interval between approximately 1779 and 1800 m (5838 - 5926 ft) (Ohio Dept. Nat. Res., 1986) All injection intervals were hydraulically fractured. I Instantaneous shut in pressures (IGIP) (top hole, after stimula-l tion) obtained within the Maynardv111e dolomite and Mt. Simon I
30 Formation were 152 bars and 159 bars in Calhlo well #1 (Resources Services, 1986) and 139 bars and 165 bars in Calhio well #2, respectively (Resources Services, 1980). The ISIP measured at the Environmental Brine well site was 114 bars within the injec-tion interval (Ohio Dept. Nat. Res., 1985). Under the conditions of a controlled scientific experiment ISIP is directly related to the minimum horizontal stress (S ) at the test depth. ISIP measured under the prevailing conditions can only be used as an indication of the possible maximum value of S hmin*
- 4. REGIONAL SOLUTION MINING Solution mining of salt deposits has taken place in north-eastern Ohio since the late 1880's. Dunrud and Nevins (1981) list two active and five abandoned operations within approximately 100 km (62 miles) of the epicentral area (Figure 13) (Table 8)
( including a Painesville, Ohio mine listed as possibly abandoned l l around 1977. With the exception of the questioned Painesville mine, the sites listed as active are greater than 75 km (47 miles) from the epicentral area.
- 5. HIGH PRESSURE INJECTION INDUCED SEISMICITY Most cases of fluid injection are not associated with any seismicity. However, in the last decade the high pressure injec-tion of fluids into the earth has been associated with the onset or increase in seismicity at a few sites worldwide. The favored explanation of the mechanism by which these earthquakes are l
triggered (Martin, 1975; Lockner et al., 1982) is the effective I lI _ -
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m M M M M M M M M M M M M M Table 8 DATA PERTAINING TO SOLUTION MINING OF EVAPORITE DEPOSITS IN OHIO nea . -i sedi. e. nefe,eetie. ,ee.ned m .. nef. eesiae mes teien Solet tee toe st t ee Typesel depth Type of toast Istteemed tend eine aseseos seene Ceess y to) to top depeens li, elf ted Seriese Sete et eesf ace ef fected by field er seee of dees et perieb pesied eteested et eveportte se d = dose pot retene emboidense emboidense emboidensel eres and se esse se puedesses some b a bodded see reported velues of outsidense me . esosage fes dete(s) abewe Date F9999CiuG 79
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33 stress theory of Terzaghi as applied by Hubbert and Rubey (1959). In this model, injection increases the pore pressure along exist-ing fractures reducing the frictional strength through reduction of the effective normal stress. If the shear stress along the I fracture is greater than the sum of the frictional resistance and the cohesive strength then slip occurs. An extension to this model involving the transformation of high strength barriers into high stress asperities through aseismic creep ultimately leading to failure has been invoked to explain certain observed features I of injection induced seismicity near oil fields (Pennington and Davis, 1985; Davis, 1985: Pennington et al., 1986). Aseismic creep is postulated to occur in regions of relatively higher pore pressure leading to the formation of high stress asperities in locked regions of relatively lower pore pressure. This model has I been particularly useful in explaining features associated with fluid injection to enhance petroleum recovery where fluid extraction occurs simultaneously. A direct correlation between fluid injection and the trigger-ing of earthquakes was first identified by Evans (1966). This I relationship was based on empirical evidence of the temporal correlation between waste injection at the U.S. Army's Rocky Mountain Arsenal near Denver, Colorado and earthquake activity surrounding the site. In controlled experiments at Rongely 011 Field, Colorado (Raleigh et al., 1976), and near Matsushiro. Japan (Ohtake, 1974), investigators confirmed the suspected link between deep well injection and seismic activity. Seismic acti-I
34 vity has been induced by high pressure fluid injection associated with secondary recovery techniques for petroleum production (e.g., Teng et al., 1973: Rogers and Malkiel. 1979: Harding, 1981: Davis, 1985), solution mining of evaporite deposits (Fletcher and Sykes. 1977: Wong et al.. 1985), and with such projects as fluid stimulation for the hot dry rock geothermal system at Fenton Hill, New Mexico (Pearson, 1581: House and McFarland, 1985). The largest reported events associated with deep well injection and petroleum production are Mz 5.5 (Denver) and M z 5.0 (Cogdell Oil Field). The only documented cases of induced seismicity associated with solution mining occurred at Dale. NY (Fletcher and Sykes, 1977) and in southeastern Utah (Wong et al., 1985). In both instances the largest earthquakes had magnitudes around 1.0. A magnitude 2.7 earthquake (2/73) near Dale. NY was determined by Fletcher and Sykes (1977) to be of tectonic origin. Many instances of injection induced sels-micity have been investigated. Pertinent details of the better documented cases are presented in Table 9 and are described below. Rocky Mountain Arsenal Routine injection of waste fluids at the Rocky Mountain Arsenal well near Denver, Colorado began on March 8, 1962. Fluids were injected into Precambrian crystalline basement at a depth of 3671 m ( 12.044 ft) with a maximum top hole pressure of 72 bars (1050 psi) (Evans. 1966) and average monthly bottom hole pressures ranging to = 415 bars (6020 psi)(Figure 14). Initial I <
35 Table 9 DATA PERTINENT TO INJECTION RELATED SEISMICITY. NOTE Injection pressures are cited either as top hole pressure (THP) or bottom hole pressure (BHP). I Other pertinent pressure related data (e.g., pore pressures (initial - Po; otherwise Pp). hydrofrac data (al, a2, a3), the reported ratio of bottom hole pressure to lithostatic pressure (BHP /LP), etc) are recorded under Other Pressure History. I Hydrological parameters reported for each site include transmis-sivity (T). storativity (S), permeability (k), and coefficient of diffusivity (a). The volumu of fluid injected (gross and net) is reported in cubic meters. I Distances are given in kilometers and injection rates in liters / min. I Time delays are the time lags between injection phases (increases, decreases, etc) and changes in seismicity patterns. Dimensions of the epicentral area defined by the spatial extent of the earthquakes are given in kilometers. The range of earthquake magnitudes (where applicable) and the l maximum magnitude event are described under EQ magnitudes. l Fault plane solutions (where available) are described. I B-values calculated for the periods of study are given under b-values. l l l References References for each item appear in brackets (e.g., [1]) and r e f e r-il l l 5 to the reference list accompanying the table. In those cases described by a single reference this reference is reported with j the case heading and is not repeated. l Unit Conversions l Units in the table are generally those of the SI system. Conversion factors to English units are listed below. l l l 1 bar = 14.504 psi 1 1/ min = 0.264 gallons / min l 1 km = 3280 ft = 0.62 miles 1 m 3 = 264 gallons 1 m= 3.28 ft I
uell Denver (Rocky Nt. Arsenal) Natsushire. Japaa [12] Oslo, NT [3] lajectJoe pas TNP 72 bare [2] TMP 120 bare
/
Nas avg monthly SSP = 14-30 bara Well 831 man TMP 82-78 bare Pressures 435 bare (7) Po a 269 bare (7) Eigh pressure lose at well #11 l Other eve 830 bare [7] 3 separate lajettiene l Level la met! felt et 8 50 14-23. 14-20 bare Calculated Polly (a=0.8) Pressure N! story 0.074 t/ala withis I et 812 a = 113 bare der efter shutdown f71 (42 bare ?NP). 8 e=T/ Sal.08 a 10 cm /e 2 ke 30-300 a e 3:30 -3 3s30 cm 07, 2 mydrological 1 e a 0.5-da10agereg/s 1 Properties T.S free (8l cm
- k. eDarcy reste volume of 3 Fleid 8.2 x 30 m [20] 2883 e Peeped l Depth of well 3.673 km [7] 3.8 km 0.43 km LJ CD 3/62-9/s3 478 1/ala .
tajectlen 10/63-8/44 0 1/ala [7] 120 to 200-300 1/ala 2-3 x avg. rate et Denver Bates 8/64-4/65 171 1/ela 4/65-2/66 307 1/ min h Dist. ace from Ctese to well Well to EQs (alcro eg. set) (7] 2-4 km Nest 5 2 km
*(10/71 - 11/71)
Time Delay 7 mks from start of Imjection. 9.3-4.8 days 2 km e 90 days (omset) Setween lajec- to days (avg. during lajectlen). 4 2-4 km 2 km e 2 days (lajec. halt) l tien & EQs f71 Depth Estemt 4.5-S.S km (7) 1.5-7.5 km 0.3-3.1 km of EOs Epicentral to km x3 km (a60*W sS.S km x 4 km Length a 2.3 km area surroundfar well) f71 alone C-L fault. EQ Magaltudes Nam. S.O. S.25-5.5. 5.1 Mas. 2.8 -1.1 5 N s 0.8 (4/67. 8/67. 11/67) f71 Strike o!!p [7] Strike s!!p. buried Thrust faultlag (mas EQI Fault Plane Solution NSS*W omrellel to C.L. fault b-values 0.80-0.90 during lajecties 2.9-2.1 lbefore. dartsg. 1.1-3.3 f?! efter infeetton) e300 telt EQs [20) Soares of micro EQs. Seismic!ty a 1 eveat/mo prior temarks t 1000s too small to feel. 3250 oveats during to lajection. Smeras after lajection period. lajection (up to 40 eventa/ EQ onset Pp 32 bare above Selsmicity lacreased fol- day). 8/4/71 to 11/11/71 > taltial. [4] lowlag tajections. 800 events. EQs lie along mapped fealt. M 2.7 EQ (2/73) EQs occurred on searby believed to be tectoalc. fault. l .
l dU EU
- m um e well Reagely oil Field. C0 Sleepy nellow Oil Fleid. Los Angelse Seela O!! Fielde N*hreeke flg)
Injertlen TMP =m3 bara [4] Tur 58 bare (Lemelag Group) I rressures Tur 22 pel (seegen SS Group) I (4/42-8/84) (Menteen) [38) l Po a 170 boro, el.s2.e3 l Otaer S$2. 427. 384 bare [13] l I Pressure man. Pp (1987)=290 bere. Nistory Some melle respond rapidly l to chenees la other welle. ] i Hydrelegical k (weber Ssl,= 1 muercy (13) 2.9 Darcles (Reagan SS) Propertsas T-15-30 m 10* aDercy-ce [1e] l . Volume of Through 6/70 Fluid Tetelm9.7 e g0'3 e Total e 2. Sal 0 0 m3 Pumped Net =2.3 a 10 e [4.9] Met m -e.9x10 0 3m Depth lajection et 1050-!!30 m and of well = 2 km [4] IISC 1170 a [17] 914-1524 a V,a lajection a 17.660 1/ela es of 1964 Rates (98 welle) [9] DIstante from Close to welle [33] Close to we!! [17.18] < 1 -a S km well to EQs flee Delay EQs stopped I day-few see. Floeding began 1954. Between lajec- following lajection Noeltering began 2/71. tion & Eos decrease. 1931 Depth Estent 2 km (near melle) Noet C 4 km [38] 2-16 km of EOs 3-5 kan t su of wells) 1831 feest > 5 kel Epicentre! Width =lke. length =4 km (13l Area EQ Magaltedes Suares of alcro EQe. Mez. N=2.9 [17] Naz. Me 3.2 Man. N=3.1 fl31 f3/79-3/801 (2/71-12/71) Fault Plane Strike ally (13) Reverse. morse! [17.18) Oblique ally Solution l b-values 0.43-0.96 [13) Remarks $ wares. [33] la EQs (3/79-3/80) [17] 47 EQs (0.9 5 N 5 3.2) 10/69-5/74 > 1400 EQs recorded 2/8/71-12/31/11. EQs perellel to aspped a 250 evente (4/82-8/84) [18) 14 oil fleide la Basis. surface realt. EQ onset preneure m257 bara Background seteelcity le high.
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** 3 3 to ** to D W me W E e8 O44 e S 90 == 3 JS b e b e9 Se eg& A e G e e e aO e g es ee e to es ee e e as to a 3 es a ee 3 ee ed no e3g ea w ue me g e e me % g ay a yg me g g a eig es e ee a es g a se e ,3 y se p g
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g g g M M M M M M "l R fl fl T' l _f 1 .f~~l. [ ' Well Calblo welle 83 and 82 Lake Cosatv. Ohio enetronmental Srles Sers. Lake County. Ohjo 1901 References I* "'I' II'* Injectlem Men. TMP = 312 bars mes. Tur = 55 bere. * '*"* II'* Pressures (11.21] Avg. daily pressuse p
- 4. Gibbe et at. (8973)
* *' "E I' Nydrefrac. lastantaneone shut Nydrofrec. imetantaneous shut la pressures 184 bara (1779-
* '# "E ' * * '
Other la pressures 152 bara (1870- 7. Nealy et at. (1988) Pressure !?IS a). 159 bare (1807-1847 al. 1806 m) 8. Releh and Bredehoeft (1981) N! story 139 bare (1889-1710 m). 165 bare 9. Museon (1970) (1813-1858 al f14.151 30. Ohio Department of Natural Resources (1988)
- o av oteen a to eC om gency (1985)
Nydrological k
E
= eDarcy range * *
- II '
Properties [14] I *
- 0 (10's of aDarcy in fractures) 3,_ ,, ,*II ,,',, vic
- a ( 980)
* *"'*** '#' *** II I Volume of ' * *I'#' "" "I
- I ' I Fluid Cathio 1 1.02 s 10 8 3
,3 3089 m 3 '
Pumped Calhto 2 1.59 a 10 m (10/85-12/85) I g ,' ,*, * 'g*" ,",I , I I * *
* "E *
- I I Depth Calblo 1 1851 km l33] * ** '" ** ** #
of Well Calh'a 2 1882 km (14] = 1820 m 21. Weston Geophrelcel,pers. come. (1988) u M3 Injectica 201 246. or 326 1/ala. [11) Avg. 1023 m 3/ .month Sates Dietence from weii to cos a li um Tlee Delay Calbte 1 s 37 ,e. - Betueen imjec- Calhlo 2 m 4 yrs. m 3 me. tion & f0s Depth Estent Main sheCk 5-8 km of EOs Aftershocks 3-8 km Epicentral Tight cluster Area EQ Magattudes Malm shock a, 3.0 Aftershocks Tist -0.1, 5 N < 2.5 Fault Plane strike slip Solution b-values e 0.3 - 0.8 Remarke No injection prior to 10/85.
E 40 pore pressures at this depth were estimated to be around 269 bars (z 3900 psi) (Healy et al., 1968). Hsieh and Bredehoeft (1981) [ calculated that a 32 bar (= 460 psi) increase in pore pressure was required to trigger seismicity. Approximately 6.2 x 10 5 ,3 F (= 164 million gallons) of fluid were injected at average rates to 478 liters / min (126 gal / min) before the well ceased operation in February, 1966 (van Poollen and Hoover, 1970). Seismicity began approximately seven weeks following the start of injection and was correlated with injection volume at an average time lag of ten days (Figure 15). High quality hypocen-I ters (January-February, 1966) were located at depths of 4.5 to 5.5 km (2.8 - 3.4 miles) within an epicentral area approximately 10 km long by 3 km wide (6.2 x 1.9 miles) surrounding the well and striking N60 W (Figure 16). Focal mechanism solutions indi-cated right lateral strike slip faulting on a northwest oriented plane. Approximately 100 events were felt and thousands too small to be felt were recorded (van Poollen and Hoover, 1970). B-values, a measure of the magnitude distribution of an earthquake sequence, ranged from 0.80 to 0.90 (Healy et al., 1968). The larger the absolute value of a b-value the greater the ratio of small magnitude events to larger ones. The largest events of magnitudes 5.0, 5.3, and 5.1 occurred in 1967 (4/10, 8/9. and 11/26, respectively). An epicentral area similar to that outlined by the events of January-February, 1966 (Figure 16) was defined by the aftershocks of the 8/9/67 event and the ,I 4/10/67 event (Healy el al., 1968). I I
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B I Figure 14. Average monthly bottom hole pressures at Rocky Mt. I Arsenal well and comparison with seismicity. 5
42 I jI 1 1 l 80 R 70 - EARTHQUAKE FREQUENCY a 0 60 =
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lN/ECTED- - J M M J S N J 'M M J S N J M 'M J S N J f.f '.i 'J N A A A U E O A A A U E O A A A U E O A A A U 0 l N R Y L P V N R Y L P V N R Y L P V N. R Y L . V 1962 1963 1964 19G5 (From Evans,1966) I I I Pigure 15. Correlation between seismic activity and volume of injected fluid at the Rocky Mt. Arsenal well. I I I
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E ,# : ..,. r 7 ( R.M.A."T w.n - , ROCKY M O U N T AIN ARSENAL I . Eartnqueme Epicenter 4sm ave. i DENVER w Afterineos of 10 April 1967 earthquake A I r After of
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[ ROCKY uoVNTAIN ARSENAL i i I
.s .n .m DENVER (From Healy et al.,1968)
Figure 16. Epicentral area surrounding the Rocky Mt. Arsenal during January-February 1966.
44 i Matsushiro. Japan One of the few experiments in earthquake control occurred at 3 Matsushiro, Japan. In 1970, 2883 m (0.76 million gallons) of water were injected at a depth of 1800 m (5905 ft) near the Matsushiro fault zone using top hole pressures of 14 to 50 bars (203 - 725 psi) and rates of 120 to 300 liters / min (32 - 79 { gal / min). Permeabilities along the fault were estimated to range from 10 to 100 mDarcles (Ohtake, 1974). During the two month duration of the experiment, several hundred events were triggered within 4 km (2.5 miles) of the { well, at depths ranging from approximately 1.5 km to 7.5 km (0.93
- 4.7 miles). Seismicity increased following injection with a
~ delay of 5 to 9 days at distances of 2 to 4 km (1.2 - 2.5 miles). Activity was significantly greater during the injection than either before or after as seen in the center panel of Figure 17. B-values ranged from 1.9 - 2.1 before, during, and after the injections. The maximum magnitude for the sequence of earthquakes was 2.8. Strike slip focal mechanism solutions were obtained (Ohtake, 1974). Penton Hill. New Mexico Several hundred microcarthquakes of magnitudes -4 to -2 occurred within 0.4 km (0.25 miles) of a 3050 m (10,000 ft) borehole during the injection of 460,000 liters (121.520 gal) of fluid in a 5.5 hour hydraulic stimulation at the hot dry rock geothermal site. These shear failure events were located up to I I
m k 45 [ E h 3Mh(h.S!('Y, A 8
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01/24/70 03/09/70 03/31/70 l (From Ohtake,1974) P I I Figure 17. Map view (top) and vertical cross sections (bottom) showing locations of events triggered by deep well injection at Matsushiro, Japan. The hypocenters in the depth sections are projected to the vertical I plane through points AB. I I
I 46 30 m (98 ft) away from the expanding hydraulic fracture (Pearson, 1981) (Figure 18). House and McFarland (1985) describe the results of another hydraulic fracturing experiment at the Pen ton 11111 site. Water 3 (7600 m . 2.0 million gallons) injected at a depth of 3400 m (11,150 ft) at a rate of approximately 1.6 m / 3 min (423 gal / min) triggered 850 seismic events in the vicinity of the well. SEISMICITY CORRELATED WITH PETROLEUM OPERATIONS The association of seismicity with fluid injection for secon-dary petroleum recovery has been established, but few cases are l well documented. Shurbet (1969) alludes to an increase in sels-micity associated with petroleum production and water flooding projects in the Permian Basin near Kermit. Texas. Milne (1970) I studied the a b 5.1 Snipe Lake. Alberta, Canada, earthquake of March 8, 1970, and noted the event occurred in an area where prior seismicity had not been reported. Within 80 km (50 miles) of the epicenter were located 646 oil or gas wells. Injection had been employed at 56 wells beginning six years earlier. The I net result of which was a reservoir pressure somewhat below the virgin reservoir pressure. In a later review of induced seismi-city Milne and Berry (1976) described the event as appearing "to be the only known Canadian example of an earthquake probably induced by water injection into a producing field". Insufficient details were given of the seismicity or well locations, pumping I " " " " "" " " " " " " ' ' "'""" " '"- """"" " '"" I I
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MS. 270 mm. (From Pearson,1981) i I Figure 18. Microseismic events located near hydraulic fracturing site at Fenton Hill, NM and projected to (a) a hori-i zontal plane, (b) a vertical plane perpendicular to the hydraulic fracture plane, and (c) a vertical plane parallel to the hydraulic fracture plane with elapsed times since initiation of injection. I I
l u I 48 L this event was injection related. However, several indisputable cases of induced seismicity have been associated with water flooding projects. L Rangely Oil Field, Colorado The most famous and best documented case of injection in-duced seismicity related to petroleum production occurred in the Rangely 011 Field. Investigators were able to control the frequency of seismic activity through variations in the reservoir fluid pressure. Secondary water flooding within the Rangely 011 Field began in late 1957 at a depth of approximately 2 km (6700 ft). Through f 7 3 June, 1970, 9.7 x 10 m (25,690 million gallons) of water were injected at a top hole pressure of approximately 83 bars (m 1200 psi) representing a net increase of 2.3 x 10 6 ,3 (596 million gallons) (Munson, 1970; Gibbs et al., 1973) after petroleum withdrawal (Figure 19). Water was being injected at an average rate of 17.660 liters / min (4666 gal / min) as of 1964 (Munson, l 1970). Pressures in the reservoir had risen above the virgin reservoir pressure of 170 bars (m 2470 psi) by 1962 and were as high as 290 bars (m 4200 psi) by 1967. Hydraulic fracture data I obtained at a 2 km (m 6700 ft) yielded stress values of S Haax (=a g) 552 bars, a 427 bars, and S 314
=
2 (vertical) = hmin I"#3) = bars (m 8000, 6200, 4550 pai, respectively). Using these stres-ses, Raleigh el al. (1976) calculated a critical pore pressure of 257 bars (m 3730 psi) for the triggering of earthquakes. Seismicity was first located at Rangely 011 Field upon I I
F 49 L s- { [ c g i I ka- ' { s t - 550 E 1, - ! 8 9 I ' a40 [' I $ C
-as a 1, ou '.o,'..w' s.',,. ' a u ' ,... ' .,n ' .. u ' ,
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--- n u.o 4 rivio l- rivia J 6 AleC tt0 A withdrawal snieCiton (From Raleigh. et al.,1976)
Figure 19. Seismicity correlated with injection volume and pressures at Rangely 011 Field, CO. Stippled bars in I the bottom figure indicate events located within 1 km of the injection wells.
L 50 installation of the Uinta Basin Observatory in 1962. Instrumen-tal records were not available prior to this time (Raleigh et al., 1976), Between October, 1969, and November, 1970, over 900 earthquakes were accurately located within the Rangely fleid, 367 l of which occurred within 1 km (0.6 alles) of the bottom of the injection wells. Seismicity appeared to be correlated with in-jection volume and pressures. The earthquakes tended to occur as l swarms, sometimes followed by main shock - aftershock sequences (Figure 19). Hypocenters clustered in two groups, one located at l l' depths of 2 to 2.5 km (1.2 - 1.6 miles) (near the wells and within the injection zone) and the second group clustered at depths between 3 and 5 km (1.9 - 3.7 miles). Seismicity was l concentrated along a vertical zone approximately 1 km wide by 4 km long (0.6 x 2.5 miles), and parallel to a mapped fault (Figure , 1 20). Focal mechanism solutions indicated predominantly right lateral strike slip faulting on northeast trending planes plunging 10* - 20* to the southwest. B-values ranged from 0.81 f to 0.96 during the study period. The maximum magnitude recorded at Rangely 011 Field was 3.1 (Raleigh et al., 1976). Sleepy llollow 011 Field. Nebraska Water injection at bottom hole pressures to approximately l 172 bars (m 2495 pal) within the Lansing Group (1050 to 1170 m) (3440 - 3840 ft) and 142 bars (2055 psi) with the Sleepy Hollow sandstone (1150 - 1170 m) (3770 - 3840 ft) resulted in the trig-gering of earthquakes within the Sleepy llollow 011 Field. The I I
51 2' ~
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0n 1 ini.ca a b ..n, ..n. ..n. i. 2- s, f* g h ------- * (055 -- --- - -- - - o5 1 s. ~,+ . ..: ,,',- w ((,- [. , ,yr , , . . .,3- .<.i. 4. - 4 ..p. y l ,. Oct 1969 Oct 1970 Nov 1970 Jul 1971 , Aug 1971 Oct 1971 0 -. - - injec . ion , injection i injection weHS , wells wells
- i. .
I 4 ~ 2-Sff -- - ,- - - - ' phf@---I gi-------- ~ 3 g.W- :pW .. ., gy-E -- 1- ., < a , G*;;, 4,, 4 . + .. Nov 1971 Aug 1972 , Sep 1972 . May 1973 Jun 1973 May 1974 (From Raleigh et al.,1976) Figure 20. Rangely seismicity as a function of time. (a) Bottom hole pressure contours are in bars. (b) Vertical sections trend N-S. 52 . earthquakes were located near the well and most w e. r e shallower than 2 km (1.2 miles). Sixteen events were located between March, g a 1979, and March, 1980. The maximum magnitude recorded was 2.9 (Rothe and Lui, 1985). An additional 250 events were recorded within the active field between April, 1982, and June, 1984 (Steeples, 1985) (Figure 21 and 22) at a time when top hole pressures ranged to z56 bars (810 psi). I Los Angeles Basin. California Fourteen oil fields operate within the Los Angeles Basin where water flooding began in 1954. Total fluid injection as of 1970 was 2.5 x 10 8 ,3 (67,300 million gallons) with a net injec-tion of -6.9 x 10 0 m 3 (-1810 million gallons) at depths of approximately 910 to 1520 m (2990 - 4990 ft). Earthquakes with depths ranging to 16 km (9.9 miles) with the majority deeper than 5 km (3.1 alles) were located predomi-I nantly along the Newport-Inglewood fault. Activity appears to be correlated with injection volume from nearby wells (Figure 23) Approximately 50 events with magnitudes (Mg) ranging to 3.2 occurred in the basin between February 6, 1971, and December 31, 1971. A single event focal mechanism solution indicated predomi-I nantly oblique slip motion (Teng et al., 1973). I Cordell Oil Field. Texas Water flooding between 1952 and 1982 resulted in yearly net injections between -1.6 x 10 6 ,3 and 4.0 x 10 6 ,3 (-420 to 1050 million gallons) with top hole pressures to approximately 220 I I F 53 L [ E [ [ l 70 . b= e_- 5 O Lonsan9 ~ sc S b vn- - ! = bm s
- 4 30 -
40 g g . "x c--~ - r~ =} \* so _ = a 6F T Lc l0 A M J J A S O N 0lJ F M A M J J A 5 0 N 0 f f M A M J l982 3983 3984 (From Steeples,1985) I I I I Figure 21. Average monthly seismicity and pressures for the Lansing Group and Reagan sandstone within the Sleepy Hollow 011 Field. NE. I I l l l 54 l l 1
- I I
i - 0 C. b : 4 I : ~ i p T 0 0 o o 00 d e %oh0 a # o gag o od n I O gg D pg> ooa ao i y 4 i no$ a o o l 0 0 0 o o o 3 o o o o M g og O I 8 o o i 3 o I o e o 1 I > ' C. <i (D 0 - % m , n e s e a o - % m , n e s e a o ~ (HM) HLd30 (HM) Hid30 v .c Q e C 4 .f*1 3 9 *j g a <r R :'*U g... o OO 'I"'}s....I***1 m A * -c 3* g' {,# 0 0 di e , ~ L; l "g, > O O . .s a we e # C s..'QJTD p ~ ":J't..: .I O G3 y - U " E I O O aN O O E ** O b MM x< - g- , I E l . M E O 7 3 Da E ? I I I I I 55 I I 20 ' ' ' i i i i i , , , I s IS - 2 w I > W g 10 - I 5 in 2 3 2 5 . i9 71 I o e i i i i JAN FEB .YAR AFRIL MAY JU.NE JULY AUG SEPT OCT NOV OEC g ' ' ' ' i i i i , , I e lO - i t 197 528 ~ e a$ I 6 - o e I 5 5 2 w t 4 - I u z " 3 .d ? I (From Tong et al.,1973) I l Pigure 23. Correlation of seismic activity with net fluid W injection at the Inglewood Oil Field, CA. I 56 bars (3190 psi). Injection has taken place at depths of approxi-mately 2071 m (6796 ft) (Harding et al., 1978; Davis, 1985). Over 50 earthquakes have been attributed to the Cogdell field since 1977 (Figure 24). I Accurate locations for the pegiod (May, 1979 - March, 1980) indicate seismicity was shallow (0.1 - 6.5 km) (.0.6 - 4.0 miles) with 90% of the events at depths less than 3 km (1.9 miles) (Davis, 1985). The maximum magnitude event attributed to Cogdell was a 4.7 (Harding, 1981) (Mg=4.75 - 5.0 b (Harding et al., 1978). I Permian Basin. Texas Seismicity has been associated with several fields in the Central Basin Platform of the Permian Basin, Texas (Figure 25) where water flooding continues with top hole pressures in excess of 138 bars (2000 psi). Over 400 earthquakes with magnitudes ranging from -0.3 to 3.9, many occurring in swarms, were cata-logued by Rogers and Malkiel (1979) for the period December, 1975, through July, 1 9 7 ,7 . Depths generally ranged from 0 to approximately 5 km (3.1 miles), but few locations were of a quality better than C. B-values calculated for the period were 1.04 - 1.28. Focal mechanism solutions obtained from Keystone I field data indicated predominantly normal faulting (Orr and Keller, 1981; Rogers and Malkiel, 1979). I SOLUTION MINING OF EVAPORITE DEPOSITS Dunrud and Nevins (1981) cataloged 107 producing and aban-doned solution mining projects in the United States. Documented I I - - - - I 57 I 15 1.0 . . . s"V"% I' o- +- -e .OJ O E sta menes . .,3 W * !!t D/LP tWPAP frtheates , ' ;< I 5 0.4 02 I l i , g - M ' ' O.0 I 52 54 56 56 60 62 64 66 66 70 72 74 76 78 80 82 YE.AA 15 - - 30 I = 0 t rin res , [ 20 I 14rreer 10 - --0 l4et Fluid Injected o ( 3 1 N vorwn /y., O / 10 I Erthwakes 5-N n $ M136L5 o E ,o 7 , p !' 0 0 -10 52 54 56 56 60 62 64 66 66 70 72 74 76 78 80 82 YEAR (From Davis,1985) Figure 24. Comparison of seismicity,at Cogdell Oil Field with the net volume of injected fluids and the ratio of the bottom hole pressure (BHP) to the lithostatic pressure (LP). I . I z 58 1or toy 0 q, g o , A g o G P Q Q 0 g a J .^t }% DOLLARHIDI p 4m J g 37 - - - 3,. ? 9 [ Uep O f$k'yls"$'\Q'"* O + I O @ fig'gi?- Ptcos[ 0 l % 0 % ! d @ Pd ? ? $ I ,,, ? '? e [] b d k,,, nor I0r (From Rogers and Malklel,1979) I I Figure 25. Locations of earthquakes associated with oil = production within the Central Basin Platform of the Permian Basin. Texas. I I 59 histories of induced seismicity surrounding these projects are rare. In one of the few documented cases of seismicity corre-lated with solution mining Wong et al. (1985) reported shallow (<2 km, 1.2 miles) seismicity (M g generally < 1) at a potash mine in southeastern Utah. Solution mining has taken place in New York and Ohio since the late 1800's. Both these states have experienced low level seismicity in historical time. Accurate correlation of sels-micity with solution mining in such areas is not possible without accurate earthquake locations and injection histories. Informa-tion of a sufficient quality is not generally available. In a detailed study Pletcher and Sykes (1977) were able to correlate seismic activity with mining at a site in western New York. Attica - Dale. Western New York Salt mining with top hole pressures to 120 bars (1740 psi) and injection rates two to three times those utilized at the Rocky Mountain Arsenal has been spatially and temporally associated with microseismic activity in the Attica - Dale area of western New York. Six injection wells were employed with depths of approximately 430 m (1410 ft). The well operating at the time of the study conducted by Fletcher and Sykes (1977) was located approximately 50 m (164 ft) from the trace of the Clarendon - Linders fault. Seismicity occurred in swarms with up to 80 events per day. More than 800 microcarthquakes (magnitudes ranging from -1.1 to 0.8) were located close to the operating wells between August 4 I I 60 I and November 11, 1971 (Figure 26). B-values ranged from 1.1 - 1.5. The largest event of the sequence occurred 0.6 km below the bottom of the injection well. The low level of background activity (less than one event per month) prior to high pressure injection, the dramatic increase in activity following injection, the spa-I tial association of seismicity with the injection, and the rapid cessation of activity upon decrease in injection pressure below 52 - 55 bars (750 - 800 psi) strongly suggest this activity was injection induced. An earthquake of magnitude 2.7 which occurred about 7 km west of brine field in 1973 was determined to be unrelated to the injection by Fletcher and Sykes (1977). A predominantly thrust faulting focal mechanism solution was obtained indicating motion along a plane parallel to the Clarendon - Linden fault.
SUMMARY
Summarizing, seismic activity has been triggered by a variety of fluid injection projects (Table 9). The correlation between earthquakes and injection can only be established through the spatial and temporal association of accurately located events with known injection histories. Of the cases for which adequate information exists, several similarities are apparent. Earth-quakes are generally located near the injection well and often along nearby faults. Swarms with large numbers of low magnitude events are common. Accordingly, b-values are around 1.0 and sometimes greater than 1.0, often higher than those obtained for I I
i t I ' PUMPS OFF ; P#*N I s g *c 0
, PRES 5URE or
- n wELL Y Oct S-64
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o IS 40 25 30 $ o o 20 25 30 4 NOV.1971 DEC. JAN.1972 (From Fletcher and Sykes,1977) I Figure 26. Seismicity correlated with injection pressures during solution mining near Dale. NY. I I I
62 tectonic sequences in the region (as noted by Gupta and Rastogi, 1976) for tectonic and induced sequences in India. Documented cases of injection induced seismicity exist, but in many in-stances insufficient information is available to establish a valid correlation, particularly in tectonically active regions. The injection at the Calhio Chemicals site is similar to sites where seismicity has been correlated with injections in several ways. The volume of fluids injected is within the range reported at other sites as are the observed formation permeabili-ties (mDarcy range). Injection pressures are greater than at many other sites and injection rates are comparable. Considering the distance involved, the time delay between injection and the Leroy earthquakes is theoretically possible. However, in comparing the seismicity observed at Leroy with activity associated with injection several important differences are noteable. The distance between the injection point and the initial hypocenters is much greater than reported in any other instance. The time delay between the start of injection and the onset of seismicity, though plausible, is much longer than in any other case. The activity at Leroy was tightly clustered in both time and space. Injection induced seismicity is characteristi-cally more diffuse temporally and spatially with many more small magnitude events than occurred at Leroy. Accordingly, the b-value obtained for the Leroy sequence (= 0.5 - 0.6) is much lower than values characteristic of induced seismicity. Though the physical parameters related to the Calhlo injections are I I
63 similar to those in cases of injection related seismicity, the seismicity patterns observed at Leroy are quite different from such activity.
- 6. REGIONAL TECTONIC EARTHQUAKES Several earthquakes with magnitudes greater than 4.0 have occurred in the eastern United States and adjacent Canadian pro"inces since the mid 1960's. These earthquake sequences of tectonic origin (Figure 27) (Table 10) are quite similar in several respects.
Such earthquakes are temporally and spatially diffuse. How-ever, the historical record often contains reference to similar events. Hypocenters calculated for these events are generally deeper than 5 km. Associated aftershocks are usually few in number and often tightly clustered. Only in three instances were more than 25 aftershocks recorded. Accordingly, b-values asso-l ( clated with these sequences are predominantly less than or equal to 1.0. These characteristics contrast sharply with the similar-ities observed in instances of injection induced seismicity pre-viously described, particularly in the small numbers of observed shocks with relatively greater numbers'of larger magnitude events. l Temporal and spatial patterns of seismicity associated with l the Leroy, Ohio sequence are quite similar to other tectonic sequences. Only 13 tightly clustered aftershocks were recorded 2 (through 4/15/86) with an epicentral area of al km (=0.4 miles 2) and a depth range of 3 to 6 km (= 1.9 - 3.7 miles) (main shock = I
W M M M M M M M M M M M M M M M M M M 1 Cunningham, V A ' 2 Dixfield, ME 15 3 La ncaster, P A 1 13 "' 4 Gaza, NH g 5 B a th, M E 2 6 C go 4 a Mir amic hi, N.B. L i l
# L e 5 7 Goednow, NY 7],
8 Sharpsburg, KY t t
- I4 [
-II 9 St. Dona t, Quebec ]Fj I 3 10 North Gower, Ontario 11 Ardsley, NY \
'"#' + 0%
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- 12. Quebec-ME border y, 13 Maniwaki, Quebec 9 [# 8 1 g 14 Attica, N Y 15 ,
St-fidele, Queb e c 18 16 5. Central Illinois , j7 17 La f ayette, G A M A GNITUD E 18 Knoxville, TN t e 4.0 - 4.4. e 4.5 - 4.9' ' e 5.0 - 5.4-P 4 5.5 - 5.9
-{ 30* N i
80*W 1 Figure 27. Locations of eastern U.S. tectonic earthquakes with M2 4.0 which has occurred since the mid 1960's.
M M M M M M M M M M M - M M Table 10. DATA PERTINENT TO RECENT EASTERN U.'S. EARTHQUAKE SEQUENCES OF TECTONIC ORIGIN EQ Attica. NY Date 1/1/88 EQ Attica. NY Date 6/12/07 EQ 3. Central Illinois Date 11/0/68 Loc. 42.8'N 78.2*N O.7. 13624 Loc. 42.9* 78.Z* O.T. 19:09 Loc. 37.95'N 88.48'N O.7. 17:01 Magnitudels) a NNI, Negnitude(s) a v1 Magnitude (s) a b*6*s b 4.s [35] WI b'4*0 !IOI NNI m NNIo YII IIII Pocal 19 km [33] Depth 2-3 km [18] 2-3 km [10] 23 km [17] (Revleleh waveel (Revleich waveel 25 km f341 Faultlnc Reverse a rt. lateral on NNE Reverse a rt. lateral on NNE Reverte (P-eate EMI plane (P-aale ENE) plane (P-exto ENE) [34] strike dl2. strike dl2, strike d12. Ist andal: 120' 00*S 320' 60*$ N0l*W 47's [le] [let 2nd nodel: 020' 70*E 020' 70*E NIS*E 45'N Rupture Length Equivalent Radius Selsaic Noment 2.1 x 10 22 dyne-ce [18] 1.5 a 10 22 dyne-cm [18] 9.7 a 10 23 dyne-cm [17] (N 1.3 x 10 dyne-ce [35] 8.0 m to dyme-cm l351 Stress Drop Felt Aree 1.484.000 km 2 g33y Foreshocks Aftershocks Depth Range Number Duration b-values 1.0 [20l 1.0 [20] Nax. Nietoric Vill (1929) Will (1929) Earthquake Geology Several km of gently dipplag Several km of gently dipping Silurlan and Devonian sedir Silurian and Devonian sedimen-mentary rocks overlie Gren- tary rocks overlie Grenville ville basement. basement.
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EQ St.Donat. Quebec Date 2/18/78 EQ Bath. ME Date 4/38/79 EQ St-Fidele. Quebec Date S/39/79 Loc. 46.32 74.11 0.T. 14:48 Loc. 43.93*N 69.80*N O.7. 02:34 Loc. 47.67*N 09.90*W 0.T. 22:49 l Magnitude (s) a bLg * **I ""I o V Magnitude (s) a bLt
=4.0 MMI, V [23] Magnitude (s) a bLg=5.0 MMI, W l Foral 7 t 3 km (5 e e km Pa + Sa) 30
- 2 km (preferred-after-Depth (8-10 km sP + pP) [19] 4 km [6] 8.7 km [8] shocks) (15]
6-11 km (surface unvest Faultlag Reverse (P-axis WSW) Reverse (P-aute EW) Reverse / thrust (15] strike dig, strike (12_ 11gjk e dj g, N20*W 40*NE N-S 45'E 046* 76*SE (preferred) let nodal: [19] (23] (Rake *3tt*) 2nd nodel N20*W 50*SW N-S 45*w 353* 43' (Rake *200*l Rupture 2 Length al km (main + aftershocks) Aftershock eres*2.3-4.7 km f151 Equivalent Avg. disteCatton*12 cm f151 Radius Se t saic Moment 0.8 x 10 22 dyne-cm (19] 1.3-3.7 0.7 a 10 23 e dyne-ce Stress Drop e50 bars (15] Felt 150 km from epicenter Felt e Aren 70.000 km 2 (19] 55.000 km 2 1231 fl51 Foreshocks Man. M=3.0 0.4 M ggggy -3.0 m gLg bLg =3.4 Aftershocks Mas, a Aftershocks do not [19] [8] correlate ulth nodal planes or lie along a stagle plane. [15] Depth Range 7 km , 3-7 km 9.5 t I km Number 3 19 lufthin 90 days) Il 5 days 6 days Duration b-values 1.04 (EPRI/RAI Seismic .84 (New England) [9] 0.72 (histortral + Source Zone) f241 Instrumental EOs) ISI Man. Historic M = 5.0 124] 5.5 as 12/10/1940 Earthquake OssTypee. NH M e 7 (1925) [36] Geology Region with many St. Laurence Rift tage uncertain). Precambriaa. Grenville Paleozoic faults. Logan's Line (inferred suture) Province. 1.1 b y. old separates Precambrian platform orogenic belt. (NW) from Paleosolc mappe structurce (SE). Charlevoix meteorite tapact crater, e 9
QM M M MW _C
}
EQ Sharpehurg. KY Date 7/27/80 EQ Niremacht. N. Brunaulck Date 1/8/82 EQ Niraatch!. N.8runsulck Date 1/11/82 Loc. 34.17'N 83.81*W 0.7. 18:52 Loc. 47.00*N 88.8*W 0.7. 12:53 Loc. 47.00 88.8 0.7. 21:43 MMI, Magnitude (s) a ""3 e y-vl Magnitude (s) a MMI, Macultude(s) a b =5.2 b"8*7 b=6.4 (MEI51 Focal 8 km INE15) Depth 15 km [23] 7 2 3 km [40] 7 km (40] 12 km (181 faftershocks. surface wavest Faulting P-axis EW Reverse Reverse strike 412_ strike d12. etrike (12. Ist nodal: N30*E 50*SE (preferred) 185* 50*W (fault plane) 332' 48'E (fault plane) (rt, lateral s.o.) (18] (Rake = 120*) (Rake = 58*) [40] 2nd model: N60*w vertical 332' 48*g [40] Nupture Length = 8 km Length = 4.5 - 6.5 km I.ength Width = 4 km 2 Width = 4 km 2 (40] Aftershock aren=30-50 km Area = 18-28 km Equivalent 25-37 cm Radius Distcention*2.0-3.4 cm favr. dislocation) f401 Ch 24 00 Selselr Moment 4.3 x 10 23 dyne-cm 2.2 2 0.7 s 10 dyne-cm [40] Stress Drop 2.8-8 bars 35-70 bare Felt 382.000 km 2 l Area 670.000 km 2 [21] 880.$00 km 2 [121 f121 Foresharks Long and complex sequence. See N!ramicht. Neu Aftershorks Max. a bLg =2.2 4 evente N 2 4.5 Mas, a =b 5.4 8tunsulck (1/8/82) Thle is the largest (18] b-value = 0.8 [40] aftershock of the sequence. Depth Range 1-14 km suost al2 kas Number < 70 800 events N 2 3.0 Duration el me. (through 8/30/82) b-values 0.88 [20] 3.07 (regional) (24] 0.84 (New England) ISI Max. Historic This EQ (7/27/80). This EQ (1/8/82). Earthquake Geology Hypocenter in Precambrian Appalachtaa orogenic belt. basement near or within Devonian Plutone l sone of Grenv!!!e Front and in the East Continent Regional strees = EW compreselon. Gravity Nigh and old rift zone.
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Lancaster. PA Date 4/23/84 EQ Canninghne. VA Date 8/17/84 EQ North Gover. Ontario Date 10/13/03 EQ Loc. 39.92*N 78.30*W 0.7. 20:38 Loc. 37.87'N 78.32*w 0.7. 18:05 Loc, og,10*N 75.75'W 0.7. 04:30 Magnitude (s) o btg ***I ""I o V Magnitude (s) e g =4.1 MM I, V- VI [25) Magnitude (s) M, . 4.0 MMS, V Focal 12 km (eftershocks) Depth [38] 4.5 km (aftershocks) [29] 8.2 2 3.7 km (7) Faulting Thrust (P-astealS4*) Reverse 8 rt. lat. on east .P aute ESE dipping plane (P-aals ENE) [7] strike d12. Strike djgt strike- 112. 82*E (preferred) N25*W 39*NE let nodal: 071* 75* 010' [29] (Rake =tS* jeft-lat. s.o.) (Rake =98*) $$8*W 78'NW 223* I?* (preferred) 188* 80*5W 2nd nodal: (Rake-348* rirht-reversel fnske.83*1 f3el Nuptur,e small (38) 3 km (map view - NNE tread) Length 4-5 km depth (29] . Equivalent Displacement =0.5 cm Pedius f381 Selsmic Moment 2a 10 23 dyne-ce [14.38] -J Stress Drop 30 bars (static) o Felt 2 Area 80.000 km 2 f38] =98.000 km 2 f251 30.000 km g,y 1 (4/19/04) Foreshocks a bLg= .0 [25.29] None [7] Aftershocks Mas, a =1.7 10 well-recorded none [7] (1.29] [38] Depth Range 4-5 km Number 3 (within I week) >10 (10 day survey) Duration b-values 3.04 (regional) [24] 0.98 (regional) (24) 0.93 (Central VA Selsete tone-EPRIl 1241 Mas. Historic M = 5.0 [24] Thle EQ (4/23/84) Earthquake Next largest M*4.3 (1889) VI 11/02 8852 fil VI 12/28 1929 [7] Geology Grenville Precambrian in Appalachlane with Mesozoic Ottawa-Bonnechere Graben, pull-apart bastaa. Overprinting Age unknown (Post- along name structural line. Martic Ordivician). Line (lower Paleozoic outure) trende EW. Jurassic dikes at a high angle to Martic Line end Gettysburg Boein.
o o ra r L _FT F-l l gQ Lafayette. GA Date 10/9/85 30 Ardaley. NY Date 10/89/85 gQ Leroy, ON Date 1/31/06 Loc. 34.76*N 85.21*W 0.7. II:54 Loc. 40.98*N 13.e3*W 0.T. 20:07 Lec. 43.4S' N 83.1S* W 0.7. 18:48 magnitudese) n g-e.0 mgt, V Magnitude (s) e,.S.O mul, V: l magnstudetel N 4.0 mus, sV 133 Focal S km (local met
- aftershocks)
[23] 5-8 km l Depth 11.5 (28) Faultlag Strike ally on NS er Eu trending Strike-slip (P-aste ENEl Strike ally [ I plane. [24] strike dA strike dA l WNW steep (preferred) NNg-$$W steep Ist model (left lateral s.o.) WNW-gSg steep 2nd nodal 12al Ruptwre I km (28) 2 Length Aftershock area at km Equivalent Radius l ..,s.,. ,..ent Stress Drop =a c.* Felt Area 10,000 km 2 (331 = 940 km 2 fint. VI Foreshocks I (1 min, before main) [20] Naz. M*2.0 Mas. N =3.2 (10/21/85) Tight cluster 4ftershocke 8 N > 0.5 -0.1 < N < 2.S Aft $rshocks have substantial 126) component of reverse motion. 128] Depth Range 4.0-5.6 ka 3-6 km Number Several (10/9-10/20/84) 24 13 (thru 4/15/86) Duration b-values 0.96 (regional) l24) e 0.5 - 0.6 Max. Mistoric Ne 5.0 (NY City. 8/11/1884) garthquake V (3/9/1943) Geology Tacontaa highly deformed (ductile) and metamorphosed See report by Westen rocks (Manhattan Prong). Geophysical. Cameron's Line (CL) (Palessolc outure) meer epicenters but faulting as at high angle to cL.
I 72 i B References I 1. 2. 3. Armbruster and Seeber (1985) Barstow at al. (1988) Bashes et al. (1982) I 4. 5. 8. 7. 8. 8ellinger et al. (1978) Brown and Ebel (1985) Chiburls and Ahner (1980) Davison et et. (1984) Ebel (1983)
- 9. Ebel (1984)
- 10. Ebet and McCaffrey (1984)
I 11. Ebel and McIver (1985)
- 12. EPRI (1988)
- 13. Gordon et et. (1970)
- 14. Resegawa (1983)
- 15. Basegame and Metallier (1980)
I 18. Herreann (1978)
- 17. Herrmann (1979) l
! 18. Herrmann et al. (1982)
- 19. Horner et et. (1979)
- I',
20. 21. Horner et et. (1978) Nauk et al. (1982)
- 22. Pu!!! ei et. (1983)
- 23. Pulli et al. (1980)
- 24. Rondout Associates (1985)
'I 25. 28. 27. 28. Scharnberger and Novell (1984) Schechter et at. (1985) Schlesinger-Miller et al. (1982) Seeber et al. (1988a) I
- 29. Seeber et et; (1984a)
- 30. Seeber et al. (1984b)
- 31. Seeber et et. (1998b)
- 32. Seeber et al. (1984c)
- 33. Shand and Long (1985)
- 34. Stauder and Nutt!! (1970) iI 35.
38. 37. 38. Street (1978) Street and Turcotte (1977) Suares et et. (1984) Wahstr6m (1985) 39.
- 40. Metailler Wetailler(1975) et et., (1984)
- 41. Yang and Aggaruel (1981) t I
i i I
'I I
I 73 5 5 - 6 km) (3.1 - 3.7 miles). The b-value obtained for this sequence was approximately 0.6. Several significant earthquakes are recorded in the historical record for northeastern Ohio. The largest earthquake noted within 80 km (50 miles) of the epicen-tral area was aM = 4.7 event on March 9, 1943. There appear to be no significant differences between characteristics of the Leroy earthquake sequence and other tectonic sequences studied in the eastern United States. lI 7. DISCUSSION AND CONCLUSIONS In the various sections above we have presented data from which we can assess the validity of the suggestion that the Leroy earthquake of January 31, 1986 was associated with the injection of fluids in the two deep wells. The various arguments for and against the association are taken in turn. Factors favoring the Leroy earthquake being induced by fluid injection
- a. Large volumes of fluids have been injected in the two deep wells. These volumes and the pumping rates are comparable with other wells where seismicity is known to have been asso-ciated with fluid injection (Table 9).
- b. The range of permeabilities in the rocks (millidarcies) is comparable with other wells which have been associated with induced seismicity (Table 9).
- c. With these permeabilities, the time lags between injec-tion of fluids and the onset of seismicity are consistent with I
I
74 available models.
- d. There exists the possibility that small microearthquakes (with magnitudes less than 2.0) could have remained undetected.
Factors against the Leroy earthquakes being induced by fluid injection
- a. There were very few earthquakes (< 15) compared to known cases of induced earthquakes (100s to 1000s) (Figure 27).
- b. The Leroy earthquakes were associated with low b-values (0.5-0.6) (i.e. the relative ratio of the number of small earth-quakes to larger earthquakes), whereas for induced earthquakes the b-values are usually in the 0.8-1.1 range.
- c. The Leroy sequence was relatively short compared to those near injection wells which can last for several months or years.
- d. There was an absence of intense seismicity in the vici-nity of the Calhio wells. A large number of earthquakes often persisting over long periods of time is a characteristic feature of documented cases of induced earthquakes.
- e. There was a lack of any known felt (magnitude 2 2.0) earthquakes in the corridor between the wells and the epicentral area of the Leroy earthquake. Although this does not preclude undetected microseismicity with lower magnitudes, it would be
,ig,1y uniik.1, to have a 1arg. n..b.r 0, ve,y s.ali ..rthq..kes g,
and no felt event. 8 I - - _ __m
75 INDUCED EARTHQUAKE SEQUENCES (2132) 3 { (1314) b 1500 -
/
'/ 7
[ (DAYS)
/ /
1000 - E / i Q
/ (596)
(821) [ j (328) 500 - / S $ h . (395) (90) 5 $ j (1155)
/ / / / /
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/ / / [/ /
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1.5 - 1.0 -0.5 1.0 0 0 0 (2-3) APPROXIMATE MAGNITUDE THRESHOLD Figure 27. A comparison of the number of events in documented cases of well injection induced seismicity with the Leroy sequence. Note the differences in the recording periodsin parentheses, and the detection threshold.
L 76 f l Factors favoring Leroy earthquake being a tectonic event
- a. By tectonic event we mean a " natural" earthquake that occurs in response to plate tectonic stresses - as opposed to having been induced by pressure transients from the wells super-imposed on the plate tectonic forces. The clustered pattern of seismicity of the main shock and the aftershocks is similar to b other tectonic events.
- b. The small number of aftershocks (Figure 28) and low b-values is similar to other tectonic events in the area.
- c. The duration of the aftershock sequence is also similar to that for other tectonic earthquakes.
- d. The magnitude of the main shock (5.0) is not anomalously large and is comparable to other earthquake sequences recorded in the region (Table 10).
- e. The Leroy earthquake occurred in a region of known historical seismicity including a magnitude 4.7 event in 1943.
Thus its occurrence was not surprising. Other Microearthquakes
- a. The March 12, 1986 microearthquake, described in Section 2 above, was associated with an energy release, roughly one hundred millionth ( .$. 0 -8) of that associated with the Leroy earthquake. It occurred close to the wells - in a distance range where other examplet of induced earthquakes have occurred.
However, in over 90 days of recording with sensitive instruments, no other comparable event has been detected in the vicinity of the wells, or between the wells and the epicentral area of the
I I
=
7 M I
-2 NO. OF AFTERSHOCKS 8
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78 Leroy earthquake. Also, the Leroy cluster is at a depth range between about 3 and 6 km (1.9 and 3.7 alles) compared to about f 1.76 km (1.09 miles) for this event. Thus it is not likely that this event is associated with the l Leroy cluster. It is possible that it is a natural event or - possibly associated with the Calhio wells,
- b. The two 1983 earthquakes occurred within 5 km (3.1 miles) of the Calhlo wells (Figure 5) and about 9 years after the l
initial injection of fluids. However, there is a fair amount of uncertainty about their depths. The nearest station used to I locate them was at John Carrol University, nearly 50 km (31 miles) away. The other stations were located at distIances of 100 L km (62 miles) or greater. According to Dr. LeBlanc the best depth estimates (which yield the lowest travel time residuals) are between 2 and 4 km (1.2 and 2.5 miles). Given the epicentral proximity to the deep wells, and an elapse of nine years, and uncertainties in depth estimates it is not possible to rule out that these two events may have been induced by the injection of fluids. It is equally likely that these events were minor tectonic events the like of which have occurred in the past. However, in neither case do they appear to be spatially or temporally associated with the Leroy sequence. Conclusion After evaluating the various factors enumerated above we conclude that the possibility that the Leroy earthquakes were l l
79 induced by well injection is highly unlikely, although it can not I be completely ruled out. It is much more likely that the Leroy sequence was a "run of the mill" tectonic earthquake and its L aftershocks. r~ L f L I 5 I I I
80 BIBLIOGRAPHY Armbruster, J.G. and L. Seeber, The April 12, 1984 Martic earthquake and the Lancaster Seismic Zone in eastern Pennsyl-vania, Preprint, 1985. Barstow, N.L., J.A. Carter, and A. Suteau-Henson, Focal depths of shallow local earthqukes from comparison of polarization filtered data with synthetics, Earthquake Notes,_57, No. 1, 18, 1986. Basham, P.W., D.H. Weichert. F.M. Anglin, and M.J. Berry, New probabilistic strong ground motion maps of Canada: A compila-tion of EQ source zones, methods and results. Earth Physics Branch, Energy Mines and Resources, Ottawa, Canada, Open File, No. 82-33, 1982. Bollinger, G.A., C.J. Langer, and S.T. Harding. The eastern Tennessee earthquake sequence of October through December, 1973, Bull. Seis. Soc. Am., 66, 525-547, 1976. Borcherdt, R.D., Preliminary report on aftershock sequence for earthquake of January 31, 1986 near Painesville, Ohio (Time 5 Period: 2/1/86-2/10/86), 1986, 109 pp. U.S.G.S. Open File Report 86-181, Brown. E.J. and J.E. Ebel. An investigation of the January 1982 aftershock sequence near Laconia, New Hampshire, Submitted to Earthquake Notes, 1985. Chiburis, E.F. and R.O. Ahner, eds., Seismicity of the Northeastern United States April 1, 1979-June 30, 1979, North-eastern U.S. Network Bulletin No. 15, published by Weston E Observatory of Boston College, 1980. Costain, J.K., and G.A. Bollinger, A hydrological model for intraplate seismicity in the southeastern United States, Earthquake Notes, 56, No. 3, 67, 1985. Costain, J.K., G.A. Bollinger, and J.A. Speer. Hydroseismicity: A 8 hypothesis for intraplate seismicity near passive rifted margins, Earthquake Notes, 57, no. 1, 13, 1986. Davis, S.D., Investigations of natural and induced seismicity in the Texas panhandle, M.A. Thesis. University of Texas at Austin, Austin, Texas, 1985. Davison. F.C., M.C. Chapman, J.W. Munsey, and G.A. Bollinger, A note on the Cunningham, Virginia earthquake of August 17, 1984, in the Central Virginia Seismic Zone. Earthquake Notes, i 55. No. 4, 26-33, 1984. 5 I
81 7 Dunrud, C.R. and B.B. Nevins, Solution mining and subsidence in v- evaporite rocks in the United States, U.S.G.S. Misc. Inf. Series, Map I-1298, 1981. _j Ebel, J.E., A detailed study of the aftershocks of the 1979 earthquake near Bath, Maine, Earthquake Notes, 54, No. 4, 27-7 40, 1983.
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Ebel, J.E., Statistical aspects of New England seismicity from 1975 to 1983 and implications for past and future earth-quakes, Dull. Seis. Soc. Am., 74, 1311-1330, 1984. Ebel, J.E. and J.P. McCaffrey, S.J., Hypocentral parameters and I focal mechanisms of the 1983 earthquake near Dixfield, Maine, Earthquake Notes, 55, No. 2, 21-24, 1984. Ebel, J.E. and J.D. McIver, A study of the source parameters of some large earthquakes of northeastern North America, submitted I to Bull. Seis. Soc. Am., 1985. EPRI Earthquake Catalog, unpublished, 1986. Evans, D.M., The Denver area earthquakes'and the Rocky Mountain Arsenal disposal well, The Mountain Geologist, 3, 23-36, 5 1966. l Fletcher, J.B. and L.R. Sykes, Earthquakes related to hydraulic mining and natural seismic activity in western New York state, J. Geophys. Res., 82, 3767-3780, 1977. I Prohlich, C., Seismicity of the central Gulf of Mexico, Geology, 10, 103-106, 1982. I Prohlich, C. and D.B. Dumas, The seismicity of the Gulf of Mexico, EOS Trans. Am. Geophys. Union, 61, 288, 1980. Gibbs, J.F., J.H. Helay, C.B. Raleigh, and J. Coakley, Seismicity in the Rangely, Colorado, area: 1962-1970, Bull. Seis. Soc. I Am., 63, 1557-1570, 1973. Gordon, D.W., T.J. Bennett, R.B. Herrmann, and A.M. Rogers, The I south-central Illinois earthquake of November 9, 1968: Macro-seismic studies, Bull. Sels. Soc. Am., 60. 953-971, 1970. Gupta, H.K. and B.K. Rastogi, Dans and Earthquakes, 1976, Elsevier Scientific Publishing Co., Amsterdam, 229 pp. Harding. S.T., Induced seismic Cogdell Canyon Reef 011 Field in Summaries of Technical Reports, Volume XII, National Earth-quake Hazards Reduction Program. U.S.G.S. Open-File Report 81-833, 547, 1981. I I
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84 Pennington, W.D., S.D. Davis, S.M. Carlson, J. DuPree, and T.E. Ewing, The evolution of seismic barriers and asperities caused by the depressuring of fault planes in oil and gas fields of south Texas. Bull. Sels. Soc. Am., in press, 1986. Phillips, D.E. and D.H. Oppenheimer, Induced seismicity in the Geysers Geothermal Area, California, J. Geophys. Res., 89, 1191-1207, 1984. f Pulli, J.J., J.L. Nobelek, and J.B. Sauber, Source parameters of the January 19, 1982, Gaza, N.H., earthquake. Earthquake Notes, 54, No. 3, 28-29, 1983. Pulli, J.J., R.R. Stewart, J.C. Johnston, K.M. Tubman, and A. Michaels, Field investigation and fault plane solution of the Bath, Maine earthquake of April 18, 1979, Earthquake Notes, 51, No. 4, 39-46, 1980. Raleigh, C.B., J.H. Healy, and J.D. Bredehoeft, An experiment in earthquake control at Rangely, Colorado, Science. 191. 1230-1237, 1976. Resources Services, Inc., Well Report, Injection Well No. 2. Calhio Chemicals. Inc., Perry, Ohio, 1980. Resources Services, Inc., Memo containing data pertaining to the hydrofracturing procedures used in Calhio Chemicals, Inc. injection well No. 1, 1986. Rogers, A.M. and A. Malkiel, A study of earthquakes in the Permian Basin of Texas-New Mexico, Bull. Seis. Soc. Am., 69, i 843-865, 1979. Rondout Assoc., Inc., Tectonic framework and seismic source zones of the Eastern United States, Electric Power Research I Institute / Seismicity Owners Group, Draft 85-7, 1985. Rothe, G.H. and Lui, C.-Y., Possibility of induced seismicity in I the vicinity of the Sleepy Hollow Oil Field, southwestern Nebraska, Bull. Sels. Soc. Am., 73, 1357-1367, 1983. Scharnberger, C.K. and B.F. Howell, Intensities and structural setting of the earthquakes of 19 April and 23 April, 1984, Lancaster County, Pennsylvania, Earthquake Notes, 55, No. 3, I 12, 1984. Schechter, B.D., D.J. Reinbold, and A.C. Johnston, Source parameters and aftershocks of the Lafayette, GA earthquake of Oct. 9, I 1984. Geol. Soc. Am. Abstracts with Programs, 17, 133, 1985. I I
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I 87 APPENDIX I. CONCERNS EXPRESSED BY PROFESSOR AHMAD In his testimony on April 8, 1986 before the House Committee on Interior and Insular Affairs. Subcommittee on Energy and Environment, Dr. Mold U. Ahmad of the Ohio University expressed several concerns. Some of these pertained to the Leroy earthquake and the possible role of fluids injected in the two deep Calhio wells. In particular he suggested that his review of the historical seismicity data, injection history at Calhio wells suggested that the injection of fluids in the Calhio wells had induced the earthquakes in the Leroy sequence. The paragraphs below address the comments made in his written testimony. General Remarks
- 1. The status of seismicity in Dr. Ahmad's testimony was not up to date. The more recent data regarding number of events, locations, etc, have been incorporated in Section 2, and will also be available in the report by Weston Geophysical.
- 2. The information regarding the structural trends and Woollard's data is completely out of date and current data /
thinking do not support the concept of a mega-linear trend from New Madrid to the St. Lawrence rift zone in Canada (see Dr. l Hinze's report for details). In his response to the concerns 9 raised by OCRE, Dr. Pomeroy also cautioned against such " linesman-ship". I
- 3. The Pittsburgh-Washington and the Tyrone-Mt. Union are two lineaments identified by analyses of Landsat images and po-I I
88 s tential field data by Lavin et al. (1982). According to those 7 authors there was lateral movement of a block contained by these lineaments during the late Pre-cambrian to Lower Ordovician time (600-450 million years ago) and vertical displacements in Paleo-zoic times (to about 300 million years ago). Since then, there is no evidence of lateral or vertical movement on these features, 1.e. there is no evidence that these are active faults as implied ~ by Professor Ahmad. Hence his classification of these features as " Cleveland-Pittsburg (sic) Washington strike slip fault" and "Tyrone MT (sic) Union strike slip fault" are incorrect. I 4. Next. Dr. Ahmad appeals to "hydroseismicity", a mecha-nism according to which "... natural water flow can trigger l l earthquakes by increasing the fluid pore pressure in the rocks I and lubricating an already stressed fault..." This is based on a i news story in Science News by Stefi Weisburd - following a talk l given by Costain et al. Dr. Ahmad in his oral testimony was critical of the U.S.G.S., NRC and the utility for not incorpo-l I rating "hydroseismicity". I We are thoroughly familiar with this idea. In fact, it is not new at all. The idea of seismic activity triggered by changes in rainfall patterns is not new and has been explored in research concerned with other earthquake sequences, expecially in Japan. In its current form. Costain and Bollinger (1985) and Costain et al. (1986) offer it as a speculative model to explain all intraplate seismicity in the southeastern United States. It I I
89 is one of about a dozen speculative models that have been sug-gested in the last five years or so. The use of this model as a general mechanism for seismicity on a regional basis and at ~ depths of 10-20 km is very speculative and full of scientific ~ loopholes. It is by no means an accepted " theory" that can be applied to explain the temporal and spatial pattern of seismicity observed at Leroy. ~
- 5. The study of earthquakes in the Denver area associated with the Rocky Mountain Arsenal was by Healy et al. (1968) whereas the seismicity in the vicinity of the Rangely 011 Field was by Raleigh et al. (1976) and not by "Healy and others, 1961" as stated by Professor Ahmad (see section 5 above). Also, the l
Baldwin Hills Reservoir is in California not Louisiana as stated by Professor Ahmad. l
- 6. Describing the magnitude 3.8 earthquake in Louisiana in 1983, "... occurring about 2 miles south of Browning Ferris Industries injection well at Lake Charles, Louisiana". Dr. Ahmad I "
quotes his own unpublished presentation to assert that, ...the injection well increased the pore pressure and lubricated an already stressed fault". No supporting data or evidence are provided for this assertion. This earthquake has been studied by various workers in Louisiana and Texas and according to them it is not associated with the wells and appears to be similar to an earlier earthquake offshore (Pennington, Personal Comunication, 1986: Don Stevenson, State Seismologist. La., Personal Communica-I I
90 tion, 1986). That a offshore earthquake occurred on July b 4.8. 24, 1978 and it was suggested that events in the Gulf of Mexico occur along zones of weakness associated with Mesozoic rifting (Frohlich and Dumas, 1980; Frohlich, 1982). However, others ascribe them to flexuring because of the sediment load in the Gulf. ii
- 7. Dr. Ahmad's description of the induced earthquakes near i
l= Snyder, Texas was based on a thesis by Davis (1985) and the pre-print of a forthcoming paper in the Bulletin of Seismological Society of America by Pennington et al. (1986). We reviewed these and also an abstract of a talk by Pennington and Davis I (1985) with respect to the impact on hypotheses concerning the cause of the Leroy, Ohio earthquake of 1/31/86. Their model for induced seismicity relates to petroleum operations and is based on the premise that regions of high pore pressure undergo aseismic creep while regions of lower pore pressure (often associated with fluid withdrawal) cannot move aseismically and become high strength barriers. Continued aseismic creep leads to increased stress at the locked barriers resulting in the transformation of these high strength barriers into high stress asperities. Stres-ses at these asperities continue to build until failure occurs seismically. This model represents a logical extension of the Mohr Coulomb failure criteria (Jaeger and Cook, 1979) which is often invoked to explain seismic activity. Such a model is a good application of the laboratory results of Lockner et al. (1982) and the suggested cause of seismicity at the Geysers I ! l l 5
91 geothermal field (Phillips and Oppenheimer, 1984). This model is particularly useful in explaining the spatial patterns of sels-micity associated with fluid WITHDRt.WAL and simultaneous injection. Using the best estimates of the pore pressure increases resulting from the Calhio injections it is unlikely that this model can be invoked to explain the spatial or temporal pattern of seismicity observed near Leroy, Ohio. I 8. Assuming the injection pressure history at the well site, Dr. Ahmad calculated the excess pore pressure at an epicen-tral distance corresponding to the site of the Leroy earthquakes. Assuming radial flow in a homogeneous layer he obtained an excess pore pressure of about 100-200 feet of head at the epicentral W location or about 3-6 bars. This estimate is in agreement with that obtained by U.S.G.S. (Wesson, Personal Communication). If the flow is along a channel (as was modeled for Denver (Hsieh and Bredehoeft, 1981)), the excess pore pressure is likely to be greater within the channel and lesser outside it. However, there is no known evidence of such a channel near Leroy. 1 3 9. While concluding, Dr. Ahmad makes some sweeping state-
- g ment that invites a comment. For example, "...We believe that l g large and destructive earthquakes will occur in the East..."
Yes, but the crucial question is where and with what return periods? There are several studies under way (e.g. by EPRI, LLNL. and others under NRC sponsorship) aimed at arriving at the I L I
D - 92 answer to the above question. He also asserts that ..PNPP is ' surrounded by at least four known faults and two earthquakes of about magnitude 5 within a ten mile radius in the past four years. The presence of high pressure deep injection wells have increased the possibility of future earthquakes in this area..." ~ The existence of any one of these four faults has not been
-demonstrated either in Dr. Ahmad's testimony (or in the litera-
~ ture). Only one magnitude 5.0 event is known to have occurred in that area, and that was the Leroy 1/31/86 event. The association a of seismicity with injection wells in Ohio is arguable at best and has not been demonstrated. Hence, the assertion that there l 1s an increased possibility of future earthquakes because of injection is perhaps both wrong and misleading. I I I l I . I I 'I I I I
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